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HARVARD UNIVERSITY

isk

Ernst Mayr Library

of the Museum of

Comparative Zoology

F a

Velie 77 ae nN i

VOLUME 106 JUNE 2003 ISSN 0303-2515

ANN

ELON Es

saso.

CN 2 shoo ee

PetroSA

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BULLOUGH, W. S. 1960. Practical invertebrate anatomy. 2nd ed. London: Macmillan.

FISCHER, P. H. 1948. Données sur la résistance et de la vitalité des mollusques. Journal de conchyliologie 88:

100-140.

FISCHER, P. H., DUVAL, M. & RAFFY, A. 1933. Etudes sur les échanges respiratoires des littorines. Archives de

zoologie expérimentale et générale 74: 627-634.

KOHN, A. J. 1960a. Ecological notes on Conus (Mollusca: Gastropoda) in the Trincomalee region of Ceylon. Annals

and Magazine of Natural History (13) 2: 309-320.

KOHN, A. J. 19605. Spawning behaviour, egg masses and larval development in Conus from the Indian Ocean. Bulletin

of the Bingham Oceanographic Collection, Yale University 17 (4): 1-51.

THIELE, J. 1910. Mollusca. B. Polyplacophora, Gastropoda marina, Bivalvia. In: SCHULTZE, L. Zoologische und

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ANNALS OF THE SOUTH AFRICAN MUSEUM

ANNALE VAN DIE SUID-AFRIKAANSE MUSEUM

Volume 106 Band

June 2003 Junie

THE FORAMINIFERA OF THE LATE VALANGINIAN

TO HAUTERIVIAN (EARLY CRETACEOUS)

SUNDAYS RIVER FORMATION OF THE

ALGOA BASIN, EASTERN CAPE PROVINCE,

SOUTH AFRICA

By BRAR

I. K. MCMILLAN NcT 08 2003

HARVARD

INIVERSIT®

The Council of Iziko Museums of Cape Town

(incorporating the South African Museum)

gratefully acknowledges the financial contribution of

CNR

Sasol

PetroSA

bhp billiton

Pioneer Natural Resources

Forest Exploration International South Africa (Pty) Ltd

towards the cost of publication of this paper.

‘... we set out and took the road to the Ados Drift, on Sundays River. At noon we reached some hovels

near the drift, where we found a slave, a Hottentot woman and a few children, got some milk and butter |

and had a miserable dinner. I had hoped to have gained an opportunity of examining the steep banks of

the river but now saw with concern that I could not possibly reach the limestone rocks on the opposite

shore. They have many extraneous fossils embedded in them...’

C. I. LATROBE—Journal entry for 9th April 1815

(Latrobe 1818)

‘l believe it is not generally known that the eastern bank of the Zwart-kop River, together with the

banks of the Zondag River, are rich in marine petrifactions ...’

C. H. GRISBROOK 1830

‘,.. and then having exhausted the time we had allotted to this locality, we proceeded on to the

Sunday's River. It was almost dark when we arrived at the base of the cliffs beyond Roe’s, and whilst

pitching our tent near where the road turns round into the Koegakama Kloof, the dark line of cliffs

appeared so inviting that had there been but a moon we should certainly have scaled them at once, tired

as we were. Next morning we were up at break of day, and ere I had finished my coffee, a loud hurrah!

from the cliffs above me, summoned me with a bound to the spot. My friend Bain had gone off without his

coffee and got the start of me. There he stood, half dressed, with a splendid gryphoea incurva in his

hand, beckoning us to come. “The cliffs are Liasic then!” we both exclaimed; and now commenced a

most exciting scene, gryphoeas, trigonias, ammonites, gervillias, exogyras, nautilli, whole and in

fragments, were thickly strewn over the sides of the cliff, lying uncovered by the rains of years. Each

fresh discovery was announced by a louder shout of triumph. ’

W. G. ATHERSTONE 1856—

Describing a field trip to the Zoetgeneugd Cliffs

(Atherstone 1857)

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 3

CONTENTS

PAGE

Daal LOG AMES at aRrt 3 1 5. tc Fee oSae erst eaten Reema ane Mas acoas van a cabebnluidsendee inguswatinaeliasdendes seasissoweeacudaaancteurvoenetee 5

Sted Ml Otrea poder een eee hatsaecs eae er mamene ceseisein te caecr aerate aes uch avgittenebaiiioce vate nacadthedlens'Seemateabonanannnenceretlacausctoctes 7)

ithemundays Rayver—Upper Algood boum@any «occ Jeti .ccc cL cscacdsteueonncostevestechecSosdgecudeleaeesecnenets i

MNeWGiEKwOOd—SUnday SANIVEE DOUNGALY 645...1.haiesseteovhssouncccvslogeewecasstsacdonsssbeaeedeaboateessbvasodestes 9

Previous work on foraminifera of the Sundays River Formation .........00..:...s.000s0eessssoressesoseveeesenee 13

Ey eley es BUGIS S sesmen ners heeteamect eae est ait es tie, Me sdete es'eeainvraatianissnuadidMeidaun Rios eta ouined xada exon eaaipus sedated ansaweues I3

IEC OG eaten meme A Weed Carta Ae oer Uicean See Ms wack encarta lads uooal Saunton oilevasdc este oiled vatera paeeeanee 17

Boron@ le ameeoulC rope te tial. 22st le.0soen ccopeesdtdteiadeawartanaaesile- doesn assasdigeavagliagergeseendaebewsveeesostevetsense 18

IBS Rett Oe Sess 6 asain cde ties aeeene ee sea eis we ai ned se ciidod avienensbacBecnoemamiedhoncidanas Nedeedeaseddeenatmeacenes 18

SHINS Oe MOVES er me dy) Nocatee dete dais strosacfeor vee. eler veMoainsnis a loses niuh sons a Wide encoaatucanaunnteene 20

(O) TU CTO) OS ies ett Be Ro te ee nn OP cm eer Re er er pw)

FnO CESS MM Cg IA UOC Siren ante tcnctesnrcl as ce Keeacnalsgeds fas glections sanellt vexnaafwnaraeuontceusnecteetin saiemawansndeanetvenss 22

Comparison of Sundays River Formation foraminifera with elsewhere...............ccc:ccccccessseeeeeeees 22

FSM MMMM A AN gO MT LS sete ars Pee minsa a emai ooh chs bce 2a aa od sda ala hod se Selena on doenalon me cee tases 22

SDP iSie 249~ Meo Zaimtab iQue RUGS s/c sssa nodes 2s: aus ennshiesienssessdecaeseecnacguateiber sneenecsnnvassnsoreueerees 25

PRO CHOMIS WC AV SARE VICK. Is OMA OM. <.:ec Gene laceAinerectuans <odssanbanduaeesdsnnzedesesstodeateesdusce ded seoteencodaac=stdeaedrea™ 2d

ID hate) tte tech POM eset iaseen we ee ett ys 28 eee Seahe Pina Ry Acne Sess sohadae sacificwdeQaiheaibes daae deucasadsnteuevadvarercueeaaee 27

Foramintieral biozonation of the Sundays River FormatiOM......:.0..00c..:080..cccceenescessesvneccacessorenncansgebecnens 33

| ES IDR) ORS 210, ie ar een ok na enn A Oe ee ee re 38

ES) Ayes Fal AUS Lon Val AMM eh oe ee Breet NAL ANS Meh Meat saOLememredss cide shh x uatjeitcedels tn eastinsddouhieeacuuenedvatca les sareeee maul waaay ones 35

em (cll chin Cui AIM eae Ae coed aria ed wigde hose tess Secs sanenad cen ea aateiibana teat SuaSvansd Ua nensiea vuoddcantauoraeteNtees aes oeeatres: 36

Outcrop/subcrop-map of the Sundays Raver FOrmMation ..c......0...sacsecascastscdenenassnarnartanadeevarederiocoeas 39

BiIOZOMES. TAG Ie Sr ans (te ATES Beak sends Bek rch a veeetedoactadsoosdivunoesi sade cdaseadenseedbde spoeiecbanadenonadDeentostaancsaston 39

SUMAN tal US NC OM UO liewleae ee. 6 eae sb A ce dedi Loaves donee Passsde svosssabsauautede@annnebidacstins beds duskagsloentgont tieedtnainede: 4]

Foraminiferal biostratigraphy of the Valanginian and Hauterivian of the

SOMUR UM HUM AOC Hee ue ese cet tee ge seen Oe stn prica twos ub bag aeeicl nc Secu Sowa dae a daiin Mate wah ouatuonten de aaeaeae tena eabeene 43

Siow Ao Aus ASMTINOMEC TOPOS ete haa ch es Conran abswecvsnsnd dsvadeni baat cas dsahadetseanatledgpusdvean dosenaedeneudaavareseeny aedeuncaes 44

Rare o Ve CN Ale © CMV INOMMNCIALS cde, e4dcc farsduwadcessasssbcesves¥scsdoctiavseraccesssingiaavenatiduceceadeees teed sheds tegueeseesinss 61

'Lislite Sy UGH ICT Te N21 Resa Re ee coh RR ee re eer oe eR 61

Fe ois yaa od cate pele UA ee oe eth ate Meet SO. Dos hc cely hd salah ete ealea dncdge Man demeoatoleornar ounesan addons sane Mlebameaats: 62

TPA ie ACU Fela eee ret era ees ee as st Nao onast a dls enes eae nates onemeuavendse tee sauconee tr esaesnonedetsndonncwaadaians 63

Oxy Senblevelsaind Water temper arUne 5. xcs. cccnHbs tacts sadracedeae canscanenstvaceeeasacttesawasecdsessnenssetieléctendddeceens 65

Palaeoecology of foraminifera groups of the Sundays River Formation ..............:cccssceesseeeseeeeees 66

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eastern Cape, South Africa.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION y)

INTRODUCTION

Within the Cape Fold Belt, composed mainly of Palaeozoic (Ordovician to

Carboniferous) rocks, are a series of basins containing latest Jurassic to earliest

Cretaceous sedimentary sequences. These basins are generally half-graben types, which

have been infilled with a variety of continental, marginal marine and continental-shelf

sediments (McLachlan & McMillan 1976 and references therein). The Algoa Basin is the

largest of those developed onshore, containing a sediment pile up to 4 500 m thick, and it

also possesses the most marine sequence.

Offshore, extensive seismic exploration and deep drilling undertaken by SOEKOR (Pty)

Ltd have revealed the presence of extensions of the onshore basins, lying beneath the

present day Agulhas Bank. The arrangement of the Mesozoic Algoa Basin, both on and

off the present coast, 1s shown in Figure 1. The tectonic history of the offshore Algoa

Basin was detailed by Bate & Malan (1992), its Early Cretaceous stratigraphy by

McMillan et al. (1997), and its petroleum geology and exploration potential by Malan

(1993) and Broad & Mills (1993).

The onshore portion of the Algoa Basin is composed of two major depressions: the

larger Sundays River Trough and the Uitenhage Trough. The Uitenhage Trough is a

typical half-graben, bounded to the north-east by the Coega Fault, an extension of the

offshore St Croix Fault system (Doherty 1993). In contrast, the Sundays River Trough is a

more complex, faulted depression that lacks clear bounding faults (Hill 1972, 1975; Lock

et al. 1975: 222). The basin floor in the Uitenhage Trough shallows steadily southwards,

away from the Coega Fault, and is not affected by major faulting. In contrast, the basin

floor in the Sundays River Trough is fractured by a series of faults trending

west-north-west to east-south-east, aligned roughly parallel to the northern margin of the

basin. These divide the Sundays River Trough into three compartments: a half-graben

north of the Commando Kraal Fault, a central horst (the Addo Nose) plunging to the east,

and a more depressed area to the south of the Colchester Fault (Battrick 1974) that

shallows southward to the ridge underpinning Coegaskop and the St Croix Island group.

Depocentres (maximum thicknesses of preserved sedimentation) occur just to the north of

the Commando Kraal Fault (intersected by borehole CK 1/68) and south-west and

north-east of the distal end of the Colchester Fault (intersected by borehole AL 1/69). The

faulting can be best defined on the basement (Horizon D) surface (see Fig. 2), as the poor

quality of the onshore seismic data hinders fine resolution of the faulting at higher

stratigraphic levels. None the less, during sedimentation of the Sundays River Formation,

differential subsidence rates can be seen to have occurred in the north, centre and south of

the Sundays River Trough and the Uitenhage Trough, that, coupled with varying rates and

types of sediment input are clearly reflected in differences in foraminifera assemblages

across the basin. Offshore, the basin fill of the Sundays River Trough progressively onlaps

the upthrown side of the St Croix Fault in a southward direction, until the upper Sundays

River Formation unconformably overlies basement (D = 1At1) (see Fig. 2).

Apart from the sliver of Suurberg Group volcanic rocks along the northern rim of the

Algoa Basin (Hill 1972, 1975; McLachlan & McMillan 1976; Marsh et al. 1979), the

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Structural and stratigraphical relationships of major lithological units in the onshore

and nearshore Algoa Basin. Orientation of section line shown in Figure |. All depths

(feet in CK 1/68 and metres in VO 1/71 and Hb-D1) are measured from Kelly

bushing datum.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION ye

basin 1s surrounded and underlain mainly by Ordovician—Silurian Table Mountain Group

quartzites, Devonian Bokkeveld Group black slates, and Devonian—Carboniferous

Witteberg Group black slates and sandstones. Deep boreholes drilled to basement in the

Sundays River Trough (AD 1/68, AL 1/69,,BR 1/71; Ck 1/68, CO 2/70, CO 3/71,

KE 1/71, NA 1/69, NA 2/70, NA 3/70, SH 1/74, SM 1/76, SV 1/71, VO 1/71) all bottomed

in Bokkeveld slates, whereas those drilled to basement in the Uitenhage Trough all

bottomed in Table Mountain quartzites (BT 1/74, ST 1/71, SW 1/08). The Mesozoic

sedimentary basin infill consists of early conglomerates, then lacustrine, estuarine and

fluvial claystones and sandstones, and finally marine claystones and sandstones.

STRATIGRAPHY

The earliest records of the fossiliferous nature of the onshore Algoa Basin were

provided by Latrobe (1818), who recognized fossils at the Addo Wagon Drift, and by

Grisbrook (1830), who noted the presence of shell beds near the mouth of the Swartkops

River (Amsterdamhoek) and along the Sundays River (probably Zoetgeneugd). Early

palaeontological studies have been summarized by McLachlan & McMillan (1976).

Lithostratigraphic studies have divided the sequence into a lower half of up to 2 400 m of

minor conglomerates (Enon Conglomerate Formation), non-marine sandstones

(Swartkops Sandstone Member) and mainly red and green claystones with sandstones

(Kirkwood Formation). Near the base of the last-named 1s a non-marine to shallow marine

green-grey or mostly black claystone, which in the Uitenhage Trough has yielded

foraminifera, and is termed the Colchester Shale Member. The upper half of the sequence

consists of up to 2 000 m of shallow-marine and shelf claystones and sandstones, usually

displaying a coarsening upward cyclicity on a fine scale, termed the Sundays River

Formation. The stratigraphic relationship of these lithological units is given in Figure 2,

and details and relationships of the various units were discussed by Hill (1972, 1975),

Winter (1973, 1979), McLachlan & McMillan (1976, 1979) and Shone (19765, 1978),

amongst others. Dingle ef a/. (1983) provided a critical overview.

Of the macrofossil remains 1n the Sundays River Formation, ammonites have provided

the most detailed age information. Ammonite datings support a Late Valanginian age for

the Sundays River Formation (Spath 1930; Cooper 1981) but, because available outcrops

tend to expose only the lowest levels of the sequence (which are also dated microfaunally

as Late Valanginian), it is not clear how much of the Sundays River Formation sequence is

actually ammonite-bearing. The trigonioid bivalves have recently been the subject of a

monograph by Cooper (1991).

The Sundays River—Upper Algoa Boundary

The upper surface of the Sundays River Formation 1s marked by an unconformity

characterized by extensive erosion. Planation of the Sundays River Formation surface has

probably occurred since earliest Barremian times, so that today the most complete

sequences are near the basin axis, and progressively less and less is preserved towards the

basin margins (Fig. 3). It is for this reason that the Hauterivian interval of the axially sited

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interpreted outcrop/subcrop of foraminifera biozones (defined in the text).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 9

borehole AL 1/69 has been selected for detailed foraminifera study, since it could well be

considered a type-section for the upper Sundays River Formation.

Unconformably overlying the Sundays River Formation are the calcarenites and

aeolianites of the upper Algoa Group (Pliocene and Pleistocene), together with various

alluvial, dune and river terrace accumulations (see McMillan 19905, and references

therein). From studies of the onshore and offshore Algoa Basin, and the eastern Cape

towards East London, it is clear that marine ‘transgressions’ inundated the onshore Algoa

Basin in Late Campanian—Maastrichtian, earliest Eocene, and Middle Eocene times

(lower Algoa Group). Where drilled or studied in outcrop, no trace of the rocks laid down

at these times now exists over the Algoa Basin. It is clear that repeated deposition—erosion

cycles were responsible for erosion of underlying rock units, including the topmost

Sundays River Formation. A similar situation prevailed during the Pliocene and

Pleistocene deposition—erosion episodes of the upper Algoa Group. Thus, the present

remnant of Sundays River Formation within the onshore Algoa Basin probably reflects

rather poorly the original distribution of the Formation. That this is the case is supported

by the arrangement of depositional facies over the area of the Sundays River Formation

(see Figs 21-24).

Winter (1973) described the Sundays River Formation as consisting of compacted grey

clays, silts and sands, which form cyclical sequences (often showing upward coarsening)

that are probably due to intermittent subsidence of the basin and consequent fluctuating

sedimentary infilling. The surface stratotype of the Sundays River Formation, defined by

Winter (1973), is located on and about the farm Zoetgeneugd (modern spelling

Soetgenoeg), where high cliffs have been formed by back-cutting by the Sundays River.

The Kirkwood—Sundays River Boundary

Comments on the nature of this major lithological change have been presented by

Winter (1973, 1979) and McLachlan & McMillan (1976). The transition across the

boundary in fully-cored borehole CO 1/67 is shown in Figure 4. Earlier (unpublished)

reports by Venter (1972a, 1972c, 1972d, 1972e) contain a more detailed analysis of the

boundary in deep boreholes than has been presented to date in published work. Winter

(1973: 26, figs 3a, 6) noted that changes in shale specific gravity, reflecting a sudden

increase in shale compaction, at the top of the Kirkwood Formation ‘not only suggests an

unconformity, but also perhaps the very different compaction history of desiccated clays

of a red bed sequence, which may also account for the very slow increase with depth’.

Thus, the original comments of Winter (1973) are somewhat ambiguous as to whether

there is an unconformity at the Kirkwood—Sundays River formational boundary, or not,

reflecting the uncertainties previously voiced by Venter on this subject. However,

McLachlan & McMillan (1976: 199) again postulated an unconformity on the basis of

changes on the shale density graphs and dipmeter logs. Winter (1979: 188)

accommodated both options, by stating ‘the lower boundary of the (Sundays River

Formation) may interfinger with the Kirkwood Formation or be an unconformity’. This

perhaps reflects arguments by Shone (1978), who viewed the Kirkwood Formation as

grading laterally into the Sundays River Formation. Shone (1978: 325) made additional

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Boundary

environment from the foraminifera study, and depths of studied samples.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION ll

comments on the clay compaction curve presented by Winter (1973, fig. 3a), and disputed

the resulting interpretation of an unconformity at the Kirkwood—Sundays River

formational boundary. However, Shone (1978) instead suggested an unconformity

between the Enon Conglomerate Formation and the Kirkwood Formation, based on the

difference in the palaeoslope during Enon times compared with Kirkwood Formation

times.

Three outcrop localities have been described that suggest the Kirkwood Formation

interfingers with the Sundays River Formation. Rigassi (1968: 9, pl. 23) described such a

section at the Airedale brick-clay quarries, noted also by Rigassi & Dixon (1972: 519), but

McLachlan (in McLachlan & McMillan 1976: 207) found no unequivocal evidence of

such a relationship. Secondly, Shone (19764: 17) noted the gradation of facies from

Bezuidenhouts River bridge to Dunbrody, but found the precise relationship of the lateral

gradation to be unclear. Fossil data from these outcrops shows there to be a steadily

increasing marine influence basinwards, although on the fine scale some fluvial red beds

and estuarine oyster-bearing grey claystones have been found interbedded west of Blue

Cliffs Station (McLachlan & McMillan 1976, fig. 7, site 1). Thirdly, north of Uitenhage,

Rogers & Schwarz (1901: 4) identified marine beds outcropping beneath Enon

conglomerates, but Haughton (1928) recognized that the conglomerates occurred on the

upthrown side of the Coega Fault, and the marine beds on the downthrown side (see also

McLachlan & McMillan 1976: 199, fig. 4). Thus there seems to be no clear evidence of

major interfingering of the Kirkwood and Sundays River formations in outcrop, as

concluded by McLachlan & McMillan (1976).

Venter (1972a) utilized well logs, sandstone percentage graphs, rate of penetration

while drilling, dipmeter results, shale density logs, calcimetry and clay mineral

distributions to establish correlations between boreholes within the Kirkwood and

Sundays River formations. Subsequently, Venter (1972e) analysed electric logs and

lithologies across the Kirkwood—Sundays River formational boundary, with the specific

aim of attempting to determine if an unconformity exists at the boundary. He concluded

that the well logs display only small peaks that generally are small and lack diagnostic

features (see Winter 1973, fig. 2; Winter 1979, fig. 6; herein Fig. 4). None the less, some

log markers were established. Sandstone percentage graphs were affected by the

‘shaling-out’ of the formation towards the basin centre, and the presence of many small

sandstones and few diagnostic ones, that led to difficulties in confirming correlations from

one borehole to the next. Fluctuations of penetration rate seem to be related to the type of

environment, with continental section generally drilling at a slower rate than marine

section; no clear correlations were obtained using this method alone but it had some value

when related to sandstone abundance. Venter (1972a) remarked on the abrupt change in

dip seen at the top of the Kirkwood Formation on dipmeter logs from all the boreholes he

studied. Other, apparently localized changes in dip occur in the lower Sundays River

Formation and the upper Kirkwood Formation. As noted previously, shale density graphs

show a steeper gradient for the Kirkwood Formation than for the Sundays River

Formation. Although some features proved of local correlation value, percentage calcite

and percentage dolomite values from calcimetry provided only a poor correlation.

1 ANNALS OF THE SOUTH AFRICAN MUSEUM

Similarly, little success was gained with correlation using clay mineral compositions.

Venter (1972a) concluded that lithological correlation within the onshore Algoa Basin

was incomplete and ineffective, and that subdivision was limited to sedimentary cycles

that were mainly of a local nature. Despite Venter’s (1972e) attempts to correlate green

claystone beds and borehole logs above and below the boundary, he was unable to |

determine if an unconformity occurs at the Kirkwood—Sundays River formational

boundary, due to discontinuity of lithologies, and the limited, localized sedimentary

cycles evident in the borehole logs. Log correlations by Venter and by subsequent

SOEKOR analysts suggested that, over most of the onshore Algoa Basin, the

Kirkwood—Sundays River formational boundary is conformable. Comparisons between

the interval zonation based on the foraminifera proposed herein, and the most detailed of

the log correlations for the lower Sundays River Formation and upper Kirkwood |

Formation suggests marine conditions developed virtually synchronously across the

entire onshore Algoa Basin.

There is no evidence for truncation of topmost Kirkwood Formation beds either in the

basin depocentre or towards the margins; nor is there any clear indication of onlap of basal

Sundays River Formation beds towards the basin margins or to identifiably proximal

localities. Examination of the cored sections available across the Kirkwood—Sundays

River formational boundary in the basin centre (borehole CO 1/67) and towards the

margins (boreholes AD 1/68 and PA 1/68) suggests there is a relatively rapid gradation in

depositional environment from fluvial to hyposaline to near-normal marine over about

100 m of vertical section in all three sections. Similar rates of change of depositional

environment also seem to occur in the other cuttings borehole sections, but unfortunately

cavings variably obscure the picture.

Comparisons of well log correlations with the foraminifera interval zonation in the

lower Sundays River Formation proposed herein suggest an essential concurrence

between the two. Both studies were undertaken without knowledge of the other (Venter

1972a and Leith 1975—on the well logs; McMillan 1980 to 1992—on the foraminifera),

so that no attempt has been made to effectively merge the two. It can be seen that there are

particularly clear differences in the two correlations in the SH 1/74 section, and these

differences remain unresolved (Fig. 7). Fewer log markers have been defined in the upper

Kirkwood Formation, but these again reflect the same parallel trends seen in the Sundays

River Formation. .

Detailed examination of the fully-cored CO 1/67 sequence (Figs 4, 81) across the

Kirkwood—Sundays River formational boundary indicates that the appearance of normal

marine conditions in the northern Algoa Basin over the Kirkwood surface was rather more

erratic than previously supposed. Red beds with minor greens range up to 3 416 ft, above

which is a greenish interval that is probably non-marine in depositional environment. A

short phase of shallow marine conditions at 3 356 ft, marked by abundant agglutinated

foraminifera (mostly Ammobaculites and Haplophragmoides) is followed by an

essentially regressive phase (3 350 to 3 311 ft). Environments of this interval are

estuarine, sediments are generally greenish-grey in colour and contain Miliammina

latrobei sp. nov. exclusively. These marine-influenced events (3 356 to 3 311 ft) fall

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 13

within an interval of poor high-gamma response (see Fig. 4, and for areal extent, Fig. 9).

This is interpreted to indicate a minor episode of tectonic warping, leading to dislocation

of river catchment areas and consequent trapping of coarser clastic bed load on land,

followed by an abrupt, short-lived increase in subsidence rate. This event is so

discontinuous that it clearly cannot be considered a marine condensed section. Between

3 311 and 3 256 ft there is no microfauna and only rare gastropods occur, which may

suggest that this portion of the section accumulated in either riverine or estuarine

conditions. Above 3 256 ft the first consistent shallow marine assemblages appear and,

though very variable at first, become abundant and diverse above 2 957 ft.

The depth of the unconformity postulated by Winter (1973: 26) and McLachlan &

McMillan (1976: 199, 206) on the basis of wireline log data does not correspond with the

first appearance of marine conditions at 3 356 ft. The compaction break was identified at

3 373 ft (1028 m) (Winter 1973) or 3 368.5 ft (1 027 m) (Winter 1979, figs 4, 6) in

CO 1/67, which appears to be just below the highest incontrovertible red claystones. It is

evident that this transgressive episode over red beds occurs widely, and can be seen in

borehole PB—A1 at 2 467 ft (752 m) in Pletmos Basin (see McLachlan et al. 19765) and in

the offshore Algoa Basin in borehole Hb—D1 (see Fig. 2). The transgression was probably

induced by abrupt tectonic subsidence of the northern rims of these basins. In the

southern, offshore Algoa Basin, the Late Jurassic to Early Cretaceous succession is

generally marine throughout, and a transgression is not seen, even though depositional

environments are rarely deeper than inner shelf, and usually only transitional or marginal

marine. However, severe planation on the 6At1 surface has mostly removed beds coeval

to the Sundays River Formation (see McMillan et al. 1997) in the offshore Algoa Basin. In

the clayier, more distal shelf sections seen in the southern Gamtoos Basin, diverse

foraminifera faunas occur across the boundary equivalent in time to the base of the

Sundays River Formation (identified seismically as horizon J1), but a major change

occurs in the species present. Underlying beds dated as Early Valanginian are

distinguished by the distinctive informal species ‘fat Lagena sp.’ (see McMillan et al.

9 7 pieer3)):

In all cases in the present study, the position of the top Kirkwood Formation is placed at

the first appearance down-hole of red beds, following Winter’s (1973) interpretation, as in

Figures 2, 9 and 10.

PREVIOUS WORK ON FORAMINIFERA OF THE

SUNDAYS RIVER FORMATION

Early studies

Earliest work on the foraminifera of the onshore Algoa Basin was undertaken by Union

Oil and P. Bronnimann, then with Paleolab. No details are available of these unpublished

studies, except for the comments of Rigassi (1968: 14) who, basing his conclusions on this

work and additional studies by palaeoconsultants, attempted a foraminifera zonation of

the Sundays River Formation into five units. Data were derived essentially from outcrop

samples, together with samples from fully-cored borehole CO 1/67, at that time still

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and Brenner & Oertli (1976) with Valicenti & Stephens (1984).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION [5

drilling. This zonation relied heavily on the Late Cretaceous Epistomina zonation

established in Zululand by Smitter (1957), but its use for the Early Cretaceous rocks is

erroneous. Although some of the foraminifera names employed by Rigassi (1968) have

persisted, in general terms his zonation has proved to be unworkable. The age of the

Sundays River Formation at this time was considered to range between Valanginian and

Aptian—Cenomanian. However, two years later, Rigassi (1970: 18) reported that

foraminifera, ostracod, bivalve and cephalopod assemblages from the CO 1/67 borehole

indicated a Valanginian to Early Hauterivian age, but no further comments were made on

foraminifera zonation schemes.

At about the same time, H. M. Beer (February 1968) and E. M. Beer (December 1968)

reported first on proposals, and secondly on results of surface sampling from the Sundays

River Formation. Some 162 samples were examined, most of which were derived from

outcrops in the Sundays, Coega and Swartkops River valleys, together with a number

from the Nanaga area. Foraminifera faunas recovered consisted essentially of

agglutinated forms, and notable species recognized included Ammobaculites aequale

(Roemer) and Astacolus gibber Espitalié & Sigal.

Between 1967 and 1971 the majority of the deep drilling of the onshore Algoa Basin

was undertaken, and a much clearer picture of the Sundays River Formation and its

foraminifera emerged. Unpublished reports on the micropalaeontology of most of these

boreholes were available to the author and provided a foundation for this study: CO 1/67

(Maync 1969b); CK 1/68 (Maync 1969a); AL 1/69 (Maync 1970); AL 1/69 and CO 1/67

(Church et al. 1970); AL 1/69 (Roveda 1970); CO 1/67 and AD 1/68 (E. M. Beer 1970);

CO 2/70 (Bagnall et al. 1971a); NA 2/70 (Church et al. 1971); ST 1/71 (Bagnall et al.

19715); BR 1/71 (Bagnall et al. 1971c); AD 1/68, CO 1/67, CO 2/70, AL 1/69 (H. M. Beer

1971); KE 1/71 (Bagnall et al. 1971d); SV 1/71 (Bagnall et al. 1971e); CO 1/67 (Bagnall

et al. 1971f); VO 1/71 (Bagnall et al. 1972a); CO 3/71 (Bagnall et al. 19726); NA 3/70

(Church et al. 1972); and CO 1/67, CO 2/70, CO 3/71, AD 1/68, AL 1/69, VO 1/71 and

KE 1/71 (E. M. Beer 1973). However, only the reports by E. M. Beer (1970) and Rigass1

(1970) contain illustrations of a few identified species. Compilations of these data have

been undertaken by Venter (1971, 19726), H. M. Beer (1971) and Bagnall et al. (1972c).

Summaries of the various early biozonations proposed are shown in Figure 5.

The compilation work of Bagnall et a/. (1972c) concluded that microfaunas of the

Sundays River Formation were not varied enough to allow for biozonation. Attempts were

made to correlate abundance peaks of particular foraminifera species or groups

(calcareous/agglutinated ratios in particular), and of types of macrofaunal debris, with

some success. Eight biozones were recognized, based on relative occurrences of

foraminifera, and on calcareous/agglutinated ratios. Using borehole sections KE 1/71 and

CO 2/70 as ‘type-sections’, Bagnall et a/. (1972c), from a study of all the microfaunal

data, recognized four periods of open marine conditions interspersed with four periods of

restricted marine conditions within the Sundays River Formation. They were able to

identify all eight biozones only in the depocentre of the basin (AL 1/69 area), but were

unsure of the extent of the later biozones towards the basin margins. The most distinctive

biostratigraphic horizon recognized at this time was based on the first down-hole

16 ANNALS OF THE SOUTH AFRICAN MUSEUM

appearance of the ostracod Cytherella sp. | or Cytherella ‘oblique’ (later formally named

C. algoaensis by Brenner & Oertli (1976)), but no age implication was yet possible from

this horizon.

In their attempts to obtain an age for the Sundays River Formation, Bagnall et al.

(1972c) noted that comparison with European foraminifera faunas tends to indicate a

Neocomian age. Comparison with foraminifera from the Majunga Basin, Madagascar

(Espitalié & Sigal 1963) indicates rather a Portlandian to Valanginian age. In this regard,

particular mention was made of the species Astacolus microdictyotos Espitalié & Sigal,

which ranges from Portlandian to Valanginian in the Majunga Basin and occurs through

most of the Sundays River Formation. A Neocomian age was concluded, with a

possibility of Valanginian alone; however, Bagnall et a/. (1972c) felt that a Late Jurassic

age could not be entirely ruled out.

Venter (1971, 19725) subdivided the Sundays River Formation into seven biozones,

based on foraminifera identified in the various reports completed to that time. These

foraminifera biozones show some similarity to those of the Bagnall et al. (1972c) study,

but several aspects of his correlation are now evidently anomalous. All biozones were

recognized in all but the most marginal holes (AD 1/68, BR 1/71). Of particular note was

the apparent overstep of biozone 3 on to biozone 5 (numbered from the top), and the

wedging out of biozone 4 1n the BR 1/71 area and, to a partial degree, in the VO 1/71 area.

In contrast, H. M. Beer (1971), studying the results of four boreholes, recognized four

sedimentary cycles within the Sundays River Formation that were associated with

particular foraminifera and ostracod species. All four cycles occur in the basin axis

(AL 1/69), with a progressive loss of the upper-most cycle 4 and condensing of lower

cycles | and 2 towards the basin margin (AD 1/68).

E. M. Beer (1973) identified four foraminifera biozones, the older two of which were

considered Late Valanginian in age, and the younger two as Hauterivian. The

Valanginian—Hauterivian boundary identified by E. M. Beer is markedly higher in the

sequence than the Cytherella algoaensis horizon subsequently utilized to mark the

boundary by Brenner & Oertli (1976). Of the four biozones, the basin margin borehole

AD 1/68 intersected only the lowest biozone D, whereas the basin axis holes AL 1/69,

KE 1/71 and CO 2/70 intersected all four. The present study is in general agreement with

this interpretation. E. M. Beer (1973) made no comments on the implications of an erosive

upper surface to the Sundays River Formation. ;

Other microfaunal work on the Sundays. River Formation has concentrated on the

taxonomy of the ostracod assemblages, different aspects of which have been examined by

Dingle (1969) and Valicenti & Stephens (1984), working on outcrop material, and

Brenner & Oertli (1976), who concentrated on the deep borehole sections. An analysis of

the foraminifera species of a single clay sample from Coega Brick Pits was reported by

Meiring (1973). Palynological studies have been undertaken by Scott (1971, 1976) on

northern borehole CK 1/68, but the majority of palynological work on other boreholes

remains in unpublished reports of SOEKOR.

Ostracod research has tended to concentrate on the taxonomy of the assemblages:

age-dating has been rather imprecise. Brenner & Oertli (1976: 477) concluded that the

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 17

sequence was of Valanginian and Hauterivian age. They proposed that the ostracod

Cytherella algoaensis be utilized as a marker for the Valanginian—Hauterivian boundary,

based on its first down-hole appearance (local extinction point). Work from foraminifera

studies tends to confirm this subdivision of the Sundays River Formation, if Reinholdella

valendisensis (Bartenstein & Brand) and Reinholdella hofkeri (Bartenstein & Brand) can

be considered reliable down-hole markers for the top of the Valanginian.

Later work

Later foraminifera work has concentrated on other South African outcrops and

borehole sections of the same age as the Sundays River Formation. McLachlan ef al.

(19765) detailed the microfaunas (foraminifera and ostracods) of the Brenton Formation

at its outcrop along the banks of Knysna Lagoon, and of the nearby offshore borehole

PB—A1: forty-four foraminifera species, one new, were recognized in rocks equivalent in

age to the Sundays River Formation. Subsequently, both the Brenton and PB—A1 material

has been extensively re-examined, and a much larger number of species is now known

from the Brenton outcrop in particular. Furthermore, it has proved possible to recognize

much the same foraminifera biozonation in the PB—A1 section as that described herein for

the Sundays River Formation, and a correlation of the two sequences, with Brenton and

Mngazana, is now possible (see Fig. 8). Revisions of the Brenton and PB—AI article,

together with some additions, are included herein under the relevant foraminifera species

in the systematic section. Additional work on the Brenton Formation foraminifera has

been detailed by E. M. Beer (1972) and Stapleton & E. M. Beer (1977).

The Brenton Formation was regarded as Late Valanginian in age, equivalent to the

oldest part of the ‘Sundays River Formation’ in PB—A|I and of the true Sundays River

Formation in the northern Algoa Basin, a correlation that is still regarded as correct.

McLachlan et al. (1976b: 348) noted that the seismic horizon ‘C’ (now IAtl

unconformity) was originally considered to lie at the top of the lower sandy portion of the

Sundays River Formation equivalent in PB—A1. Despite their suggestion that 1Atl was

more likely present at the top of the Sundays River Formation equivalent in PB—A1, it is

now clear, from both improved seismic and microfaunal data, that the 1 Atl unconformity

does in fact lie at the top of the sands at 480 m below K.B., and thus within the Sundays

River Formation equivalent. Further offshore in Pletmos Basin, as at the Ga—A boreholes,

1Atl is compounded with 6At1 and the upper Sundays River Formation equivalent, of

latest Valanginian and Hauterivian age, 1s missing.

In the northern Algoa Basin, the stratigraphic horizon of 1At! can be located using

foraminifera, but its exact seismic position cannot be determined. Both seismic sections

and electric borehole logs from this onshore area have been of rather poor and variable

quality. By comparison with PB—A1 and other offshore borehole sections, the 1 At]

unconformity must lie almost at the top of the Lenticulina coegaensis sp. nov. biozone

(Late Valanginian biozone Ba). A slight lithological change can be seen here, with clayier

sediments below and sandier sediments above, but the change 1s not a consistent one.

The second rock succession studied for its microfauna, and of similar age to the

Sundays River Formation has been the Mngazana Formation of the Transkei coast

18 ANNALS OF THE SOUTH AFRICAN MUSEUM

(McLachlan et al. 1976a). Sediments from two half-grabens, the Mngazana and Mbotyi —

basins, were studied but the latter yielded only plant debris. The sediments at Mngazana

consist of conglomerates, lignitic sandstones, mudstones and occasional limestone lenses,

but nevertheless, 32 species of foraminifera were obtained. The foraminifera indicate a

Late Valanginian (Biozone B) age, slightly later than that of Brenton. The j |:

chronostratigraphic position given for the Mngazana foraminifera assemblage on Figure 8 |.

is the oldest possible position: the latest position possible is immediately above the 1Atl | |

uncomformity, that is, within the range of the Lenticulina coegaensis sp. nov. biozone.

Subsequent unpublished work on Mngazana samples has shown that Radiolaria are

very much more abundant than first thought, particularly in the calcareous samples. Most

common are spherical Radiolaria, but dictyomitrid types, and four- and five-armed cross

morphotypes also occur. The specimen originally postulated by McLachlan et al. (1976a) —

as algal (/ncertae sedis A, fig. 18 (no. 23)) 1s almost certainly referable to the radiolarian

genus Praeconocaryomma. Similar forms occur in the Hauterivian to Barremian

Radiolaria assemblage detailed by Bouysse et al. (1983) from the West Indies. In some of

the Mngazana samples, Radiolaria are more common than either foraminifera or |

ostracods. One notable foraminifera to have come from the subsequent re-examination of

Mngazana material is Astacolus microdictyotos Espitalié & Sigal.

BOREHOLE AND OUTCROP MATERIAL

Deep boreholes

The locations of boreholes and outcrops studied are shown 1n Figure 3. Table | gives

location details of deep boreholes. All depths given in this study are depths below Kelly

bushing, sited some 6 or 7 m above ground level on the drilling platform. All 17 rotary

boreholes were examined over a 10-m interval, using cuttings samples. Fully-cored

borehole CO 1/67 was examined for the most part also at about 10 m (30 ft) interval,

although AD 1/68, PA 1/68 and some sections of CO 1/67, especially the

Kirkwood—Sundays River transition, were studied at 6-m (20 ft) or 3-m (10 ft) intervals,

or even less. In some of the rotary holes, short cores had been cut in the Sundays River

Formation: BR 1/71 (1 core), MV 1/79 (2 cores), AL 1/69 (8 cores), SM 1/76 (1 core),

SV 1/71 (1 core), NA 1/69 (6 cores) and CK 1/68 (5 cores). Two of the later boreholes

(NA 3/70, SM 1/76) recovered runs of side-wall cores, some of which also provide, as do

the normal cores, much in situ information. This has been related to the results obtained

from cuttings samples, the latter variably subject to down-hole caving, in order to

optimally interpret the stratigraphic ranges of the foraminifera species encountered.

Complete sets of cuttings, with cores of all the deep boreholes drilled to date in the

onshore Algoa Basin, as well as the CO 1/67, AD 1/68 and PA 1/68 continuous cores, are

held by the Geological Survey at their Silverton depot in Pretoria. The following numbers

of samples were studied during the course of the present work: AD 1/68 (37 samples),

AL-1/69- (201); BR 1/71 (61); CK. 1/68 (190), COmye7 Gas) VCO 70(O)) FeOr vi

(107); CP l/77 (16), KE, 1/7113), MV 1/79.(68), NAS W69N ASO) FINA 2 7 Oates

NA 3/70 (119), PA 1/68 (20), SH 1/7499), SM: 1/76(42).S TP W7 6) SV 7 ings):

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 19

SW 1/08 (0), SW 2/68 (7), and VO 1/71 (121), a full total of 2 022 cuttings, core and

sidewall core samples.

Two boreholes were drilled for testing logging equipment, in the grounds of former

SOEKOR depots. SW 2/68 was drilled adjacent to the south-west side of the former

Swartkops sanatorium building (now demolished). Since the original Swartkops borehole

is believed to be sited beneath the building, the distance between the two borehole sites 1s

negligible. A comparison of lithology tops, such as top of Kirkwood Formation red beds,

shows SW 1/08 and SW 2/68 sections to be virtually identical. Total depth of SW 2/68 is

300 ft (91.5 m). Further north, CP 1/77 was drilled in the Motherwell area: total depth 1s

150 m. Normal cuttings samples, mostly at a 10 m sampling interval, were available from

both holes. Cuttings samples from these two boreholes are held only by SOEKOR at Parow,

Cape Town.

TABLE 1

Localities of deep boreholes studied.

Borehole Farm Latitude Longitude ete ae $0

AD 1/68 Riverside (Addo Drift) 33°335'06"S 25 39'53"E 28

AL 1/69 Platterug 33,41 15'S 25°56'02"E 87.8

BR 1/71 Brak River Outspan 33°42'16"S 25°41'00"E 90.48

CK 1/68 Commando Kraal 33° S1'08"S 2) 32'00"E 67

CO 1/67 Colchester 33°41'12"S 25 47°32°E 2)

CO 2/70 Ingleside 33°40'13"S 25° 47'22"E 104.4

CO 3/71 Vetmaakvlakte 33°40'57"S 25°47'41"E 8.9

Clea Wiig Coegaskop 33°47'14.5"S 25° 35/4 1E 86

KE 71 Kenkelbosch Outspan 33°39'40"S 25.52 lose 86.71

MV 1/79 The Downs (Melville 308) 33°45'15"S 25, A533. 6 62

NA 1/69 Nanaga 33°33'40"S Z5 57 10"R 331

NA 2/70 Moria 33°34'12"S ZS SD 225 EB 205.22

NA 3/70 Buffelshoek 33°34'15"S 25°95 308 186.83

PA 1/68 Gorah 33°28) 22)'S 25. 33 320 307

SH 1/74 Ingleside 215 33339 12"5 25. 45'19"E 9

SM 1/76 Springmount 33°41'17.04"S 26 0221.85" E 80

ST 1/71 — Saltpan 33°46'30"S 25. 32 00"E 115.28

SV 1/71 Sea View 33°39'12"S 26°06'06"E 94.2

SW 1/08 Swartkops 33°52'47"S 25° 30'43"E Gal

SW 2/68 Swartkops 33° D2 47"S 25330435 6.1

VO 1/71 Vetmaakvlakte Oos 33°42'10"S 25 50'26"S 6.6

A number of the rotary, cuttings holes are very clean and little affected by down-hole

caving: particularly noticeable in this respect are AL 1/69 and MV 1/79. Boreholes

CO 2/70, CO 3/71, VO 1/71, and KE 1/71 suffer particularly acutely from down-hole

caving. In particular, mud circulation losses in CO 2/70 have led to small, poor quality

cuttings samples throughout the interval 274 to 530 m that are clearly not representative:

this would seem to be the most affected borehole section of all those studied.

20 ANNALS OF THE SOUTH AFRICAN MUSEUM

It should be noted that some of the early boreholes (CO 1/67, AD 1/68, PA 1/68,

CK 1/68, AL 1/69, NA 1/69) and part of SM 1/76 were originally logged in feet, whereas

later holes were logged in metres. For those that were drilled in feet, all bagged cuttings |

samples and cores, and the lithologs, were marked up in feet. For ease of relocating |

specific samples and depths, the original imperial measurements have been referred to in |

this study. :

The ostracods from the deep boreholes studied by Brenner & Oertli (1976, table 1) |

were from two different sets of processing. Most of their material was derived from

microfaunal processing by Dr E. M. Beer at the Geological Survey, Pretoria. Subsequent

processing (of the three NA boreholes, and PA 1/68, SV 1/71 (Sea View) and SH 1/74)

was undertaken at SOEKOR in Johannesburg. Thus, the foraminifera described in the

present study are from the same set of samples, and processed in the same manner as those

few ostracods detailed by Brenner & Oecertli (1976) from the above six boreholes.

However, most of their ostracods, from the other 10 holes, can only be related indirectly to

the results of the present work, as they originate from a different sample set, often at

different depths, and with different processing methods (soaked overnight in water, and

sometimes hydrogen peroxide was used for indurated samples—E. M. Beer (1970)).

Shallow boreholes

Between August 1970 and June 1971 over 34 shallow boreholes were drilled through

the Pliocene—Pleistocene upper Algoa Group and into the topmost Sundays River

Formation. Locations of the boreholes containing cores used in this study are shown in

Figure 3. These shallow holes were drilled for geophysical purposes and, in general, no

rotary cuttings were collected. However, a substantial number of short cores were cut in

the topmost Sundays River Formation, and these have been sampled and processed for

microfaunal elements. The 39 samples are very clean, being from cores, and since it has

been possible to selectively sample claystone intervals, abundant, well-preserved

microfaunas have been found frequently. However, the precise sampling of these cores

tended to highlight the same problem seen in attempting to relate the results from cored

borehole CO 1/67 with data from adjacent cuttings boreholes. The rotary samples are

essentially a mix of lithologies intersected over a 10-m interval, and microfaunas from

such samples thus tend to be ‘smoothed’. Core samples, in contrast, yield a microfauna

from a discrete 5-cm or thinner interval, so that in the cores from both the deep boreholes

and the shallow holes, microfaunas tend to be much more variable from sample to sample

than they are 1n adjacent cuttings holes. The shallow boreholes were logged, and the cores

measured out in feet. Samples thus bear imperial depths, for the same reasons as given for

the deep non-metric boreholes. These cores are held at the Geological Survey, Silverton,

Pretoria.

Because of the short core-sample intervals in the Sundays River Formation, the

foraminifera assemblages from the shallow boreholes have proved difficult to date to a

precise biozone. In most cases this has been achieved from their geographical position

relative to dated tops of the deep boreholes. Table 2 lists the samples and shows their

interpreted ages: some data are incomplete or unclear because of deterioration of these

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 21

cores since drilling. Because of the shallow depth of burial of the topmost Sundays River

Formation, preservation of foraminifera is good, and a number have been illustrated. The

top of the Sundays River Formation, at whatever stratigraphic level, tends to yield the

best-preserved foraminifera tests, where weathering processes have not been intensive.

TABLE 2

Samples studied from shallow boreholes.

Borehole pena Samples studied Base U. j WB) Interpreted

no. depths below K.B. Algoa Gp. — Borehole Biozone

SB 1 Buffelshoek Core 1: 180' L227 184'3 IV

Core 1: 183'6"

SB 2 Buffelshoek Core 3: 263' 130' 266'9" IV

SB 3 Buffelshoek Core 1: 179'6" 130' 2138" Il

Core. 3: 206'

SB:5 Hopewell Core 12 176'6" / 181' 2

Core 12 180!

SB 6 Wicomvale Cored) 70' 120' 179" raul

SB 7 Doornkloof Core 2: 269'3" 192' 283' Il

Core 2: 270'9"

SB 8 Congaskraal Core ?: top / / I

Core: ?: 389° (top)

SB 9A Platterug Core 16-232 6" 252 294' II

Core 1::285'

Core 2; 290

SB 10 Congaskraal Core ?: 360'6" \ / I

Core ?: ?363' (1' from bottom)

SB 13A Tankatara Core 17129! i 182' VII

Core 2: 180'6"

SB 15 Nieuwjaarskop Corei2: 2110’ 183'6" 2366" U

Core 3: 222

Cores: 22>

Core 4: 229"

SB 18 Hopewell Core 3: 302'6" / 310' q

SB 21 Cypherfontein Core 3: 418'6" i 419! Hl

SB 24 Sea View Core 1: 457'6" 3726" 460' Il

SB 25 Sea View Core 1: 796'9" 695' 7170 IV/V

SB 26 No data Core 72378'6" 276" 383' ?

SB27, Sundays River Core 1189" (top) 120' 196'3" IV

mouth Core |: 196'3" (?bottom)

SB 28 Vetmaakvlakte Core I: 188’ 147' 194' VI

Core 1: 193'9"

SB 29 Vetmaakvlakte Core’?7: 218'6" ' / VI

SB 31 Vetmaakvlakte Core 1;,91'6" 20! OF 3” IV

SB 32 Vetmaakvlakte Core 1: 146' 100' 199' IV

Core 1: 148'

Core 2: 192"? (?2' below top)

Core 2: 199"? (?bottom)

SB 35 Doornkloof Core ?: top / i I

ANNALS OF THE SOUTH AFRICAN MUSEUM

Outcrops

Outcrops (Fig. 3, Table 3) have been sampled over a wide area of the Algoa Basin by

Mr I. R. McLachlan and Mr C. Reabow, both of SOEKOR (Pty) Ltd. The majority of

outcrops expose the Late Valanginian—lower part of the Sundays River Formation—and

only the cliff exposures behind Colchester Station reveal the upper, Hauterivian portion.

The Valanginian outcrops expose rocks that vary considerably in their depositional

environment, from hyposaline and transitional (Dunbrody, The Look Out) to middle and ||’

outer shelf (Coega Brick Pits). The outcrops again provide control on the interpreted |

stratigraphic ranges of the foraminifera species recognized in the boreholes, since they

also provide detailed in situ point data and a tie to the macrofossils. The variability of core |

results, discussed above, also holds true for the 122 outcrop samples, for the same reasons. | |

The establishment of a detailed foraminifera biostratigraphy from the boreholes has |

helped achieve a close correlation between the borehole and outcrop sections. More ||

specific detail on the outcrops is provided subsequently in this article (see p. 44).

Processing methods

All samples were processed by standard micropalaeontological methods. All cuttings

were sampled at a standard quantity (250 g) and processed using a Quaternary ammonium

surfactant detergent (Tinegal PAC) of the type described by Zingula (1968). Irregular

quantities of from 250 g to occasionally perhaps 500 g were sampled from the cores and

outcrops. All samples were washed through 150-mesh (106 micron) sieves, and residues

dried and separated into 30-mesh (500 micron), 60-mesh (250 micron), and 150-mesh

fractions for ease of picking. Picking of specimens from processed cuttings samples was

to a standard maximum of 400 foraminifera tests; from cores and outcrop residues the

same procedure was followed, though more were picked in some cases where test

preservation was particularly good (e.g. Coega Brick Pits).

COMPARISON OF SUNDAYS RIVER FORMATION FORAMINIFERA

WITH ELSEWHERE

Increasing research on time-equivalent rocks of the Sundays River Formation in

southern South America has revealed the presence of very similar foraminifera faunas.

The foraminifera of the Sundays River Formation do not compare particularly well with

those of the Majunga Basin, Madagascar (Espitali¢ & Sigal 1963), although a few species

occur in common. There is also only little similarity with the foraminifera of the Speeton

Clay (Berriasian to Aptian) of north-east England and the time equivalent sequences of

north-west Germany. No definite comparison is yet possible with anywhere else in the

world. This is particularly unfortunate in the case of those continents previously

constituents of East Gondwana: India, Australia and Antarctica.

Argentina and Chile

Distinctive foraminifera assemblages have been described to date by many authors

from the Early Cretaceous of southern Argentina and Chile. These include those described

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 23

by Bertels (1990), Kielbowicz et a/. (1983), Malumian & Masiuk (1975), Malumian &

Nanez (1983), Masiuk & Vina (1986a, 19866, 1987), Musacchio (1978, 1979, 1980,

1981) and Simeoni (1985) on Argentinian faunas, and by Martinez & Ernst (1965) and

Cafion & Ernst (1974) on Chilean faunas. Many derive from outcrops where associated

ammonite data are available. However, it appears that the majority of the illustrated

faunas are not very diverse, and generally not as diverse as faunas from time-equivalent

rocks in southern Africa. The reason for this is unclear.

_ Berriasian—Valanginian

Some of the oldest Cretaceous assemblages of foraminifera described to date are those

- from the Springhill Formation of the Bahia de la Lancha area east of Lago San Martin,

Santa Cruz Province, Argentina (Kielbowicz et a/. 1983) and in southern Chile (Martinez

| & Ernst 1965; Canon & Ernst 1974: 46). Ammonites (Jabronella, Neocosmoceras and

_ Delphinella) from the Santa Cruz exposures, described by Riccardi (1977, 1988), suggest

| a Berriasian, or Berriasian to earliest Valanginian age. The foraminifera described by

| Kielbowicz et al. (1983) were determined as Valanginian. Although they compare closely

- to assemblages of the lower part of the Sundays River Formation (Late Valanginian in

_ age), they are also similar to those seen in South African Early Valanginian or latest

_ Berriasian marine rocks distal of the Kirkwood Formation red beds. The presence of

_ Lenticulina nodosa (Reuss) and Dorothia australis sp. nov. (as Marssonella kummi

_ Zedler) indicate an age for the Springhill Formation of no older than latest Berriasian, in

— South African terms. This is reinforced by the occurrence of Planularia tricarinella

_ (Reuss) (as Cristellaria tricarinella) in the Chilean Springhill Formation (Martinez &

_ Ernst 1965), a species present in the latest Berriasian to Early Valanginian (though also

_ early Barremian) of South Africa. Also notable in the Springhill assemblages detailed by

~ Kielbowicz et al. (1983) is the finely, uniformly reticulated, surface-ornamented

_ Astacolus microdictyotos Espitalié & Sigal tests, also seen in examples from the

- Portlandian to Early Hauterivian of South Africa. Lacking in the Springhill Formation is

A. gibber Espitali¢ & Sigal, again suggesting a pre-Late Valanginian age. It should be

_ noted, however, that offshore seismic work by Carbone (1990) indicates the Springhill

_ sandstones and Pampa Rincon claystones to be interbedded, so that the Springhill

_ Formation is evidently a diachronous sandstone facies (see also Biddle et a/. 1986).

Valanginian—Hauterivian

From the Pampa Rincon Formation of Tierra del Fuego and Estratos con Favrella of

~ southern Argentina and Chile, regarded by Malumian & Masiuk (1975) as Valanginian—

_ Hauterivian, Pseudopolymorphina martinezi (Canon & Ernst), Lenticulina nodosa and

Astacolus gibber are found to be common. Unfortunately, no mention is made by

~ Malumian & Masiuk (1975) of associated macrofaunal elements such as ammonites,

since their study was based on borehole cuttings. Natland et al. (1974) reported on

| Favrella ammonites in outcrops of Rinconian age (probably Hauterivian rather than

Oxfordian to Kimmeridgian as originally defined). Riccardi (1988) has regarded the

Favrella faunas as of Early Hauterivian to earliest Barremian age.

24 ANNALS OF THE SOUTH AFRICAN MUSEUM

Foraminifera assemblages of about the same age have been described from the

Katterfeld Formation of Chubut, Argentina (Masiuk & Vina 19865, 1987), dated as Early

Hauterivian, and from the Agrio Formation of Neuquén, Argentina (Musacchio 1978,

1979, 1981; Simeon 1985; Masiuk & Vina 1986a, 19865), dated as Late Valanginian or

Early Hauterivian to Late Hauterivian or Early Barremian. Similarities occur with the ©

Sundays River Formation but generally only with individual described species rather than |

whole assemblages. Little comment is made on microfaunal—macrofaunal associations by |

the authors, although Masiuk & Vina (1986a) reported Crioceratites andinus (Gerth) in

association with one foraminifera assemblage studied from the upper part of the Agrio |

Formation, and Olcostephanus cf. atherstoni (Sharpe) and Olcostephanus curacoensis

Weaver with a different, lower, assemblage. The former assemblage is regarded as Late

Hauterivian, the latter as Late Valanginian in age. The latter seems to be the only ||

Argentinian one published to date that is clearly associated with Olcostephanus

ammonites.

Musacchio (1979) determined the presence of two foraminifera assemblages in the |

Hauterivian of the Agrio Formation. The Early Hauterivian assemblage appears to be very |

much the poorer, and none of the foraminifera species appears to be age diagnostic:

ammonites in association with this assemblage include Holcoptychites neuquensis

(Douvillé) and Pseudofavrella spp. The second, Late Hauterivian assemblage contains |

diverse foraminifera. However, the presence of hedbergellids (Musacchio 1979, pl. 5 |

(figs 20, 25)) strongly suggests that later Early Barremian foraminifera are also |

represented in this second assemblage, as the illustrated examples are very similar to

Praehedbergella sigali (Moullade), as understood in South Africa. The Late Hauterivian |

assemblage is associated with diverse species of Crioceratites ammonites. It seems

possible that the foraminifera described by Masiuk & Vina (1986b) from their upper |

Agrio Formation sample, and those described by Musacchio (1979) from Site 5 (Rio |

Agrio), are from the same, or almost the same locality. Just to the east of this site, at Agrio |

del Medio are Early Barremian rocks with Plesiospitidiscus and Spitidiscus (Leanza & |

Wiedmann 1992). |

Hauterivian—Barremian

Malumian & Nafiez (1983) illustrated a foraminifera assemblage from the upper Rio

Mayer Formation of Santa Cruz province, southern Argentina, which is dominated by

Epistomina caracolla (Roemer) s.l. This assemblage is very similar to South African ones

from an organic-rich, high-gamma claystone interval developed locally on the continental

shelf in the Bredasdorp and Pletmos Basins and at the base of the Cretaceous drift

succession in Zululand, and regarded on foraminifera grounds as later Early Barremian in

age. Malumian & Najfiez (1983) reported the presence of Hatchericeras patagonense

Stanton and other ammonite species with the studied sample, again suggesting an Early

Barremian age (Riccardi 1988). Bertels (1990) also studied the Rio Mayer Formation,

apparently the same Bahia de la Lancha, Lago San Martin section from which Kielbowicz

et al. (1983) studied the Springhill Formation foraminifera. The assemblage described by

Bertels (1990) from the basal Rio Mayer Formation clearly shows close similarities with

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 7)

the foraminifera from the upper Sundays River Formation, as Lingulina trilobita sp. nov.,

Paralingulina hexacarinata (Espitalié & Sigal) and the Psilocitharella kochii

(Roemer)—P. arguta (Reuss) group mutually occur. Overlying beds in the Rio Mayer

Formation contain a poor fauna with Lenticulina nodosa (Reuss), that may prove to be

Barremian and Early Aptian in age. However, the more diverse assemblages recognized

by Bertels (1990) in the upper third of the Rio Mayer Formation, characterized by Tritaxia

sp. aff. 7. pyramidata Reuss and Glomospira charoides Jones & Parker, are clearly unlike

any Barremian—Early Aptian assemblages known in South Africa, and must be of Late

Aptian (to ?Early Albian) age. These species do occur widely in the South African Late

Aptian and Albian, primarily in slope environments. From essentially the same outcrop,

Favrella species of ammonites occur in the basal Rio Mayer Formation, suggesting a

Hauterivian age, whereas in the upper part of the formation Aptian and Albian species

occur (Aguirre Urreta 1986; Riccardi 1988).

DSDP Site 249, Mozambique Ridge

Riegraf (1989) described Valanginian—Hauterivian foraminifera assemblages from

cores 26-31, DSDP hole 249, leg 25, in the south-western Indian Ocean. This section

unconformably overlies vesicular amygdaloidal glassy basalt. The assemblages are

diverse, and contain a number of species in common with those of the Sundays River

Formation, but also a number of forms that suggest these basal sediments intersected in

hole 249 are later in age than the uppermost Sundays River Formation, later than

Hauterivian. Although Lingulina mngazanaensis sp. nov. (as Lingulina sp. B),

Lenticulina nodosa (Reuss), Astacolus microdictyotos Espitalié & Sigal, and Citharina

harpa (Roemer)—C. pseudostriatula Bartenstein & Brand occur in common, the presence

of Planularia tricarinella (Reuss) (as Palmula crepidularis (Roemer)), Gavelinella

barremiana Bettenstaedt, and, possibly Pseudopolymorphina ‘carinata’ (as Globulina

bucculenta (Berthelin), but only plate 2 (fig. 18) of Riegraf 1989) suggest a later age.

Planularia tricarinella and Pseudopolymorphina ‘carinata’ occur in association in the

later Early Barremian of the southern offshore (McMillan et a/. 1997) and in the basal drift

Cretaceous of the Zululand onshore boreholes, and for this reason the DSDP 249 assem-

blages detailed by Riegraf (1989) are considered to be essentially of Barremian age rather

than Valanginian—Hauterivian. It is as yet not clear 1f Pseudopolymorphina ‘carinata’ is

synonymous with P. martinezi Canon & Ernst, known from southern Chile and Argentina

(Canon & Ernst 1974: 75, pl. 2 (fig. 8a—c); Malumian & Masiuk 1975: 594, pl. 1

(fig. 2a—c), pl. 2 (fig. 1)), since the degree of inflation of the later chambers is seemingly

much greater in the South American than in the South African specimens. Other features

of these tests, however, such as the apical spine, the acute, often carinate periphery and the

manner in which the test tapers up to the aperture, are all remarkably similar.

AGE OF THE SUNDAYS RIVER FORMATION

Comparisons between the foraminifera species of the Sundays River Formation and

those of several regions elsewhere in the world have been made above, but precise datings

26 ANNALS OF THE SOUTH AFRICAN MUSEUM

of the Formation using foraminifera have proved to be rather difficult to achieve. A

summary of the following data is shown in Figure 6. In the northern Algoa Basin, the most

complete borehole section of the Sundays River Formation is that of AL 1/69. The latest

assemblages (Biozone I) of AL 1/69 do not contain any of those benthonic foraminifera

that herald the appearance of the calcite-walled Rotaliina. In Europe, Gavelinella

sigmoicosta (Ten Dam) is the precursor of the Gavelinel/a lineage, and this appears 1n the

latest Hauterivian or earliest Barremian (Bartenstein & Bettenstaedt 1962; Fletcher 1973;

Bartenstein & Kaever 1973; Malapris-Bizouard 1974). Subsequently, in the Early

Barremian, the Conorotalites lineage commences (Bartenstein & Bettenstaedt 1962). -

Foraminifera faunas in the highest Sundays River Formation are diverse, and there is no |

reason to suppose that early species of either Gavelinella or Conorotalites were prevented

in some way from inhabiting the Algoa Basin embayment. At about the Hauterivian—

Barremian boundary, hedbergellid planktonic foraminifera begin to appear in the

Mediterranean region (Moullade 1974), and there is a marked diversification of the group

at this time (Banner & Desai 1988, fig. 1), and an extension of geographic range, from low

western latitude-restricted to low and high latitudes. Thus, rock sequences dated as later

Early Barremian (post 6At1) in the southern offshore Pletmos and Bredasdorp basins —

contain the earliest planktonics seen in South Africa: Gorbachikella kugleri (Bolli) and,

less commonly, Praehedbergella sigali (Moullade), and some Gavelinella spp. also

occur. This later Early Barremian planktonic event has also been recognized in the North

Sea (King etal. 1989, fig. 8.5). In contrast, planktonic foraminifera are absent throughout

the Sundays River Formation and its time equivalents around southern Africa, in all |

marine depositional environments studied.

Comparison with benthonic foraminifera faunas from the oldest marine beds of the

Zululand onshore boreholes reveals some species in common with the Sundays River |

Formation, but these are mostly species that range through much or all of the Sundays

River succession. These oldest Zululand marine sediments are regarded as of much the —

same age as the (?Late) Barremian outcrops, detailed by Kennedy & Klinger (1975) as

containing crioceratitid and other ammonites. More recently, Kennedy & Klinger (1990)

have reported Hatchericeras patagonense Stanton from these outcrops, suggesting an ;

earlier Barremian age. As noted above, occasional floods of Epistomina caracolla —

(Roemer) s.l. occur in the Zululand later Early Barremian, that have analogues in the

Pletmos and Bredasdorp Basins, and in the Rio Mayer Formation of Argentina (Malumian —

& Nafiez 1983): these Epistomina are morphologically distinct from those of the Late

Valanginian and Hauterivian. Lenticulina nodosa (Reuss), Astacolus gibber Espitalié &

Sigal, A.microdictvotos Espitalié & Sigal, and forms similar to Reinholdella valendisensis

(Bartenstein & Brand) also occur in the Zululand later Early Barremian. However, other —

aspects of these benthonic foraminifera assemblages tend to be unlike those of the

Sundays River Formation, particularly the agglutinated, Pseudopolymorphina,

Pseudonodosaria and other nodosarid species. Despite the rather ambiguous state of

available data, it is felt that the highest Sundays River Formation beds are slightly older

than the oldest of the later Early Barremian rocks of Zululand, and are latest Hauterivian

in age.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 27,

The lower third of the Sundays River Formation is characterized by the presence of the

two benthonic aragonitic foraminifera Reinholdella valendisensis (Bartenstein & Brand)

and R. hofkeri (Bartenstein & Brand), which in north-west Europe range from the basal

Berriasian to the Valanginian—Hauterivian boundary (Fletcher 1973; Bartenstein 1976a,

1976b). These two species first appear down-hole near the first down-hole occurrence of

Cytherella algoaensis Brenner & Oertli, and have been taken to mark the foraminiferal

top of the Valanginian in the Sundays River Formation. However, more recent Northern

Hemisphere records of the species suggest that R. valendisensis may range locally as high

as Late Hauterivian (Jansa et al. 1980) and R. hofkeri as high as Late Barremian (Ascoli

1976) off the Atlantic coast of Canada. For the present study, these two species are

retained as local index fossils for the Valanginian. It is intriguing how very rarely these

species of Reinholdella have been reported in the literature from the Early Cretaceous

succession of Argentina (only Masiuk & Vifia 1986a have identified R. hofkeri), when

compared with their widespread distribution around South Africa.

The presence of Trocholina infragranulata Noth in the outcrops at Brenton and

Mngazana, in association with assemblages that compare very closely to those of the

lowest Sundays River Formation, suggest that the Formation at oldest is of

mid-Valanginian age (see Bartenstein 19765). Southern offshore boreholes drilled by

SOEKOR indicate that Astacolus gibber Espitali¢é & Sigal ranges no further down section

than mid-Valanginian (base Sundays River Formation equivalent). This species occurs

through almost all of the Sundays River Formation. In the offshore Pletmos, Gamtoos and

Algoa basins, the Valanginian can be divided into two: a late Valanginian portion, in

which foraminifera faunas are very similar to those of the lower Sundays River

Formation, and an early Valanginian portion, in which the foraminifera are mostly

dissimilar. For all these reasons, the oldest Sundays River Formation is thus regarded as

being of mid-Valanginian age.

LITHOSTRATIGRAPHY

As mentioned previously, the stratotype of the Sundays River Formation was

designated the Zoetgeneugd Cliff outcrop by Winter (1973); a subsurface stratotype was

also designated: borehole CO 1/67 from 30 m to | 028 m (preferentially 100 ft and

3 373 ft, since the borehole was drilled, and the core marked up in feet). However, apart

from the preliminary lithological work of Venter (1972/), and the comments on the

ostracod faunas by Brenner & Oertli (1976) and Valicenti & Stephens (1984), no precise

attempt has been made to relate the surface and subsurface stratotypes. Much of the

lithology of the Sundays River Formation is composed of repetitive claystones and

sandstones, both variably silty, and variable in thickness. A typical interval of the upper

Sundays River Formation in CO 1/67 (Biozones VII to VIII) 1s illustrated by Winter

(1973, fig. 2). Because of the repetitive nature of the Sundays River sequence, lithological

marker beds are rare, and subdivisions can be made most easily only on palaeontological

and log/seismic characteristics.

Venter (1972a, 1972c, 1972d, 1972f, 1972g) subdivided the Sundays River Formation

ANNALS OF THE SOUTH AFRICAN MUSEUM

AMMONITE DATUMS

> SIGNIFICANT SPECIES

AGE

HATCHERICERAS

PATAGONENSE

“R__ APPROXIMATE BASE OF

ZULULAND SUCCESSION

eit

APPROXIMATE TOP OF

SUNDAYS RIVER FORMATION

"ES

SOLOALIIGOYSIN SNIOIVLSV

y¥y38si9 SNIOOVLSV

—_ VLYNIEVS,, VNIHdYOW A1O0doanaSd

ld¥3719Ny VTTANIHIVEHOS

Sa Veal

NVINSAYYVa

el Ves

NVIAIYSLAVH

OLCOSTEPHANUS

SPECIES

SUNDAYS RIVER FORMATION

K__ APPROXIMATE BASE OF

VLVINNVY VNITOHDONL

SISNAVOS IV V 11S Yd¥3SHLAD

IYSNSOH V1130 10H Niau

SISNASIGNA TVA ;V11S0 1OHNI3ZY

Z dNOUD SOLOALOIGOYDIN SNIOOVLSV ©

Cm oe 6 oe i, ee et

TS VSOGON VWNITINOILN|AT

good

LLLLLLLL Lo

VS VIIOIVEVS VNINOLSId3

S3ONVY

Nvadouna,

aly AIYV4A Sy ANYVA

NVINIDSNV IVA NVISVIYNS4

Figure 6.

Interpreted stratigraphic ranges of age-diagnostic foraminifera species

utilized in establishing the age-span of the Sundays River Formation.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 29

into four members, based on the CO 1/67 fully-cored stratotype section: from bottom to

top these are the Amsterdamhoek, Soetgenoeg, Addo and Vetmaak Members. Their

- relationships have been shown by Winter (1979, fig. 6). A number of smaller-scale rock

units were also recognized by Venter (1972c) that show distinctive characteristics in the

CO 1/67 stratotype. The four members were determined in other deep borehole sections

~ by Leith (unpublished data) during the early 1970s, when exploration drilling was at its

height. Since then, with declining economic interest in the onshore Algoa Basin, no

further lithostratigraphic work has been undertaken on the type Sundays River Formation

within SOEKOR. Indeed, with the increasing realization of the complex variations evident

in depositional environment, and consequent variations in lithotype, in synrift and

transitional rift rocks of the same age from the different offshore basins (Bredasdorp,

Pletmos, Gamtoos and Algoa), the whole question of formalized lithostratigraphy has

been avoided in SOEKOR hydrocarbon exploration activity.

The four Members recognized by Venter (1972c) and Winter (1979) have been

accorded formal status (SACS 1980: 579). As pointed out by Winter (1979: 188),

however, almost all other boreholes drilled to date in the onshore part of the Algoa Basin

are rotary, cuttings holes, so that correlation must be achieved either via electric log

markers, or via biostratigraphy. Electric log correlations were attempted by Venter and

Leith in the early 1970s, but again the repetitive, cyclical nature of the Sundays River

Formation has led to the identification of few clear-cut, distinctive log horizons.

According to Winter (1973: 31) and MacKeith et al. (1976), seismic reflectors too are

often intermittent and correlations between boreholes are thus hindered. ‘Shaling-out’ of

sandstone intervals basinwards also limits any proposed lithostratigraphic scheme. The

electric log correlations shown in Figure 7 are based on a table compiled by Leith in

October 1975, plotted against the microfaunal biozonation described herein. Only those

boreholes in which electric log correlations have been attempted are included. It 1s clear

that although similar trends are evident in both the log and foraminifera correlations,

sufficient difference exists between the two that the boundaries of the four established

lithostratigraphic members cannot be clearly defined across the entire Sundays River

Trough. Similar doubts exist over precise positionings of boundaries of the four

lithostratigraphic members in the various outcrops of the Sundays River Formation.

Furthermore, the use of the four names Amsterdamhoek, Soetgenoeg, Addo and

Vetmaak, based primarily on farm names of outcrops, indicates a stratigraphic

relationship of these outcrops that is not confirmed from this foraminifera study.

Because of the incomplete status of lithostratigraphic subdivisions of the Sundays

River Formation, they have not been considered further in the present study. Much

additional work is necessary to establish the Members defined by Venter (1972c), and

formalized by Winter (1979) and SACS (1980), across the Sundays River Trough, to

determine the Member(s) of the topmost part of the Sundays River Formation in the basin

axis (especially in boreholes KE 1/71 and AL 1/69), and to determine the

lithostratigraphic status, if any, of the five ‘Zones’ of the Amsterdamhoek Member, the

five ‘Zones’ of the Soetgenoeg Member, and the two divisions of the Vetmaak Member

defined by Venter (1972c) in the CO 1/67 cored hole.

SH 1/74

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KEY

ALL DEPTHS BELOW KELLY BUSHING

IN METRES OR FEET (3311').

~ ELECTRIC LOG MARKERS DETERMINED

BY EElimHGliSi7s:

BOUNDARIES OF

BIOZONATION.

FORAMINIFERA INTERVAL

VERTICAL SCALE 1:10 000

Figure 7.

Comparison of the foraminifera-based interval biozonation proposed here with log correlations

(Leith 1975, unpublished) for particular boreholes. No hori

the fit.

ANNALS OF THE SOUTH AFRICAN MUSEUM

C0377)

CO 2/70

zons have been amended to improve

FORAMINIFERA OF THE SUNDAYS RIVE

KEI/7\

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Figure 7 (CONTINUED).

R FORMATION 31

SVI/7I CK 1/68

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GROUP AND

ALLUVIUM

600

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ANNALS OF THE SOUTH AFRICAN MUSEUM

A ee

STAGE } BRENTON | | pB-a At nrerenete MNGAZANA

mot oo ww =

Wott > 1

{

BIOZONE al

Reinholdetia platterugensis

? BIOZONE {BIOZONE I

?? Later Epistomina hechti |Later Epistomina hechti

750

BIOZONE I BIOZONE I

Amphicorynoa pletmosiana Amphicoryna pistmosiana

960!

BIOZONE IZ to Wl BIOZONE IZ

Pseudopolymorphina

colchesterensis

BIOZONE YW

Earty Epistomina hechti

Pseudopolymorphina BIOZONE WZ

coichesterensis Dorothia inglesidensis

BIOZONE WIL

Vaginulinopsis cf. matutina

BIOZONE WE

Later poor zone

Top Reinholdelia v.

«<—___ plettanbdergia

1140°

| BIOZONE Vil to X

BIOZONE IX

Retnhoidelia

valendisensis

plettenbergia

Eoguttulina sp. B.

BIOZONE X BIOZONE X

Dorothia australis Dorothia australis

BIOZONE A

Reinholdelia hofkeri

Reinholdetia valendisensis

BIOZONE A

Rainholdella hofkeri

Reinholdelia vaiendisensis

1500

ARARARARC 1A tt) 1575)

BIOZONE Ba

Lenticulina cosgaensis

BIOZONE Bb on

col

BRICK PITS

Lenticuling coegaensis

Sculptobaculites

goodiandensis

AMSTERDAM -

HOEK AND

WIT. -G.R. Rd.

BIOZONE B

Lenticulina coagcensis

Pre ak OM raat

BIOZONE C BIOZONE C

Poor zone Earlier poor zone

AIREDALE

2250'

BIOZONE D

Astecolus moar ee

BIOZONE D

Miliammine pisces!

BIOZONE D

Astacotus PA joiederd

2487

RED AND GREEN

LITHOLOGIES

RED AND GREEN

LITHOLOGIES

REDS + GREENS

+ CONGLOMS.

Figure 8.

Interval biozonation of the Sundays River Formation based on foraminifera, compared

with biozonations of the time-equivalent section in the north Pletmos Basin (PB—A1

borehole and Brenton outcrop) and the Mngazana Basin. Interpreted stratigraphic

ranges of studied Algoa outcrop sections are also shown.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 33

FORAMINIFERAL BIOZONATION

OF THE SUNDAYS RIVER FORMATION

Ten Hauterivian and five Late Valanginian foraminifera biozones have been

recognized in the Sundays River Formation. The biozones are formally described here;

they have been numbered from the top of the section downwards, since most of the data

upon which they are based have been derived from borehole sections affected by cavings.

Biozone tops are marked by first down-hole appearance of selected species or other

characteristics, so that this biozonation is essentially an interval zonation as defined by

Hedberg (1976). For distinction, the Hauterivian biozones are denoted with Roman

numerals, and the Late Valanginian ones with Roman letters. The interpreted

chronostratigraphy of the foraminifera biozonation and relationships with other published

time-equivalent sections are shown in Figure 8. The interval biozonation for all studied

deep boreholes, with the lithology, 1s shown in Figure 9*. Foraminifera abundance is

displayed against the interval biozonation of the deep boreholes in Figure 10*.

LATE HAUTERIVIAN

Biozone I.

Reinholdella platterugensis Zone (Partial Range Zone)

Definition. Interval from the first down-hole appearance of Reinholdella

platterugensis to the first down-hole appearance of Epistomina hechti.

Notes. This biozone 1s preserved only in the basin axis around boreholes KE 1/71 and

AL 1/69. Maximum thickness is 90 m in AL 1/69. The upper surface of Biozone I is

everywhere unconformable, and overlain by the Pleistocene upper Algoa Group.

Outcrops may occur in the Spring Valley area, but these are probably very limited.

Diverse foraminifera faunas occur through most of the interval, but some weathering and

leaching appears to have occurred immediately below the Hauterivian—Pleistocene

unconformity. Foraminifera faunas generally remain diverse throughout Biozones I to

VII, reflecting a predominance of clay lithologies. This uniformity of the top seven

biozones distinguishes them, and permits them to be separated as Late Hauterivian in age.

Biozone I.

Upper Epistomina hechti Zone (‘Total’ Range Zone)

Definition. Interval between first down-hole appearance of Epistomina hechti and the

first down-hole appearance of Amphicoryna pletmosiana.

Notes. Biozone II is also confined to the boreholes of the basin axis: KE 1/71 and

AL 1/69. Maximum thickness of 120 m occurs in KE 1/71; the AL 1/69 section, probably

more precisely, is 73.2 m thick. Again, outcrops of Biozone II are confined to the

Zoekamma-Spring Valley area, and the biozone is mostly concealed beneath the

* Figures 9 and 10 are fold-out charts placed at the back of this Volume.

34 ANNALS OF THE SOUTH AFRICAN MUSEUM

Pleistocene deposits of the upper Algoa Group. Foraminifera faunas are diverse and |

abundant for the most part, though there are some sandy intervals in which only

Ammobaculites subaequalis Myjatliuk and Bullopora laevis (Sollas) predominate.

Biozone I.

Amphicoryna pletmosiana Zone (Partial Range Zone)

Definition. Interval between the first down-hole appearances of Amphicoryna

pletmosiana and of Pseudopolymorphina colchesterensis.

Notes. Biozone III is also confined to the basin axis, in boreholes AL 1/69, KE 1/71,

SV 1/71 and CO 2/70. There is a strong possibility that this biozone is also represented at

the top of the Sundays River Formation in VO 1/71, but the microfauna recovery was not

good enough to confirm this. The faunas of Biozone HI are much the same as for the

overlying zone. Average thickness of biozone is 100 m.

Biozone IV.

Pseudopolymorphina colchesterensis Zone (Total Range Zone)

Definition. Interval between the first down-hole appearance of Pseudopolymorphina

colchesterensis and its last appearance, which exactly equates to the second down-hole

appearance of Epistomina hechti.

Notes. Biozone IV has been recognized at or near the top of the Sundays River

Formation in boreholes CO 2/70, CO 3/71, VO 1/71, SM 1/76, NA 3/70, and probably

also in CK 1/68. It may also occur in NA 1/69 and NA 2/70 at top-hole, but the facies there

is too marginally marine for the biozone species and its associated foraminifera to occur.

The biozone outcrops in the upper two-thirds of the kloof section studied at Colchester Cliff.

Foraminifera faunas remain much as above. Average thickness of Biozone IV is 100 m.

Biozone V.

Lower Epistomina hechti Zone (‘Total’ Range Zone)

Definition. Interval between second major down-hole appearance of Epistomina hechti

and first down-hole appearance of Dorothia inglesidensis. )

Notes. The lower Epistomina hechti zone occurs in all of the boreholes listed under

Biozone IV, together with CO 1/67. Due to differences in facies, it cannot be identified on

the basis of the foraminifera in SV 1/71, NA 3/70, NA 2/70, NA 1/69 and CK 1/68, but

thicknesses and adjacent biozones indicate it to be present. Biozone V probably outcrops

in the cliffs facing the Sundays River about the farm Ingleside 215 and in the lower

Colchester Cliff: elsewhere it is obscured by the upper Algoa Group. Foraminifera faunas

remain much the same as above. Thickness varies from 90 m (CO 3/71) to 10 m

(KE 1/71): minimum thicknesses prevail 1n the basin axis.

Biozone VI.

Dorothia inglesidensis Zone (Partial Range Zone)

Definition. Interval between first down-hole appearance of Dorothia inglesidensis and

first down-hole abundance of Vaginulinopsis ct. V. matutina.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 35

Notes. The distribution of Biozone VI is exactly the same as that of overlying

Biozone V, except that it can also be recognized in borehole SV 1/71. Biozone VI may

outcrop in the cliffs along the eastern margin of the Sundays River valley. During this

interval, foraminifera faunas begin to decline in diversity and abundance.

Biozone VI.

Vaginulinopsis cf. V. matutina Zone (Partial Range Zone)

Definition. Interval between first down-hole abundance of Vaginulinopsis ct.

V. matutina and the abrupt decrease in foraminifera diversity and abundance at the top of

the Upper Poor Zone.

Notes. This biozone must outcrop or subcrop beneath the upper Algoa Group in the

area west of the Sundays River valley, on the farms Tankatara and Melville, and also

subcrop north of the NA boreholes, amongst other places. However, because of the

marginal marine facies in the north and east, the precise interval of the biozone cannot be

determined tn these areas. The decline in foraminifera diversity and abundance continues

through Biozone VII.

EARLY HAUTERIVIAN

Biozone VII.

Upper Poor Zone (Assemblage Zone)

Definition. Interval between abrupt decrease in foraminifera diversity and abundance,

and first down-hole appearance of Eoguttulina sp. B.

Notes. Biozone VIII has much the same geographical distribution as Biozone VII. In

the cleaner cuttings boreholes least affected by down-hole cavings, the top of

Biozone VIII is clearly evident, but in the less cleanly drilled holes, cavings obscure the

abrupt decrease in foraminifera. Only after caved material has been identified and excluded,

using the cleaner holes as comparisons, can the top of the biozone be identified in the

poorer holes. A different problem exists in the case of the fully-cored borehole CO 1/67,

where diversities of foraminifera fluctuate widely even in adjacent samples, partly in

response to the cyclical lithology. Since, through selection, the cored samples studied

have tended to be clayey, occasional core samples from Biozone VII in CO 1/67 contain

abundant faunas that are not represented in nearby cuttings holes where the sampling interval

is3m,5 mor 10m. Asa result, the top of Biozone VHI in CO 1/67 has been estimated.

Foraminifera faunas of Biozones VIII, LX and X tend to be dominated by agglutinated

foraminifera, particularly of the genera Haplophragmoides and Ammobaculites. The

diverse nodosarid and Epistomina—Reinholdella aspects of the overlying beds are generally

lacking. For these reasons the three biozones have been regarded as of Early Hauterivian

age, although there is no available faunal evidence to confirm precisely such an age.

Biozone IX.

Eoguttulina sp. B Zone (Partial Range Zone)

Definition. Interval between first down-hole appearance of Eoguttulina sp. B and the

36 ANNALS OF THE SOUTH AFRICAN MUSEUM

first down-hole appearance of Dorothia australis.

Notes. Biozone IX is again characterized by poor foraminifera assemblages.

Eoguttulina sp. B is one of only a few species that first appear down-hole in the Early

Hauterivian. Thicknesses of this biozone show some variation, from about 247 m in

SM 1/76 down to less than 100 min CO 1/67. This time period appears to have been one of

substantial re-organization of the sedimentation process in the Algoa Basin, following the

major, but abrupt, tectonic disturbance that occurred in latest Valanginian times

(responsible for the 1Atl unconformity). Because of this, and the high frequency of

sandstones over this interval in consequence, Foguttulina sp. B cannot be recognized

everywhere, and the foraminifera faunas remain poor.

Biozone X.

Dorothia australis Zone (Partial Range Zone)

Definition. Interval between first down-hole appearance of Dorothia australis and first

down-hole appearance of Reinholdella valendisensis.

Notes. Biozone X, on the basis of the distribution of Dorothia australis, can only be

recognized intermittently in the onshore Algoa Basin, because of the fairly sandy nature of

this part of the section. Offshore, the biozone is widely developed in the Bredasdorp,

Pletmos, Gamtoos and Algoa basins. It is the highest biozone recognized in the Uitenhage

Trough, adjacent to the bounding Coega Fault. In the Sundays River Trough, Biozone X

probably outcrops in the vicinity of borehole BR 1/71, and probably also in the Canteen

Kop area in the eastern Sundays River valley.

LATE VALANGINIAN

Biozone A.

Reinholdella valendisensis Zone (Partial Range Zone)

Definition. Interval between first down-hole appearance of Reinholdella valendisensis

and the first down-hole appearance of Lenticulina coegaensis sp. nov.

Notes. As mentioned earlier, Reinholdella valendisensis and R. hofkeri have been used

to mark the top of the Valanginian, both in the Algoa Basin and elsewhere in the southern

offshore of South Africa. The first down-hole appearance of the ostracod Cytherella

algoaensis Brenner & Oertli usually occurs within Biozone A.

Biozone A is not always easy to recognize in the northern Algoa Basin. In those

boreholes that intersected a more sandy sequence, the two species of Reinholdella are

rare, occasionally even absent, as far down as the top of Biozone B. In such cases, the top

of Biozone A can only be recognized by the occurrence of tests of Epistomina caracolla

that are preserved with a dark, rich golden-brown colour, profoundly different from the

pale colour of Hauterivian tests of this species. However, when the sequence is clayier,

common Reinholdella valendisensis and R. hofkeri, with abundant Epistomina caracolla,

appear very abruptly, and provide a clear upper boundary for this zone. Because of the

major change in test preservation from the top of Biozone A and downwards, and the

abrupt appearance of the biozone markers, it seems likely that some form of unconformity

=—

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 37

or hiatus occurs at this level, although the duration of any time gap cannot be determined

from the foraminifera data. Examination of offshore borehole sections in the Pletmos and

Gamtoos basins (boreholes drilled to date in the offshore Algoa Basin do not intersect a

sufficiently shallow marine, shelf sequence to allow a comparison) has revealed no

obvious seismic break at the level of the first down-hole appearance of R. valendisensis.

Biozone Ba.

Lenticulina coegaensis sp. nov. Zone (Partial Range Zone)

Definition. Interval between first down-hole appearance of Lenticulina coegaensis sp.

nov. and the first down-hole appearance of abundant Sculptobaculites goodlandensis.

Notes. Foraminifera faunas are generally very much more diverse and abundant in

Biozones Ba and Bb, excluding those areas in the north and east in which estuarine and

transitional environments prevailed. The dominant foraminifera are the Epistomina

caracolla group, which, with Reinholdella hofkeri and R. valendisensis, ensures that most

assemblages from Biozones Ba and Bb are composed mainly of aragonitic-walled

species. This preponderance 1s in direct contrast to the foraminifera-rich interval in the

Late Hauterivian, where nodosarids predominate. The dominance of aragonitic shells in

much of the Late Valanginian appears to correspond to the predominance of Cytherel/a in

Late Valanginian ostracod assemblages, and its lesser frequency in the Hauterivian

(Brenner & Oertli 1976; Valicenti & Stephens 1984).

At or near the top of Biozone Ba lies the time-equivalent level of the major offshore

unconformity seismically designated 1 Atl. This, at least in part, is evident in borehole

lithologies as a change from sands and rare clays above to clays and rare sands below.

Attempts to identify the unconformity with compaction breaks on the borehole electric

logs have not proved particularly successful, possibly because the quality of the logs is

often rather poor.

Biozones Ba and Bb combined (Biozone B) can be recognized extensively in the

offshore portions of the Pletmos, Gamtoos and Algoa basins, where both the first

down-hole, and last down-hole appearances of Lenticulina coegaensis sp. nov. have

proved to be of stratigraphic significance.

Biozone Bb.

Sculptobaculites goodlandensis Zone (Partial Range Zone)

Definition. Interval between first down-hole appearance of abundant Sculptobaculites

goodlandensis, and the abrupt decrease in foraminifera diversity and abundance at the top

of the Lower Poor Zone.

Notes. Foraminifera assemblages of Biozone Bb are essentially the same as those of

Biozone Ba. Sculptobaculites goodlandensis appears to be confined to the onshore Algoa

Basin, so that the distinctions of the two biozones cannot be made offshore. The Coega

Brick Pits, northernmost cutting of the Uitenhage to Graaff-Reinet Road, the upper

three-quarters of the Zoetgeneugd Cliff outcrop, and the Amsterdamhoek exposure are all

of Biozone Bb age.

38 ANNALS OF THE SOUTH AFRICAN MUSEUM

Biozone C.

Lower Poor Zone (Assemblage Zone)

Definition. Interval between abrupt decrease in foraminifera abundance and diversity

(near to last down-hole appearance of Lenticulina coegaensis sp. nov.) and the first

down-hole appearance of Miliammina latrobei sp. nov., or top red beds.

Notes. Poor foraminifera assemblages, dominated by Ammobaculites and

Haplophragmoides species, with calcareous forms such as Lenticulina nodosa and

Astacolus calliopsis are typical in the interval of Biozone C. Subsequent to the major

decrease in abundance and diversity that marks the top of the biozone, there is a fairly

steady decline in both parameters through the biozone, with the lower part being virtually

devoid of all types of foraminifera. Because of caving problems in a number of the rotary — |

holes, the sequence of events 1s somewhat obscured over this interval, but the degree of

caving can often be determined from the presence or absence of obviously caved tests

occurring in the underlying red beds samples of the non-marine Kirkwood Formation. The

fully-cored CO 1/67, AD 1/68 and PA 1/68 sections are also of help in determining the

true foraminifera abundance through this interval. The lowest part of the Zoetgeneugd

Cliff, the middle cutting on the Uitenhage to Graaff-Reinet Road, and the Airedale

outcrops are referable to Biozone C.

Biozone D.

Miliammina latrobei sp. nov. Zone (Total Range Zone)

Definition. Interval between first down-hole appearance of Miliammina latrobei sp.

nov. and the first consistent down-hole appearance of red and green beds (top Kirkwood

Formation).

Notes. This biozone can not be extensively recognized, partly because of the difficulty

of obtaining Miliammina latrobei sp. nov. specimens from cuttings samples. The full areal

distribution of the biozone 1s thus in some doubt. The biozone is evident in cored borehole

CO 1/67, and in the northern and eastern boreholes where marginal marine and estuarine

facies predominate (NA holes, PA 1/68 and CK 1/68). Miliammina latrobei sp. nov.

seems to be confined to estuarine and possibly other reduced salinity environments, as are

most Miliammina species at the present day. Thus it appears that Biozone D, of all those

recognized in the northern Algoa Basin, is the one most likely to suffer facies-induced

diachroneity. The outcrops of The Look Out and Dunbrody areas are referred to

Biozone D—since M. latrobei sp. nov. occurs in the stratigraphically highest of these, at

The Look Out, and at the low-level bridge just to the west. Foraminifera here are sparsely

present, or more often absent.

In the CO 1/67 section (Figs 4, 81), which is probably fairly representative of all the

basin centre wells, core sampling was undertaken at close intervals, with some parts of the

section being sampled at as close as 2-foot intervals. It is clear that microfaunas in the

lower part of Biozone C are very poor, but these rocks are distinctly marine, since they

contain numbers of gastropods, bivalves and echinoderm skeletal fragments. Foramin-

ifera appear more consistently from the top of Biozone D downwards, but they are almost

exclusively Miliammina latrobei sp. nov. Near the base of Biozone D, at 3 356 ft

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 39

(1 022.9 m), a sudden, marked increase in foraminifera occurs, with large numbers of

Ammobaculites and Haplophragmoides tests (one or two species of each). No attempt has

been made to develop this Ammobaculites—Haplophragmoides interval as a formal

biozone, as it has only been recognized in the CO 1/67 section, and, given the

circumstances, can only be expected to be found either in the other cored boreholes

(AD 1/68 and PA 1/68), both of which are proximally sited, or in outcrop, most of which

also expose proximal facies. Below this level, from 3 356 to 3 420 ft (1 022.9 to

1 046.9 m), foraminifera are absent. At 3 420 ft, the first massive red and green claystones

occur. Top of the Kirkwood Formation is taken at 3 373 ft (1 028.3 m). In all other

boreholes the top of the Kirkwood Formation is taken as first down-hole appearance of red

(and minor green) claystone lithologies.

OUTCROP/SUBCROP MAP OF THE SUNDAYS RIVER FORMATION

Figure 3 illustrates the outcrop and subcrop beneath the upper Algoa Group of the

Sundays River Formation, based on the biozones recognized in the top-hole portions of

the boreholes, together with the outcrops, and reflecting the major structural features of

the basin. The widespread minor faulting throughout the Sundays River Formation

succession clearly renders this a generalization.

BIOZONES, FACIES AND TIME LINES

Some comment is necessary on the chronostratigraphic value of the biozones proposed

above. Examination of many Pletmos, Gamtoos and offshore Algoa borehole sections has

shown that this biozonation of the Sundays River Formation can be used in the parts of

these three basins that accumulated under normal marine, continental-shelf conditions.

The biozonation begins to fail in marginal marine and estuarine environments, and with

increasing distance down the continental slope. In addition, regions affected by

substantial freshwater and sediment input off river mouths, even though perhaps at a

middle-shelf water depth, or where poorly oxygenated conditions prevailed, tend to have

supported insufficient diversity of foraminifera for the biozonation to be effective. The

only biozone that is an exception 1s, clearly, the lowest—Biozone D, distinguished by

Miliammina latrobei sp. nov.

In general, the foraminifera results compare with those of the ostracod studies (Brenner

& Oertli 1976; Valicenti & Stephens 1984), as shown in Figure 5, but the precise

relationships of the various ostracod and foraminifera biozones remain to be determined.

Close similarities in the electric log correlation and foraminifera biozonation also affirm

the basic synchroneity of the biozonation presented herein (Fig. 7). Concern for a

comparison of results in this way is necessary to establish conclusively that the

foraminifera (and ostracod, palynological and ammonite) zones reflect synchronous

events. It is clear, from the distribution of the foraminifera biozones recognized so far in

the Late Valanginian and Hauterivian of the Pletmos, Gamtoos and Algoa basins, that

they are probably more-or-less synchronous in the areas of these basins where

ANNALS OF THE SOUTH AFRICAN MUSEUM

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Distribution of ammonites in outcrops and borehole cores of the Sundays River Formation

and suggested correlation with the foraminifera-based interval biozonation.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 4]

continental-shelf sedimentation occurred throughout the time period. Inconsistent errors

between, for example, the foraminifera and ostracod biozonations are more likely to be

due to variations in sampling, processing, sieving and picking each sample studied.

AMMONITE CONTROL

Ammonites have been widely reported from the Sundays River Formation since the

earliest days, but their potential stratigraphic value has been somewhat clouded by the

frequent lack of detailed collecting-site data. Ammonite faunas were described primarily

by Sharpe (1856), Tate (1867), Kitchin (1908), Spath (1930), and in particular detail by

Cooper (1981, 1983); all later authors commented on the dominance of the genus

Olcostephanus and the relative sparsity of other forms. Cooper (1981, 1983) recognized

23 ammonite species or varieties, one belemnite and one nautiloid. Of the ammonites, 15

are referable to Olcostephanus and indicate a Late Valanginian age. Despite their

presence in outcrops, no ammonites or belemnites (as microscopic fragments occurring in

association with the microfaunas) have been found in the core, cutting or outcrop samples

of this study.

Since ammonites have been reported from several of the outcrops studied for

foraminifera and reported on in the present work, some attempt is made here to correlate

known ammonite assemblages with known foraminifera assemblages, as detailed in

Figure 11. As can be seen, most of the outcrops bearing ammonites expose the lower

portions of the Sundays River Formation, of Late Valanginian age, particularly within

Biozones Ba, Bb and possibly C. The only ammonite finds from outcrops exposing higher

stratigraphic levels are: (1) the Eodesmoceras haughtoni Spath specimen from Salt Pan,

adjacent to borehole ST 1/71 site; and (2) the Bochianites africanus (Tate) and

Partschiceras rogersi (Kitchin) specimens from the kloof behind Colchester (Site Q of

Rogers 1906) and, in the case of the former species, from two adjacent sites, all in the

vicinity of boreholes VO 1/71, KE 1/71 and the three CO holes. These occurrences of

ammonites, on the basis of the foraminifera studies presented here, are regarded as Early

Hauterivian (Salt Pan) and Late Hauterivian (kloof behind Colchester and adjacent sites),

respectively. In addition, Shone (1976b: 23) reported the presence of Bochianites sp. at

41 m (134 ft 6 in) in the cored section of borehole CO 1/67 (Late Hauterivian Biozone V

on the basis of the foraminifera). The apparent record of Rogersites (otherwise

Olcostephanus) at 360 ft (109.7 m) in the CO 1/67 cores by Rigassi (1968: 11, 13, 16)

seems questionable, given the large size of most Olcostephanus specimens as against the

3.5 inch top-hole core diameter, and the unlikely chance of a major part of the

ammonite(s) being recovered within the encompass of the core diameter. The record of

Olcostephanus (as Rogersites) atherstoni (Sharpe) by Engelbrecht et a/. (1962: 16) from

Vetmaak Vlakte (presumably Colchester Cliff), reported by unknown earlier authors, 1s

the only other occurrence of this genus from high in the Sundays River sequence, and it

must be regarded with some suspicion since it appears not to have been corroborated by

later work.

The ages interpreted from the ammonites from higher in the section seem to

42 ANNALS OF THE SOUTH AFRICAN MUSEUM

SGALE ABOUT 2:4

14 974 — KEY —

41975

Grey claystones

” 14976

= 44977 Sandstones

= Mere Shell beds

pe Calcareous nodule beds

14980 Soekor sample numbers

41984

20 14456 &

FACE SLOPE

ABOUT 2:4

Sit

asl

iT, |

> |

oO H

or 4

14993 |

ca!

11994 « 11962 a !

Oo |

Te pee FACE APPROXIMATELY

11993 VERTICAL

411996

441997

11998

44 999

44442 44 454

euae 14455 é

12001 a

11 444 E

44450 oO

i1aas 2

12003 eo atiee

412004 44484 rs

14 446 =

44984 3

12005 3

4443 11482 a FLOOR OF

RIVER FLOOD

ee STREAM aaa, BANK QUARRY

BED

COLCHESTER ZOETGENEUGD COEGA

CLIFF CLIFF BRICKWORKS

(COMPOSITED)

DATA FROM VALICENT!I AND STEPHENS (1984)

igure 2:

Lithologies and levels of studied samples of three outcrops:

Coega Brick Pits, Colchester Cliff and Zoetgeneugd Cliff.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 43

accommodate the ages gained from the foraminifera. Partschiceras rogersi is also known

from the Early Valanginian and Early Hauterivian of Madagascar, and Cooper (1981)

concluded that it was a relatively long-ranging species. In the case of Bochianites

africanus, the genus 1s regarded as ranging from the Portlandian to the Hauterivian, and

too little is known from elsewhere of the stratigraphic range of the species (Cooper 1981).

Eodesmoceras haughtoni 1s referred to a genus with two subgenera that are not clearly

distinguished: E. (Eodesmoceras) ranging from Valanginian to Early Hauterivian and

E. (Miodesmoceras) typical of the Barremian (Cooper 1981).

FORAMINIFERAL BIOSTRATIGRAPHY OF THE VALANGINIAN AND

HAUTERIVIAN OF THE SOUTHERN CAPE

Figure 8 correlates the foraminifera biozonation of the Sundays River Formation

proposed here with those of Pletmos Basin borehole PB—A1, the Brenton Formation and

the Mngazana Formation. Re-examination of offshore borehole PB—A1 (originally

detailed by McLachlan et a/. 1976b), following extensive re-processing of samples in the

late 1970s, showed the first indications that a very similar foraminifera zonation could be

constructed for the proximal parts of both the Pletmos and Algoa Basins. Later work has

extended this biozonation to the offshore Gamtoos Basin, where a similar section

(boreholes Ha—F1 and Ha—N1) occurs, although onshore there the sequence is essentially

non-marine (boreholes LO 1/69 and MK 1/70).

The marine beds outcropping at Brenton are correlated to PB—A1 borehole on the

presence of Astacolus beerae Brenner & McMillan at both localities, a species that 1s

confined to a thin interval immediately overlying red and green, non-marine beds at

PB—A1, and has been taken to be an approximate equivalent of Biozone D of the Sundays

River Formation. The relatively early age of the Brenton Formation is confirmed too by

the absence of Lenticulina coegaensis sp. nov., a species that ranges down to the base of

Biozone B or Bb in both PB—A1 and in the Algoa Basin boreholes.

In the case of Mngazana, the presence of Lenticulina coegaensis sp. nov. (as

Lenticulina bifurcilla Bartenstein & Brand) indicates a Biozone B age, slightly later than

the Brenton Formation. Other species, such as the large, rather compressed and many

chambered test of Lenticulina nodosa (Reuss) (McLachlan et a/. 1976a, fig. 16 (no. 18))

and Lagena cf. sulcata (Walker & Jacob) (the Mngazana form) are typical of Late

Valanginian, and Berriasian to early Late Valanginian rocks, respectively. The Mngazana

outcrop is here regarded as being referable to the earlier part of Biozone B, although it

may possibly be of latest Biozone B age (just later than the |Atl unconformity).

The reprocessing and re-study of borehole PB—Al has revealed a much more

distinctive and diverse foraminifera fauna in the lower marine unit (Colchester Member

equivalent) than was first reported by McLachlan ef al. (1976b). The foraminifera

assemblages of this unit show some comparison with those of the Colchester Member of

the Uitenhage Trough, Algoa Basin, and both are regarded as Portlandian in age on the

basis of their contained foraminifera.

44 ANNALS OF THE SOUTH AFRICAN MUSEUM

THE ALGOA BASIN OUTCROPS

Samples studied from Amsterdamhoek, Coega Brick Pits, Colchester Cliff, Uitenhage

to Graaff-Reinet Road, and Zoetgeneugd Cliff are the same as those studied for Ostracoda

by Valicenti & Stephens (1984). The levels of samples studied from Coega Brick Pits,

Colchester Cliff and Zoetgeneugd Cliff are shown in Figure 12. Samples studied are listed

in Table 3.

Airedale

The Airedale exposures lie close to outcropping Kirkwood Formation red beds on the

north side of the Coega River valley. Samples were collected by I. R. McLachlan.

Microfaunas are poor in all four samples studied (Fig. 13). The assemblages are referred

to the Late Valanginian Biozone C because of the poor faunas and the proximity of the

locality to the red beds. The microfauna recovered so far is not conclusive enough to

confirm this placing. Olcostephanus-dominated ammonite assemblages have been

recovered from localities around Coega, to the south-east, and at Welbedachtsfontein

(Haughton 1928; Spath 1930; Cooper 1981) to the north-west, both of which are

approximately along strike to the Airedale site. There is some indication that the basal

marine beds on Welbedachtsfontein contain Olcostephanus species (Haughton 1928: 27;

Spath 1930).

Amsterdamhoek

Five samples collected by I. R. McLachlan from the Amsterdamhoek railway cutting

provided a diverse and abundant foraminifera fauna (Fig. 14). About 18 m of section is

?Sculptobaculites goodlandensis

Haplophragmoides spp.

SN}

Ammobaculites spp.

Key to symbols/No. of specimens

O 12 8 35 6-15 O 1649 Figure 13.

@ 50+ Distribution of foraminifera in Airedale outcrops.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 45

exposed at the sampled site, but Shone (19764) recorded a total of some 70 m of section.

Tankard et al. (1982, fig. 12.4, section 4), basing their section on work by Shone (19765),

show the exposure to be composed predominantly of claystones, with minor, usually thin

sandstones, that in part show coarsening upward cycles. The abundance of Epistomina

caracolla (Roemer) s.]., with Reinholdella hofkeri (Bartenstein & Brand) in the basal

sample and Sculptobaculites goodlandensis (Cushman & Alexander) near the top of the

section, indicates that the exposure is probably all of Biozone Bb age, Late Valanginian.

Calcareous foraminifera are rare in the highest sample studied, and it seems likely that

some leaching has occurred here.

Ammonites from the Amsterdamhoek railway cutting and vicinity are primarily of

Olcostephanus species (Rogers & Schwarz 1901; Rogers 1906; Kitchin 1908; Cooper

1981), and emphasize the Late Valanginian age. Reinholdella hofkeri (as Conorboides)

was previously recognized from this locality (Rigassi 1968, pl. 12).

Coega Brick Pits

Thirteen samples were collected by I. R. McLachlan and C. Reabow. The samples

derive from adjacent quarries, termed North Quarry and South Quarry by I. R. McLachlan,

located just west of the railway line and about 3.5 km north of Coega Station. The section

shown by Valicenti & Stephens (1984) and reproduced here (Fig. 12) 1s a composite of the

two quarry sections. A total of about 18 m of Cretaceous section 1s exposed, the upper half

in North Quarry, the lower half in South Quarry. Foraminifera faunas are generally

abundant and diverse, although three samples provided only poor faunas. One of these, the

highest sample collected, is probably leached, as it derives from a short distance below the

Sundays River/upper Algoa Group boundary unconformity. The entire section is referable

to Biozone Bb of the Late Valanginian (Sculptobaculites goodlandensis biozone). Results

of studying the Coega Brick Pits samples are shown in Figure 15.

Olcostephanus species predominate in ammonite collections made at Coega Brick Pits

and surrounding localities, reinforcing the Late Valanginian age interpretation. There is

some indication that the basal marine beds in the Coega area contain ‘numerous

specimens’ of Olcostephanus (Haughton 1928: 27).

Colchester Cliff

The small vailey (or kloof) in the substantial cliff just north-east of Colchester railway

halt (near to Rogers 1906, Site Q) in the lower Sundays River valley yielded variable

faunas from 21 samples collected by I. R. McLachlan and C. Reabow. The majority of the

Colchester Cliff section is obscured by scree and soil. The exposed sequence in the kloof

appears to be extensively leached, which is unfortunate since this is the only major

outcrop studied in the Hauterivian part of the Sundays River Formation. Agglutinated

foraminifera predominate in most of the samples, and in all cases pyrite is oxidized. Only

in a few samples do calcareous species occur, the most frequent of which is Pseudo-

polymorphina colchesterensis sp. nov. Some spherical Radiolaria are present. Results are

shown in Figure 16. The outcrop is probably mostly referable to Late Hauterivian

Biozone IV, but the latest Biozone V may occur near the base. Borehole CO 2/70, drilled

ANNALS OF THE SOUTH AFRICAN MUSEUM

a2 &

eS Ss az

S ASG. Hats ; > PA a

s Bese S e = iS = 4 ie

~ ™- . le ° be)

2 pes Se gases sas = pete 2 ;

Su 2 Se SS ooon Sa eS = 3 4s nN ae = a

SS 5 2 So 2 NS = SS aoe, 2 SS oy fos

Rr 6.8 Set SS BSc oe tee So Sa = Sa eS SO ie

S SSD SPR ea he Sew SS tos So GR oes CU as

SNES) SS On Sa oy So 2 = a ~ 7 OA

SS igs GS FS PSS Sh 3 8s 2k fe eee eee

e © ££ © S es s es Se 8 8 8S LS A SL Sls | see

SS se Ss 8S 8 FSS SSE SS SS 8S SS Soe eee

SS SSERSSRSRSESSE SS 22S SSS 8 =

S SS SS Rss SS SS SS S = 2 oes ben BOS

SS REsS Pe PSPs SS PER SS Shs BS See

-™ SS SS es RS ey = == SO) ayer

Oe eA nQan eseayneeaes OO2Z2 3 2 Oo] eae

114442;0 O @ @©OoO0 000 808 000 © 0 0 © © O16 OO OOROFere

11461 OO sO Ox) © =42=50 Oo --- - - O--

11460;-— - - —- —~ O O- - - -~- ~ -~- ~ @- - =~ =~ = = =

11459 O----O0O00® - @©O0OO0O -

11458 | — - - - = = = = = =~ O- = + = = =~ =~ =~ =~ O- =~ -~ = = |=

Key to symbols/No of specimens O 1-2 © 3-5 6-15 O 16-49 @ 50+

Figure 14.

Distribution of foraminifera in Amsterdamhoek railway-cutting outcrop.

to the north-west of the sampled outcrop, on top of the Colchester Cliff, also intersected

Biozone IV, and perhaps the basal Biozone III, in the topmost Sundays River Formation.

The section studied for foraminifera is about the same locality from which the ammonites

Partschiceras rogersi (Kitchin) and Bochianites africanus (Tate) (Rogers 1906; Kitchin

1908; Cooper 1981) derive.

Dunbrody area

In the vicinity of the confluence of the Bezuidenhouts and Sundays rivers in the

northernmost Algoa Basin are a number of outcrops sited across and close to the boundary

of the Kirkwood and Sundays River formations. Details of these sites are given in

McLachlan & McMillan (1976, fig. 7). At the time of that publication, it was believed that

these outcrops, mostly of marginal marine deposits, were referable to the Colchester

Member, which was considered to outcrop and subcrop beneath the Sundays River

Formation in the Dunbrody area (McLachlan & McMillan 1976, fig. 9). However, the

absence of any identifiable Colchester Member in any of the northernmost Algoa

boreholes (AD 1/68, CK 1/68, NA 1/69, NA 2/70, NA 3/70 and PA 1/68), and the lack of

any marine fossils in the Colchester Member of the Sundays River Trough would appear

to preclude such an interpretation. The Colchester Member in the Sundays River Trough

is now regarded as extending no further north than the Barkly Bridge area, and it is

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 4

& foo)

oetgeneugdia

Eoguttulina cf. E. liassica

?Saccammina sp.

Sculptobaculites goodlandensis

Haplophragmoides sp.A

Ammobaculites sp. A

Tristix acutangula

Lingulina simplicissima

Ammobaculites sp. G

?Ramulina sp.

Vaginulina spp.

?Lingulina sp.

?Textularia

?Frondicularia sp.

?Gaudryinella sp.

Miliammina sp.

Astacolus spp.

?Dorothia sp.

Dorothia australis

Comspira sp.

e|;9o |e Haplophragmoides spp.

O | Astacolus explicatus 8.1.

° Haplophragmoides sp.B

O |®

0 12D |% |e

O |O Haplophragmoides sp.C

~ 3 OLCUCh: eee a ee ee

0®0-000000 00 0-©-- 0000 ~ _|i14s9|

0®000-0 O 0 0} 114s |

Key to symbols/No of specimens O 1-2. © 3-5 6-15 O 16-49 @ 50+

Figure 14 (CONTINUED).

probably bounded on its northern and eastern sides by the Colchester Fault (see Figs | and

2). The oyster beds and grey claystones and sandstones of the Dunbrody area are thus

referred to the basal Sundays River Formation, in keeping with the interpretation of the

boundary recognized by Haughton (1928). Unfortunately, foraminifera evidence to

confirm this interpretation is sadly lacking: nearly all of the samples studied from the

Dunbrody area are devoid of foraminifera. Localities sampled by I. R. McLachlan during

the 1970s include Dunbrody Bridge (Site 13), Paaltjieskraal (Site 4), Zoutklip (Site 5),

Bezuidenhouts River (west of Site 10), Blue Cliff Station (Site 2), Dunbrody Station

(Site 10), and Mfuleni (Site 15). Productive samples with foraminifera (two only) are

shown in Figure 17. No ammonites have been reported from any of these outcrops.

The Look Out area

Downstream from the Dunbrody area, along the Sundays River at The Look Out, occur

the first beds with diverse and abundant marine macrofauna (Site 14 on fig. 7—

McLachlan & McMillan 1976). Ten samples were collected by I. R. McLachlan from The

Look Out cliff proper, one from the first low-level bridge 0.5 km upstream from The Look

Out, and one sample from Castle Cliff, 0.5 km further upstream. The ten samples from

The Look Out derive from the same site as that detailed in a vertical section (RS 112) by

Shone (19764, fig. 5), but precise positioning of our samples against the vertical section

48 ANNALS OF THE SOUTH AFRICAN MUSEUM

S Ss S =

= =) = 5

D So 5 8 n 2

- > SIRS) S 3 =

iS = LS = 22 S 5S 3

aS) oS = 8 =: = 3 2 = < = . cS s

80 S. S aos a Ss § 8 s Ss a

Y ES S824 ¢ s 822 -3n oS S

30 Ny 2s =s Ff << a ~ tn ay eS Se feel vw SS 4 & is)

Z Se, fey 8 & § Ss x eee AS 2S SO) OS) SS See SSS € S

A esl Sisk OS SS 8 Za 8) i a Ss 8 8 gS 2 S YS SS & &0

8. Oe SS aoe Se SG SS SS nS im foo eS Se Sea oe _

SBS eee Se SSB eS § Fas Se Sa 8 8 S Seow 6 Sa eee

Pee = Q oF SS Sy Oe ss as iS SS fe at = 8 = = aes

S33 NSS BS SB Se S88 FR Se S Oe 8 & Ss & Sb SRSRS ss 6 eee

Ss SS Ss SS SF GS & OS S 8 & SS 5S As SS SSS SF SS 8S © SSeS

SS ES & 8 8 es 8 ES =o 8 8 CoS Se S S sho 2 Soke = oa eee

Ses ay SSS os = Sse SSeS 5292’ SSMS SRS e VRS SFSP BYP = &F Se |S

S Sse SO RES = So 8 SS SSS Ss 8S S80 so & S58 52 oe

Sy TS 6S = SL) 8 aha SS Se) Ss eo) = =

S&S see SS ESS SSS SSS FSS ESS ES BS ee = oe ee

~ ~ gS = pt SS ~ & WES GS gS aoce oS =

sme &§ SERS SSF FSS Se s SSSS SESS 8 HF APES S Seo aoe.

Oem £ Se OG Yas Hh 8 48 8 2 Se See eS eyes See eee

(OO Om OO) -

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Figure 15.

Distribution of foraminifera at Coega Brick Pits.

has not proved possible. Despite the diverse and abundant macrofauna at The Look Out

cliff, only rare tests of Miliammina latrobei sp. nov. were found, and it may be that

leaching of the outcrop has occurred. A small, very distinctive, exclusively agglutinated

foraminifera assemblage characterized by Plectinella castlecliffensis sp. nov. occurs at

the low-level bridge outcrop. The presence of M. /atrobei sp. nov. here too again suggests

hyposaline conditions of deposition prevailed. Rare agglutinated foraminifera (Haplo-

phragmoides sp., ?Ammobaculites sp.) with crinoid ossicles and blocks of Jnoceramus

prisms were found in the sample from Castle Cliff. Results are shown in Figure 18.

Ammonites have not been found in The Look Out area, but occur some 4 km

downstream on Summerville Estate (Buck Kraal) where Bochianites africanus (Tate) has

been reported (Rogers 1906—sites G, H; Cooper 1981).

Uitenhage to Graaff-Reinet Road

A number of exposures were cut into the basal Sundays River Formation near the town

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 49

€

“~

—

“

~ ~~

S nH

8 So

kc fad SS) 4

Q a S) 2 853

x Ss 3 Ae. = Sears -

\S) v = a 2 = 2) Ee S = on

= ~ _ 3 ny A se bn S = an iz

SY . ~ Sera aa — SL Ss 20 x & & = ne

i Law A . Nn ; > 8S ple eS ney ~ on

> oy a < x Se a Z *S 3 © s iy ‘s) = s S 4 4

mn 8S B c 2 5 q ee ~

Beas oe ie ae © CS Sees bo Lee See PSR Ge

Ea = S) 5 = S +e] . ft : , é ae A ~ $ S 2. =

Ree pS =o Os a 8 S ose s Ss f= gam & = SNe

Pos ieee aw ts EO ~ . 5 , OO FR SS os = ES US : VY qi + Oo S a 3

NIB Sy eC Obe Oy oe FS BO BS tee ieee SS S SS ou cs eS ts Gg) MS io 33 Se 6p 8 CS US

PES REE GS ERS REESE SSP ee ee See ee CS Pe Pe EE

% 2 t 3 ~ . Ss 4 = ~ - ~

Rass ese eee oo SO tres oe rs SSO a eS re te 4 S ss © © © FE Sa &

2 ; ~ Ped

eS BOs, CeO eS EO ic wc ae SS ORS ao OG "SOS SS ee fo. SS S . EF Ss 8

3 ~~ a = S ~ ey z GS ~ ~ = ~~ SS = te in = ~ = b§ = S es Fimey ~ _ =e ~ S = « >

sos Teer EOS BC ES eS RS Ac Se eS ne ESN eS eS eS IS Cf eS eS SS SS is SS a a a

FS ee See aes SO) OD) SO. eS eS ers ie SS SO BS ES oO EO oS aS SS Ss © ETS 6 8 SS & 8 fF 8

~—s 4 & ~» ) ~ rs: LJ ~~ ¢ a lon ~ t ~— ~ a

eS eS OS eS Ges So ES S S S SO es) AS OS) ES SERS FSS aS tS Ss SS SG SS & SR SSE

S & § SERS Sees © s§ 8 8 © & 8 B&B & & H& S S ES RE oy te ee, eS OS Gk (Eg VO GSS

s.3 sos 8 R OS § bg :

Y ~ 3 = Ss om 3 oD 5 = a Ss HON we ~~ x ~ ~ ~ eF) it) D = & a = Pd aed 20 SS = 8 20 =

eS SS) ff 5 ‘ 2 ace Waeeice | dv ws em em A H = oO Rk A a © VE LC KS KX 8S Ba

= = : = r ¢

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Figure 15 (CONTINUED).

of Uitenhage during the late 1970s, in the reconstruction of the main road north to

Graaff-Reinet. These outcrops lie near to the westernmost limit of the Sundays River

Formation in the Uitenhage Trough. Red Kirkwood Formation claystones are exposed

just to the south near to sample 11463; and again to the west, a little north of Uitenhage

town. Red claystones also outcrop a short distance to the north, on the upthrown side of the

Coega Fault. Samples studied derive from the basal Sundays River Formation, and were

collected by I. R. McLachlan.

From the presence of large numbers of Epistomina caracolla (Roemer) s.]. and a few

examples of Lenticulina coegaensis sp. nov. in sample 11464, this sample must be

referable to Late Valanginian Biozone Bb at oldest. The basal Sundays River Formation

sample 11463 is probably referable to Biozone C: it contains echinoid shell, but no fora-

minifera. The stratigraphically higher samples 11465 and 11466 contain Sculptobaculites

goodlandensis (Cushman & Alexander) and thus are probably also of Biozone Bb age.

Results are shown in Figure 19. Sample 11464 proved to be unique in all of the Sundays

50 ANNALS OF THE SOUTH AFRICAN MUSEUM

5 RS 2

S < az) a

So Ss & iS

8 ae me S =

ay S § © s&s Ss s Oo Ss

Le Ore) bs SS S so 2 Ss

x oh SS SS & SS : > + SSeS &s S a

: eee Gre 2 S&S 2 ee i d Boe sas oS Ze

MO ie. a oe Bae ey 16 w aes SS AS Ss) & 3 2s

QS, Cass SoS SS Ses 's See ats Ss 2 =e Soe oS Ss S

See SSS ES TS Ce RS SRO ee SS ey SS aoe Sa as

ee See SESS) Sas RS ee ee ese SES ZS Ss 5 ey S& So 8

BSS Pe ER ESS 8 saa ec eS FSF OL Lec Sse eee

SS era, So eertos co NS 8 9S Ge CS SS eeu eS SSeS Go CE Be Go Sim Ss) as

sso |g Fe Ss ss Se Ss we SES 1S 2S) Sas s a = § § 6 = eee ge

esS es S88 8 FFs 8S SEES S 8S 8s 88 88 8 2 See ee

aos OS SSS Ses OO oS SS oS OS cor ca eae eo eS Bees oS eS ees S$ 33

SS CRBS PSE SSSSSESs ss Sst test sts ses 22a ee

FEE SRB SSS 8S SS S EF 8 § § & SSS & bo Sas eS ee eee

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Figure 16.

Distribution of foraminifera in the kloof, eastern end of the Colchester Cliff

(near site Q of Rogers (1906)).

River Formation samples studied in this project because of its unusually high numbers of

simple miliolid tests of Vinelloidea buchenroderi sp. nov. and Nodobacularia sp. A.

These, with Bullopora laevis (Sollas) and some indeterminate attached agglutinated

forms, clearly indicate an environment influenced by highly oxygenated and turbulent

waters in a littoral or sub-littoral setting.

Ammonite assemblages collected from the railway cutting north of Uitenhage (Rogers

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Dil

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& Schwarz 1901) and from the vicinity of Cuyler Manor, east of Uitenhage (Rogers &

Schwarz 1901; Haughton 1928; Spath 1930) are dominated by Olcostephanus species

(Cooper 1981) and again emphasize the Late Valanginian age of the samples studied for

foraminifera. There is some suggestion by Haughton (1928: 27) that the basal marine beds

on Cuyler Manor, east of Uitenhage, contain Olcostephanus species.

D2 ANNALS OF THE SOUTH AFRICAN MUSEUM

anaensis

BS)

ic)

?Lingulina mnga

Ammobaculites sp.

Figure 17.

Distribution of foraminifera in

the marine beds near Dunbrody Bridge (site 13).

Key to symbols/No of specimens All other samples from the Dunbrody area proved

O i2 devoid of foraminifera.

Ammobaculites sp.

Ammobaculites sp. B

Miliammina latrobei

Plectinella castlecliffensis

?Ammobaculites spp.

Globulina prisca

Pyrulina cylindroides

Trochammina spp.

?Glomospira sp.

?Miliammina latrobei

?Ammomarginulina sp.

O | Haplophragmoides spp.

Figure 18.

Distribution of foraminifera at sites

Key to symbols/No of specimens O 1-2. © 3-5 6-15 in the | ook Ouraren

O 16-49 @ 50+

Zoetgeneugd Cliff

Samples were collected by I. R. McLachlan and C. Reabow. This extensive outcrop,

cut by the Sundays River, is the surface stratotype for the Sundays River Formation. The

section exposes interbedded sandstones, siltstones and claystones, with the sandstones

showing coarsening up, and more rarely, fining up features (Tankard et al. 1982, fig. 12.4,

section 3). The studied section, examined also for ostracods by Valicenti & Stephens

(1984) is from the northern end of the outcrop, and is not as complete a section as exposed

in the highest cliffs a little to the south. Samples studied have yielded rather variable

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Ep)

foraminifera faunas. This is due in part to post-depositional leaching of the exposure, and

in part to the rather silty and sandy lithologies that dominate the section. However, the

abundance and diversity of foraminifera low in the outcrop (sample 11450), and the

presence here of Epistomina caracolla (Roemer) s.l. and Reinholdella valendisensis

(Bartenstein & Brand), with scattered Sculptobaculites goodlandensis (Cushman &

Alexander) higher in the section, would suggest that the majority of the exposure is

referable to Biozone Bb. The basal part of the outcrop is probably of Biozone C age.

Results are given in Figure 20.

Ammonites from the Zoetgeneugd and Eb en Vloed cliffs (Rogers 1906) are again

principally referable to Olcostephanus (Cooper 1981), and imply a Late Valanginian age.

This locality was one of the earliest exposures of the Sundays River Formation recognized

(see Atherstone 1857: 531) and it seems probable that most nineteenth-century records of

fossils from the ‘Sundays River’ were obtained from the Zoetgeneugd and Eb en Vloed

cliff-line. The outcrops lie 2 km to the south-west of borehole AD 1/68, where only some

200 m of the basal Sundays River Formation was intersected, and just to the east of

Kirkwood Formation outcrops on the farm Coega Kammas Kloof, as well as being

athwart the Addo Nose basement high, thus confirming the very low stratigraphic level of

the Sundays River Formation exposed here.

Ammobaculites subaequalis

Citharina austroafricana

Ammobaculites parvispira

Sculptobaculites goodlandensis

Vinelloidea buchenroderi

Ammobaculites sp. C

Ammobaculites sp. B

Haplophragmoides sp. A

Haplophragmoides sp. B

Ammobaculites sp. A

Astacolus explicatus 8.1.

Epistomina caracolla s.1.

Epistomina australis

Epistomina sp. D

Nodosaria grisbrooki

Nodobacularia sp. A

Tristix excavata

Planularia formosa

Lenticulina coegaensis

Lenticulina nodosa s.1.

Lenticulina sp.

Astacolus sp.

Astacolus gilli

Dentalina spp.

Vaginulina sp.

Lingulina spp.

Dorothia australis

Planularia spp.

Bullopora laevis

fe]

fe)

Figure. 19.

Distribution of foraminifera at three sites along the Uitenhage to Graaff-Reinet Road.

ANNALS OF THE SOUTH AFRICAN MUSEUM

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Figure 20.

Distribution of foraminifera from the northern end of the Zoetgeneugd Cliff,

outcrop stratotype of the Sundays River Formation.

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FORAMINIFERA OF THE SUNDAYS RIVER FORMATION

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Figure 20 (CONTINUED).

56 ANNALS OF THE SOUTH AFRICAN MUSEUM

TABLE3

Localities and descriptions of outcrop samples studied.

Locality: AIREDALE (page 44)

Latitude: 33°44'34"S Longitude: 25°35'51"E

Samples collected (SOEKOR Laboratory number and description)

4920—North quarry next to Coega River: basal Sundays River Formation; sandy pale grey claystone,

rare shell, no lignite.

492 1—West quarry (Upper): slightly silty grey claystone with cemented sandstone, no shell, very rare

lignite.

4922—West quarry (Lower): very silty grey claystone, very rare shell and lignite.

4923—Central quarry: basal Sundays River Formation; very sandy, very pale grey claystone, no shell, no

lignite.

4923.1—Central quarry: red claystones: topmost Kirkwood Formation.

Locality: AMSTERDAMHOEK First exposure of Sundays River Formation, in railway cutting, 2.5 km

north of Swartkops station. (page 44)

Latitude: 35°50'30"S Longitude: 25°36'25"E

Samples collected (SOEKOR Laboratory number and description)

11458—Top: fine grey claystone, no shell, very rare lignite.

11459—Fine, slightly silty grey claystone, no shell, moderate lignite.

1 1460—Fine grey claystone, no shell, some lignite.

11461—Fine grey claystone, slightly iron-stained, no shell, some lignite.

11462—Bottom: fine grey claystone, some bivalve shell, no lignite.

Locality: COEGA BRICK PITS (page 45)

Latitude: 33°45'1S"S Longitude: 25°40'00"E

Samples collected (SOEKOR Laboratory number and description)

11985—North Quarry, top: fine grey claystone, no shell or lignite.

11435—North Quarry: fine dark grey claystone, some lignite, no shell.

11436—North Quarry, middle: fine dark grey claystone, some shell and rare lignite.

11986—North Quarry: fine dark grey claystone, no shell or lignite.

11437—North Quarry, bottom: fine dark grey claystone, some shell and rare lignite.

4924—North Quarry, bottom: fine silty dark grey claystone, rare shell and lignite.

11987—South Quarry, top: fine slightly silty grey claystone, very rare shell and lignite.

11441—South Quarry: very silty grey claystone, very rare lignite, no shell.

11988—South Quarry: fine dark grey claystone, very rare shell, common lignite.

11439—South Quarry: fine dark grey claystone, some shell and moderate lignite.

11440—South Quarry: fine dark grey claystone, rare lignite, no shell.

11989—South Quarry: very silty grey claystone, no shell, very rare lignite.

11438—South Quarry, bottom: fine silty dark grey claystone, rare lignite.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 7

Locality: COLCHESTER CLIFF Near Site Q of Rogers (1906) (page 45)

Latitude: 33°41'00"S Longitude: 25°49'35"E

Samples collected (SOEKOR Laboratory number and description)

11993—Top Sundays River Formation, just below base Upper Algoa Group: fine grey claystone, no

shell or lignite.

11994—Fine grey very silty claystone, no shell or lignite.

11995—Fine grey claystone, no shell, very rare lignite.

11996—Fine grey claystone, no shell, rare lignite.

11997—Fine grey claystone, no shell, very rare lignite.

11998—Fine grey, silty claystone, no shell, moderate lignite.

11999—Iron-stained cemented nodular band, no shell or lignite.

11442—Fine grey, slightly silty claystone, no shell, some lignite.

12000—Partly iron-stained fine grey claystone, no shell, very rare lignite.

11443—Fine grey claystone, no shell, very rare lignite.

12001—Fine grey claystone, slightly shelly and very rare lignite.

11444—Fine grey claystone, very rare shell and lignite.

12002—Fine grey claystone, no shell, very rare lignite.

11445—Fine grey claystone, no shell, very rare lignite.

12003—Fine grey claystone, partly iron-stained, no shell, very rare lignite.

12004—Fine grey claystone, no shell.

11446—Fine grey claystone, no shell, very rare lignite.

12005—Fine grey claystone, no shell, very rare lignite.

11447—Fine grey claystone, no shell, some lignite.

11448—Fine grey claystone, partly iron-stained, no shell, no lignite.

11449—Bottom of exposure in stream bed: fine grey claystone, no shell, some lignite.

Locality: MARINE BEDS NEAR DUNBRODY BRIDGE (SITE 13) (page 46)

Latitude: 33°28'33"S Longitude: 25°33'44"E

Samples collected (SOEKOR Laboratory number and description)

11468—Variably cemented lignitic silty sandstone with oysters and gastropods.

11469—Fine grey claystone with rare lignite, no shell.

11470—Fine grey claystone with lignite and plant fragments, no shell.

11471—Silty grey claystone with rare lignite, no shell.

11472—Fine, slightly silty, grey claystone, with rare lignite, no shell.

11473—Lignitic grey clayey sandstone with rare oyster shell.

11474—Lignitic grey clayey sandstone with common oyster shell.

Locality: PAALTJIESKRAAL (SITE 4) (page 46)

atitude: 433°28'59"S Longitude: 25°30'28"E

Samples collected (SOEKOR Laboratory number and description)

4905—Fine grey claystone in Kirkwood Formation, doubtful shell, no lignite.

4906—Fine pinkish-grey claystone in Kirkwood Formation, no shell, no lignite.

4907—Oyster band, with partly cemented brownish-grey clayey sandstone.

58 ANNALS OF THE SOUTH AFRICAN MUSEUM

Locality: ZOUTKLIP (SITE 5) (page 46)

Latitude: 33°28'22"S Longitude: 25°30'37"E

Samples collected (SOEKOR Laboratory number and description)

4908—Fine, silty grey claystone in Kirkwood Formation, with rare lignite, shell.

4909—Fine, iron-stained brownish-grey claystone in Kirkwood Formation, no lignite, no shell.

4910—Fine grey carbonaceous claystone with plant remains, Kirkwood Formation, no shell.

491 1—Brownish-grey clayey sandstone with Unio shells in Kirkwood Formation, some lignite.

Locality: BEZUIDENHOUT RIVER (WEST OF SITE 10) (page 46)

Latitude: 33°28'35"'S Longitude: 25°31'47"E

Samples collected (SOEKOR Laboratory number and description)

4912—Fine grey claystone 2 m below oyster bed: bottom. No lignite, no shell.

4913—Fine silty brownish-grey claystone | m below oyster bed. Rare lignite, no shell.

4914—Oyster bed with iron-stained, brownish silty sandstone.

4915—Fine silty grey claystone 1 m above oyster bed. No lignite, no shell.

4916—Sandy greyish siltstone with Unio shells, about 30 m above oyster bed: top. No lignite.

Locality: BLUE CLIFF STATION (SITE 2) (page 46)

Latitude: 33°29'45"S Longitude: 25°28 16"E

Samples collected (SOEKOR Laboratory number and description)

4917—Fine brownish-grey claystone below sandstone; no lignite, no shell.

4918—Fine grey claystone, above sandstone, no lignite, no shell.

Locality: DUNBRODY STATION (SITE 10) (page 46)

Latitude: 33°28'23"S Longitude: 25°32'24"E

Samples collected (SOEKOR Laboratory number and description)

4919—Oyster band above canal: shelly, silty iron-stained sandstone.

4919.1—Fine pale grey claystone no lignite, no shell.

4919.2—Fine pale grey claystone no lignite, no shell.

4919.3A—Clayey and silty partly cemented brownish sandstone with oysters and bivalves, rare lignite.

4919.3B—Clayey and silty partly cemented brownish sandstone with rare shell and lignite.

4919.4—Grey, very cemented silty sandstone with lignite, bivalves, oysters and gastropods.

4919.5A—Grey cemented silty sandstone with oysters and bivalves, rare lignite.

4919.5B—Sandy grey claystone with rare bivalve shell and some lignite.

4919.6—Fine silty grey claystone with rare oyster shell and rare lignite.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION a9

Locality: MFULENI (SITE 15) (see also McLachlan & McMillan 1976: 206) (page 46)

Eatitude: 33°27'S1"S Longitude: 25°31'36"E

Samples collected (GSOEKOR Laboratory number and description)

4816—Top: Sandy pale grey claystone, no shell, rare lignite.

4817—Very sandy pale grey claystone, no shell, rare lignite.

4818—Slightly silty pale grey claystone, no shell some lignite.

4819—Silty grey claystone, no shell or lignite.

4820—Cemented silty sandstone, freshwater ostracods (Cypridea), very rare lignite.

4821—Friable silty sand, freshwater ostracods (Cypridea), very rare lignite.

4822—Fine pale grey claystone, some cementing, no shell, no lignite.

4823—Silty pale grey claystone, no shell some lignite.

4824—-Very silty pale grey claystone, no shell, no lignite.

4825—Fine grey claystone, very lignitic no shell.

4826—“Silty fine grey claystone, few siderite spheres, no shell, no lignite.

4827—Silty grey claystone, slight iron-staining, no shell or lignite.

4828—Bottom: silty grey claystone, abundant lignite, no shell.

Locality: CASTLE CLIFF (page 47)

eatitude: 33°23'39"S Longitude: 2535'37'E

Samples collected (SOEKOR Laboratory number and description)

18588—Claystone in cliff below massive sandstone with gastropods, oysters, bivalves, lignite.

Locality: LOW LEVEL BRIDGE (page 47)

Latitude: 33°28'26"S Longitude: 25233/53 0

Samples collected (SOEKOR Laboratory number and description)

18589—Grey claystone with rare shells; weathered sample.

Locality: THE LOOK OUT (SITE 14) (page 47)

Latitude: 33°28'26"S Longitude: 25°36'22"E

Samples collected (SOEKOR Laboratory number and description)

18590—Laminated siltstone and claystone, no shell: top.

18591—Siltstone with claystone laminae; shells (bivalves (+7rigonia) and gastropods) in fine sandstone

lenses; some lignite.

18592—Claystone with silty laminae; bivalves; lignite on siltier bedding planes.

18593—Claystone with silty laminae; bivalves (+ Perna) and lignite on silty bedding planes.

18594—Silty claystone; no fossils; lignite on bedding planes.

18595—Silty claystone; with Mytilus, gastropods and trace lignite.

18596—Claystone with 8 cm oyster band; big oysters, Perna atherstoni and other bivalves; trace lignite.

18597—Claystone with siltstone laminae; rare shell, trace lignite.

18598—Claystone, trace lignite on bedding planes, no shell.

18599—Claystone, trace lignite on bedding planes; no shell.

60 ANNALS OF THE SOUTH AFRICAN MUSEUM

Locality: UITENHAGE TO GRAAFF-REINET ROAD CUTTINGS (page 48)

Latitude: 33°47'10"S Longitude: 25°25'41"E

Samples collected (SOEKOR Laboratory number and description)

1 1463—Basal Sundays River Formation at junction of Port Elizabeth to Uitenhage and Uitenhage to

Graaff-Reinet roads: silty grey claystone, no shell or lignite.

Latitude: 33°46'45"S Longitude: 25°25'50"E

Samples collected (SOEKOR Laboratory number and description)

11464—Sundays River Formation | km north of junction: very silty glauconitic dark grey claystone,

very rare shell, no lignite.

Latitude: 33°45'47"S Longitude: 25°25'S7"E

Samples collected (SOEKOR Laboratory number and description)

11465—Sundays River Formation 2.4 km north of junction: top: fine grey claystone, slightly

iron-stained, no shell or lignite.

11466—Sundays River Formation 2.4 km north: bottom, 1.6 m below 11465: fine grey claystone,

slightly iron-stained, no shell or lignite.

Locality: ZOETGENEUGD (NORTH END OF CLIFF) (page 52)

Patitudes 33235375 Longitude: 25°38'S1"E

Samples collected (SOEKOR Laboratory number and description)

11974—Top: sandy grey claystone, with secondary gypsum, no shell, very rare lignite.

11975—Fine grey claystone, no shell, very rare lignite.

11976—Very sandy grey claystone, no shell very rare lignite.

11977—Very silty grey claystone, no shell, very rare lignite. ?Secondary gypsum.

11457—Very silty grey claystone, no shell, some lignite.

11978—Silty grey claystone, no shell, very rare lignite. Secondary gypsum.

11979—Fine grey claystone, no shell, some lignite.

11980—Silty grey claystone, no shell, some lignite.

11981—-Very silty grey claystone, no shell, some lignite.

11456—Very finely silty grey claystone, no shell, some lignite.

11982—-VVery silty grey claystone, no shell some lignite.

11983—Shightly silty grey claystone, no shell, moderate lignite.

11454—-Very silty grey claystone,very rare shell, moderate lignite.

11455—Very silty grey claystone, some cemented sandstone, oysters, moderate lignite.

11450—Very silty grey claystone, no shell rare lignite.

11451—-Very sandy greyish claystone, some cemented sandstone, some shell and lignite.

11984—Shightly silty grey claystone, rare shell, moderate lignite.

11452—-Very sandy greyish claystone, some cemented sandstone, oysters, rare lignite.

11453—Bottom: very sandy greyish claystone, some cemented sandstone, oysters, moderate lignite.

Latitudes and longitudes from 1:50 000 topographic sheets

(Gauss Conform Projection Central Meridian 25°East—Clarke 1880 Spheroid).

3325AD (KIRK WOOD) 3325BC (COERNEY) 3325DA (ADDO) 3325CD/3425AD (UITENHAGE)

3325DB (COLCHESTER) 3325DC+DD/3425BA (PORT ELIZABETH)

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 61

INTERPRETED PALAEOENVIRONMENTS

Although much discussion has been engendered over the years on the age of the

Sundays River Formation, comparatively littke comment has been made on its

environment of deposition. Shone (1976a, 1976b, 1978) examined the sedimentological

and lithological features of Sundays River outcrops and the fully-cored borehole sections

AD 1/68 and PA 1/68. He regarded the outcrops and sections studied by him to indicate

that the Sundays River Formation accumulated in a tidal-flat environment.

Valicenti & Stephens (1984), from their examination of the ostracods, regarded the

later part of the Late Valanginian, where ostracods are abundant, to have accumulated in a

warm-water, shallow-marine environment with an abundant food supply. Rare

brackish-water and marginal-marine ostracods occur at this time too, indicating a close

proximity to fluvial environments. In contrast, in the Early Hauterivian, a different, poor

ostracod fauna is preserved, which they considered as indicative of a sudden deepening

and cooling of the sea that occurred close to the Valanginian—Hauterivian boundary. In the

Late Hauterivian, ostracods once more become abundant, and they reflect a middle-shelf

environment of deposition, again with genera typical of brackish and marginal marine

facies also present.

Although not immediately evident, these lithological and ostracodal interpretations

reflect different aspects of the same depositional model. The variation and range of

depositional environments within the Sundays River Formation seem to be greater than

understood by either Shone (1976a, 19766, 1978) or Valicenti & Stephens (1984). It

appears that most of Shone’s (1976a) conclusions arguing for a tidal-flat environment

derive from outcrops and boreholes located near the northern perimeter of the Sundays

River Formation (Zoetgeneugd outcrop round to borehole PA 1/68). In contrast, the

remarks of Valicenti & Stephens (1984) are based mainly on those areas where ostracods

are common, that is, the southern outcrops (such as Coega Brick Pits and Colchester Cliff)

and the adjacent borehole sections.

LATE VALANGINIAN

Figures 21 to 24 show the distribution of the various depositional environments

recognized on the basis of the foraminifera faunas for two time-slices in the Late

Valanginian and one each in the Early and Late Hauterivian.

The basal Sundays River Formation accumulated in a marginal-marine and estuarine

environment. Poor foraminifera faunas occur widely (Biozones C and D) immediately

following the transgression over the Kirkwood Formation, suggesting that freshwater

influence remained strong throughout the onshore Algoa Basin for some time after the

initial marine incursion. Subsequently, depositional environments became more

differentiated. Shallow-marine and estuarine environments, strongly affected by

freshwater input, prevailed throughout Late Valanginian times in the north and east of the

Sundays River Formation. As has been pointed out by Shone (1976d: 40), the maximum

diversity of macro-invertebrates occurs near to the present-day coast, with least diversity

62 ANNALS OF THE SOUTH AFRICAN MUSEUM

BOREHOLE re ee*

BOUNDARY OF ALGOA BASIN A ESTUARINE AND

FAULT f MARGINAL MARINE

SHOREWARD LIMIT OF PRESERVED / © > ®

SUNDAYS RIVER FORMATION

(BIOZONE D) j e

. PROBABLE SOUTHERN LIMIT OF

TRUE KIRKWOOD FORMATION

(RED BEDS)

MARGINAL e

MARINE \_#

4) EARLIEST LATE VALANGINIAN PALAEOENVIRONMENTS _”

(ONSET OF MARINE CONDITIONS : BIOZONE D)

KILOMETRES

Figure 21.

Depositional environments of the Sundays River Formation

in the earliest Late Valanginian (Biozone D).

occurring in the north: foraminifera diversities parallel this distribution. Shone’s (1976a,

19766) arguments for a tidalite style of deposition in the north are convincing, but further

south, the diversity of foraminifera and the presence of small numbers of Radiolaria

(Fig. 77A—J) suggest an outer-shelf to uppermost-slope environment of deposition. The

two cleanest, deepest marine sections studied are MV 1/79 and AL 1/69 boreholes, and

they yielded the most diverse foraminifera faunas and the greatest numbers of Radiolaria.

However, different drilling techniques, and the resulting rather poor samples from

VO 1/71, CO 2/70, CO 3/71, and KE 1/71, make it impossible to determine the areal

extent of Radiolaria in the Sundays River Formation.

EARLY HAUTERIVIAN

As reviewed at the beginning of this section, Valicenti & Stephens (1984) interpreted a

substantial water-depth and temperature change over the Valanginian—Hauterivian

boundary, based on changes in ostracod faunas. The presence of small numbers of

Radiolaria in borehole MV 1/79 in the later Late Valanginian and in the earlier Early

Hauterivian, and only a little change in the species of foraminifera present through this

interval (though foraminifera abundances are very different), suggest that water depths

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 63

K'BSY

LIMIT OF PRESERVED BIOZONE Ba SEDIMENTS

DEPOSITIONAL ENVIRONMENT BOUNDARIES

SEDIMENT INPUT

BOREHOLE Yr:

BOUNDARY OF ALGOA BASIN WM ITTORAL

FAULT

UPPER

? scope ?

PORT

ELIZABETH

@ LATER LATE VALANGINIAN PALAEOENVIRONMENTS

(EXTENSIVE MUODY SEA-FLOOR : BIOZONE Ba)

KILOMETRES

Figure 22,

Depositional environments of the Sundays River Formation

in the later Late Valanginian (Biozone Ba).

and water chemistry changed little during this period. The same is true of the

Valanginian—Hauterivian boundary elsewhere, where it occurs in relatively clean or cored

borehole sections (AL 1/69, CO 1/67, SM 1/76). The major decline in foraminifera

abundance in the Early Hauterivian (Fig. 10) is believed to have been caused by

fluctuating sediment input into the Algoa Basin at this time. The tectonic disturbances that

caused the IAtl unconformity, and a possible Valanginian—Hauterivian boundary

unconformity were followed by increased sediment input, so that the sea-floor as far out

as the shelf-break was flooded by sand lobes. During these sandy incursions, foraminifera

numbers declined on the sea-floor; and post-depositional leaching of calcite within these

sands has further reduced the numbers of microfossils recovered.

LATE HAUTERIVIAN

In the Late Hauterivian, sea-floor conditions began to quieten again: decreased rates of

sediment input led to generally finer-grained sedimentation and a corresponding increase

in abundance and diversity of foraminifera. Leaching of the clayey sediments has been

impeded by their low permeability, and microfossil preservation remains generally good.

The marked difference between the foraminifera assemblages of clayey and sandy

64 ANNALS OF THE SOUTH AFRICAN MUSEUM

LIMIT OF PRESERVED BIOZONE Ix

DEPOSITIONAL ENVIRONMENT BOUNDARIES

SEDIMENT INPUT

BOREHOLE

BOUNDARY OF ALGOA BASIN

FAULT ;

DEVELOPMENT OF SAND LOBES Ly UPPER »

Q SLOPE °

PoRT “ »

ELIZABETH a

@) EARLY HAUTERIVIAN PALAEOENVIRONMENTS

(INCREASED SAND SUPPLY : BIOZONE TX)

9 = 40 60

KILOMETRES

Figure 23.

Depositional environments of the Sundays River Formation

in the Early Hauterivian (Biozone IX).

intervals is particularly clear in the cleanly drilled Late Hauterivian section of borehole

AL 1/69.

As in the Late Valanginian, the distal Sundays River Formation in the Late Hauterivian

would seem to have accumulated in an outer-shelf or uppermost-slope environment.

Close to the northern margin of the Formation, marginal marine and estuarine conditions

prevailed throughout the Late Valanginian and Hauterivian, most notably in the north-east

(NA boreholes). Sand lobes continued to extend southward, but are thinner and less

frequent in the Late Hauterivian. They contain abundant Ammobaculites subaequalis

Myjatliuk with occasional attached Bullopora laevis (Sollas). Presumably during episodes

of increased sediment input, when sand lobes were reaching as far as the distal parts of the

onshore Algoa Basin, conditions were too disturbed on the sea-floor to permit

argillophilic species to occupy the northern part of the Basin. Post-depositional leaching,

preferentially through the more permeable sands may well have destroyed most calcitic

foraminifera tests that were in the sands at the time of deposition. Ammobaculites

subaequalis is certainly the thickest-walled agglutinated foraminifera encountered in the

Sundays River Formation, and may have best survived leaching processes. However, the

presence of Bullopora laevis in some of the sands indicates that not all calcite has been

removed. |

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 65

LIMIT OF PRESERVED BIOZONE II

* DEPOSITIONAL ENVIRONMENT BOUNDARIES

SEDIMENT INPUT

ol.*

BOREHOLE XS

BOUNDARY OF ALGOA BASIN

FAULT

i ~~,

«oe IDOLE s

PORT

ELIZABETH

LATE HAUTERIVIAN PALAEOENVIRONMENTS

(MUDDY SEA-FLOOR WITH OCCASIONAL SAND

LOBES : BIOZONE I )

KILOMETRES

Figure 24.

Depositional environments of the Sundays River Formation in the Late Hauterivian

(Biozone III).

OXYGEN LEVELS AND WATER TEMPERATURES

At the commencement of Sundays River Formation deposition, oxygen levels were

high (Biozones D and C), and water depths were probably typical of innermost shelf

localities. During the times of Biozones Bb and Ba, water depths show a greater range,

from outermost shelf in the south to estuarine and tidal in the north and north-east but,

although foraminifera are abundant, species diversity is not very high. Species of

Epistomina, Reinholdella, Ammobaculites and Haplophragmoides predominate. In

contrast, offshore boreholes in the Algoa Basin (especially Hb—D1) do not show this

feature, and nodosarids, especially Lenticulina species, are much more common in the

time-equivalent strata. The same species of Epistomina, Reinholdella, Ammobaculites

and Haplophragmoides do occur in the offshore boreholes, but in smaller numbers.

The predominance of aragonitic species in the Sundays River Formation onshore

suggests that environments during Bb and Ba times were distinctly restricted, with

lowered oxygen levels at the sea-floor. The presence of Radiolaria at this time, as in

MV 1/79, indicates that oxygen conditions in the surface waters were probably near

normal. The offshore basement high associated with the Coega—St Croix fault system (see

Fig. 2) acted as a sill to the Sundays River Trough to the north until 1Atl (latest

66 ANNALS OF THE SOUTH AFRICAN MUSEUM

Valanginian) times, and as a consequence, sea-floor oxygen values seem to have been

somewhat reduced, and foraminifera faunas rather restricted. Unfortunately, the few,

rather shallow marine sections of this interval examined in the Uitenhage Trough (ST 1/71

and SW 2/68), and thus south of the basement high do not reveal a substantially different

assemblage. The reason for this is not clear.

It seems probable that in the silled Sundays River Trough, water temperatures were

somewhat higher than in the adjoining regions. Valicenti & Stephens (1984) and Valicenti

(pers. comm., 4 November 1986) have remarked on the frequency with which

Cytherelloidea occurs in Late Valanginian near-shore environments of the Cape south

coast. This ostracod genus ts restricted to warm waters at the present day. However, that

the northern Algoa Basin could not have been too warm is indicated by the complete lack

of any type of larger foraminifera throughout the sequence; none are known either from

other contemporaneous deposits in southern Africa.

As mentioned previously, above 1 Atl (top Biozone Ba) the Sundays River Formation

is much more sandy than below, and microfaunas are much poorer. From the thin-walled,

unornamented ostracods that occur here (latest Valanginian and Early Hauterivian),

Valicenti & Stephens (1984) have considered that water depths increased, and water

temperatures declined abruptly. In contrast, the foraminifera show little change, except in

numbers of specimens being significantly less. This perhaps 1s indicative of little change

in either water temperatures or water depths, but rather reflects a marked increase in

sediment input into the Sundays River Trough from the time of the Biozone Ba—

Biozone A boundary to the top of the Early Hauterivian. In the Late Hauterivian,

sandstones become less abundant again, and there is a consequent increase in diversity

and abundance of foraminifera faunas. The reduced oxygen levels of the Sundays River

Trough were eliminated as the offshore Coega—St Croix high subsided during the

Hauterivian, and thereafter became blanketed with sea-floor sediment.

Palaeolatitude reconstructions for the Valanginian—Hauterivian period by Smith &

Briden (1977) indicate that the south coast of South Africa then lay at about 53°S. In

fault-controlled depocentres of the Pletmos, Gamtoos and Algoa basins, sedimentation

rates for the Valanginian and Hauterivian are high, attaining 400 to 600 m (uncorrected)

per million years locally. Sediment supply and freshwater runoff from the land were

clearly considerable at this time. Foraminifera faunas of the Sundays River Formation are

considered to reflect cool, temperate marine conditions, although, as mentioned above,

the Sundays River Trough may have been a little warmer (though not tropical) during the

Late Valanginian Biozones Ba and Bb.

PALAEOECOLOGY OF FORAMINIFERA GROUPS

OF THE SUNDAYS RIVER FORMATION

The onshore Algoa Basin during Sundays River Formation times was dominated by

substantial freshwater and sediment input that together define the types of foraminifera

found. A summary of the following data is shown in Figure 25. Agglutinated foraminifera

form a substantial proportion of studied assemblages. Species of the genera

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 67

Ammobaculites and Haplophragmoides predominate in shallow marine, innermost shelf

environments where oxygen values range from near normal to greatly lowered, and

salinities are usually somewhat reduced. Large numbers of these two genera also occur at

inner- to outer-shelf locations, in association with calcareous foraminifera. In more

restricted, rather reduced oxygen conditions on the shelf, Ammoglobigerina,

Trochammina and Dorothia occur in some numbers, as in the Hauterivian of CK 1/68.

Environments affected by markedly hyposaline water, as during the basal Sundays

River transgression, are characterized by a predominance of Miliammina specimens.

Locally, hyposaline environments may be referable to a particular estuary, but the precise

situation during the basal transgression, with the widespread occurrence of ‘estuarine’

conditions at that time remains rather unclear.

Nodosarid genera such as_ Lenticulina, Astacolus, Citharina, Planularia,

Pravoslavlevia and others are found most abundantly on the shelf, but, with the exception

of Citharina, appear to avoid the innermost shelf and marginal marine conditions.

Polymorphinids, in contrast, seem to be most frequent in stressful environments. In the

Colchester Member of the Uitenhage Trough, Eoguttulina and Globulina are believed to

be associated with broad mudflats at the mouth of an estuary (McMillan 1980), but in the

Sundays River Formation they occupy a wider array of stressful environments. The two

genera also do occur in substantial numbers in marginal marine, probably reduced salinity

facies of the Sundays River Formation, but on the middle and outer continental shelf, large

numbers may be associated with short-lived periods of low sea-floor oxygen levels.

Attached forms such as Bullopora are most numerous in the thin sands of the Late

Hauterivian, where they are almost always found on large tests of Ammobaculites on the

middle and outer shelf, perhaps suggesting turbulent sea-floor conditions at these times.

Attached miliolids (Nubecularia, Vinelloidea, and ?Calcitornella) occur in two dis-

tinct environments: close to shore, in or near the littoral (Vinelloidea, as at the Uitenhage

to Graaff-Reinet Road outcrop) and further out on the continental shelf (Nubecularia and

?Calcitornella), where, with Bullopora, they occur most notably in the Late Hauterivian,

though they are not especially associated with the thin sands. Attached miliolids at the

present day often occur in environments with a high dissolved oxygen level, particularly

in protected littoral and sublittoral environments along wave-swept rocky shores. It may

be that their presence in the more offshore Late Hauterivian reflects higher oxygen values

at that time. Free miliolids (Cornuspira and Quinqueloculina) are surprisingly scarce,

occurring occasionally across the shelf. The free-living representatives of the genus

Nodobacularia are confined to nearshore localities.

The concentration of miliolids seen on the South African inner shelf at the present day

is not echoed in the Sundays River Formation, probably because of the generally

hyposaline proximal environments in the Algoa Basin. However, one species of

Quinqueloculina does occur extensively and in great numbers through the marginal

marine, mostly mudflat environments of the Colchester Member of the Uitenhage Trough

(McMillan 1980).

The aragonitic genera Epistomina, Reinholdella and Conorboides occur in variable

numbers from the inner to outer shelf, but only Epistomina appears to venture close to

68 ANNALS OF THE SOUTH AFRICAN MUSEUM

Transi- Inner Middle Outer Upper

Species a Shelf Shelf Shelf Slope

Miliammina latrobei sp. nov.

Haplophragmoides spp.

Ammobaculites spp.

Plectinella castlecliffensis sp. nov.

Globulina prisca

Astacolus gilli sp. nov.

Vinelloidea buchenroderi sp. nov.

Lenticulina nodosa s.1.

Astacolus calliopsis

Astacolus explicatus

Citharina austroafricana

Episromina caracolla

Epistomina australis

Eoguttulina anglica s.1.

Nodosaria paupercula

Dorothia australis sp. nov.

Trochammina spp.

Astacolus gibber

Sculptobaculites goodlandensis

Tristix spp.

Reinholdella spp.

Lagena spp.

Amphicoryna pletmosiana sp. nov.

Pseudonodosaria spp.

Verneuilina secreta sp. nov.

Bullopora laevis

Eoguttulina cf. E. liassica

Epistomina hechti

Lenticulina coegaensis sp. nov.

Lenticulina heiermanni

Pravoslavlevia spp.

Frondicularia nieuwjaarskopensis sp. nov.

Reinholdella valendisensis plettenbergia

subsp. nov.

Gravellina sp. A

Radiolaria

Figure 25

Interpreted depth ranges of selected foraminifera species from the Sundays River Formation.

shore, and all three genera avoid hyposaline (?and hypersaline) conditions near the

margins of the basin. Floods of Epistomina, dominating foraminifera assemblages, appear

to be typical of organic-rich shelf claystones (often with hemipelagic qualities and

characterized by high gamma electric log responses) at a number of horizons in the South

African Late Jurassic (Portlandian) and Early Cretaceous (Early Berriasian and later Early

Barremian).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 69

SELECTIVE PRESERVATION

Weathering of microfaunas from outcrops is clearly seen at a number of localities, and

leaching of microfaunas may occur in sandy intervals of boreholes. Study of many surface

outcrop samples has provided an indication of the progressive elimination of the

foraminifera faunas. Percolating groundwater containing oxygen and humic and inorganic

acids penetrates Sundays River strata. Macrofossil and microfossil shell debris begins to be

leached and precipitated elsewhere as calcite cement, vein calcite, or over other macrofossil

and microfossil material. Leached microfossils appear as corroded remnants: thick test

walls and features such as umbilical bosses and infillings, limbate sutures, peripheral keels

and prolocular areas tend to survive, whereas the thinner chamber walls are removed.

Lenticulina and Epistomina tests, for example, thus tend to show a ‘skeletal’ effect. In such

cases, the chamber infillings, exposed to percolating water, begin to deteriorate. Calcite

infillings appear to suffer at much the same rate as the foraminifera shell, but pyrite fillings,

which are usually composed of microframboidal spheres, weather rapidly to rust colour iron

oxides and carbonates. Such weakened tests are easily destroyed during insensitive sample

processing. Pyritized Radiolaria and true framboids that have been oxidized in this way also

suffer during processing. Where leached calcite re-precipitates on calcareous microfossils,

crystal overgrowths occur on calcite foraminifera shells, often developing to such an extent

that precise identification of specimens is impossible.

Further leaching selectively removes all calcareous tests, leaving exclusively

agglutinated assemblages. Of course, it may prove to be very difficult to establish whether

an agglutinated assemblage is a residue of a larger one formerly containing calcitic

species, or one that has always been 100 per cent agglutinated. Only analysis of suites of

samples from vertical sections, with comparisons of intensity of leaching, and of relative

abundances and preservation of calcareous tests, as well as comparisons between outcrop

and borehole data for the same interval, can establish the intensity of test corrosion at

outcrops. As with pyrite infillings of leached calcareous shells, pyrite-infilled

agglutinated tests show a rust-red coloration through the damaged test wall when

corroded. More intense leaching would seem to selectively remove those agglutinated

tests with a calcite cement, leaving the exclusively siliceous forms as the most resistant

remnant of Sundays River Formation faunas.

TAXONOMY

The foraminifera of the Sundays River Formation are dominated by several groups,

particularly nodosarids, epistominids and agglutinated species. Miliolids are usually rare,

and rotalids of all types, except the aragonitic genera, are absent. The majority of the

species encountered range through most or all of the Sundays River Formation, but there

are a number that are confined to specific intervals, and these have been of considerable

use in establishing the foraminifera biozonation. Summarized stratigraphic ranges of the

foraminifera detailed in the taxonomic section are shown in Figure 26 (fold out chart at

the back of this Volume). A taxonomic index is given in Table 4.

70 ANNALS OF THE SOUTH AFRICAN MUSEUM

TABLE 4

List of species and other material described, together with page and figure references.

Species Page Figures

Saccammina spp. 74 27A—B

Pelosina zoetgeneugdensis sp. nov. 74 27C—F

Ammodiscus spp. WS 27G—H

Hormosina sp. A 75 27]

Reophax spp. TT 27J, 283A—B

Haplophragmoides sp. A 79 28C-E

Haplophragmoides sp. B 81 28F—H

Haplophragmoides sp. C 81 28I-J, 29A

Haplophragmoides sp. D 82 29B-E

Haplophragmoides sp. F 82 29F-I

Haplophragmoides spp. 83 —~

Ammobaculites subaequalis Mjatliuk 83 30A—D

Ammobaculites sp. A 86 30E

Ammobaculites sp. B 86 30F-I

Ammobaculites sp. C 87 30J-K

Ammobaculites parvispira Ten Dam 87 31C-G

Ammobaculites spp. 89 —

Sculptobaculites goodlandensis (Cushman & Alexander) 89 31A—B

Placopsilina cenomana @ Orbigny 90 2y)

Textularia zoetgeneugdia sp. nov. y)| 31K

Ammoglobigerina cf. A. globigeriniformis (Parker & Jones) 93 31L-—M

Trochammina cf. T. inflata (Montagu) 94 33A—D

Trochammina sundaysriverensis sp. nov. 95 33E-H, 34A—C

Trochammina spp. 98 —

Verneuilina secreta sp. nov. 98 331, 35A—D

Verneuilina sp. B 99 35E

Gaudryinella alexandria sp. nov. 101 Sora

Dorothia sp. A 103 35J, 36A—D

Dorothia inglesidensis sp. nov. 103 36E-H, 37A—D

Dorothia australis sp. nov. 107 36I-L, 38A—B

Gravellina sp. A 109 38C—D

Plectinella castlecliffensis sp. nov. sul 39A-F

Cornuspira orbicula (Terquem & Berthelin) Hg ls) 38E—F

?Calcitornella sp. M3 38G

Nubecularia lucifuga Defrance LES 38H-K, 40A—-B

Vinelloidea buchenroderi sp. nov. 116 40C-F

Nodobacularia sp. A 118 40G

Quinqueloculina spp. 118 40H

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION

Species Page Figures

Quinqueloculina minima Tappan 118 42A

Miliammina latrobei sp. nov. E19 41A-F

Nodosaria paupercula Reuss | 42B-K

Nodosaria obscura Reuss 124 42L-N, 43A—B

Nodosaria tomaszowiensis Sztejn 124 43C_-F

Nodosaria grisbrooki sp. nov. 123 43G-J

Nodosaria cf. N. obscura Reuss 128 43M—N

Pseudonodosaria tenuis (Bornemann) 128 43K-L

Pseudonodosaria humilis (Roemer) 129 60H-K

Amphicoryna pletmosiana sp. nov. 130 430-P, 44A—C

Astacolus gilli sp. nov. I33 44D-G

Astacolus humilis (Reuss) [35 44H-I

Astacolus sp. C 136 AAJ

Astacolus microdictyotos Espitali¢é & Sigal s./. 136 45A-K

Astacolus gibber Espitalié & Sigal 140 46A—H

Astacolus schloenbachi (Reuss) 14] 46I-M

Astacolus calliopsis (Reuss) s.1. 144 47A-J

Astacolus explicatus Espitali¢ & Sigal s./. 145 48A—-K

Astacolus sp. A 147 ATK

Astacolus sp. D 148 47M

Astacolus spp. 149 47N

Citharina sp. A 149 48L

Citharina pseudostriatula Bartenstein & Brand 149 48M_N, 49A—-B

Citharina austroafricana sp. nov. 153 49C-J

Dentalina communis @ Orbigny s.1. 156 49K—M

Dentalina linearis (Roemer) leew S50A—C

Dentalina sp. B Io? 49ON

Dentalina spp. IS7 490-P

Frondicularia nieuwjaarskopensis sp. nov. 157 50D-G

Lagena alexandria sp. nov. 161 50H-—L

Lagena sp. A 162 SIA

?Lagena sp. 163 51B

Lagena algoaensis sp. nov. 163 s1C-J

Lagena hauteriviana hauteriviana Bartenstein & Brand 166 52A—B

Lagena hauteriviana cylindracea Bartenstein & Brand 167 52C

Lagena spp. 169 PAB,

Lenticulina coegaensis sp. nov. 169 52E-G

Lenticulina sp. A 171 47L, 52H

Lenticulina cf. L. saxonica Bartenstein & Brand N72 52J-—K

Lenticulina nodosa (Reuss) s.1. 172 53A-—I, 54A—-F

Lenticulina heiermanni Bettenstaedt 177 54G_J

Ae ANNALS OF THE SOUTH AFRICAN MUSEUM

Species Page Figures

Lenticulina subtilis (Wisniowsk1) 179 55A-B

Lenticulina muensteri (Roemer) s./. 180 55C—F

Lenticulina cf. L. cultrata (Montfort) 180 55G-H

Lenticulina spp. 181 —

Marginulina sp. A 181 ap)

?Marginulina pyramidalis (Koch) 181 56A

Marginulinopsis parkeri (Reuss) 181 56B

Neoflabellina cf. N. malakialinensis Espitalié & Sigal 183 56C-E

Palmula sp. 184 56F

Planularia madagascariensis Espitali¢ & Sigal s./. 184 56G-L, 57A—D

Planularia formosa sp. nov. 187 57E—M

Planularia sp. A 189 S58A

Planularia sp. B On 58B—C

Planularia sp. C 191 57N

Planularia spp. 192 58D

Pravoslavlevia frankei (Ten Dam) 92 58E-J

Pravoslavlevia pravoslavlevi (Fursenko & Polenova) 193 58K-L, 59A—C

Psilocitharella arguta (Reuss) 195 59D-G

Vaginulina spp. 196 59H-M

Vaginulinopsis sp. A Noy SON

Vaginulinopsis cf. V. matutina (d’ Orbigny) 197 60A—C

Vaginulinopsis cf. V. prima (d’Orbigny) 199 60D-—G

Lingulonodosaria nodosaria (Reuss) 200 60L—N

Paralingulina hexacarinata (Espitalié & Sigal) 201 600-P, 61A

Lingulina trilobita sp. nov. 202 61B-F

Lingulina bettenstaedti (Zedler) 205 61G—H, N

Lingulina praelonga Ten Dam 206 61I-K

Lingulina simplicissima (Ten Dam) 206 61L—-M

Lingulina mngazanaensis sp. nov. 207 62B-I

Lingulina sp. A 210 62K

Lingulina cf. L. furcillata Berthelin ANY) 62L—M

Lingulina spp. Zale 62A, J

Eoguttulina anglica Cushman & Ozawa s.1. Zl 62N-O, 64A—B

Eoguttulina cf. E. inovroclaviensis (Bielecka & Pozaryski) 212 63A—C

Eoguttulina cf. E. liassica (Strickland) 213 64C-E

Eoguttulina cf. E. polygona (Terquem) DNS 64F-—G

Eoguttulina sp. B DNS 64H-I

Globulina prisca Reuss s.1. 216 64J—N

Pseudopolymorphina colchesterensis sp. nov. 216 65A—H

Pyrulina cylindroides (Roemer) 219 66C—D

Webbinella subhemisphaerica Franke 220 65I-J

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 73

Species Page Figures

Bullopora laevis (Sollas) 22 65K-—L, 66A—B

Ramulina fusiformis Khan 223 66E

Ramulina spp. 224 66F—G

Tristix acutangula (Reuss) 224 66H-K, 67A

Tristix excavata (Reuss) 225 67B—E

Spirillina tenuissima Gumbel 228 67F—G

Conorboides sp. A 228 67H, 68A

Epistomina hechti Bartenstein, Bettenstaedt & Bolli 229 68B—H

Epistomina australis Masiuk & Vina 231 681, 69A

Epistomina caracolla (Roemer) s.1. 233 69E-I, 70A-I, 72A—E

Reinholdella valendisensis (Bartenstein & Brand) 239 72F-I, 73 A—-F

Reinholdella sp. D 245 73G—I

Reinholdella platterugensis sp. nov. 246 74A—-H

Reinholdella valendisensis plettenbergia subsp. nov. 248 741

Reinholdella sp. C 249 76A

Reinholdella hofkeri (Bartenstein & Brand) 249 76B-—G

?Colomia sp. 252 76H-I

Radiolaria ZoL TTA-J

Bivalves 253 7T8A

Mysid statoliths 253 78B, D

Arthropods: ‘shrimps’ 259 79A—D

Echinoid spines 259 78C

Crinoid ossicles 255 78E-G

Echinoderm debris pseye | 78H

Ophiuroid ossicles 257 80B

Holothurian sclerites 257 781, 80A

Hexiseds 259 80C

?Charophyte oogonia 259 80D

The suprageneric taxonomic classification used is that of Loeblich & Tappan (1964,

1974), amended by Haynes (1981). Generic revisions indicated by Loeblich & Tappan

(1986, 1988) are included. The classification is given from family level only; the above

references provide additional details.

All illustrated and described specimens, including holotypes, paratypes and

comparative material, have been deposited in the collections of the South African

Museum, Cape Town. Each individual specimen has been allocated a catalogue number,

prefixed SAM—PQ-MF, and numbered from 1133 to 1643 inclusive. For convenience,

reference to the catalogued material in the text is abbreviated by omitting the prefix

SAM-PQ. The original 2022 assemblage slides remain in the microfossil slide

collections in SOEKOR (Pty) Ltd.*, in Parow, Cape Town. In the text and captions,

references to negative numbers (e.g. F2930) refer to the SOEKOR photographic archive*,

and in the captions the biozones are placed in parentheses.

*“Now held by PASA (Petroleum Agency of South Africa) in Parow.

74 ANNALS OF THE SOUTH AFRICAN MUSEUM

Order FORAMINIFERIDA Eichwald, 1830

Family Saccamminidae Brady, 1884

Subfamily Saccammininae Brady, 1884

Genus Saccammina Carpenter, 1869

Saccammina spp.

Figs 27A-—B

Remarks

Small, subspherical tests with coarsely agglutinated walls are widely distributed

through the Sundays River Formation. Never common, none are especially distinctive,

and none show any particular stratigraphic range. These specimens may be related to the

Proteonina difflugiformis (Brady) illustrated by Bartenstein & Brand (1951, pl. 1 (fig. 3))

from the Late Valanginian of north-west Germany.

Genus Pelosina Brady, 1879

Pelosina zoetgeneugdensis sp. nov.

Figs 27C—F

Diagnosis

A Pelosina species with an elongate, spindle-shaped test.

Etymology

From its occurrence in the Zoetgeneugd Cliff outcrop.

Material

Holotype (Fig. 27C). MF1135, SOEKOR negative F250.

Paratypes (Fig. 27D—F). MF1136 to MF1138, 3 specimens, SOEKOR negatives F512,

F300, and F256.

Stratum Typicum

The Zoetgeneugd Cliff outcrop, within highest Biozone C (Late Valanginian) of the

Sundays River Formation.

Locus Typicus

Zoetgeneugd Cliff sample 11452.

Description

Test elongate, spindle-shaped, circular in cross-section, and composed of a single

chamber. Tests usually taper more rapidly to one end than the other, so that maximum test

width is rarely at mid-height. Test wall composed of variably sized, often coarse-grained

quartz particles, rather irregularly arranged, resulting in a roughened test surface. The

ratio of quartz grains to cement is high. Irregular, subcircular, unornamented openings

exist at both ends of the test.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION ip)

Remarks

Pelosina zoetgeneugdensis is distinct from other species of the genus in its elongate,

sub-cylindrical test, and in this respect, differs markedly from other Early Cretaceous

forms. Pelosina lagenoides Crespin, 1953, from the Early Cretaceous of the Great

Artesian Basin of Australia is a much more subglobular form with a relatively smooth test

wall of fine-grained particles. The test wall of P. zoetgeneugdensis is rather more

coarse-grained than is usual for the genus.

Stratigraphic range in the Sundays River Formation

Occurs in very small numbers at the top of Biozone C (Late Valanginian) at Zoetgeneugd

Cliff outcrop, and in the Hauterivian Biozones III and VII in the more distal boreholes.

Family Ammodiscidae Reuss, 1862

Subfamily Ammodiscinae Reuss, 1862

Genus Ammodiscus Reuss, 1862

Ammodiscus spp.

Figs 27G—H

Remarks

Poorly preserved tests of Ammodiscus occur rarely in the Sundays River Formation.

Several appear similar to Ammodiscus gaultinus Berthelin, particularly to the illustrations

given by Bartenstein & Brand (1951, pl. 1 (fig. 13)). However, Magniez-Jannin (1975: 26)

has regarded many of the forms previously referred to A. gau/tinus as more properly

assigned to Glomospirella; amongst these she includes the Valanginian specimens of

Bartenstein & Brand (1951). The present material is too poor to permit analysis of the

variation present in the Sundays River Formation tests.

Stratigraphic range in the Sundays River Formation

Occasional tests occur throughout, from Biozone Bb up to Biozone I, generally at more

distal localities.

Family Lituolidae de Blainville, 1825

Subfamily Hormosininae Haeckel, 1894

Genus Hormosina Brady, 1879

Hormosina sp. A

Fig. 271

Remarks

Five specimens, all broken, of a multilocular, uniserial form. The last-formed chamber

possesses a long apertural neck, as illustrated, and in this respect, the species shows some

similarity to Reophax deckeri Tappan (1940: 94, pl. 14 (figs 3a—b)), also subsequently

illustrated by Crespin (1963: 23, pl. 3 (figs 1—-10)). There is also slight similarity to some

tests of R. scorpiurus Montfort, as figured by Magniez-Jannin (1975: 27, pl. 1 (figs 9-18)).

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 27.

_ 7.

ANY

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION leh.

Comparable tests to those of the Sundays River Formation also occur in the South African

Late Aptian and Albian.

Stratigraphic range in the Sundays River Formation

All tests are from the Late Hauterivian Biozones VII to I.

Genus Reophax Montfort, 1808

Reophax spp.

Figs 27J, 28A—B

Reophax sp. Beer, 1970: 70, pl. 1 (fig. 1). Stapleton & Beer, 1977: 2, pl. 3 (fig. 8).

Remarks

Generally poorly preserved specimens of Reophax are found sporadically through the

Sundays River Formation. Some degree of variation can be seen 1n the grain size in the test

wall, and in the inflation of the chambers, sufficient to suggest that a number of species are

represented. None of these specimens possess the nearly globular chambers and

constricted sutural necks of Hormosina sp. A. A dearth of well-preserved Reophax tests in

the material precludes any attempt to identify this material to species at present.

Stratigraphic range in the Sundays River Formation

Late Valanginian (Biozone Ba) to Late Hauterivian (Biozone II). This rare genus is

restricted to shelf environments where normal marine conditions prevailed, and is never

found associated with high- or reduced-oxygen sea-floor conditions, nor with the reduced

salinity marginal facies that prevailed along the northern margin of Sundays River

Formation deposition.

Subfamily Haplophragmoidinae Maync, 1952

Genus Haplophragmoides Cushman, 1910

Remarks

Analysis of the abundant Haplophragmoides specimens from the Sundays River

Formation is greatly hampered by the variable degree of test distortion due to post-

Fig. 27 (see facing page). A—B. Saccammina spp. A. SAM—PQ—MF 1133, side view, AL 1/69, 1 000 feet

(II), F293. x 133. B. SAM—PQ—MF1134, side view, AL 1/69, 460 feet (I), F106. x 67.

C-F. Pelosina zoetgeneugdensis sp. nov. C. Holotype, SAM—PQ—MF1135, side view, Zoetgeneugd

Cliff outcrop sample 11452 (C), F250. x 106. D. Paratype, SAM—PQ—MF1 136, side view, AL 1/69,

2 410 feet (VIID), F512. x 70. E. Paratype, SAM—PQ—MF1137, side view, AL 1/69, 1 000 feet (III),

F300. X 107. F. Paratype, SAM—PQ—MF 1138, side view, Zoetgeneugd Cliff outcrop sample 11452

(C), F256. X 93. G-H. Ammodiscus spp. G. SAM—PQ-MF1139, side view, Zoetgeneugd Cliff

outcrop sample 11450 (Bb), F244. x 164. H. SAM—PQ-MF1140, side view, AL 1/69, 460 feet (1),

F112. x 138.1. Hormosina sp. A, SAM—PQ-MF1141, side view, AL 1/69, 1 480 feet (IV), F386. x 76.

J. Reophax sp., SAM—PQ—MF1142, side view, MV 1/79, 380-390 m (Ba), F646. xX 68.

78 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 28.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 79

depositional compaction within the sediment. Distinctly different morphologies can be

seen that are due solely to how tests have been aligned and compacted within the

sediment. Differences also occur if calcite or pyrite infilling of the chamber cavities has

occurred early or late in the diagenetic sequence. It has thus often proved difficult to

distinguish between species effectively within this genus, as many of the diagnostic

details of tests have been obliterated. Post-depositional compaction has particularly

affected the degree of chamber inflation and degree of lobation of the test periphery, the

depth of the umbilicus, and whether sutures are depressed or flush, straight or curved.

However, distinctive features such as the number of chambers in the final whorl, the

nature of the grains and cement composing the test wall, and even the intensity of

compaction (reflecting the thickness of the test wall) can be sufficient to compose a basic

subdivision of the group. Nevertheless, because of the relative paucity of data determined

for these Haplophragmoides morphotypes, it seems unwise to consider them as formal

species. For this reason, they are listed informally below, and little or no attempt has been

made to compare them with previously described Haplophragmoides species. Because of

their mode of preservation, the aperture of virtually all Haplophragmoides tests from the

Sundays River Formation is not visible, although it is presumed to be interio-marginal at

the base of the terminal face of the final chamber; no other details are discernible. A

comparison with the species of Haplophragmoides described by Masiuk & Vina (1987)

from the Early Hauterivian of Chubut, Argentina, gives an indication of the difficulties

that arise in attempting to use this group of foraminifera as a correlation tool.

Haplophragmoides sp. A

Figs 28C—-E

Remarks

This morphotype is characterized by a strongly compressed test with weakly inflated

chambers, usually six in the final whorl, generally with a slightly depressed umbilicus on

both sides of the test, and with a moderate grain size of angular quartz particles and

moderate quantities of cement comprising the test wall. The test periphery 1s distinctly

lobate and circular in outline, rounded to sub-rounded in cross-section, although these

features are often severely affected by post-depositional compaction. Sutures appear to be

straight and radiate, weakly depressed.

Fig. 28 (see facing page). A-B. Reophax spp. A. SAM—PQ-MF1143, side view, shallow borehole

SB-31, core 1, 91 feet 6 inches (IV), F691. X 55. B. SAM—PQ-MF1144, side view, AL 1/69,

580 feet (II), F174. X 126. C-E. Haplophragmoides sp. A. C. SAM—PQ-—MF1145, side view,

AL 1/69, 340 feet (I), F37. X 91. D. SAM—PQ-—MF 1146, side view, AL 1/69, 340 feet (I), F36. x 85.

E. SAM—PQ-MF 1147, side view, AL 1/69, 310 feet (1), F33. X 69. F-H. Haplophragmoides sp. B.

F. SAM—PQ-MF 1148, side view, AL 1/69, 1 360 feet (IV), F371. X 106. G. SAM-PQ-MF1149,

side view, AL 1/69, 3 510 feet (X), F539. Xx 96. H. SAM—PQ-—MF1150, side view, AL 1/69,

3 840 feet (X), F543. x 85. I-J. Haplophragmoides sp. C. 1. SAM—PQ—MF1151, side view,

AL 1/69, 340 feet (1), F35. x 178. J. SAM—PQ—MF1152, apertural view, AL 1/69, 1 150 feet (IV),

F340. x 95.

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 29.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION S1

Tests of Haplophragmoides sp. A occur in considerable numbers throughout most of

the Sundays River Formation. It is possible that they are conspecific with

Haplophragmoides sp. B described from the Late Valanginian and Early Hauterivian

(Biozones B to IX) of borehole PB—A1, and the earliest Late Valanginian (Biozone D) of

the Brenton Formation (McLachlan et al. 19765).

Stratigraphic range in the Sundays River Formation

Haplophragmoides sp. A ranges consistently from Late Valanginian Biozone C to Late

Hauterivian Biozone I. It appears to be absent in reduced-salinity, marginal-marine

environments.

Haplophragmoides sp. B

Figs 28F—H

Remarks

Tests of this morphotype are always severely compressed, so that the generalized

description given below little reflects the true test morphology. Eight or nine chambers in

the final whorl, weakly but variably inflated. Faintly depressed umbilicus; rather

irregularly lobate test periphery, originally rounded in cross-section but diagenetically

altered to sub-angular in most specimens; sutures slightly depressed, radiate, either

curved or straight. Test wall composed of medium-sized angular quartz particles with

moderate quantities of cement.

Stratigraphic range in the Sundays River Formation

This morphotype occurs frequently through most of the Sundays River sequence, from

Late Valanginian Biozone Bb to Late Hauterivian Biozone I. Its environmental

preferences are not as clear-cut as those of Haplophragmoides sp. A.

Haplophragmoides sp. C

Figs 28I-J, 29A

Remarks

Chambers planispirally, occasionally rather streptospirally (see Fig. 28J) arranged,

inflated and subglobular in form. Umbilicus depressed; sutures depressed, radiate,

Fig. 29 (see facing page). A. Haplophragmoides sp. C, SAM—PQ-MF1153, side view, AL 1/69,

340 feet (1), F34. x 197. B-E. Haplophragmoides sp. D. B. SAM—PQ—MF1154, side view, AL 1/69,

3 040 feet (IX), F528. x 80.C. SAM—PQ—MF1155, side view, AL 1/69, 1 240 feet (IV), F360. X 82.

D. SAM—PQ—MF 1156, apertural view, AL 1/69, 790 feet (III), F227. x 120. E. SAM—PQ—MF1157,

side view, AL 1/69, 790 feet (III), F226. x 131. F-I. Haplophragmoides sp. F.

F. SAM—PQ—-MF1158, side view, AL 1/69, 4 500 feet (Ba), F562. x 100. G. SAM—PQ-—MF1159,

side view, MV 1/79, 80 m (X), F570. X 67. H. SAM—PQ—MF1160, side view, MV 1/79, 80 m (X),

F571. X 71. 1. SAM—PQ-MF1161, side view, AL 1/69, 3 840 feet (X), F544. x 73.

8&2 ANNALS OF THE SOUTH AFRICAN MUSEUM

straight to weakly curved. Five or six chambers in the final whorl. Test periphery

distinctly lobate throughout, very broadly rounded in cross-section. Test subglobular in

overall shape. Test wall composed of moderately sized, often rather platy quartz grains

with moderate cement. This morphotype differs from Haplophragmoides sp. D in

possessing fewer chambers in the final whorl and in its more nearly globular test.

Stratigraphic range in the Sundays River Formation

Restricted to Late Valanginian Biozones Ba and A, and to Late Hauterivian

Biozones VII to I. This morphotype is most frequent in distal, more normal marine

environments.

Haplophragmoides sp. D

Figs 29B-E

Remarks

Test rather more compressed than those of Haplophragmoides sp. C, with seven

inflated chambers 1n the final whorl. Test periphery lobate, circular in outline and broadly

rounded in cross-section. The umbilicus is slightly depressed on both sides of the test.

Sutures weakly depressed, straight or faintly curved, radiate. Test wall composed of

moderate to fine-grained quartz material, with moderate to rather high quantities of

cement.

Stratigraphic range in the Sundays River Formation

Early to Late Hauterivian (Biozone X to top Biozone III). Typical of distal, outer-shelf

environments with relatively normal sea-floor conditions.

Haplophragmoides sp. F

Figs 29F-I

Remarks

The test is always strongly compressed due to diagenesis, with a roughly circular

outline. Seven or eight chambers in the final whorl, indistinct, except when test is

moistened. Sutures flush to very slightly depressed, indistinct, straight, radiate. Test wall

composed of moderate, occasionally coarse-grained, angular quartz particles with

moderate quantities of cement. These tests, as with those of Haplophragmoides sp. B, are

so severely compressed that they probably little reflect the form of the original test of the

living species.

Stratigraphic range in the Sundays River Formation

Restricted to the Late Valanginian and Early Hauterivian (Biozones Ba to X) in deeper

marine environments.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 53

Haplophragmoides spp.

Remarks

The majority of Haplophragmoides tests from the Sundays River Formation are either

badly deformed by post-depositional compaction, or are damaged, so that identification is

not possible. These indeterminate specimens of Haplophragmoides spp. range from

Biozone D to Biozone I, in almost all environments seen in the Sundays River Formation,

except the truly estuarine facies of the northern-most Algoa Basin.

Subfamily Lituolinae de Blainville, 1825

Genus Ammobaculites Cushman, 1910

Remarks

Similar comments to those given for Haplophragmoides are valid also for

Ammobaculites, especially in the case of the smaller, thin-walled species. Again, wall

texture, as well as chamber arrangements in the coiled and uncoiled parts of the test

remain useful features, even if little can be discovered of the degrees of inflation of

chambers, depression of sutures, and the nature of the test periphery. Compare the

morphotypes described here with those Ammobaculites species detailed by Masiuk &

Vina (1987) from the Early Hauterivian of Chubut, Argentina.

Ammobaculites subaequalis Mjatliuk, 1939

Figs 30A—D

Ammobaculites subaequalis Myatliuk, 1939: 44, pl. 2 (fig. 19a—b). Lloyd, 1959: 311, pl. 54

(figs 16-17). lovcheva, 1962: 48, pl. | (fig. 18).

Haplophragmium subaequale (Myjatliuk). Bartenstein & Brand, 1951: 273, pl. 3 (figs 62a-—c,

63a—b, 64a—b). Hanzlikova, 1965: 60, pl. 1 (figs 3-4, 6).

Haplophragmium aequale (non Roemer) Beer, 1970: 8.

Ammobaculites aff. A. abnormalis Crespin. Rigassi, 1970: pl. 83 (2 figs).

Haplophragmium coprolithiforme subaequale (Mjatliuk). Bielecka, 1975: 308, pl. 1 (figs 9-10),

pl. 2 (figs 1-2).

Remarks

Sundays River Formation tests are allocated with some hesitation to Ammobaculites

subaequalis. Almost all northern Algoa Basin examples possess compressed tests that are

usually ovate in cross-section, whereas European descriptions indicate Ammobaculites

subaequalis to be roughly circular in cross-section. The difference may be due to

post-depositional compaction of the Algoa tests. In the appressed nature of the chambers,

the arrangement of the initial coil, and the simple aperture, the European and South

African tests compare closely. The references given above provide an indication of the

range of authors’ interpretations of the species from the latest Jurassic and Early

Cretaceous of Europe.

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 30.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 8&5

There appears to be confusion in the literature between the two genera Ammobaculites

and Haplophragmium, particularly regarding the morphologically similar Ammobaculites

subaequalis and Haplophragmium aequale (Roemer). The latter species was described as

possessing a multiple, cribrate aperture with a labyrinthic internal chamber wall (Ten

Dam 1946). In contrast, Loeblich & Tappan (1964: C244) regarded the interior as simple,

the aperture a single opening, and the initial coil streptospiral, whereas the initial coil of

Ammobaculites is planispiral.

Examination of Sundays River Formation tests failed to reveal any with a cribrate

aperture. The interior of the chambers in broken specimens (Fig. 30D) can be considered

as ‘pseudolabyrinthic’, but clearly is not truly labyrinthic. The chamber wall 1s composed

of small and large quartz grains, the latter being aligned so that on the exterior of the test

wall they are flush, but on the interior they protrude substantially into the chamber cavity,

and result in a very roughened and ragged surface to the internal chamber wall. None of

the South African tests display a clearly streptospiral initial coil, although irregularities in

positioning of individual chambers do occur.

Occurrence

Mjatliuk (1939) described Ammobaculites subaequalis from the Early Volgian

(Portlandian equivalent) of the Volga Basin, Russia. Later records include Late Oxfordian

to Kimmeridgian Klentnice Beds of the Czech Republic (Hanzlikova 1965);

Kimmeridgian of southern England (Lloyd 1959); Early Kimmeridgian and Middle

Portlandian of Poland (Bielecka 1975); Aptian of Bulgaria (lovcheva 1962); and Middle

Bajocian to Early Hauterivian of north-west Germany (Bartenstein & Brand 1951). The

species occurs extensively in the South African Late Jurassic and Early Cretaceous, with a

total range of Portlandian (Colchester Member of the Uitenhage Trough—McMillan

1980) to Early Aptian. The species appears strongly facies controlled, and is often

associated with oxygenated, sandy and turbulent substrates that were probably rather

stressful environments for foraminifera.

Stratigraphic range in the Sundays River Formation

Small but consistent numbers occur through most of the sequence (Late Valanginian

Fig. 30 (see facing page). A-D. Ammobaculites subaequalis Mjatliuk. A. SAM—PQ—MF1162, side

view, Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F87. x 17.

B. SAM—PQ-MF 1163, side view, AL 1/69, 1 570 feet (VI), F423. x 53. C. SAM—PQ-MF1 164,

apertural view, AL 1/69, 3 290 feet (IX), F532. x 63. D. SAM—PQ-—MF1165, final two chambers

broken in half, showing interior, shallow borehole SB—15, core 3, 212 feet (II), F680. x 41.

E. Ammobaculites sp. A, SAM—PQ—MF1166, side view, AL 1/69, 340 feet (I), F38. x 224.

F-I. Ammobaculites sp. B. F. SAM—PQ—MF1167, side view, AL 1/69, 340 feet (I), F39. xX 82.

G. SAM-PQ-MF1168, side view, AL 1/69, 3 070 feet (IX), F529. x 78. H. SAM-PQ-MF1169,

side view, AL 1/69, 3 450 feet (IX), F537. X 121. I. SAM—PQ—MF1170, apertural view, AL 1/69,

1 060 feet (IH), F322. x 344. J-K. Ammobaculites sp. C. J. SAM—PQ-—MF 1171, side view, AL 1/69,

1 270 feet (IV), F367. x 59. K. SAM—PQ-MF1172, side view, Uitenhage to Graaff-Reinet Road

outcrop, sample 11464 (Bb), F85. x 68.

56 ANNALS OF THE SOUTH AFRICAN MUSEUM

Biozone C to Late Hauterivian Biozone I). However, the species is especially abundant

and generally predominant in sandstone intervals in the Late Hauterivian, often in

association with attached Bullopora and less frequently with attached Nubecularia

species. Ammobaculites subaequalis is absent in reduced-salinity environments.

Ammobaculites sp. A

Fig. 30E

Remarks

Tests of Ammobaculites with two to three visible chambers in the initial coil, followed

by up to five rectilinear chambers that are inflated and subglobular. Sutures distinct,

depressed, horizontal in uncoiled part of test. The test wall is composed of very large

quartz grains with moderate cement. Tests are circular in cross-section. Aperture a

subcircular opening at the terminal point of the final chamber, typical of the genus.

This species is usually little affected by post-depositional compaction, probably

because the test wall is so coarsely grained. However, only occasional tests are perfectly

preserved, and the example illustrated is a rarity.

Stratigraphic range in the Sundays River Formation

Ranges through much of the Sundays River Formation (Biozone Bb to I, Late

Valanginian to Late Hauterivian), but is commonest and most persistent in the Late

Hauterivian (Biozones VI to I).

Ammobaculites sp. B

Figs 30F-I

Remarks

Tests are similar in morphology to those of Ammobaculites sp. A, but they differ in a

number of salient points. The initial coil consists of three visible chambers, and is

followed by up to six rectilinear, uncoiled chambers. The chambers are more appressed

and not nearly as globular as those of Ammobaculites sp. A. Chambers weakly inflated;

sutures vary from faint and flush to distinct and depressed, horizontal. Aperture terminal,

an irregular subcircular opening (Fig. 301), which is usually not entirely visible on tests.

Test wall composed of fine-grained quartz particles with occasional larger grains and

moderate cement. Cross-section of the adult part of the test is circular to subcircular.

Stratigraphic range in the Sundays River Formation

Moderate to abundant through much of the sequence, from Late Valanginian

Biozone Bb to Late Hauterivian Biozone I. Ammobaculites sp. B 1s less common through

most sections of the Early Hauterivian.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 87

Ammobaculites sp. C

Figs 30J-K

Remarks

Severely compressed tests, with a test wall of fine to moderate-sized quartz grains set

in moderate amounts of cement. Two or three chambers visible in the initial coil, with up

to four inflated chambers in the rectilinear portion. Sutures depressed, horizontal, straight

in uncoiled portion, and indistinct in initial coil. The aperture is always obscured, but

presumably terminal and simple in form. These tests have been much affected by

post-depositional compaction.

Stratigraphic range in the Sundays River Formation

Scattered occurrences from the Late Valanginian (Biozone Bb) to the Late Hauterivian

(Biozone IV). The species may occur locally in abundance, especially in the Early

Hauterivian.

Ammobaculites parvispira Ten Dam, 1950

Figs 31C-—G

Haplophragmium aequale (non Roemer) Chapman, 1892a: 323, pl. 6 (figs 1-3).

Ammobaculites parvispira Ten Dam, 1950: 10, pl. 1 (fig. 8a—b). Neagu, 1965: 4, pl. 1 (figs 1-3).

Magniez-Jannin, 1975: 40, pl. 1 (figs 19-26).

Remarks

Many specimens of Ammobaculites from the Sundays River Formation are referable to

this conservative species. Some variation 1s evident in South African tests 1n the shape of

the chambers, which may be more or less globular and correspondingly less or more

appressed, and in the size of the initial coil, the latter being larger in some specimens than

is typical. Gradation can be seen from Ammobaculites parvispira towards Ammobaculites

sp. B.

Occurrence

Described from the Albian of the Netherlands (Ten Dam 1950). Other records are from

the Albian Gault Clay of Folkestone, England (Chapman 1892qa), and the Albian

(Magniez-Jannin 1975) and the Early Aptian (Damotte & Magniez-Jannin 1973) of the

Aube district, France; farther east the species occurs in the Albian of the Romanian Plain

(Neagu 1965).

Stratigraphic range in the Sundays River Formation

Occurs throughout the Sundays River Formation (Biozones C to I), and appears to

range from marginal-marine to outer-shelf environments.

8&8

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 31.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 59

Ammobaculites spp.

Remarks

The majority of Ammobaculites tests from the Sundays River Formation are either

deformed or damaged to such an extent that a specific identification 1s not possible.

Ammobaculites spp. range from Biozone D to Biozone I in a wide range of environments,

including marginal marine and reduced-salinity (?estuarine) biofacies.

Genus Sculptobaculites Loeblich & Tappan, 1984

Sculptobaculites goodlandensis (Cushman & Alexander, 1930)

Figs 31A—B

Ammobaculites goodlandensis Cushman & Alexander, 1930: 8, pl. 2 (figs 7-8). Tappan, 1940: 96,

pl. 14 (figs 8a—b, 9). Tappan, 1943: 481, pl. 77 (fig. 9a—b). Loeblich & Tappan, 1949: 250, pl. 46

(fig. 14a—-b). Bartenstein & Brand, 1951: 271, pl. 3 (fig. 49a—b). Crespin, 1963: 39, pl. 9

(figs 1-4). Bartenstein et al. 1966: 139, pl. 1 (figs 1-2).

Sculptobaculites goodlandensis (Cushman & Alexander). Loeblich & Tappan, 1988: 76, pl. 60

(figs 5—6, 12-16).

Remarks

There are substantial differences in authors’ illustrations of this species (see references

above), the most notable being the variation in grain size of the test wall. Cushman &

Alexander (1930) noted that the periphery of the species was ‘broad and truncate’,

although not all tests subsequently referred to this species exhibit the feature. Sundays

River Formation tests possess wide, but rounded, margins to the test, with the periphery

sometimes strongly lobate, a trait that appears to depend on the coarseness of the grains

used to construct the test. Most tests are as illustrated, but occasional ones display one or

two uncoiled, rather globular chambers, which are rectilinear in arrangement. All Algoa

Fig. 31 (see facing page). A-—-B. Sculptobaculites goodlandensis (Cushman & Alexander).

A. SAM—PQ-—MF1173, side view, Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb),

F83. xX 38. B. SAM—PQ-MF1174, side view, MV 1/79, 480-490 m (Bb), F661. x 79.

C-G. Ammobaculites parvispira Ten Dam. C. SAM—PQ-—MF1175, side view, AL 1/69, | 960 feet

(VII), F476. x 67. D. SAM—PQ—MF1176, side view, AL 1/69, 2 060 feet (VIII), F489. x 48.

E. SAM—PQ—-MF1177, side view, AL 1/69, 2 130 feet (VID), F493. x 101. F. SAM—PQ-MF1178,

side view, AL 1/69, 4 440 feet (A), F556. X 65. G. SAM—PQ—MF1179, side view, Uitenhage to

Graaff-Reinet Road outcrop sample 11464 (Bb), F84. x 89. H-K. Textularia zoetgeneugdia sp. nov.

H. Holotype, SAM—PQ—MF1181, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb), F248.

x 97.1. Paratype, SAM—PQ—MF1182, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb),

F246. X 76. J. Paratype, SAM—PQ—MF1183, side view, Zoetgeneugd Cliff outcrop sample 11450

(Bb), F249. x 92. K. Paratype, SAM—PQ-—MF1184, oblique side view, Zoetgeneugd Cliff outcrop

sample 11450 (Bb), F247. x 93. L-M. Ammoglobigerina cf. A. globigeriniformis (Parker & Jones).

L. SAM—PQ—MF1190, ventral view, AL 1/69, 1 570 feet (VI), F434. x 220.M. SAM—PQ-MF1191,

dorsal view, AL 1/69, 2 080 feet (VIII), F490. x 164.

90 ANNALS OF THE SOUTH AFRICAN MUSEUM

Basin tests are coloured a rich and deep red-brown and, when well preserved and free of

sediment, have a distinctive appearance.

Occurrence

Cushman & Alexander (1930) described Ammobaculites goodlandensis from the

Goodland Formation (Albian) of the southern United States. Later records include:

Middle Cenomanian Grayson Formation (Tappan 1940), Late Albian Duck Creek

Formation (Tappan 1943), and the Albian Walnut Formation (Loeblich & Tappan 1949),

all of Texas and Oklahoma, U.S.A.; Aptian—Albian Lower Wilgunya Formation, Great

Artesian Basin, Australia (Crespin 1963); Late Valanginian of north-western Germany

(Bartenstein & Brand 1951); and possibly Late Aptian—Early Albian Maridale Formation —

of Trinidad (Bartenstein et al. 1966).

Stratigraphic range in the Sundays River Formation

Confined to the Late Valanginian (Biozone Bb). One or two possible occurrences have

been recorded in Biozone Ba. The species has not been found m South Africa outside of

the Sundays River Formation in the onshore Algoa Basin. Sculptobaculites goodlandensis

is typical of lowered oxygen, near-normal salinity, continental-shelf environments, and

does not occur close to shore in any facies.

Subfamily Placopsilininae Rhumbler, 1913

Genus Placopsilina d’Orbigny, 1850

Placopsilina cenomana @ Orbigny, 1850

enh, 32

Placopsilina cenomana @ Orbigny, 18506: 185, no. 758. Loeblich & Tappan, 1964: C247, fig. 159

(nos 1—2). Winter, 1970: 9, pl. 1 (figs 24-31), pl. 2 (figs 38-40), text-fig. 8.

Remarks

A single specimen of Placopsilina was found. It is low, spreading and strongly

compressed, and appears referable to Placopsilina cenomana. It shows close similarities

with the examples illustrated by Winter (1970) from the Early Kimmeridgian of southern

Germany. The initial coil of the Sundays River example is very incomplete. The test is

attached to a fragment of mollusc (?bivalve) shell and possesses a finely agglutinated wall

of small quartz particles.

Other illustrations of Placopsilina cenomana are of distinctly different forms—see

Chapman (1892a, pl. 6 (fig. 4)) and Espitalié & Sigal (1963, pl. 4 (fig. 5), as Placopsilina

cf. cenomana), for example. Because of the wide variety of forms assigned to this name,

its stratigraphic range remains unclear.

Stratigraphic range in the Sundays River Formation

The single specimen is from the Late Valanginian Biozone Bb.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 9]

Figure 32.

Placopsilina cenomana @ Orbigny. SAM—PQ—MF 1180, surface view,

MV 1/79, core 2, 544.0 m (Bb). x 103.

Family Textulariidae Ehrenberg, 1838

Subfamily Textulariinae Ehrenberg, 1838

Genus Textularia Defrance, 1824

Textularia zoetgeneugdia sp. nov.

Figs 31H-K

Diagnosis

A slender, elongate Textu/aria with up to seven pairs of chambers, broadly rounded

test periphery, weakly depressed, almost horizontal sutures, and a moderately coarse

quartz grain size in the test wall.

Etymology

Adjective, from its occurrence at Zoetgeneugd Cliff outcrop.

Material

Holotype (Fig. 31H). MF 1181, SOEKOR negative F248.

Paratypes (Figs 31I-K). MF1182 to MF1184, SOEKOR negatives F246, F249, and

F247 and SAM-—MF1185 to MF1189, five additional specimens from sample 11450,

Zoetgeneugd Cliff.

Stratum typicum

Zoetgeneugd Cliff, basal Biozone Bb, Late Valanginian, Sundays River Formation.

Locus typicus

Zoetgeneugd Cliff sample 11450.

Description

Test elongate, slender, slightly compressed, with maximum width and depth of test at

or near final chamber. Test periphery usually sub-linear, very faintly lobate in the later

92 ANNALS OF THE SOUTH AFRICAN MUSEUM

part of the test. Test margin broadly rounded in cross-section. Chambers arranged

biserially throughout, in up to seven pairs, and closely appressed. Chambers increase

slowly and regularly in size as added. Later chambers are a little wider than high, and are

slightly inflated. Sutures initially indistinct, flush, later becoming weakly depressed, and

sub-horizontally aligned. The median suture forms a neatly constructed zigzag. Aperture

interio-marginal, a low, slit-like opening at the base of the last-formed chamber, centrally

placed and terminating on either side, well short of the test margins. The aperture is

evident only in a few specimens. Apical point of the test rounded and unornamented, but

usually this part of the test is damaged or broken off. Test wall fairly rough, composed of —

scattered moderate to coarse-grained quartz particles set in finer quartz material and

cement.

Remarks

Textularia zoetgeneugdia appears to be confined to shallow, marginal marine,

well-oxygenated, near-normal salinity environments. The species is unusual for Early

Cretaceous Textularia in possessing such an elongate, compact shape. It differs from

T. anacooraensis Crespin (1953, 1963) from the Aptian—Albian Lower Wilgunya

Formation of the Great Artesian Basin, Australia, in possessing more nearly horizontal

sutures, but the overall shape of the test is similar. Textularia zoetgeneugdia differs from

T. bettenstaedti Bartenstein & Oertli (1977) (see also Bartenstein & Kovatcheva 1982),

from the Early Cretaceous of Bulgaria, north-west Germany and elsewhere in Europe, in

lacking the ‘coal dust’ (?graphite) particles over the lower parts of the chambers and the

sutures, and in being a little more compressed, although the forms are clearly similar. The

chambers of 7. zoetgeneugdia are lower and less inflated, and the early part of the test

more tapering than 7. minuta Berthelin (see Reuss 1863, pl. 9 (fig. 1 la—b); Magniez-Jannin

1975, pl. 3 (fig. 35—36)), a species typical of the western European Albian. Textularia

foeda Reuss, which ranges from the Late Hauterivian to the Middle Albian of north-west

Germany (Bartenstein & Bettenstaedt 1962), possesses about eleven distinctly inflated

chambers with ?graphite speckling and oblique, depressed sutures. Tests assigned to

T. foeda occur in the Late Aptian to Middle Cenomanian of the South African southern

offshore region, and are markedly different in chamber shape, test outline, depression and

angle of sutures, and number of chambers from 7. zoetgeneugdia.

Stratigraphic range in the Sundays River Formation

Apparently confined to the Late Valanginian (earliest Biozone Bb).

Supplementary note

One of the reviewers (W. R.) of this publication has pointed out that Textularia

zoetgeneugdia sp. nov. 1s better placed in the essentially Mesozoic genus Textulariopsis

Banner & Pereira (1981) than in Textularia. Textulariopsis was characterized by these

authors as possessing imperforate solid walls, whereas Textularia was distinguished by

perforate test walls, and was considered to range from the Eocene to the present day. As

far as can be established, Textularia zoetgeneugdia tests are imperforate, and the

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 93

author agrees that this species should more properly be Textulariopsis zoetgeneugdia

sp. nov. However, through circumstances beyond anyone’s control, it has proved

impossible to amend some figures containing the original name (Figs 20 and 26 in

particular), so that to keep the text and figures coherent, the original text has been retained.

Textulariopsis zoetgeneugdia differs from Textulariopsis texhomensis Loeblich &

Tappan (1982: 68, pl. 2 (figs 38-39)), described from the Late Albian Duck Creek

Formation of Texas, in lacking the inflated, rather globular chambers of the later part of

the test, and the corresponding strongly depressed sutures and lobate test margin, as well

as lacking the long, slender taper to the initial portion of the test.

Family Trochamminidae Schwager, 1877

Subfamily Trochammininae Schwager, 1877

Genus Ammoglobigerina Eimer & Fickert, 1899

Ammoglobigerina cf. A. globigeriniformis (Parker & Jones, 1865)

Figs 31L—M

see Lituola nautiloidea Lamarck globigeriniformis Parker & Jones, 1865: 407, pl. 15 (figs 46-47),

(?also pl. 17 (figs 96—98)).

see Haplophragmium globigeriniforme (Parker & Jones). Chapman, 1892a: 324, pl. 5 (fig. 16).

Trochammina globigeriniformis (Parker & Jones). Lloyd, 1959: 317, pl. 54 (fig. 31), text-fig. 5c.

Wernli, 1971: 315, pl. 8 (figs 4, 9a—c). Kuznetsova, 1974: pl. | (fig. 3a—b). Barnard & Shipp,

1981: 9, pl. 1 (figs 11-12). Coleman, 1981: 114, pl. 6.2.1 (fig. 11).

‘Trochammina’ sp. cf. T. globigeriniformis (Parker & Jones). Masiuk & Vina, 1987: 292, pl. 2

(figs 4-8, 11).

Remarks

Small specimens of Ammoglobigerina occur in lowered oxygen sequences of the

Sundays River Formation, and seem best assigned to Ammoglobigerina cf.

A. globigeriniformis. These are part of a well-known group, occurring sporadically

through most of the north-west European Jurassic, but less recorded from the Early

Cretaceous. The Barremian to Aptian Trochammina gerochi Bartenstein & Kovatcheva

(1982) may fall within this globigeriniform group. The taxonomic status of the group is

confused, since Trochammina globigeriniformis was first described from present-day

sediments of the North Atlantic Ocean, and it is not clear whether the Jurassic and

Holocene forms are conspecific.

Parker and Jones (1865) illustrated several rather different specimens under this name,

and the refigured lectotype illustrated by Loeblich & Tappan (1964, fig. 173 (no. 2a—c)) is

of a very different form than the Jurassic and Sundays River Formation examples.

Loeblich & Tappan (1964) based their understanding of the species on the specimen

illustrated by Parker & Jones (1865, pl. 17 (fig. 96)), and thus it appears that the Parker &

Jones specimens figured as pl. 15 (figs 46-47) are possibly a separate unnamed species.

The latter illustrations compare best with the Jurassic and Sundays River tests.

The Sundays River Formation tests can be divided into two groups: those with a high

94 ANNALS OF THE SOUTH AFRICAN MUSEUM

trochospiral coil, which may almost attain the height of tests of Gravellina on occasion,

and those with a much lower trochospire, such as that illustrated in Figure 31M.

Said & Barakat (1958) described Trochammina bartensteini from the Bathonian of

Gebel Maghara. They remarked that this species may be the same as Bartenstein &

Brand’s (1937) T. globigeriniformis from the German Lias and Dogger. It differs from

Holocene tests of the latter species (sensu Jato) 1n 1ts smaller, more depressed test and its

less lobate periphery. The illustrations of 7. bartensteini given by Said & Barakat (1958)

are not too clear, but this name may prove to be available for Jurassic ‘Trochammina

globigeriniformis’ tests. The similar 7. canningensis Tappan (1955) from the Jurassic of

Alaska possesses more chambers (four to seven) 1n the final whorl, and the shape of the

test is different.

Masiuk & Vina (1987) described specimens of this group from the Late Valanginian

and Early Hauterivian of the Katterfeld Formation of Chubut, Argentina. The Sundays

River Formation tests are very similar, but their peripheries are generally less strongly

lobate. However, in many tests, having been variably distorted as a result of compaction,

this feature is difficult to quantify. None of these Argentinian or South African tests show

similarity to the species Ammoglobigerina praeglobigeriniformis, described by Soliman

(1972) from the Late Turonian and Coniacian of the Russian Carpathians. Notable

differences in the Russian species are the narrow umbilicus, and the more appressed, less

lobate chambers, particularly evident in the final whorl.

Occurrence

Lias and Dogger (Bartenstein & Brand 1937; Coleman 1981), and Late Jurassic (Lloyd

1959; Barnard & Shipp 1981) of north-west Europe.

Stratigraphic range in the Sundays River Formation

Ammoglobigerina cf. A. globigeriniformis occurs sporadically through most of the

sequence (Biozones Bb to I), but is at its commonest in lowered-oxygen environments,

particularly through the CK 1/68 section, in the northern Sundays River Trough. There

appear to be no differences in the stratigraphic ranges of the high- and low-spired tests.

Genus Trochammina Parker & Jones, 1859

Trochammina cf. T. inflata (Montagu, 1808)

Figs 33A—D

see Nautilus inflatus Montagu, 1808: 81, pl. 18 (fig. 3).

see Trochammina inflata (Montagu). Bartenstein & Brand, 1951: 280, pl. 4 (figs 97a—c, 98a—c).

Remarks

The various forms of Trochammina from the Jurassic and Cretaceous that have been

referred to the extant marsh species Trochammina inflata are almost certainly not

conspecific, but morphologically they are very close. The Sundays River Formation

specimens appear closest to the illustrated specimen given by Bartenstein & Brand (1951,

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 95

pl. 4 (fig. 97a—c)). All of these tests contain four or five inflated chambers in the final

whorl, a wide depressed umbilicus, straight or weakly curved, radiate, depressed sutures

on the ventral side and oblique, backward-curving, depressed sutures on the dorsal side.

Tests similar to the Sundays River shells occur also in the Portlandian Colchester Member

of the Uitenhage Trough, onshore Algoa Basin (McMillan 1980).

Stratigraphic range in the Sundays River Formation

This form occurs intermittently in the later Early and Late Hauterivian (Biozones VIII

to I). The species is typical of near-normal marine conditions on the middle to outer shelf,

in contradistinction to true extant 7rochammina inflata, which is confined to mudflats and

marshes with low salinities.

Trochammina sundaysriverensis sp. nov.

Figs 33E—H, 34A-—C

Diagnosis

A species of Trochammina characterized by a concavo-convex or plano-convex test,

with six to eight inflated chambers in the final whorl, oblique depressed dorsal sutures,

weakly curved, radiate, depressed ventral sutures, and a broad, shallow umbilicus.

Material

Holotype (Figs 33E, 34A—C). MF1196, SOEKOR negative F123.

Paratypes (Figs 33F—H). MF1197 to MF1199, three specimens, SOEKOR negatives

F93, F126, and F306.

Etymology

From its occurrence in the Sundays River Formation.

Stratum typicum

Biozone I, Late Hauterivian, Sundays River Formation.

Locus typicus

AL 1/69, cuttings sample at 520 feet.

Description

Test concavo-convex or plano-convex in overall shape, with dorsal side weakly

concave or flat, and ventral side strongly convex. Test outline circular, with a distinctly

lobate periphery; in cross-section the margin is broadly rounded, but oriented slightly

towards the dorsal side. Chambers arranged in a low trochospiral coil, increasing in size

slowly and steadily as added, with from six to eight in the final whorl. Initial chambers

flush, later chambers in final whorl distinctly inflated. Sutures initially indistinct, flush;

later sutures distinct, depressed: on dorsal side weakly curved or straight, rather oblique,

and on ventral straight to weakly curved, radiate. Aperture usually obscured, but

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 33.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 97

apparently partly interio-marginal, at base of the terminal face of the last-formed

chamber, umbilical to extra-umbilical in position, not reaching as far as the test periphery;

a low elongate slit in form. Umbilicus wide, shallow. Surface of test variable, moderately

smooth to rather rough, composed of small angular quartz grains and finer material, set 1n

moderate quantities of cement.

Remarks

Trochammina sundaysriverensis is most readily distinguished by its flat or concave

dorsal side. In this respect it shows some similarity to 7. subinflata, described by Crespin

(1963) from the Early Cretaceous of the Great Artesian Basin. However, it lacks the

strongly inflated final chamber and rapid increase in chamber size of that species, but

possesses rather more chambers 1n the final whorl. It does not display the angled, lobulate

periphery and convex dorsal, concave ventral side of 7. limbata (Chapman), first

described from the Aptian Bargate Beds of southern England (Chapman 1894d), and later

from the Hauterivian of the Netherlands (Ten Dam 1946). Trochammina sundays-

riverensis also shows some slight similarities to some specimens of Trochammina aff.

T. lattai Loeblich & Tappan, as figured by Damotte & Magniez-Jannin (1973) and

Magniez-Jannin (1975) from the Aptian and Albian of France. However, these French

shells exhibit a rapid increase in chamber size, are biconvex, and possess backward

curved dorsal sutures. Trochammina neocomiana Myjatliuk, as described by Espitalié &

Figure 34.

Trochammina sundaysriverensis sp. nov. A-C. Holotype, SAM—PQ—MF1196, AL 1/69,

520 feet (1). A. Ventral view. B. Side view. C. Dorsal view. All x 144.

Fig. 33 (see facing page). A—D. Trochammina cf. T. inflata (Montagu). A. SAM—PQ—MF 1192, ventral

view, AL 1/69, | 210 feet (IV), F348. x 92. B. SAM—PQ-MF 1193, ventral view, AL 1/69, 760 feet

(I), F217. X 78. C. SAM—PQ-—MF1194, dorsal view, AL 1/69, 610 feet (II), F182. x 123.

D. SAM—PQ-MF1195, side view, AL 1/69, 1 360 feet (IV), F372. x 124. E-H. Trochammina

sundaysriverensis sp. nov. E. Holotype, SAM—PQ—MF1196, dorsal view, AL 1/69, 520 feet (1),

F123. X 126. F. Paratype, SAM—PQ—MF1197, dorsal view, AL 1/69, 490 feet (1), F93. x 152.

G. Paratype, SAM—PQ—MF 1198, side view, AL 1/69, 520 feet (I), F126. x 153. H. Paratype,

SAM-—PQ-MF1199, side view, AL 1/69, 1 030 feet (III), F306. xX 135. I. Verneuilina secreta sp.

nov., paratype, SAM—PQ-—MF 1200, side view, AL 1/69, 940 feet (III), F275. x 133.

9S ANNALS OF THE SOUTH AFRICAN MUSEUM

Sigal (1963) from Cenozone D (Late Portlandian to Early Valanginian) of the Majunga

Basin, Madagascar, although rather plano-convex with a flat dorsal side, reveals a very

convex ventral side, remarkably globular chambers, and a narrow, deep umbilicus.

Stratigraphic range in the Sundays River Formation

Late Hauterivian (late Biozone IV to Biozone I). As with most Trochammina tests

from the Sundays River Formation, 7rochammina sundaysriverensis 1s found only in the

more distal localities, well away from marginal marine environments.

Trochammina spp.

Remarks

Scattered tests referable to Trochammina occur throughout most of the Sundays River

Formation sequence, but they cannot be identified to specific level either because of

damage or post-depositional distortion of tests.

Family Verneuilinidae Cushman, 1911

Genus Verneuilina d’ Orbigny, 1839

Verneuilina secreta sp. nov.

Figs 33], 35A—D

Diagnosis

A conical species of Verneuilina characterized by broadly rounded test peripheries,

subglobular chambers usually arranged in three vertical columns, and a moderately

roughened test wall containing angular quartz grains.

Etymology

Secretus, -a, -um (L.): adjective from its distinct morphology, and from being one of

very few Southern Hemisphere Verneuilina species, its remoteness and rarity.

Material

Holotype (Fig. 35A). MF1201, SOEKOR negative F173.

Paratypes (Figs 331, 35B—D). MF1200, MF1202 to MF1204, four specimens, SOEKOR

negatives F275, F326, F327, and F427.

Stratum typicum

Biozone II, Late Hauterivian, Sundays River Formation.

Locus typicus

AL 1/69, cuttings sample at 580 feet.

Description

Test conical, with maximum width at level of last-formed chambers. Periphery of test

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 99

initially continuous, later strongly lobate; in cross-section test outline is broadly rounded.

Chambers triserially arranged throughout, usually in three vertically aligned columns,

although occasional tests show some distortion at particular levels to this arrangement.

Chambers subglobular, with little overlap on previous ones, much inflated in the final

portion of the test, increasing slowly and regularly in size as added; generally twice as

wide as high; arranged in five to six whorls. Sutures initially indistinct, flush, later

becoming distinct, depressed, with the spiral suture almost horizontally aligned. Aperture

interio-marginal, at the base of the final chamber, in form apparently a low elongate slit,

but not well preserved in any of the specimens. Apical portion of test broadly rounded,

through usually damaged. Surface of test roughened; test wall composed of coarser

angular quartz grains with finer material and relatively little cement.

Remarks

The specimen shown in apical view is somewhat distorted, and in side view ts clearly

triserial, despite the rather polyserial form suggested in Figure 35C. Tests of Verneuilina

secreta are distinct from most Northern Hemisphere species assigned to the genus,

principally in the globular chamber form and the broad and rounded, rather than acutely

angled, margins of the test. For this reason, there must exist some doubt as to whether this

is a true species of Verneuilina. From the size of tests, and the conical test outline, these

specimens cannot be considered juveniles of another genus, such as Verneuilinoides.

Tests of Verneuilinoides neocomiensis (Myatliuk) and Verneuilinoides inaequalis

Bartenstein & Brand, typical of the European Early Cretaceous, are very nearly

parallel-sided when adult: in contrast, Verneuilina secreta remains distinctly conical.

Verneuilina secreta 1s one of several species in the South African Early Cretaceous

which perhaps constitute a lineage of forms in the austral province. Similar species are

known from the Barremian and the Late Aptian to Early Albian of the southern offshore of

South Africa. The only South African species that 1s strongly triangular 1n cross-section 1s

Verneuilina howchini Crespin, which is confined to the Early Barremian to Early Aptian

of the southern offshore.

Stratigraphic range in the Sundays River Formation

Confined to the Late Hauterivian, Biozones VII to I. The species is found in the more

distal intersections of the Sundays River Formation.

Verneuilina sp. B

Pigs3 or

Remarks

One in situ specimen of Verneuilina occurs in Late Valanginian Biozone A. It is clearly

related to Verneuilina secreta sp. nov. in its test morphology, but it is more slender and

less conical than the Late Hauterivian species. For the present it is regarded as a separate

species.

100

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 39:

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 101

Genus Gaudryinella Plummer, 1931

Gaudryinella alexandria sp. nov.

Figs 35F-I

Diagnosis

An elongate, rather gracile species of Gaudryinella with initial triserial chambers, later

inflated biserial to cuneate, subglobular chambers, and with depressed sutures and

terminal aperture.

Etymology

Noun in apposition; from borehole AL 1/69, named for the magisterial district of

Alexandria, in which the borehole was drilled.

Material

Holotype (Fig. 35G). MF1207, SOEKOR negative F271.

Paratypes (Figs 35F, H, 1). MF1206, MF1208, MF1209, three specimens, SOEKOR

negatives F298, F163, and F297.

Stratum typicum

Late Hauterivian Biozone III of the Sundays River Formation.

Locus typicus

AL 1/69, cuttings sample at 910 feet.

Description

Test elongate, moderately gracile, almost parallel-sided, with maximum width usually

at or near level of final pair of chambers, and compressed. Test periphery variably lobate;

in cross-section test margins are broad and well rounded. Chambers initially triserially

arranged, increasing rapidly in size as added, arrayed in three whorls; subglobular in form

and flush to inflated in external view. Later chambers biserially arranged, increasing in

size steadily as added, with final few chambers cuneate and about as wide as high. The

chambers overlap previous ones to some degree, and the final chamber is often distinctly

larger than the earlier ones. The initial triserial part constitutes about one quarter of the

Fig. 35 (see facing page). A—D. Verneuilina secreta sp. nov. A. Holotype, SAM—PQ—MF1201, side

view, AL 1/69, 580 feet (II), F173. X 103. B. Paratype, SAM—PQ—MF 1202, side view, AL 1/69,

1 090 feet (III), F326. X 138. C. Paratype, SAM—PQ—MF 1203, apical view, AL 1/69, 1 090 feet (III),

F327. X 140. D. Paratype, SAM—PQ—MF 1204, apertural view, AL 1/69, 1 570 feet (VI), F427.

X 132. E. Verneuilina sp. B, SAM—PQ—MF 1205, side view, MV 1/79, 310-320 m (A), F654. X 121.

F-I. Gaudryinella alexandria sp. nov. F. Paratype, SAM—PQ—MF1206, side view, AL 1/69,

1 000 feet (III), F298. x 126. G. Holotype, SAM—PQ—MF 1207, side view, AL 1/69, 910 feet

(III),F271. xX 120. H. Paratype, SAM—PQ-—MF 1208, side view, AL 1/69, 520 feet (I), F163. x 102.

I. Paratype, SAM—PQ—MF 1209, apertural view, AL 1/69, 1 000 feet (III), F297. X 260. J. Dorothia

sp. A, SAM—PQ—MF1210, side view, AL 1/69, 2 360 feet (VIII), F499. x 126.

102 ANNALS OF THE SOUTH AFRICAN MUSEUM

total test height. Sutures initially indistinct, flush, becoming clearer, depressed, lightly

and uniformly curved, and reaching the test periphery at an angle of from thirty to fifty

degrees to horizontal. Aperture terminal, sited at the apex of the last-formed chamber; in

shape an elongate-ovate to sub-circular opening, and unornamented. Test surface lightly

roughened: test wall composed of moderate sized, angular quartz grains set in medium

quantities of cement.

Remarks

Gaudryinella alexandria differs from G. sherlocki Bettenstaedt (1952), from the

Barremian to Early Albian of north-west Europe, in its cuneate, rather than regularly

biserial later part of the test, and in its more slender form with compressed, subglobular

chambers. Comparative illustrations of G. sherlocki are given by Sherlock (1914, pl. 18

(fig. 2)), Bettenstaedt (1952, pl. 1 (figs 1—5)), Bartenstein & Bettenstaedt (1962, pl. 38

(fig. 14), table 18 (part 2)), Bartenstein et al. (1966, pl. 1 (figs 38—40)), and Hart et al.

(1981, pl. 7.2 (figs 4-5)). Hart et al. (1981) noted that what variation is seen 1n the species

is due to distortion of tests after burial. Gaudryinella alexandria \acks the separated,

globular chambers of tests of Gaudryinella aff. sherlocki as described and illustrated by

Crittenden (1983: 22, pl. 2 (figs 22—25)) from the Early Aptian of southern England. The

forms illustrated as Gaudryinella aff. sherlocki by Damotte & Magniez-Jannin (1973)

exhibit a different chamber morphology in the later part of the test than either G. sherlocki

or G. alexandria. Gaudryinella alexandria lacks the fully rectilinear arrangement of

uniserial chambers seen in tests of G. tealbyensis Bartenstein (1956), and also does not

show the nearly circular cross-section of this English Hauterivian species. It differs from

G. pusilla Magniez-Jannin (1975) in wanting the nearly globular, strongly inflated

chambers of the terminal part of the test.

Stratigraphic range in the Sundays River Formation

Late Hauterivian (upper Biozone IV to Biozone I). Restricted to outer shelf, near

normal marine environments.

Genus Dorothia Plummer, 1931 s./.

A variety of forms are here allocated to the genus Dorothia s.1. Dorothia sp. A and

Dorothia inglesidensis sp. nov. are narrow, almost parallel-sided forms that are the

earliest species of a series that ranges through the South African Cretaceous from the

Early Hauterivian to the top of the Santonian. These forms typically possess a conical

polyserial initial portion (four or five chambers to the whorl), circular in cross-section,

that occupies a quarter or a third of the total test height, followed by a long, regular,

biserial portion, with the typical Dorothia aperture of a low interio-marginal slit at the

base of the final chamber. The test wall is dominantly composed of agglutinated material,

and calcareous matter, apart from cement, is at a minimum. It has not yet proved possible

to determine if the test wall is canaliculate in Dorothia sp. A., Dorothia inglesidensis

sp. nov., or in other members of this group.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 103

Desai & Banner (1987) emended and expanded on the two genera Dorothia and

Marssonella, and it thus seems that narrow, parallel-sided forms fall well outside the strict

definitions of emended Dorothia and Marssonella, as well as Praedorothia and

Protomarssonella, presented by these authors. Loeblich & Tappan (1988) also did not

distinguish such forms, reflecting perhaps the wide interpretation given by them

previously to Dorothia (Loeblich & Tappan 1964). For the moment, Dorothia is thus here

considered sensu lato, although subdivision is clearly warranted. The third species

encountered in the Sundays River Formation, Dorothia australis sp. nov., can confidently

be referred to Dorothia s.s., as re-defined by Desai & Banner (1987).

Dorothia sp. A

Figs 35J, 36A—D

Remarks

Small numbers of poorly preserved, apparently rather distorted tests referable to

Dorothia occur in the Hauterivian. These are elongate, with a long, gently tapering

polyserial portion of the test. Later biserial chambers are weakly inflated, increasing in

width slowly to a maximum at the final pair of chambers. The aperture is a narrow

interio-marginal slit at the base of the final chamber, and usually sited in a slight recess. It

is possible that poorly preserved tests of the following species, Dorothia inglesidensis

sp. nov. have been included here, since their stratigraphic ranges overlap and their test

morphologies are not dissimilar. Because of their poor preservation, examples of

Dorothia sp. A are not easily compared to other species from elsewhere in the world. The

test illustrated as Spiroplectammina cushmani Crespin by Beer (1970, pl. 1 (fig. 5)) seems

to lack an initial coil, unlike Crespin’s species, and is probably referable to Dorothia

sp. A, since Spiroplectammina or Spiroplectinella species are entirely lacking in the

extensive microfaunas examined at SOEKOR from the Sundays River Formation.

Stratigraphic range in the Sundays River Formation

Later Early Hauterivian to Late Hauterivian (Biozones VIII to I), middle to outer shelf.

Dorothia inglesidensis sp. nov.

Figs 36E—H, 37A—D

Textularia sp. aff. foeda Beer, 1970: 9, pl. 1 (fig. 4a—b) (non Reuss).

Diagnosis

A slender, parallel-sided species of Dorothia with a circular cross-section, inflated and

rather high chambers that are especially evident in the final pair of the test.

Etymology

From its occurrence in the CO 1/67, CO 2/70 and CO 3/71 boreholes, drilled adjacent

to the Ingleside Cliff, just west of Colchester Cliff.

104 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 36.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 105

Material

Holotype (Figs 36E, 37A—B). MF1215, SOEKOR negative F666.

Paratypes (Figs 36F—H, 37C—D). MF1216 to MF1219, four specimens, SOEKOR

negatives F500, F426, and F416.

Stratum typicum

Biozone VI, Late Hauterivian, Sundays River Formation.

Locus typicus

Shallow borehole SB—9A, Core 1, 282 feet 6 inches.

Figure 37.

Dorothia inglesidensis sp. nov. A-B. Holotype, SAM—PQ—MF 1215, side and apertural views

respectively, shallow borehole SB—9A, core 1, 282 feet 6 inches (II). X 113. C—D. Paratype,

SAM—PQ—MF 1219, side and apertural views respectively, showing initial portion of test,

SEL1/74, 90m V1).ix 127.

Fig. 36 (see facing page). A—D. Dorothia sp. A. A. SAM—PQ—MF 1211, side view, AL 1/69, 2 410 feet

(VII), F513. x 88. B. SAM—PQ—MF1212, edge view, AL 1/69, 2 470 feet (VIII), F514. x 88.

C. SAM—PQ-MF 1213, edge view, AL 1/69, 940 feet (III), F276. x 137. D. SAM—PQ—MF1214,

edge view, AL 1/69, 1 480 feet (IV), F377. X 123. E-H. Dorothia inglesidensis sp. nov. E. Holotype,

SAM-—PQ-MF1215, side view, shallow borehole SB—9A, core 1, 282 feet 6 inches (II), F666. X 137.

F. Paratype, SAM—PQ-MF 1216, side view, AL 1/69, 2 360 feet (VII), F500. x 112. G. Paratype,

SAM=PO=MPI217,. side view, AL): 1/69; 1570) feet (V1), F426. x 98. .H.. Paratype,

SAM-—PQ-MF1218, edge view, AL 1/69, 1 540 feet (VI), F416. x 84. I-L. Dorothia australis

sp. nov. I. Paratype, SAM—PQ—MF 1220, side view, MV 1/79, 250-260 m (A), F634. x 112.

J. Paratype, SAM—PQ—MF 1221, side view, AL 1/69, 4 470 feet (A), F560. x 164. K. Holotype,

SAM-—PQ-MF 1222, side view, MV 1/79, 90 m (X), F574. X 123. L. Paratype, SAM—PQ-—MF 1223,

edge view, MV 1/79, 140 m (X), F586. x 156.

106 ANNALS OF THE SOUTH AFRICAN MUSEUM

Description

Test elongate, narrow, parallel-sided, occasionally showing maximum test width at

level of last formed pair of chambers. Test periphery lobate, broadly rounded, with

cross-section of adult part of test circular to sub-circular. Chambers arranged in an initial

polyserial portion, with 3-4 whorls apparently of 4-5 chambers each; this part of the test

tapering. Later part of test displays up to five pairs of biserially arranged chambers,

increasing moderately and regularly in height as added. Later chambers inflated. Early

biserial chambers are about as wide as high, whereas the later ones are one-and-a-half or

two times higher than wide. The final pair of chambers is particularly high, and indicates

some degree of overlap of the later chambers on earlier ones. Sutures initially rather

indistinct, flush or weakly depressed, becoming distinct, depressed, and with a clear

central zigzag suture; sutures reach the test periphery at a low angle of about 10 degrees;

sutures straight, rarely weakly curved. Aperture interio-marginal, located at the base of

the last-formed chamber, and sited at the foot of a prominent, nearly vertical

interio-marginal face of the final chamber. Form of aperture a low, elongate, rather arched

slit, which terminates well short of the test periphery. Surface of test lightly rugose,

composed of moderate to fine-grained quartz particles, some angular, set in moderate

cement.

Remarks

None of the tests assigned to Dorothia inglesidensis are complete: in all cases the

earliest part of the shell is missing. Occasional damaged examples of the early part occur,

sufficient to gain a full understanding of the species, as illustrated in Figure 37C—D.

Dorothia inglesidensis differs from D. filiformis (Berthelin) in possessing more

compact, much less globular or subglobular chambers, and a neater, tighter biserial

arrangement than the latter species. Authors’ interpretations of D. filiformis vary—

compare the illustrations of Sherlock (1914, pl. 18 (fig. 4)), Chapman (18928, pl. 11

(fig. 7)), Crespin (1963, pl. 16 (fig. 8)), Hart et a/. (1981, pl. 7.1 (figs 11-12)), Bartenstein

et al. (1966, pl. 1 (fig. 43)), and Magniez-Jannin (1975, pl. 8 (figs 1-2)), but

D. inglesidensis 1s distinct from all of these. Many illustrations of D. filiformis, however,

suggest the initial portion of the test is triserial and trilobate, although authors’

descriptions may not confirm this. There is thus a possibility that some tests included

under this name should be better referred to the genus Gaudryinopsis (see Loeblich &

Tappan 1988: 133, pl. 140 (figs 26—32)). Dorothia inglesidensis lacks the apertural

arrangement and compact polyserial portion of D. invenusta of Dailey (1973).

Stratigraphic range in the Sundays River Formation

Restricted to the latest Early and earlier Late Hauterivian (late Biozone VIII to top

Biozone VI), in more distal, middle to outer shelf localities: and one occurrence only in

Biozone ?II.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 107

Dorothia australis sp. nov.

Figs 36I-L, 38A—B

Dorothia pupa (non Reuss): McLachlan et al. 19766: 352, fig. 11 (no. 5).

Marssonella kummi (non Zedler): Kielbowicz et al. 1983: 321, pl. | (fig. 3, possibly fig. 2).

Diagnosis

A Dorothia species characterized by up to four pairs of inflated, biserially arranged

chambers in the later part of the slightly compressed, conical test, with weakly depressed,

horizontally aligned sutures and convex septa. Test consists of an initial more conical

portion and a later less rapidly widening part. Canaliculi present.

Etymology

From its occurrence in the Southern Hemisphere, in the austral province.

Material

Holotype (Fig. 36K). SAM—MF 1222, SOEKOR negative F574.

Paratypes (Figs 36l1, J, L, 38A—B). MF1220, MF1221, MF1223 to MF1225, five

specimens, SOEKOR negatives F634, F560, F586, F584, and F606.

Stratum typicum

Early Hauterivian Biozone X of the Sundays River Formation.

Locus typicus

MV 1/79, cuttings sample at 90 m.

Description

Test generally conical, with maximum width and depth at the level of the last-formed

pair of chambers. Test periphery lobate in the later part of the test, weakly arched in the

initial part; very broadly rounded, subcircular in cross-section. Test slightly compressed,

so that final portion is usually distinctly wider than deep. Initial part of test conical and

increasing rapidly in width: composed of chambers arranged in a trochospire of two or

three whorls, apparently with about four chambers in each whorl. Later part of test less

rapidly widening, but still conical; composed of three, occasionally four pairs of biserially

arranged chambers, increasing rather slowly and steadily in size as added; inflated,

especially at the test periphery but less so close to the zigzag suture, so that in fully adult

tests this suture lies in a depression. Terminal faces of final pair of chambers broad, gently

arched, inflated. Sutures initially indistinct, flush, becoming distinct in the biserial part of

the test, lightly depressed, straight, and aligned about horizontally to the test periphery.

Aperture interio-marginal, an elongate slit in a recession at the base of the final chamber,

so that the interio-marginal suture constitutes a distinct, gently sinuous curve over the

terminal face. Apical point of test broad and rounded. Test surface faintly roughened, with

wall composed of numerous small angular quartz grains set in abundant cement, leading

108 ANNALS OF THE SOUTH AFRICAN MUSEUM

to an unusually smooth-walled agglutinated test when compared with other Sundays

River Formation species. Canaliculi present.

Remarks

Earlier distinctions by McLachlan et al. (19766) between ‘Dorothia kummi (Zedler)’

and ‘Dorothia pupa (Reuss)’ were based to some degree on damaged and undamaged

tests, respectively. Subsequent offshore drilling in the Pletmos, Gamtoos and Algoa

basins through the Valanginian and Early Hauterivian has shown that the species is

widespread, and is also subject to some variation as a consequence of post-depositional

compaction. Tests from the Sundays River Formation are generally little affected by

compaction, although the specimen in Figure 36J is certainly distorted. Offshore, tests

akin to that of Figure 36K are commonest, and it is for this reason that this particular test

has been chosen as holotype. It 1s also possible that some variation seen is due to

dimorphism between the sexual and asexual generations, but this aspect remains to be

followed up.

The ‘Dorothia pupa’ of McLachlan et al. (19766) is characterized by an unusually

strongly inflated final chamber, but falls well within the morphological range accepted

here for Dorothia australis. In contrast, the Mngazana and Brenton tests of ‘Dorothia

Aummi’ (McLachlan et al. 1976a, 19766) lack the inflated chambers, lobate periphery and

inflated terminal face of D. australis, and would seem to be a different species, but it

remains doubtful if they should be referred to Zedler’s (1961) species. The Neuquén,

Argentina, test of Marssonella sp. illustrated by Musacchio (1979) from the Late

Hauterivian 1s clearly not referable here, but at least one of the two tests (pl. 1 (fig. 3))

figured by Kielbowicz et a/. (1983) from the Valanginian of south Patagonia seems to be

identical to D. australis.

All of the above tests referred to D. australis compare closely with the north-west

European species Marssonella kummi Zedler, described from the later Hauterivian of

northern Germany. Illustrations of M. kummi are given by Zedler (1961, pl. 7 (fig. la—c)),

Ten Dam (1946, pl. 87 (fig. 9a—b)), Michael & Pape (1971, pl. 1 (fig. 3)), Bartenstein et al.

(1971, pl. 1 (fig. 2)), Bartenstein & Brand (1951, pl. 4 (fig. 80a—b)), Bartenstein &

Bettenstaedt (1962, pl. 35 (fig. 11a—b)), and Bartenstein & Kaever (1973, pl. 6 (fig. 105)).

A possibly similar form, described as Protomarssonella kummi (Zedler), occurs in the

Berriasian to Valanginian Barrow Group of ODP Site 762 off north-west Australia (Jones

& Wonders 1992).

However, Dorothia australis differs from Protomarssonella kummi in lacking a nearly

flat terminal face to the test (unless damaged), in possessing significantly more inflated

later chambers and correspondingly more depressed sutures, a distinct vertically aligned

depression superimposed over the zigzag suture, and in lacking the “bullet-shaped’ outline

of P. kummi. The test of P. kummi figured by Guillaume & Sigal (1965) from the Late

Hauterivian part of the Barremian stratotype section exhibits very much more inflated

final chambers than is typical for the species. A comparison of the illustrated tests of

P. kummi listed above, with those of M. oxycona (Reuss) and ‘Dorothia’ levis

Magniez-Jannin, figured by Magniez-Jannin (1975) is of value.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 109

Although the Southern Hemisphere tests here referred to D. australis and the European

P. kummi are morphologically close, there are distinct differences, and 1t seems best to consider

the austral province occurrences as a separate genetic stock from those of the boreal province.

Occurrence

Dorothia australis ranges through the Late Valanginian and earliest Hauterivian

(Biozones C to X) of Pletmos Basin borehole PB—Al (McLachlan et al. 19764). In

Argentina the species is known from the Valanginian Springhill Formation of southern

Patagonia (Kielbowicz et al. 1983). The species occurs extensively in the Pletmos,

Gamtoos and Algoa basins off the south coast of South Africa, where it appears in small

numbers in the Late Berriasian, ranges through the Early Valanginian and becomes

abundant in the Late Valanginian and earliest Hauterivian, before disappearing at the top

of Biozone X.

Stratigraphic range in the Sundays River Formation

Late Valanginian to early Early Hauterivian (Biozones C to top X). The species is

ecologically sensitive, being absent from almost all marginal marine environments, and

absent from areas of the sea-floor affected by sand or uninterrupted silt deposition. It is at

its most frequent in the clayier Biozones Bb and Ba, above which it 1s rarer and rather

erratically distributed.

Supplementary note

It may be mentioned here that the Portlandian tests from the Colchester Member

equivalent of borehole PB—A1 assigned the name Dorothia subtrochus (Bartenstein) by

McLachlan et al. (19765: 352, fig. 11 (no. 6)) should more properly be referred to either

Trochammina or Tritaxis. This form has now been recognized elsewhere in the

Portlandian, in the Bredasdorp—Infanta Basin off the south coast of South Africa. The

species displays three or four chambers in later whorls. It may well be conspecific with the

Tritaxis? aff. Valvulina ?fusca (Williamson) of Musacchio (1979, pl. 1 (fig. 6)) from the

Callovian of Neuquén, Argentina.

Genus Gravellina Bronnimann, 1953

Gravellina sp. A

Figs 38C—D

Remarks

Seven tests referable to Gravellina occur in the Late Hauterivian (Biozones III to I) of

AL 1/69 and adjacent distal boreholes. The tests are not well preserved, but they are very

high-spired, quadriserial throughout, and display globular to subglobular chambers

arranged in four vertical columns. They are reminiscent of a species of Gravellina typical

of the earliest Barremian of Pletmos Basin, and the two occurrences may well be of the

same species. In South Africa, Gravellina is confined to deep marine, slope environments

low in oxygen and rich in organic debris.

110 ANNALS OF THE SOUTH AFRICAN MUSEUM

2 atu

Figure 38.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION ee

Family Textulariopsidae Loeblich & Tappan 1982

Genus Plectinella Marie 1956

Plectinella castlecliffensis sp. nov.

Figs 39A—F

Diagnosis

A small, slender, tapering Plectinella with inflated chambers, oblique sutures, a

terminal, elongate-ovate aperture and an extremely fine-grained test wall.

Etymology

Named after the adjacent ‘Castle Cliff exposure of the Sundays River Formation in the

Sundays River Valley.

Material

Holotype (Fig. 39A—B). MF 1228.

Paratypes (Fig. 39C—F). MF1229, MF 1230.

Stratum typicum

Exposure at first low-level bridge over the Sundays River just upstream from The Look

Out, Biozone D, Late Valanginian, Sundays River Formation.

Locus typicus

Low-level bridge near The Look Out, SOEKOR sample 18589.

Description

Test elongate, slender, small, slightly compressed, with maximum width and depth at

the lower part of the final pair of chambers. Test periphery lobate throughout; margin

broadly rounded throughout. Chambers arranged biserially in up to four pairs and closely

appressed. Chambers increase steadily in size as added and are generally a little higher

than wide through the entire test. Later chambers are distinctly to strongly inflated.

Sutures distinct, moderately to strongly depressed, oblique and declining to test periphery

Fig. 38 (see facing page). A-B. Dorothia australis sp. nov. A. Paratype, SAM—PQ-—MF 1224, apertural

view, MV 1/79, 140 m (X), F584. x 212. B. Paratype, SAM—PQ—MF 1225, apertural view, MV 1/79,

180-190 m (X), F606. X 206. C—D. Gravellina sp. A. C. SAM—PQ-—MF1226, ventral view, AL 1/69,

760 feet (II), F216. x 171. D. SAM—PQ—MF 1227, dorsal view, AL 1/69, 1 030 feet (III), F312.

x 187. E-F. Cornuspira orbicula (Terquem & Berthelin). E. SAM—PQ-—MF1231, side view,

AL 1/69, 640 feet (II), F199. x 142. F. SAM—PQ—MF 1232, side view, AL 1/69, 370 feet (1), F42.

x 151.G. ?Calcitornella sp., SAM—PQ—MF 1233, test attached to Ammobaculites, AL 1/69, 670 feet

(II), F208. x 45. H-K. Nubecularia lucifuga Defrance. H. SAM—PQ—MF 1234, test ?not attached,

AL 1/69, 4 110 feet (A), F550. x 172. I. SAM—PQ—MF1235, test attached to agglutinated

foraminifera shell, AL 1/69, 1 540 feet (VI), F420. x 75. J. SAM—PQ—MF1236, test attached to

Ammobaculites sp., AL 1/69, 3 350 feet (IX), F534. xX 75. K. SAM—PQ—MF 1237, test attached to

Ammobaculites sp., AL 1/69, 2 190 feet (VIII), F494. x 80.

112 ANNALS OF THE SOUTH AFRICAN MUSEUM

Femur so}

Plectinella castlecliffensis sp. nov. A-B. Holotype, SAM—PQ—MF 1228, side and apertural

views, exposure at first low-level bridge just upstream from The Look Out, SOEKOR

sample 18589 (D). x 128. C—D. Paratype, SAM—PQ-—MF 1229, side and apertural views,

SOEKOR sample 18589 (D), x 171. E-F. Paratype, SAM—PQ—MF 1230, side and apertural

views, SOEKOR sample 18589 (D). x 233.

at an angle of about 45° to horizontal. The median suture forms a weakly depressed, gentle

zigzag. Aperture terminal to sub-terminal, an elongate-ovate or sub-circular opening

areally sited, with some occasional evidence of a faintly thickened lip around the opening.

Apical end of test narrow, acute, and composed of a prominent, small, globular

proloculus. Test wall extremely fine-grained, thin-walled, and composed exclusively of

quartz grains.

Remarks

Loeblich & Tappan (1964) included Jurassic and Cretaceous biserial agglutinated

forms with terminal apertures in the present-day genus Pseudobolivina. These included

Arenovirgulina aegyptiaca of Said & Barakat (1958) and Plectinella virgulinoides of

Marie (1956). More recently, the Jurassic and Cretaceous species have been separated

from Pseudobolivina (see Banner & Pereira 1981; Loeblich & Tappan 1982, 1988) and

are referred to Plectinella, of which Arenovirgulina 1s a junior synonym.

The examples from the basal Sundays River Formation are mostly distorted through

compaction, although the 10 specimens utilized in the description given above provide a

good indication of the undistorted test morphology. Plectinella castlecliffensis differs

from Callovian P. aegyptiaca (Said & Barakat) in the more clearly inflated chambers, the

obliquely oriented sutures, the more terminally sited and more nearly sub-circular

aperture, and the absence of any twisting in the plane of addition of the biserial chambers.

None of the Jurassic species of ‘“Pseudobolivina’ described by Souaya (1976) from

Arctic Canada display inflated chambers in the style of Plectinella castlecliffensis.

Bimonilina variana Eicher (1960), described from the Albian of Wyoming was

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION LI3

subsequently referred by authors to Pseudobolivina, following Loeblich & Tappan

(1964). More recently, the genus Bimonilina has been re-instated (Loeblich & Tappan

1982, 1988). The aperture of Bimonilina 1s a thin, vertically aligned elongate slit rather

than the sub-terminal, sub-circular opening of Plectinella and Pseudobolivina. It is not

clear whether all references of ‘Pseudobolivina variana (Eicher) from the Albian,

Cenomanian and later Cretaceous rocks principally of North America are of true

Bimonilina. Plectinella_ castlecliffensis appears to lack the inflated chambers of

Bimonilina reciprocata Loeblich & Tappan (1982: 63, pl. 1 (figs 18—22)) from the Fort

Worth Formation (Late Albian) of Texas. Because the Sundays River tests are clearly

compressed, it 1s difficult to make an effective comparison between the elongate apertural

openings of the two species.

Stratigraphic range in the Sundays River Formation

Confined to the basal Sundays River Formation, Late Valanginian Biozone D. The

species has been encountered only in the Look Out area, northern Algoa Basin. It occurs

only in association with marginally marine, possibly estuarine genera, such as

Miliammina, where more normal marine genera such as Haplophragmoides are absent.

Family Cornuspiridae Schultze, 1854

Subfamily Cornuspirinae Schultze, 1854

Genus Cornuspira Schultze, 1854

Cornuspira orbicula (Terquem & Berthelin, 1875)

Figs 38E—-F

Spirillina orbicula Terquem & Berthelin, 1875: 17, pl. 1 (fig. 12a—c).

Cornuspira orbicula (Terquem & Berthelin). Bartenstein & Brand, 1951: 279, pl. 4 (fig. 89a—c).

Remarks

Occasional specimens, mostly poorly preserved and always pyrite infilled, occur in the

Late Hauterivian (Biozones II and I). These seem best referred to Cornuspira orbicula,

described originally from the Middle Lias of France. The original description of the

species indicates that the test surface 1s ‘lisse, translucide’, and no mention is made of test

perforations that would indicate the species is a true Spirillina. Most later authors have

considered the species to be porcellaneous in its wall construction, and their precedent is

followed here.

Genus Calcitornella Cushman & Waters, 1928

?Calcitornella sp.

Fig. 38G

Remarks

Three porcellaneous-walled, attached specimens seem to be non-septate and referable

to Calcitornella. However, it may be that they are referable to Nubecularia lucifuga

114 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 40.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 115

Defrance (see below), with the chambers elongated and not at all inflated, so that the

septal divisions are not evident in external view. The few specimens have somewhat

precluded any attempts at thin sectioning. The illustrated ?Calcitornella test is attached to

a fragment of an Ammobaculites, although it is not possible to determine which species.

All ?Calcitornella sp. tests are from Biozone II of the Late Hauterivian, in the most distal

borehole sections.

Family Nubeculariidae Jones, 1875

Genus Nubecularia Defrance, 1825

Nubecularia lucifuga Defrance, 1825

Figs 38H—-K, 40A—B

Nubecularia lucifuga Defrance, 1825: 210, pl. 44 (fig. 3, 3a—d). Jones & Parker, 1860: 455, pl. 20

(figs 52-56). Arnold, 1967: 622, text-figs 1-12. McLachlan et al., 1976a: 328.

Remarks

In a detailed examination of Recent living specimens, and comparison between them

and fossil material, Arnold (1967) has drawn attention to the confusion surrounding the

taxonomy of Nubecularia lucifuga and its allied species. He concluded that “in the light of

(Arnold’s) study of variability in natural and culture populations, careful examination of

original descriptions of the thirty-odd species of living and fossil Nubecularia (and a not

insignificant number of species assigned to other genera as well!) suggests quite strongly

that almost half of them should more properly be assigned to N. /ucifuga’. Following

Arnold (1967), all Nubecularia specimens from the Sundays River Formation have been

assigned to N. lucifuga.

This species was originally described from the Eocene of northern France (Defrance

1825), and has since been widely recorded, particularly from present-day, high-energy,

highly oxygenated, shallow marine environments. The extant species 1s particularly

common along those parts of the east coast littoral of South Africa that possess a rocky

substrate. In contrast, all tests of N. /ucifuga from the Sundays River Formation are from

Fig. 40 (see facing page). A—B. Nubecularia lucifuga Defrance. A. SAM—PQ—MF 1238, test attached to

Ammobaculites subaequalis fragment, AL 1/69, 1540 feet (VII), F422. x 103.

B. SAM-—PQ-MF1239, test attached to Frondicularia nieuwjaarskopensis, shallow borehole

SB-15, core 2, 210 feet (II), F677. X 61. C—F. Vinelloidea buchenroderi sp. nov. C. Holotype,

SAM-PQ-MF1240, attached to lithic grain, Uitenhage to Graaff-Reinet Road outcrop,

sample 11464 (Bb), F62. x 67. D. Paratype, SAM—PQ—MF 1241, attached to lithic grain, Uitenhage

to Graaff-Reinet Road outcrop sample 11464 (Bb), F63. x 112. E. Paratype, SAM—PQ—MF 1242,

attached to lithic grain, Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F64. x 90.

F. Paratype, SAM—PQ—MF1243, single chamber only attached to lithic grain, Uitenhage to

Graaff-Reinet Road outcrop sample 11464 (Bb), F6l. xX 105. G. Nodobacularia sp. A,

SAM-—PQ—MF1251, side view, single chamber only, Uitenhage to Graaff-Reinet Road outcrop

sample 11464 (Bb), F71. X 108. H. Quinqueloculina sp., SAM—PQ-MF 1252, side view, AL 1/69,

1240) feet (EV); F359. * 215.

116 ANNALS OF THE SOUTH AFRICAN MUSEUM

more distal, middle- and outer-shelf environments. A deeper marine milieu is perhaps also

suggested by the specimen from the earliest Late Valanginian of the Mngazana Basin

(McLachlan et al. 1976a). This difference either indicates a wider range of environmental

preferences in the Mesozoic than in the Cainozoic, or that two different species or

subspecies are being considered.

Occurrence

Jones & Parker (1860; see also Adams 1962: 162) recognized the species in the

Pliensbachian (Early Jurassic) of Chellaston, near Derby, England. Ten Dam (1950)

described N. triloculina from the Albian of the Netherlands, but Arnold (1967) obtained

cultured individuals of N. /ucifuga stock ‘indistinguishable’ from N. triloculina tests. The

species occurs in small numbers in the Portlandian Colchester Member of the Uitenhage

Trough, onshore Algoa Basin (McMillan 1980), and in the Late Valanginian (Biozone B)

in deeper waters (?) at Mngazana, Transkei (McLachlan et al. 1976a).

Stratigraphic range in the Sundays River Formation

Very rare in the Late Valanginian Biozones Bb and Ba, and scattered occurrences,

occasionally in some numbers in the Late Hauterivian (Biozones VII to I); absent

elsewhere.

Genus Vinelloidea Canu, 1913

Vinelloidea buchenroderi sp. nov.

Figs 40C—F

Diagnosis

A species of Vinelloidea characterized by an attached test, composed of a globular

proloculus, followed by a tubular, non-septate chamber of one whorl, and up to five

inflated, pyriform chambers separated by distinct, abrupt septal necks, and with an

irregular apertural opening at the termination of the test.

Etymology

Named after Baron von Buchenroder, early palaeontology enthusiast in South Africa,

who examined the eastern bank of the Swartkops River (Amsterdamhoek area) for fossils

in 1828, with C. H. Grisbrook (1830). Von Buchenroder appears to have lived at the

Swartkops River drift (Atherstone 1857: 532). The correct spelling of his name 1s unclear;

Grisbrook’s version is followed here.

Material

Holotype (Fig. 40C). SAM—MF 1240, SOEKOR negative F62.

Paratypes (Figs 40D-F). Three specimens, SOEKOR negatives F63, F64, and F6l,

SAM-—MF1241 to MF1250, seven additional tests, all from sample 11464, Uitenhage to

Graaff-Reinet Road outcrop.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Ti7

Locus typicus

Sample 11464, Uitenhage to Graaff-Reinet Road cutting, located | km north of the

basal Sundays River Formation, just east of Uitenhage town in the Uitenhage Trough.

Stratum typicum

Late Valanginian (basal Biozone Bb), Sundays River Formation.

Description

Test elongate, attached, meandering; test wall porcellaneous in construction. Test

uniserial, composed of an initial, globular, rather prominent proloculus followed by a

lower, tubular second chamber that encircles the proloculus for one whorl. Following the

second chamber are from three to five inflated, pyriform chambers which taper anteriorly

toward the following chamber. Sutures distinct, depressed; septal necks short and not

severely constricted. Aperture terminal, sited at the end of the final chamber, apparently

an irregular, subcircular and unornamented opening, although most tests studied are

damaged around the aperture. Test wall smooth, unornamented. Most tests examined are

coiled around lithic grains, and are never attached to fossil shell or other organic debris: in

most cases they encircle grains of green or grey Palaeozoic slate rather than quartz grains.

Some damaged specimens appear to have originally attached to more than one grain.

Remarks

Tests of Vinelloidea buchenroderi are confined to one sample (11464) from one of the

road cuttings along the Uitenhage to Graaff-Reinet Road. They occur in association with

other simple miliolids—a group that, in general, 1s rare in the Sundays River Formation. It

seems likely that this assemblage reflects the proximity of wave-induced, highly turbulent

and oxygen-rich conditions close to shore. This type of littoral appears to have been rather

rare during the Late Valanginian and Hauterivian around the rim of the Algoa Basin, as

hyposaline, estuarine conditions seem much more widespread.

Similar forms are known from the littoral and sub-littoral deposits occurring at Brenton

(McLachlan et al. 19765) in the Pletmos Basin, where they occur in some numbers. The

Brenton simple miliolids were unfortunately not discussed by McLachlan et al. (1976b),

but some of them do seem referable to Vinelloidea buchenroderi.

Vinelloidea buchenroderi can be distinguished from the type species, V. crussolensis

Canu, 1913, synonymous with Nubeculinella bigoti Cushman (1930), described from the

Oxfordian of northern France, by its more prominent proloculus and coiled second

chamber, and its more regular, pyriform chambers in the later part of the test. Vinelloidea

buchenroderi preferentially attaches to lithic grains, whereas V. crussolensis seems to

select shell fragments (see Shipp & Murray 1981: 134, pl. 6.3.1 (fig. 17)).

Stratigraphic range in the Sundays River Formation

Apparently confined to the earliest part of Biozone Bb, Late Valanginian. However,

since the distribution of Vinelloidea buchenroderi is obviously strongly facies controlled,

this range is certainly artificial. Littoral and sub-littoral facies have been preferentially

118 ANNALS OF THE SOUTH AFRICAN MUSEUM

removed during latest Hauterivian—earliest Barremian tilting and planation, and

repeatedly thereafter, including during the series of regressive marine planations during

the Pleistocene (upper Algoa Group times).

Genus Nodobacularia Rhumbler, 1895

Nodobacularia sp. A

Fig. 40G

Remarks

Nine separated chambers referable to Nodobacularia occur in sample 11464 from the

road cutting 1 km north of the basal Sundays River Formation along the Uitenhage to

Graaff-Reinet Road. The chambers are from free-living tests, possess very narrow septal

necks (see illustrated specimen) and are ornamented with numbers of large, platy quartz

grains. These fragments are morphologically similar to Nodobacularia nodulosa

(Chapman), described from the Albian Gault Clay of England (Chapman 1891), but the

test ornamentation is different.

Stratigraphic range in the Sundays River Formation

Lowest Biozone Bb, Late Valanginian, but see also the comments for Vinelloidea

buchenroderi sp. nov. (p. 116).

Family Miliolidae Ehrenberg, 1839

Subfamily Quinqueloculininae Cushman, 1917

Genus Quinqueloculina d’Orbigny, 1826

Quinqueloculina spp.

Fig. 40H

Remarks

Six tests referable to Quinqueloculina have been obtained from the Sundays River

Formation. All are badly preserved, but they are more nearly globular than is typical for

Q. minima Tappan. These forms appear to have no distinctive stratigraphic range.

Quinqueloculina minima Tappan, 1943

Fig. 42A

Quinqueloculina minima Tappan, 1943: 490, pl. 78 (fig. 33a—b). Loeblich & Tappan, 1949: 255,

pl. 48 (figs 12a—b, 13a—b). McLachlan et al., 1976a: 328, fig. 16 (no. 2). Magniez-Jannin, 1984:

403, pl. 1 (fig. 22).

Remarks

Scattered tests in the Sundays River Formation appear best referred to

Quinqueloculina minima. These shells are mostly poorly preserved. None possesses an

apertural tooth, and all display a low, rather crescentic outline to the aperture.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 119

Occurrence

Originally described from the Duck Creek Formation (Late Albian) of Oklahoma and

Texas (Tappan 1943), and also known from the Albian Walnut Formation of Texas and

Oklahoma (Loeblich & Tappan 1949). European records include the Aptian of Bulgaria

(lovcheva 1962), Barremian of Rumania (Neagu 1968), and Hauterivian—Early

Barremian of France (Magniez-Jannin 1984). Present also in the Late Valanginian

(Biozone B) of Mngazana Basin, Transkei (McLachlan et al. 1976a).

Stratigraphic range in the Sundays River Formation

Rare throughout, from Biozone A to Biozone I (Late Valanginian to Late Hauterivian).

Subfamily Rzehakininae Cushman, 1933

Genus Miliammina Heron-Allen & Earland, 1930

Miliammina latrobei sp. nov.

Figs 41A—F

Diagnosis

A species of Miliammina distinguished by its small size, elongate-ovate outline,

inflated, rounded chambers, broadly rounded test periphery and extremely fine-grained,

rather glassy test wall.

Etymology

Named after Abbé Latrobe, who, while on an ecclesiastical tour through the eastern

Cape in 1815, first reported the occurrence of fossils at the Addo Wagon Drift over the

Sundays River (Latrobe 1818; Meiring 1959: 15).

Material

Holotype (Figs 41A—C). SAM—MF 1254.

Paratypes. One specimen (Fig. 41D—F) and ten additional specimens from borehole

CO 1/67, core sample at 3 311 feet, SAM—MF1255 to MF1264.

Stratum typicum

Earliest Late Valanginian (Biozone D), Sundays River Formation.

Locus typicus

Borehole CO 1/67, core sample at 3 311 feet.

Description

Test small, ovate to elongate-ovate in outline, inflated; maximum width usually at or

near mid-height; periphery of test continuous, arched; in cross-section margin broadly

rounded. Height of test about two-and-a-half times as wide. Chambers arranged in a

quinqueloculine manner, increasing steadily in size as added, inflated. Chambers usually

widest at their base, and narrowing to the foramen or aperture. Sutures distinct, depressed,

120 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 41.

Miliammina latrobei sp. nov. A-C. Holotype, SAM—PQ—MF 1254, opposite side and apertural

views, CO 1/67, 3 311 feet (D). X 146. D—-F. Paratype, SAM—PQ-—MF 1255, opposite side and

apertural views, CO 1/67, 3 346 feet (D). X 103.

usually curved but locally may be sinuous: this may be a natural feature or due to

post-depositional test distortion. Aperture terminal, on the last-formed chamber, a

sub-circular opening, apparently lacking any tooth structure. Surface of test smooth,

almost glassy, greenish-olive in colour; test wall composed of abundant, very fine-grained

quartz particles set in little cement: the grain size of the agglutinated material is very

uniform.

Remarks

Miliammina latrobei tests are mostly distorted and often flattened, due to

post-depositional compaction. They are small in size when compared with the

foraminifera shells from higher in the Sundays River Formation. This species is almost

entirely restricted to core samples, and it is highly likely that it is much more extensively

distributed through the basal Sundays River Formation than is seen in the samples studied.

Since the species is confined to hyposaline, possibly estuarine environments, its

distribution through time may prove to be more extensive on the persistently hyposaline

northern perimeter of the Sundays River Formation than further south, as in the latter

region the ‘estuarine’ conditions associated with the marine transgression at the base of

the sequence were of short duration and soon gave way to more normal marine

environments. Unfortunately, available borehole data from the northernmost Algoa Basin

do not confirm such a stratigraphic distribution.

Miliammina latrobei can be distinguished from M. valdensis Bartenstein & Brand

(1951: 277, pl. 13 (figs 360a—c, 361a—b)) in its wider chambers revealing a clear taper

from base to top, unlike the rather tubular chambers of the German species. The outline of

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 12]

M. latrobei tests 1s elongate-ovate, often tending toward sub-rectangular, whereas

M. valdensis is oval in outline. Miliammina latrobei is without the distinct apertural neck

of M. olgae Bielecka (1960), and clearly differs from the narrow, elongate M. jurassica

Haeusler (1882).

Stratigraphic range in the Sundays River Formation

Confined to hyposaline, ?estuarine environments in the earliest Late Valanginian

(Biozone D). It may range higher in the northernmost, persistently marginal marine facies

of the Sundays River Formation.

Family Nodosariidae Ehrenberg, 1838

Genus Nodosaria Lamarck, 1812 s./.

The genus Nodosaria has been considered here in the broad sense. As detailed by

Loeblich & Tappan (1988), various genera have been erected through the years that

separate groupings of ‘Nodosaria’ on the basis of the test ornamentation, chamber

morphology and aperture characteristics. Thus, it seems probable that N. paupercula

Reuss should be more properly referred to the genus Pyramidulina, and perhaps also

N. obscura Reuss and Nodosaria cf. N. obscura as understood herein. In contrast,

N. tomaszowiensis Sztejn may be better referred to the genus Nodomorphina, although

tests studied lack the compressed initial part, distinguished by a rectangular cross-section,

and are without longitudinal costae at the test angles, since Sundays River tests are

circular in section throughout.

Nodosaria paupercula Reuss, 1845

Figs 42B—-K

Nodosaria paupercula Reuss, 1845: 26, pl. 12 (fig. 12). Neagu, 1965: 21, pl. 5 (fig. 18).

Magniez-Jannin, 1975: 197, pl. 12 (figs 35-36).

see Nodosaria (Dentalina) paupercula Reuss. Chapman, 1893: 593, pl. 9 (figs 13-14).

Nodosaria cf. N. raristriata (non Chapman): Espitali¢é & Sigal, 1963: 55, pl. 25 (figs 7-8).

Remarks

The Sundays River specimens appear to compare well with descriptions and

illustrations of Nodosaria paupercula in Europe. However, these South African examples

are distinctly older, being Valanginian and Hauterivian rather than Albian, and it may well

be that more than one species 1s included under this name. Only detailed morphometric

analysis is likely to distinguish different assemblages.

The tests from the Sundays River Formation show some variation in the degree of

inflation of the chambers, the intensity of the ornamentation of vertically-aligned ribs, and

in the degree to which the tests taper towards the proloculus. In all specimens, the ribs

either fade away as they reach the short conical, terminal part of the final chamber, or they

continue weakly and link with the teeth of the radiate aperture (Figs 42J—K). In the case of

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 42.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 123

the Albian tests from Europe, the ribs either fade away before reaching the base of the

button-like apertural neck (Chapman 1893) or they continue and merge with it (Magniez-

Jannin 1975, pl. 12 (fig. 36)). The specimen of NV. paupercula illustrated by Tappan (1940,

pl. 16 (fig. 11)) from the Middle Cenomanian Grayson Formation of Texas possesses a

much more elongate test, with distinct septal necks between each chamber.

Espitalié & Sigal (1963) noted the presence of shells very similar to N. paupercula in

Cenozone F (Hauterivian to ?Barremian) in the Majunga Basin, Madagascar. The

Sundays River Formation individuals compare particularly well with their form (Espitalie

& Sigal 1963, pl. 25 (fig. 7). However, Espitalie & Sigal (1963: 55) erroneously compared

their Majunga tests instead with the species Nodosaria (Dentalina) raristriata Chapman

(1893), a long, very slender species described as being ‘filiform’, and clearly more typical

of Dentalina s.\. than Nodosaria s.1.

Occurrence

Described by Reuss (1845) from the Bohemian Cretaceous, and subsequently recorded

from the Gault Clay (Albian) of Folkestone, England (Chapman 1893), the Albian of

France (Magniez-Jannin 1975) and the Albian of Rumania (Neagu 1965). In the Southern

Hemisphere it occurs in the Hauterivian to ?Barremian of Madagascar (Espitalie & Sigal

1963). Nodosaria paupercula has also been identified in the Hauterivian (Biozones IV to

II) of Pletmos Basin borehole PB—A1 and in the earliest Late Valanginian (Biozone D)

Brenton Formation, following a re-examination of the work presented by McLachlan er

al. (19766). Further offshore, in the Pletmos, Gamtoos and Algoa basins, N. paupercula

ranges from mid-Early Valanginian to Early Barremian.

Stratigraphic range in the Sundays River Formation

Occurs in small numbers throughout most of the sequence, from Late Valanginian

Biozone Bb to Late Hauterivian Biozone I, although Early Hauterivian occurrences are

few.

Fig. 42 (see facing page). A. Quinqueloculina minima Tappan. SAM—PQ-—MF1253, side view,

MV 1/79, 240-250 m, (A), F624. x 162. B—K. Nodosaria paupercula Reuss. B. SAM—PQ-—MF 1265,

side view, AL 1/69, 1 000 feet (III), F287. x 78. C. SAM-PQ-—MF1266, side view, AL 1/69,

1 720 feet (VII), F454. x 107. D. SAM—PQ—MF 1267, side view, AL 1/69, | 270 feet (IV), F364.

x 57. E. SAM—PQ—MF 1268, side view, AL 1/69, 370 feet, (I), F46. x 68. F. SAM—PQ—-MF1269,

side view, AL 1/69, 460 feet (1), F103. x 63. G. SAM—PQ-—MF 1270, side view, AL 1/69, | 930 feet

(VII), F465. x 73. H. SAM—PQ—MF1271, side view, AL 1/69, 520 feet (1), F129. x 70. I. SAM—

PQ—MF 1272, side view, AL 1/69, 1 630 feet (VII), F440. x 72. J. SAM—PQ-—MF 1273, apertural

view, AL 1/69, 580 feet (ID, F169. x 180. K. SAM—PQ—MF1274, apertural view, AL 1/69,

1 540 feet (VI), F419. x 160. L—-N. Nodosaria obscura Reuss. L. SAM—PQ—MF 1275, side view,

shallow borehole SB—28, core 1, 188 feet (VI), F689. x 75. M. SAM—PQ-MF1276, side view,

AL 1/69, 1 930 feet (VII), F466. x 117. N. SAM—PQ—MF 1277, side view, AL 1/69, 490 feet (1),

F114. x 140.

124 ANNALS OF THE SOUTH AFRICAN MUSEUM

Nodosaria obscura Reuss, 1845

Figs 42L-N, 43A—-B

Nodosaria obscura Reuss, 1845: 26, pl. 13 (figs 7-9). Bartenstein & Brand, 1951: 312, pl. 10

(figs 247-248). Malumian & Masiuk, 1975: 590, pl. 2 (fig. 8). Magniez-Jannin, 1975: 192,

pl. 12 (figs 22-34), text-fig. 105. Malumian & Nafiez, 1983: 376, pl. 1 (fig. 6).

Nodosaria (Dentalina) obscura Reuss. Chapman, 1893: 593, pl. 9 (fig. 16).

Remarks

Occasional Nodosaria tests are present in the Sundays River Formation that show

variation in the degree of inflation of the chambers, the intensity, number and bladed or

rounded nature of the vertically aligned ribs, and in the tapering or domed termination to

the last-formed chamber. Tests generally possess from seven to ten ribs. The apical point

of the test is usually acutely angled, but may also be slightly spinose on occasion. These

tests compare well with the range of variation seen in assemblages of N. obscura from the

French Albian (Magniez-Jannin 1975). Bartenstein (1954) and Magniez-Jannin (1975)

have regarded N. fontannesi (Berthelin) as a junior synonym of N. obscura.

Occurrence

Widely reported in the Cretaceous, and described originally by Reuss (1845) from the

Cretaceous of Bohemia. Later records include the Albian of Folkestone, England (Gault

Clay) by Chapman (1893); the Albian of the Aube region, France (Magniez-Jannin 1975);

Valanginian—Hauterivian Pampa Rincon Formation, Tierra del Fuego (Malumian &

Masiuk 1975); and the Barremian Rio Mayer Formation of Santa Cruz Province, Argentina

(Malumian & Nafiez 1983). The species is widespread but always rare in continental shelf

sediments of Valanginian, Hauterivian and possibly Early Barremian age off the south

coast of South Africa.

Stratigraphic range in the Sundays River Formation

Occasional specimens occur from Late Valanginian Biozone Bb to Late Hauterivian

Biozone I.

Nodosaria tomaszowiensis Sztejn, 1957

Figs 43C—F

Nodosaria tomaszowiensis Sztejn, 1957: 53, 228, pl. 6 (fig. 48).

Lenticulina (Nodosaria) aff. fontannesi (non Berthelin): Damotte & Magniez-Jannin, 1973: 33,

pl. 4 (fig. 11).

Nodosaria sceptrum (non Reuss): McLachlan et al. 1976a: 328, fig. 16 (no. 3).

Nodosaria aff. fontannesi (Berthelin) var. flexocostata [sic] (non Khan): Musacchio, 1979: 258,

pl. 4 (fig. 5).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Pe)

Remarks

With some uncertainty, a number of references to Early Cretaceous slender Nodosaria

tests, ornamented with up to ten vertically aligned ribs are assigned to N. tomaszowiensis.

These forms possess more ribs than is usual for N. orthopleura Reuss, which is

characterized by five or seven. These tests are not as robustly built as those of NV. obscura

Reuss or N. fontannesi (Berthelin), and they appear to lack the stronger, more prominent

ribs of N. fontannesi var. flexocarinata Khan (1950). If reference to N. tomaszowiensis

proves to be inappropriate, it may be that this group warrants a new name.

Occurrence

Valanginian of Poland (Sztejn 1957), Aptian of France (Damotte & Magniez-Jannin

1973), Late Hauterivian of Neuquén (Musacchio 1979), as well as the Barremian Rio

Mayer Formation, Santa Cruz Province, Argentina (Malumian & Nafiez 1983), and earlier

Late Valanginian (Biozone B) of Mngazana Basin, Transkei (McLachlan ef a/. 1976a).

Stratigraphic range in the Sundays River Formation

Small numbers from Biozone Bb to Biozone II, generally at more distal localities.

Nodosaria grisbrooki sp. nov.

Figs 43G—J

Diagnosis

A species of Nodosaria distinguished by fine to moderately developed grooves

vertically aligned on the test surface, mostly continuous but some infrequent, with the

apical end of the test bluntly pointed, and a terminal, centrally sited, radiate aperture.

Etymology

Named after Mr C. H. Grisbrook, apothecarist of Graaff-Reinet and palaeontology

enthusiast, who with Von Buchenroder, examined the fossils of the Amsterdamhoek

outcrops in 1828 (Grisbrook 1830).

Material

Holotype (Fig. 43G). MF1284, SOEKOR negative F627.

Paratypes (Figs 43H—J). MF1285 to MF1287, three specimens, SOEKOR negatives

F82, F79, and F599.

Stratum typicum

Late Valanginian Biozone A, Sundays River Formation.

Locus typicus

Borehole MV 1/79, cuttings sample 240—250 m.

ALS OF THE SOUTH AFRICAN MUSEUM

126

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vn A

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Figure 43.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 127

Description

Test elongate, almost cylindrical, slightly tapering, with maximum width of test at the

level of the last-formed chamber. Test circular in cross-section. Chambers uniserially

arranged throughout, rectilinear, never arched, with up to six chambers in most tests.

Chambers increase very slowly and regularly in height as added, with later chambers a

little wider than high. Sutures usually indistinct, becoming faintly evident and very lightly

depressed between the final few chambers. All sutures are horizontal. Aperture terminal, a

circular and radiate opening, centrally placed on the final chamber. Apical end of test

bluntly pointed. Surface of test ornamented by fine, vertically aligned grooves, usually not

too distinct, but occasionally more in evidence, in which case the intervening surfaces of

the test have a rope-like appearance. Differences in the surface ornamentation may be due

to diagenetic corrosion of tests. Test wall thick and robustly built.

Remarks

The majority of tests found are the same as those illustrated in Figure 43G (holotype)

and Figure 43J. It may well be that the specimen shown in Figure 431 displays the

ornamentation closest to the original shell, when its occupant was alive, but clearly this

cannot now be confirmed. The species possesses a distinctive surface ornamentation that

1s rather unlike previously described Early Cretaceous Nodosaria species.

The test referred to Lingulina sp. aff. L. nodosaria Reuss by Masiuk & Vina (1986a)

from the Late Hauterivian of the Agrio Formation, southern Argentina, displays a fine

ornamentation similar in intensity to that seen in N. grisbrooki. However, the Argentinian

test is characterized by an elongate, slit-like aperture, and thus is clearly a Lingulina. Its

slightly constricted sutures compare closely with those of the test illustrated here in

Figure 43H.

Fig. 43 (facing page). A—B. Nodosaria obscura Reuss. A. SAM—PQ—MF 1278, side view, AL 1/69,

790 feet (III), F221. x 147. B. SAM—PQ-MF1279, side view, AL 1/69, 1 480 feet (IV), F376.

xX 126. C-F. Nodosaria tomaszowiensis Sztejn. C. SAM—PQ—MF 1280, side view, shallow borehole

SB-15, core 4, 229 feet (ID), F684. x 93. D. SAM—PQ—MF 1281, side view, Colchester Cliff outcrop

sample 11444 (IV), F704. x 150. E. SAM—PQ—MF1282, side view, Colchester Cliff outcrop

sample 12001 (IV), F711. X 61. F. SAM—PQ-MF 1283, side view, shallow borehole SB—15, core 2,

210 feet (II), F675. x 116. G-J. Nodosaria grisbrooki sp. nov. G. Holotype, SAM—PQ-—MF 1284,

side view, MV 1/79, 240-250 m (A), F627. x 113. H. Paratype, SAM—PQ—MF 1285, side view,

Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F82. x 35. I. Paratype,

SAM—PQ—MF 1286, side view, Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F79.

x 99. J. Paratype, SAM—PQ-MF1287, side view, MV 1/79, 180-190 m (X), F599. x 143.

K-L. Pseudonodosaria tenuis (Bornemann). K. SAM—PQ-—MF1290, side view, MV_ 1/79,

400-410 m (Ba), F647. x 146. L. SAM-PQ—MF1291, side view, shallow borehole SB—29, core ?,

218 feet 6 inches (VI), F690. x 81. M—N. Nodosaria cf. N. obscura Reuss. M. SAM-PQ-MF1288,

side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb), F232. x 66. N. SAM—PQ-—MF 1289, side

view, Zoetgeneugd Cliff outcrop sample 11450 (Bb), F233. x 123. O-P. Amphicoryna pletmosiana

sp. nov. O. Paratype, SAM—PQ—MF 1293, side view of final chamber, neck broken off, AL 1/69,

790 feet (III), F219. x 76. P. Paratype, SAM—PQ—MF 1294, side view of proloculus with apertural

necks COW/G7 7642 fect Vil), F139" x 1100.

128 ANNALS OF THE SOUTH AFRICAN MUSEUM

Stratigraphic range in the Sundays River Formation

Present in small numbers from the Late Valanginian (Biozone Bb) to the Early

Hauterivian (Biozone VIII). The species has also been found to occur in Pletmos Basin

borehole PB—A1, in the highest Biozone C (at 1 500 feet) of the Late Valanginian,

following revision of the work by McLachlan et al. (19765).

Nodosaria cf. N. obscura Reuss, 1845

Figs 43M—N

see Nodosaria obscura Reuss, 1845: 26, pl. 13 (figs 7—9).

Remarks

Several tests of Nodosaria from sample 11450 (basal Biozone Bb, Late Valanginian)

near the base of the Zoetgeneugd Cliff outcrop are clearly related to N. obscura, as

discussed above, but reveal some distinct differences. These tests are substantially more

tapered, possess up to nine bladed, vertically aligned ribs, with more inflated chambers

and correspondingly more depressed sutures. In their test morphology they come close to

N. harrisi Vieaux (see Magniez-Jannin 1975, pl. 12 (figs 38-42)), but they lack the

delicately structured apertural neck of that species.

Stratigraphic range in the Sundays River Formation

Apparently confined to the earliest part of Biozone Bb in the Late Valanginian. This

form may be restricted to shallow marine, well-oxygenated, normal marine environments.

Genus Pseudonodosaria Boomgaart, 1949

Pseudonodosaria tenuis (Bornemann, 1954)

Figs 43K—L

Glandulina tenuis Bornemann, 1854: 31, pl. 2 (fig. 3a—b).

Pseudoglandulina tenuis (Bornemann) Bartenstein & Brand, 1951: 315, pl. 13 (fig. 349). Sztejn,

1957, 230Npilne (ig. 53). Beer, 1970. 17 ple 3g 33)

Pseudonodosaria tenuis (Bornemann) Winter, 1970: 35, pl. 4 (figs 127-128).

Pseudonodosaria sp. Butt, 1979: 259, pl. 1 (fig. 23).

Remarks

Few tests of a simple Pseudonodosaria, with weakly inflated chambers. The species is

less sturdily constructed than P. humilis (Roemer). These tests compare closely with the

specimen illustrated by Bartenstein & Brand (1951), but do not exhibit the distinctly

inflated chambers of those figured by Winter (1970).

Occurrence

Described by Bornemann (1854) from the Lias of G6éttingen, Germany, and later

recorded from the latest Hauterivian of the Speeton Clay, north-east England (Fletcher

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 129

1973), the Middle and Late Valanginian of north-west Germany (Bartenstein & Brand

1951), the Portlandian (Bielecka & Pozaryski 1954) and Late Valanginian (Sztejn 1957)

of Poland, the Early Kimmeridgian of southern Germany (Winter 1970) and the

Barremian of DSDP Site 397 off Cape Bojador, north-west Africa (Butt 1979). There are

also a number of references to the species in the Late Jurassic of Germany.

Stratigraphic range in the Sundays River Formation

Too few specimens occur to permit a precise statement on the range of

Pseudonodosaria tenuis, but identified specimens occur in the Late Valanginian and

Early Hauterivian (?Biozones Ba to VIII).

Pseudonodosaria humilis (Roemer, 1841)

Figs 60H-K

Nodosaria humilis Roemer, 1841: 95, pl. 15 (fig. 6).

Pseudoglandulina humilis (Roemer). Bartenstein & Brand, 1951: 315, pl. 10 (figs 266-271).

Bartenstein et al., 1957: 37, pl. 7 (figs 153, 154, 155a—b).

Pseudonodosaria humilis (Roemer). Dailey, 1973: 66, pl. 9 (fig. 12). Magniez-Jannin, 1975: 198,

text-fig. 106. Lott et a/., 1986: 44, fig. 51. Bertels, 1990: 274, pl. 6 (fig. 11).

Pseudonodosaria gr. humilis (Roemer). Malumian & Masiuk, 1975: 590, pl. 1 (fig. 7).

Pseudoglandulina humilis gr. (Roemer). McLachlan et al., 1976a: 334, fig. 16 (no. 23).

Remarks

Magniez-Jannin (1975: 199) has pointed out that Reuss (1863), describing Glandulina

mutabilis, remarked that the short and broad forms of his species were identical to

Nodosaria humilis as described by Roemer (1841). Both Fuchs (1967) and

Magniez-Jannin (1975) have concluded that these two species must be synonymous.

Examination of tests referred to Pseudonodosaria humilis from South Africa indicates

that all are uniserial and rectilinear in their chamber arrangement, and none contain an

initial polyserial portion typical of the Polymorphinacea. The species also occurs widely

in the offshore Pletmos, Gamtoos and Algoa basins off South Africa, where it is

particularly frequent in Early and Late Valanginian rocks (Biozones E to B). The

extensive development of deep marine, anoxic or poorly oxygenated sea-floor

environments in the latest Valanginian and Hauterivian (1Atl to 6At1l) preclude its

occurrence in rocks of that age in the distal Pletmos, Gamtoos and Algoa basins.

Occurrence

Pseudonodosaria humilis was originally described by Roemer (1841) from the

Barremian of northern Germany. Other records include Albian (Magniez-Jannin 1975)

and Aptian (Damotte & Magniez-Jannin 1973) of France; latest Valanginian to earliest

Barremian (Fletcher 1973) and Valanginian to Hauterivian (Lott et al. 1986) of the

Speeton Clay, north-east England; Hauterivian—Barremian to Aptian—Albian of

California (Dailey 1973); Barremian (Bartenstein et al. 1957) and Aptian—Albian

130 ANNALS OF THE SOUTH AFRICAN MUSEUM

(Bartenstein et al. 1966) of Trinidad; Cenozones A to F (Late Bathonian to ?Barremian)

and older in the Majunga Basin, Madagascar (Espitalie & Sigal 1963); the Valanginian—

Hauterivian Pampa Rincon Formation (Malumian & Masiuk 1975) of Tierra del Fuego,

the Valanginian Springhill Formation of southern Patagonia (Kielbowicz et al. 1983) and

the Hauterivian lower Rio Mayer Formation (Bertels 1990), Argentina; and the Late

Valanginian (Biozone B) of the Mngazana Basin, Transkei (McLachlan et al. 1976a).

Stratigraphic range in the Sundays River Formation

Present very rarely in the Late Valanginian (Biozones Bb and Ba) and the Early

Hauterivian, but relatively frequently in the Late Hauterivian (Biozones VII to I). In

contrast to its extensive occurrence in Late Valanginian rocks off the south coast of South

Africa the species is scarce during this time period probably because of the lowered

oxygen conditions on the sea-floor in the Sundays River Trough. The species is not typical

of marginal marine conditions of any type, and is at its most abundant on the middle and

outer shelf.

Genus Amphicoryna Schlumberger, 1881

Amphicoryna pletmosiana sp. nov.

Figs 430-P, 44A—-C

Dentalina cf. multicostata Beer, 1970: 10, pl. 1 (fig. 8) (non d’Orbigny).

?Amphicoryna sp. McLachlan et al. 19766: 352, fig. 11 (no. 7).

Diagnosis

An Amphicoryna species with numerous fine vertical ribs ornamenting the exterior,

some of which extend up the rather short and sturdy apertural neck, and with inflated,

globular chambers.

Etymology

Named after its first published occurrence in the borehole PB—A1, drilled in 1970 on

the northern margin of the Pletmos Basin.

Material

Holotype. MF 1292, SOEKOR negative F1054, see McLachlan et al. (19765, fig. 11

(105-7):

Paratypes (Figs 430—P, 44A—C). MF1293 to MF1297, five specimens, SOEKOR

negatives F219) F 1399375, 220 and F437.

Stratum typicum

Late Hauterivian, Biozone III, Pletmos Basin.

Locus typicus

Borehole PB—A1, cuttings sample at 930 feet.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 137

Description

Test elongate, uniserial, rectilinear or very faintly arcuate, with slow rate of increase in

chamber size. Maximum width of test generally at mid-height of final chamber. Test

composed of three or four chambers, globular in shape, and overlapping previous ones to a

small degree. Sutures strongly marked, indented, and horizontal. Aperture apparently

circular, developed at the termination of a rather short and wide neck. In none of the

specimens studied is the aperture well preserved, and the neck is somewhat irregularly

terminated. Surface ornamentation composed of numerous vertically aligned ribs, from

thirty to fifty in number. Ribs in well-preserved examples sharply defined, narrow, with

rounded peaks, and never bladed; in corroded specimens the ribs are more broadly

rounded. The majority of the ribs are continuous over sutures, although a little subdued.

Occasional ribs extend for less than one chamber. At the apical end of the test, the ribs fade

to a fairly smooth and unornamented area. About sixteen or twenty of the ribs continue

from the last-formed chamber and range up the apertural neck to its termination. Test wall

thick, robust.

Remarks

No complete tests of this species have yet been encountered in either the Pletmos or

Algoa basins. The majority of specimens consist only of detached single chambers, and all

Sundays River Formation examples found so far are in this state, with the slight exception

of the specimen illustrated as Fig. 430. However, enough fragments exist to establish the

nature of the species. Amphicoryna pletmosiana is a very distinctive species, even when

fragmented tests are predominant, and its occurrence is the basis of an easily recognizable

biozone. Beer (1970) first illustrated this species, using the name Dentalina cf.

multicostata d’Orbigny, from the Late Hauterivian of borehole CO 1/67.

The genus Amphicoryna 1s best known from the Neogene and the Quaternary, and one

extant species, A. scalaris (Batsch), is widely known around South Africa. However,

earlier records of the genus are very sparse, and an Early Cretaceous occurrence of the

genus seems unusual. The apertural neck, in its height and width, is not comparable to the

delicate necks seen on later Cainozoic examples of the genus. Even so, this species is

clearly distinct from all other Nodosaria species known in the South African Valanginian,

Hauterivian and Barremian by its apertural neck and constricted sutures, and it therefore

clearly merits separation from them into another genus. No similar species have been

found in available literature.

Stratigraphic range in the Sundays River Formation

Ranges from Biozone VII to the top of Biozone III in the Late Hauterivian. The species

is typical of middle- and outer-shelf environments, both in the Algoa and the Pletmos

basins. It would seem to be able to survive on relatively sandy substrates, as tests are

common in silty sandstone core samples from borehole CO 1/67.

LZ ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 44.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 133

Genus Astacolus de Montfort, 1808 s./.

Remarks

The genus Astacolus is here considered in the wide sense. Astacolus calliopsis (Reuss)

s.L., A. schloenbachi (Reuss), and Astacolus sp. C in particular, as understood herein, may

be better referred to the genus Hemirobulina (see Loeblich & Tappan 1988).

Astacolus gilli sp. nov.

Figs 44D-G

Diagnosis

A species of Astacolus characterized by an elongate, mostly parallel-sided test,

elongate-lenticular in cross-section, with acutely rounded test peripheries, and maximum

width and depth of test at about proloculus level.

Etymology

Named after Dr Gill, who collected fossils from the banks of the ‘Zondag River’,

probably at Zoetgeneugd Cliff, prior to 1830 (Grisbrook 1830).

Material

Holotype (Fig. 44D). MF1298, SOEKOR negative F252.

Paratypes (Figs 44E-G). Three specimens, SOEKOR negatives F65, F491, and F251,

and five additional specimens from different depths in borehole MV 1/79; from MF1299

to MF1301, MF1639 to MF1643.

Locus typicus

Sample no. 11452, basal part of Zoetgeneugd Cliff outcrop.

Stratum typicum

Late Valanginian Biozone C of the Sundays River Formation, onshore Algoa Basin.

Fig. 44 (see facing page). A—C. Amphicoryna pletmosiana McMillan sp. nov. A. Paratype,

SAM-—PQ-MF1295, side view of final chamber with ?damaged neck, AL 1/69, 1 420 feet (IV),

F375. X 116. B. Paratype, SAM—PQ—MF 1296, apical view, AL 1/69, 790 feet (III), F220. X 88.

C. Paratype, SAM—PQ-MF 1297, apertural view, neck broken off, AL 1/69, 2 020 feet (VII), F487.

x 143. D-G. Astacolus gilli sp. nov. D. Holotype, SAM—PQ-—MF 1298, side view, Zoetgeneugd

Cliff outcrop sample 11452 (€), F252. x 38. E. Paratype, SAM—PQ—MF 1299, side view, Uitenhage

to Graaff-Reinet Road outcrop sample 11464 (Bb), F65. x 50. F. Paratype, SAM—PQ—MF 1300, side

view, AL 1/69, 2 110 feet (VIII), F491. X 67. G. Paratype, SAM—PQ—MF 1301, apertural view,

Zoetgeneugd Cliff outcrop sample 11452 (C), F251. xX 98. H-I. Astacolus humilis (Reuss).

| H. SAM—PQ-—MF 1302, side view, AL 1/69, 1 660 feet (VII), F445. x 39. I. SAM—PQ—MF1303, side

view, AL 1/69, 1 780 feet (VID), F450. xX 59. J. Astacolus sp. C, SAM—PQ—MF 1304, side view,

| MV 1/79, 170 m (X), F598. xX 98.

134 ANNALS OF THE SOUTH AFRICAN MUSEUM

Description

Test strongly compressed, with maximum width and depth at or near the level of the

proloculus. Test almost parallel-sided throughout, and elongate-lenticular in

cross-section. Test composed of relatively small initial coil, composed of over one whorl

of chambers, followed by uniserial uncoiled portion, the latter accounting for over

three-quarters of the test in adult examples. Equatorial periphery of test acutely rounded

throughout, never carinate or angled, although a thick flange with a rounded margin is

often developed along the dorsal periphery in the early uncoiled portion of adult tests.

Axial periphery initially subcircular around the coil, becoming linear, never lobate on

either ventral or dorsal margin, except occasionally at the level of the last formed

chamber. The coiled portion of the test exhibits about six visible chambers, with the

uncoiled portion containing up to ten chambers. Chambers in final part of test about five

times as wide as high. Sutures generally distinct; in initial part of test raised, limbate and

regularly curved; in uncoiled part they are strongly limbate and raised centrally, but

weakly raised to flush near to both the ventral and dorsal margins. The sutures thus tend to

be marked best along a central band by a series of elongate-ovate swellings. Sutures of

uncoiled part are gently curved, initially horizontal, but attaining an angle of about

forty-five degrees by the final chamber. Surface of test smooth, generally unornamented.

Umbilical area raised, but not infilled by any form of boss. Aperture terminal, located at

the dorsal margin, in form a radial opening. Terminal face of last-formed chamber

smooth, flat or weakly depressed. Test wall rather thick.

Remarks

Astacolus gilli is rather more compressed than is typical for the genus, and given the

uncertain boundaries of many of the nodosarid genera, could with some justification be

regarded as a species of Vaginulinopsis. However, the size of the initial coil is perhaps

sufficient to regard it as an Astacolus.

Astacolus gilli can be distinguished from A. mutilatus Espitalié & Sigal (1963) by its

fewer (six rather than twelve) chambers in the final whorl of the coiled part of the test, in

the lack of a sub-carinate margin, the lack of such an acutely triangular terminal face, even

in juvenile specimens, and in its distinctly less positive sutures. Astacolus gilli differs

markedly too from Astacolus/Marginulina humilis (Reuss): the chamber arrangement,

and more especially the height to width ratio of the last-formed chambers of A. gi//i bears

little comparison with the tests illustrated by Reuss (1863, pl. 6 (figs 16a—b, 17a—b)) or

Damotte & Magniez-Jannin (1973, pl. 3 (figs 32-39)).

Some confusion also existed initially between this species and Astacolus sp. A of

McLachlan et al. (19766: 353, fig. 12 (nos 1-4)). It is now clear that Astacolus sp. A

consists of two distinct forms, one of Portlandian and one of early Late Valanginian age.

Astacolus gilli can be distinguished from both by consistent differences in the outline of

the test, the nature of the sutures and the degree of carination of the test periphery. Some of

the Brenton Formation samples studied by McLachlan et a/. (1976b) contain very large

numbers of the early Late Valanginian (Biozone D) form of Astacolus sp. A (McLachlan

et al. 1976b, fig. 12 (nos 1, 3)). Many of these are perfectly preserved, and adult examples

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 133

show that the final uncoiled chambers always diminish significantly in size. The sutures of

the Brenton form remain raised and limbate across the entire width of the test, and through

most of the test, but they become depressed between the final few chambers. The dorsal

periphery 1s ornamented with a wide, bladed keel. The limbate sutures of the coiled part of

the test converge over the umbilicus to form a distinct nodular swelling. None of these

features are seen in Astacolus gilli.

The Portlandian Astacolus sp. A (McLachlan et al. 19765, fig. 12 (nos 2, 4)), from the

Colchester Member equivalent of borehole PB—A1, 1s distinct from A. gi//i in its weakly

limbate and less raised sutures, which are uniformly ornamented along their entire length,

the absence of a parallel-sided uncoiled part of the test and, most noticeable of all, in the

presence of a large, domed, glassy boss over the umbilicus. No similar forms to 4. gilli

have been described or illustrated to date from localities in South America or in

Madagascar.

Stratigraphic range in the Sundays River Formation

Astacolus gilli 1s confined to the highest Biozone C, Biozones Bb and Ba (Late

Valanginian) in the onshore Algoa Basin. One specimen only has been found in

Biozone VUI, Early Hauterivian (Fig. 44F). It appears to have tolerated quite a range of

environments, from sub-littoral to outer shelf, but 1s absent in hyposaline facies along the

northern margins of the Sundays River Formation. The species is also known from the

Late Valanginian Biozones D to B of borehole PB—A1, and in rocks of the same age the

species is scattered throughout the offshore Pletmos Basin, and locally in the offshore

Gamtoos and Algoa basins.

Astacolus humilis (Reuss, 1863)

Figs 44H-I

Cristellaria humilis Reuss, 1863: 65, pl. 6 (figs 16a—b, 17a—b).

see Lenticulina (Astacolus) pachynota (non Ten Dam): Zedler, 1961: 37, pl. 8 (fig. 7a—c).

Lenticulina/Marginulina/humilis (Reuss). Damotte & Magniez-Jannin, 1973: 28, pl. 3 (figs 32-39).

Astacolus neopachynota (non Bartenstein & Kaever): McLachlan ef al., 1976b: 353, fig. 11

(nos 28-29).

Remarks

There appears to be considerable variation in interpretation of Astacolus

neopachynota, especially in the width of the uncoiled part of the test. Ten Dam (1946)

illustrated Vaginulinopsis pachynota, which possesses a fairly compressed test, with

limbate, elevated and almost ribbed sutures, especially in the median portion of the test,

away from both ventral and dorsal margins. In contrast, the shells illustrated by

Bartenstein & Kaever (1973), upon renaming the species, are not quite as wide, and the

sutures of the median part of the test appear to be depressed rather than raised. The

example figured by Zedler (1961) is much closer in its morphology to the original

specimens illustrated by Ten Dam (1946).

136 ANNALS OF THE SOUTH AFRICAN MUSEUM

In South Africa, tests referable to either A. neopachynota or A. humilis occur only very

rarely, both in Pletmos Basin and the onshore Algoa Basin. They are wider and more

strongly compressed, almost flat-sided, than is typical for European 4. neopachynota.

Consequently, the South African tests have been referred to A. humilis, but even here,

some differences can be seen. In particular, there are variations in the intensity of

limbation and degree of elevation of the sutural ornament both between Reuss’s two

figured tests, and within the South African tests.

Occurrence

Described from the Upper Hils Clays (?Barremian) of northern Germany (Reuss

1863); Aptian of the Aube district, France (Damotte & Magniez-Jannin 1973); Biozone IX,

Early Hauterivian, of borehole PB—A1, Pletmos Basin (McLachlan et al. 19765).

Stratigraphic range in the Sundays River Formation

Biozone VII, Early Hauterivian, but so rare that it is probable there are too few

specimens to confidently define its full range.

Astacolus sp. C

Fig. 44J

Remarks

Although possessing a flat ventral surface to the uncoiled portion of the test,

reminiscent of species of Pravoslavlevia and Saracenaria, this ventral face is narrow, and the

single specimen found thus seems best referable to Astacolus. The specimen is characterized

by sharply incised sutures, especially in the uncoiled portion. A number of South African

species of Lenticulina and Astacolus, particularly in the Early and Late Valanginian,

possess various styles of deeply incised sutures. Most however also feature strong test

surface ribbing patterns, and Astacolus sp. C is rather unique in being otherwise

unornamented. The single specimen of Astacolus sp. C 1s from Biozone X, Early Hautertvian.

Astacolus microdictyotos Espitalié & Sigal, 1963 s./.

Figs 45A-K

Astacolus microdictyotos Espitalié & Sigal, 1963: 33, pl. 10 (figs 6a—b, 7a—d). Canon & Ernst,

1974: 73, pl. 1 (fig. 19a—c). McLachlan et al., 19766: 353, fig. 11 (nos 23-25). Kielbowicz et al.

1983: 322, pl. 1 (figs S—9). Bertels, 1990: 255, pl. 2 (fig. 2). Malumian, 1990: 448, pl. 1 (fig. 1).

Cristellaria dictvodes (non Deecke): Martinez & Ernst, 1965: 9.

Lenticulina (Astacolus) microdictyotos (Espitalié & Sigal). Beer, 1970: 13, pl. 2 (fig. 9).

Astacolus microdictyotus Espitalié & Sigal. Riegraf, 1989: 1055, pl. 2 (fig. 2).

Remarks

Espitalié & Sigal (1963) described the holotype of Astacolus microdictyotos from the

Majunga Basin, Madagascar, as being characterized by a well-developed, initial coiled

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 137

portion of the test with about nine chambers in its final whorl, followed by only two

uncoiled chambers. Such forms do not occur in the Late Jurassic and Early Cretaceous

sediments of the southern offshore (Pletmos, Gamtoos, Algoa and Mngazana basins) of

South Africa. All of the South African specimens available for study, from all four basins,

contain no more than about three-quarters of a coil, composed of five or six chambers in

the initial part of the test. The greater part of the test 1s uncoiled. The degree of sutural

limbation and ornamentation is variable, but never exceeds that of the specimen illustrated

by McLachlan et al. (19765, fig. 11 (no. 23)). Despite these differences, the southern

African tests are referred to A. microdictyotos because of the close similarity of

ornamentation; for this reason the species is considered sensu lato.

Examination of ornamentation patterns and general test outline of Astacolus

microdictyotos s.\. in the Sundays River Formation shows there to be two distinct groups

of tests, which may warrant varietal status. The first, commoner group (see Fig. 45A—G) is

characterized by a more intense surface ornamentation, with frequent elongate-ovate

depressions aligned parallel to the direction of uncoiling of the test. As noted by Espitali¢

& Sigal (1963), the ornamentation decreases in intensity toward the apertural face of the

final chamber, which itself is devoid of ornament (see Fig. 45F). In the Sundays River

Formation, this group ranges throughout the Late Valanginian and Hauterivian; offshore

the group ranges from the Berriasian up to the Early Aptian. The group is known from the

Pletmos, Gamtoos, Algoa and Mngazana basins. In the case of the Mngazana Basin,

A, microdictyotos s.l. of the first group was discovered during re-examination of the

Mngazana foraminifera subsequent to the work presented by McLachlan et a/. (1976a).

The second group, which is usually less common, is confined to the Late Valanginian

and Early Hauterivian and older rocks of the Gamtoos and Algoa basins, and is

distinguished by possessing a rather more compressed but wider test, with a finer, denser

reticulated surface ornamentation. There is a tendency for the chambers to increase

steadily in width, so that maximum width of the test is often at the level of the final

chamber. The form illustrated by Kielbowicz et al. (1983, pl. 1 (fig. 8)) is clearly of this

group. Sundays River Formation examples of this second group are illustrated in

Figure 45H-K.

A third group of Astacolus microdictyotos s.l. is known particularly from the

Portlandian of offshore borehole Hb-A1 in the southern Algoa Basin. This group contains

tests that are very elongate, almost Vaginulina-like in their test morphology, with a fine

reticulation pattern ornamenting the surface. The coarser patterning of most of the

Sundays River Formation examples 1s lacking. The Majunga Basin tests, ranging from the

Late Portlandian to the Late Valanginian, would seem to form a distinct fourth group,

characterized by their large initial coil, small uncoiled portion and fine surface reticulation

(Espitalié & Sigal 1963).

These four groups appear to have distinctly different stratigraphic ranges, and perhaps

will prove to be of assistance in biostratigraphic correlation between southern South

America, South Africa and Madagascar. It is possible that Astacolus microdictyotos s.1.

has an ancestry in the European species Lenticulina dictyodes (Deecke), which is

distinguished by a finely reticulate ornamentation closely comparable to the Southern

138 ANNALS OF THE SOUTH AFRICAN MUSEUM

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eee

Figure 45.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 139

Hemisphere species. Lenticulina dictyodes is typical of the Bajocian of north-west

Germany (Bartenstein & Brand 1937: 178; Munk 1978, pl. 4 (figs 1, 3)) and the Bajocian

to Bathonian of England (Coleman 1981: 118, pl. 6.2.3 (fig. 7); see also Morris &

Coleman 1989, fig. 6.3.8 (fig. 7)). Despite being referred to Lenticulina, this European

species is found with the final part of the test uncoiled, as figured by Coleman (1981), and

thus may be considered an Astacolus as understood in the present work.

A further form, associated with A. microdictyotos s.l. by way of its surface

ornamentation, 1s Marginulinopsis pristipellis Ludbrook (1966: 121, pl. 9 (fig. 6)), also

illustrated by Scheibnerova (1976: 72, text-figs 73-74) from the Aptian of the Great

Artesian Basin, Australia. Marginulinopsis pristipellis was formerly utilized as a

down-hole marker to define the top Late Aptian of the southern offshore of South Africa,

where it is confined to the continental shelf (McLachlan & McMillan 1979), but more

recent work indicates it to range up to the top of the Middle Albian (McMillan ef al. 1997).

Its ornamentation pattern is very fine, the test is small, subcircular in cross-section, with

an initial coil of about half a whorl and about four uncoiled rectilinear chambers in the

later part of the test. For these reasons, South African Marginulinopsis pristipellis can

clearly be distinguished from A. microdictyotos s.\., and the two are regarded as separate

species. In contrast Malumian (1990) considered them synonymous. The final record of

this style of ornamentation occurs extremely rarely in the Coniacian of the southern

offshore of South Africa, where Lenticulina-like tests display a rather sparse reticulation.

Attempts to correlate these into a lineage are probably not justifiable at present, and their

origins may well be polyphyletic.

Occurrence

Late Portlandian to Late Valanginian (Cenozone D) in the Majunga Basin, Madagascar

(Espitalié & Sigal 1963); Late Valanginian and Hauterivian of offshore borehole PB—A1,

Pletmos Basin (McLachlan et a/. 19766) and Late Valanginian of the Mngazana Basin,

Transkei (unpublished SOEKOR data), South Africa; Valanginian Springhill Formation of

the Austral Basin, Patagonia (Kielbowicz et al. 1983; Malumian 1990); Springhill

Formation and the Favrella beds of southern Chile (Martinez & Ernst 1965) and the

?Kimmeridgian—Oxfordian (Rinconian) to Barremian (Pratian) or Hauterivian

(Esperanzian) of the Magallanes Basin, southern Chile (Natland eft a/. 1974—\"text-figure

Fig. 45 (see facing page). Astacolus microdictvotos Espitalié & Sigal s.. A-G. Group 1.

A. SAM-—PQ-—MF 1305, side view, AL 1/69, 1 030 feet (III), F307. x 84.B. SAM—PQ—-MF 1306, side

view, AL 1/69, 640 feet (II), F201. X 167. C. SAM—PQ—MF 1307, side view, MV 1/79, 250-260 m

(A), F629. x 142. D. SAM—PQ—MF1308, side view, MV 1/79, 240-250 m (A), F626. x 131.

E. SAM—PQ-MF1309, side view, shallow borehole SB—32, core 1, 146 feet (IV), F692. x 64.

F. SAM—PQ-MF1310, apertural view, MV 1/79, 250-260 m (A), F633. X 139. G. SAM—PQ-

MF1311, close-up of ornamental pit, AL 1/69, 1 540 feet (VI), F411. x 1984. H-K. Group 2.

H. SAM—PQ-—MF 1312, side view, MV 1/79, 160 m (X), F595. x 50. I. SAM—PQ-MF1313, side

view, AL 1/69, 2 000 feet (VII), F481. X 85. J. SAM—PQ—MF 1314, side view, AL 1/69, 3 660 feet

(X), F541. x 96. K. SAM—PQ—MF1315, close-up of ornament, MV 1/79, 140 m (X), F582. X 1580.

140 ANNALS OF THE SOUTH AFRICAN MUSEUM

discrepancies rather confuse the range in this work); there appear to be differences in age

from the Chilean and Argentinian work on the Austral Basin. The full stratigraphic range

of A. microdictyotos s.\. in South Africa is Early Portlandian to Early Aptian.

Stratigraphic range in the Sundays River Formation

Group | ranges from Biozone Bb to Biozone I, Late Valanginian to Hauterivian.

Group 2 ranges from Biozone Bb to basal Biozone VII (Late Valanginian to earliest Late

Hauterivian). The species is absent from shallow marine and hyposaline marginal marine

facies, and is typical of middle and outer shelf locations.

Astacolus gibber Espitalié & Sigal, 1963

Figs 46A—H

Astacolus gibber Espitalié & Sigal, 1963: 36, pl. 13 (figs 8a—d, 9a—b, 10a—b, 1 la—b). Malumian &

Masiuk, 1975: 585, pl. 1 (figs 3, 4a—b). McLachlan et al., 1976a: 328, fig. 16 (no. 5); 1976b:

352, fig. 11 (nos 10-12). Masiuk & Vina, 19865: 60, pl. 1 (figs 1-5), pl. 2 (figs 2-7). Bertels,

1990: 253. pli (hie al7y.

Lenticulina (Astacolus) gibber (Espitalié & Sigal). Beer, 1970: 13, pl. 2 (fig. 8).

Lenticulina reyesi Canton & Ernst, 1974: 74, pl. 2 (fig. 6a—b).

Lenticulina (Astacolus) nodosa gibber Espitalié & Sigal. Bartenstein, 1974: 550, pl. 2 (figs 7-8,

13-15). Aubert & Bartenstein, 1976: 16, pl. 2 (figs 1-8).

Lenticulina nodosa (non Reuss): Musacchio, 1979: 254, pl. 4 (fig. 8); 1981: 478, pl. 1 (fig. 1).

Astacolus gibber gibber Espitalié & Sigal. Malumian & Nafiez, 1983: 382, pl. 2 (fig.?7—8).

Remarks

A much clearer picture is now possible, resulting from numerous additional borehole

sections and a more effective biostratigraphic correlation, of the exact relationships of

A. gibber and Lenticulina nodosa, both in terms of their morphology and _ their

stratigraphic range in South Africa. It has long been evident that A. gibber can be regarded

as the fully adult form of L. nodosa, since it possesses the final, uncoiled portion of the

test. Many specimens from the Sundays River Formation are incipiently uncoiling, and it

is often difficult to decide to which of these two ‘species’ they should be referred. It 1s

obvious that such a division 1s an artificial one, but for the stratigraphic reasons discussed

below, it is followed in the present work.

Examination of the stratigraphic ranges of A. gibber and L. nodosa in South Africa

shows them to be very different. Lenticulina nodosa first appears in the southern offshore

Pletmos, Gamtoos and Algoa basins in the Late Berriasian, initially in small numbers,

becoming abundant from the later Early Valanginian to the top of the Early Aptian, at

which point it becomes extinct off all three coasts of South Africa. In contrast, A. gibber

occurs in small numbers, and ranges in South Africa from the mid Valanginian to the

Early Aptian, the earlier part of which reflects its occurrence in the Majunga Basin of

Madagascar (Cenozones E and F, Late Valanginian to ?Barremian) given by Espitalie &

Sigal (1963).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 141

Variation can be seen in the Sundays River Formation tests of A. gibber especially in

the intensity of the sutural ribbing, the dorsal nodes at the terminations of each suture, and

in the size and intensity of the umbilical boss. The number of chambers in the final whorl

of the initial coil varies from six to ten. Those with more chambers possess larger-sized

initial coils than those with fewer chambers, with the smallest coils being composed of

just over one whorl: these differences may reflect dimorphism between the megalospheric

and microspheric generations. There appears to be some gradation towards A. explicatus

Espitalié & Sigal, as occasional tests occur with a longer uncoiled portion and an initial

coil of less than one whorl, and ornamented with poorly developed dorsal nodes and

raised sutural ribs. These forms (see Fig. 46F—H, J) have for the present been referred to

A. explicatus, the distinction being made on the size of the initial coil and the strength of the

dorsal nodes, but it is clear there is an extremely close relationship between the two species.

Occurrence

Late Valanginian to ?Barremian (Cenozones E and F), Majunga Basin, Madagascar

(Espitalié & Sigal 1963); Oxfordian—Kimmeridgian(?) to Barremian of the Magallanes

Basin, southern Chile (Natland et a/. 1974); Argentina: Valanginian—Hauterivian Pampa

Rincon Formation of Tierra del Fuego (Malumian & Masiuk 1975); Barremian Rio Mayer

Formation, Santa Cruz Province (Malumian & Nafiez 1983); also Hauterivian lower Rio

Mayer Formation (Bertels 1990); Late Valanginian and Early Hauterivian of Meseta

Senguerr borehole, Chubut (Masiuk & Vifia 19865); Early Hauterivian of the Agrio

Formation, Neuquén Basin (Musacchio 1979, 1981); and early Late Valanginian of the

Mngazana Basin, Transkei (McLachlan et al. 1976a), early Late Valanginian to Late

Hauterivian (Biozones D to ?II) in Pletmos Basin borehole PB—A1, and in the earliest Late

Valanginian (Biozone D) Brenton Formation of the southern Cape, South Africa

(McLachlan et al. 19766, and supplementary data). The species is widely distributed in

continental-shelf and uppermost slope deposits from the earliest Late Valanginian to the

Early Aptian in the offshore Pletmos, Gamtoos and Algoa basins off the south Cape coast,

South Africa.

Stratigraphic range in the Sundays River Formation

Late Valanginian to Late Hauterivian (basal Biozone Bb to Biozone 1), but generally

rare in the Early Hauterivian. The species is typical of inner to outer shelf environments,

and is not seen in marginal marine or hyposaline facies.

Astacolus schloenbachi (Reuss, 1863)

Figs 46I-M

Cristellaria schlonbachi Reuss, 1863, 65, pl. 6 (figs 14-15).

Cristellaria schloenbachi Reuss. Chapman, 1894c: 650, pl. 9 (fig. 9a—b).

Cristellaria D102 Hecht, 1938: pl. 19b (figs 20-21).

Lenticulina (Astacolus) schlénbachi (Reuss). Bartenstein & Brand, 1951: 286, pl. 5 (figs 124a—b,

125a—b).

142 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 46.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 143

Astacolus schloenbachi (Reuss). Sztejn, 1957: 47, 223, pl. 5 (fig. 40). McLachlan etal. 1976b: 353,

fig. 11 (nos 26-27). Musacchio, 1979: 258, pl. 4 (fig. 22); 1981: pl. 1 (fig. 8).

Lenticulina (Marginulina) aff. schlonbachi (Reuss). Damotte & Magniez-Jannin, 1973: 29,

text-fig. 15.

Lenticulina/Marginulina/schlonbachi (Reuss). Magniez-Jannin, 1975: 133, text-fig. 62.

Astacolus sp. McLachlan et al., 1976a: 330, fig. 16 (no. 7).

Lenticulina (Astacolus) schloenbachi (Reuss). Bartenstein & Kovatcheva, 1982: 640, pl. 2

(igs 35)

Remarks

A considerable degree of variation 1s evident in authors’ interpretations of this species,

as listed above. In the Sundays River Formation material, it has proven difficult to draw a

distinction between the Astacolus calliopsis (Reuss) group and this species. The original

illustrations provided by Reuss (1863) of the two species suggest that A. schloenbachi

displays slightly more inflated chambers than does A. calliopsis, the inflation being

evident along both the ventral, and more particularly the dorsal outline of the test. The

Sundays River Formation tests of A. schloenbachi have thus been separated from

A. calliopsis essentially on the presence of a lobate dorsal margin of the test, reflecting the

stronger inflation of the chambers and the correspondingly more depressed sutures of the

uncoiled part of the test. Being thus separated, tests of A. schloenbachi show a fair degree

of variation in the nature of the initial coil. Some specimens show only slight arching of

the early chambers (Fig. 46M), whereas others possess a coil of about three-quarters of a

whorl (Fig. 461, K, L).

Occurrence

Originally described by Reuss (1863) from the upper Hils Clays and the ‘Speeton

Clay’ of the northern German Early Cretaceous. Later occurrences include: Gault Clay

(Albian) of Folkestone (Chapman 1894c); Early Hauterivian (Hecht 1938), Middle and

Late Valanginian (Bartenstein & Brand 1951) and throughout the Early Cretaceous

(Bartenstein & Kovatcheva 1982) of north-western Germany; the Albian (Magniez-

Jannin 1975) and the Early Aptian (Damotte & Magniez-Jannin 1973) of the Aube region,

Fig. 46 (see facing page). A-H. Astacolus gibber Espitalié & Sigal. A. SAM—PQ-—MF 1316, side view,

AL 1/69, 4 110 feet (A), F551. X 63. B. SAM—PQ—MF 1317, side view, AL 1/69, 1 600 feet (VI),

F437. X 59. C. SAM-—PQ-MF1318, side view, AL 1/69, 1 600 feet (VI), F438. x 76.

D. SAM—PQ-MF 1319, side view, AL 1/69, 1 570 feet (VI), F428. x 59. E. SAM—PQ—MF 1320, side

view, AL 1/69, 1 030 feet (III), F311. < 43. F. SAM—PQ—MF1321, side view, Coega Brick Pits

outcrop sample 11436 (Bb), F158. x 66. G. SAM—PQ—MF 1322, side view, AL 1/69, 520 feet (1),

F128. X 76. H. SAM—PQ-MF1323, apertural view, AL 1/69, 580 feet (II), F170. x 71.

I-M. Astacolus schloenbachi (Reuss). 1. SAM—PQ—MF1324, side view, CO 1/67, 660 feet (VII),

F146. X 57. J. SAM—PQ—MF1325, side view, AL 1/69, 1 240 feet (IV), F358. x 147.

K. SAM-—PQ-MF 1326, side view, AL 1/69, 4 050 feet (A), F548. x 117. L. SAM—PQ—MF1327,

side view, AL 1/69, 910 feet (III), F272. x 100. M. SAM—PQ-MF1328, side view, AL 1/69,

lh S7Onteet(VINER4332x% 138:

144 ANNALS OF THE SOUTH AFRICAN MUSEUM

France; the Infra-valanginian (?Berriasian) and the Late Valanginian of central Poland

(Sztejn 1957); Late Barremian to Clansayesian (Late Aptian) of Bulgaria (Bartenstein &

Kovatcheva 1982); Late Berriasian to mid-Hauterivian in the Speeton Clay of the

Yorkshire coast, England (Fletcher 1973); the Late Hauterivian of the Agrio Formation,

Neuquén, Argentina (Musacchio 1979, 1981); and the Late Valanginian (Biozone B) of

the Mngazana Basin, Transkei, South Africa (McLachlan et al. 1976a) and the Late

Hauterivian (Biozone III) of borehole PB—A1, Pletmos Basin, off the south coast of South

Africa (McLachlan et al. 19765).

Stratigraphic range in the Sundays River Formation

Always rare and infrequent, Astacolus schloenbachi ranges from Late Valanginian

Biozone Bb to Late Hauterivian Biozone I. It is widely distributed, from marginal marine

to outermost shelf locations, but is absent in hyposaline environments.

Astacolus calliopsis (Reuss, 1863) s.1.

Fig. 47A—J

Marginulina linearis Reuss, 1863: 60, pl. 5 (fig. 15a—b).

Marginulina calliopsis Reuss, 1863: 60, pl. 5 (fig. 16a—b).

Cristellaria parallela Reuss, 1863: 67, pl. 7 (figs 1, 2a—b).

Lenticulina (Astacolus) calliopsis (Reuss). Bartenstein & Brand, 1951: 286, pl. 5 (figs 120a—c,

121a—b, 122a—b). Bartenstein et al., 1966: 149, pl. 2 (figs 151-154, 169-173). Beer, 1970, pl. 2

(figs 4a—c, 5a—b, 6a—b).

Marginulina cf. inconstantia (Cushman). Rigassi, 1970, pl. 83 (pars).

Astacolus cf. calliopsis (Reuss). Dailey, 1973: 60, pl. 8 (fig. 5). Musacchio, 1979: 258, pl. 4

(figs 9-10).

Astacolus calliopsis (Reuss). McLachlan et al., 1976a: 328, fig. 16 (no. 4); 19766: 352, fig. 11

(nos 8-9). Bertels, 1990: 253, pl. 1 (fig. 11).

Remarks

Authors’ use of the name has been followed here, in preference to the seldom used

name Marginulina linearis. Variation is evident in the degree of coiling in the early part of

the test, in the degree of depression along the sutures, and in the compression of the test. It

is thus not possible to use the name precisely, as previously used in the European

literature.

Sundays River Formation tests referred to Astacolus calliopsis s.1. show as great a

range of variation as that seen in the literature. They appear to be closest to the north-west

German forms illustrated by Bartenstein & Brand (1951, pl. 5 (figs 121a—b, 122a—b)),

which themselves are close to the Cristellaria parallela end-member of this species

complex. It is difficult to separate the Sundays River forms from A. schloenbachi (Reuss)

in one respect (see previously), and from A. explicatus Espitali¢ & Sigal in another.

Astacolus calliopsis s.\. tests can be distinguished from A. explicatus s.l. tests in the

Sundays River Formation by their smaller initial coil, which is rarely more complete than

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 145

three-quarters of a whorl. Most tests exhibit only a quarter to half a whorl. Chambers in the

later part of the test are rather more inflated, and the tests are generally not as compressed,

nor as wide, especially in the uncoiled portion, as those considered typical of A. explicatus

s.l. The sutures are usually flush to depressed, whereas those of A. explicatus s.1. tend to be

flush to weakly raised. However, in both the 4. calliopsis and A. explicatus species-

groups, such a range of variation occurs that it has proved very difficult to make an

effective division between the two.

Occurrence

Reuss (1863) described Marginulina linearis and M. calliopsis from the Minimus

Clays, and Cristellaria parallela from the upper Hils Clays of the northern German Early

Cretaceous. Bartenstein & Brand (1951) regarded the stratigraphic range of A. calliopsis

in northern Germany as mid-Valanginian to Early Hauterivian. Other records include:

Late Aptian to middle Early Albian Maridale Formation of Trinidad (Bartenstein ef al.

1966); Late Aptian to Early Albian Aiken Member of the Budden Canyon Formation of

California (Dailey 1973); Late Hauterivian of the Agrio Formation, Neuquén, Argentina

(Musacchio 1979); Hauterivian and ?Barremian lower Rio Mayer Formation, southern

Argentina (Bertels 1990); and Late Valanginian (Biozone B) of Mngazana Basin,

Transkei (McLachlan ef a/. 1976a) and the Late Valanginian to Late Hauterivian

(Biozones B to III) of Pletmos Basin borehole PB—A1 (McLachlan et a/. 19765).

Stratigraphic range in the Sundays River Formation

Astacolus calliopsis s.\. ranges from Late Valanginian Biozone B to Late Hauterivian

Biozone I, with rare examples too in the earlier Late Valanginian Biozone C. The plexus is

very variable in its abundance through its range, and may locally dominate assemblages,

as seen in its distribution through cored borehole CO1/67. It occurs in most marine

environments on the shelf, being absent only in marginal marine, hyposaline conditions.

Astacolus explicatus Espitalié & Sigal, 1963 s./.

Figs 48A-K

Astacolus explicatus Espitali¢é & Sigal, 1963: 41, pl. 17 (figs 6a—d, 7a—b). Malumian & Masiuk,

19753584, pl. 2 Cig. 9).

Marginulina cf. inconstantia (Cushman). Rigassi, 1970: pl. 83 (pars).

see Astacolus explicatus (non Espitalié & Sigal): McLachlan et al., 1976b: 353, fig. 11

(nos 20-21).

see Astacolus gibber cf. barremianus (non Espitalié & Sigal): Malumian & Nafiez, 1983: 383, pl. 2

(fig. 9).

Remarks

A large group of Astacolus specimens from the Sundays River Formation, generally

lacking a full initial coil of chambers, and with poorly developed nodes along the dorsal

margin of the test, appears best referable to A. explicatus s.1. This group is, by and large,

ANNALS OF THE SOUTH AFRICAN MUSEUM

146

Figure 47

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 147

distinct from A. gibber Espitali¢e & Sigal, although gradational tests do occur, as discussed

for that species.

In their manner of uncoiling, tests of this group compare well with the illustrated tests

of A. explicatus from the Majunga Basin (Espitalié & Sigal 1963). However, occasional

specimens (see Fig. 48F—H) suggest a similarity with A. barremianus (Michael),

described from the north-west German Barremian (Michael 1967) and later from the early

Middle Barremian of Heligoland in the North Sea (Bartenstein & Kaever 1973). Both

Bartenstein & Kaever (1973) and Malumian & Naniez (1983) have considered

A. barremianus and A. gibber to be morphologically similar, and A. explicatus 1s not far

from either in its morphology. In the meantime, the name 4. explicatus s.l. has been

utilized for this group in the Sundays River Formation, but it is clear that more detailed

work is required to resolve aspects of the relationships of these three species.

The specimen illustrated by McLachlan et al. (19765, fig. 11 (nos 20—21)) as

A. explicatus is rather different from either Sundays River Formation or Majunga Basin

tests in that it lacks the nodose dorsal margin, possesses strongly raised sutures, and 1s

rather more compressed than 1s typical, with a subrounded and acute margin to the test

(see also Remarks to Planularia sp. B).

Occurrence

Espitali¢é & Sigal (1963) described Astacolus explicatus from Cenozone F (Late

Hauterivian to ?Barremian) of the Majunga Basin, Madagascar. Other records include the

Valanginian—Hauterivian Pampa Rincon Formation of Tierra del Fuego, Argentina

(Malumian & Masiuk 1975). Specimens of A. explicatus s.l. occur extensively in the

earlier Cretaceous of the offshore Pletmos, Gamtoos and Algoa basins of South Africa

but, because of the difficulties in defining the limits of the plexus, it is of little stratigraphic

value. The plexus is best represented from the Early Valanginian to the Late Hauterivian,

with rarer occurrences in the Early Barremian, but in older rocks, additional

complications arise between it and similar Late Jurassic forms.

Stratigraphic range in the Sundays River Formation

Late Valanginian Biozone C to Late Hauterivian Biozone I, locally abundant. A very

Fig. 47 (see facing page). A—J. Astacolus calliopsis (Reuss) s.l. A. SAM—PQ—MF1329, side view,

AL 1/69, 1 480 feet (IV), F388. x 84. B. SAM—PQ—MF 1330, side view, AL 1/69, 1 480 feet (IV),

F381. xX 78. C. SAM—PQ-MF1331, side view, MV 1/79, 160 m (X), F596. x 160.

D. SAM—PQ-MF 1332, side view, AL 1/69, 700 feet (II), F210. x 60. E. SAM—PQ—MF1333, side

view, AL 1/69, 2 000 feet (VII), F479. x 112. F. SAM—PQ—MF 1334, side view, AL 1/69, 2 000 feet

(VII), F482. x 116. G. SAM—PQ-—MF1335, side view, AL 1/69, 1 570 feet (VI), F429. x 97.

H. SAM—PQ—MF 1336, side view, AL 1/69, 1 240 feet (IV), F363. x 59. I. SAM—PQ-—MF 1337, side

view, MV 1/79, 140 m (X), F583. X 73. J. SAM—PQ-—MF 1338, side view, CO 1/67, 642 feet (VID),

F143. X 42. K. Astacolus sp. A, SAM—PQ—MF 1339, side view, MV 1/79, 90 m (X), F577. X 93.

L. Lenticulina sp. A, SAM—PQ—MF 1405, side view, MV 1/79, 350-360 m (Ba), F657. X 150.

M. Astacolus sp. D, SAM—PQ-—MF 1340, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb),

F229. X 88.N. Astacolus sp., SAM—PQ—MF 1341, side view, AL 1/69, 1 360 feet (IV), F368. X 89.

148 ANNALS OF THE SOUTH AFRICAN MUSEUM

widespread species, ranging from marginal marine to outermost shelf, but absent in

hyposaline conditions.

Astacolus sp. A

Fig. 47K

Remarks

Only three poorly preserved specimens of this species have been recovered. The flat to

inflated ventral margin, bordered by two peripheral ribs, perhaps leads one to refer this

species to Saracenaria rather than Astacolus, but the flat ventral face is too narrow for it to

be an indisputable Pravoslavlevia or Saracenaria, and allocation to the genus Astacolus is

preferred.

The specimens are reminiscent of Lenticulina/Saracenaria/vestita (Berthelin) subsp.

vestita, described by Magniez-Jannin (1975, pl. 13 (figs 6a—b, 7—10)) and by Jannin

(1968), although there are clear differences. Besides the peripheral ventral rib, most

chambers of the uncoiled part of the test exhibit 2—3 ribs that are always confined to one

chamber, and die out just short of the depressed or incised sutures. In contrast,

Saracenaria vestita 1s characterized by only one such rib per chamber. Both species are

distinguished by rather bladed dorsal keels and by depressed sutures. All specimens of

Astacolus sp. A are from the Early Hauterivian (Biozones IX and X) of the Sundays River

Formation.

Astacolus sp. D

Fig. 47M

Remarks

One well-preserved example of an elongate Astacolus or Marginulina, with an ovate to

sub-circular cross-section to the uncoiled part of the test, from sample 11450,

Zoetgeneugd Cliff (earliest Biozone Bb, Late Valanginian). The surface ornamentation of

few, often rather irregular ribs is intense, the ribs themselves being markedly bladed.

Chambers are weakly inflated, particularly in the final part of the test; sutures, which are

not clear without moistening the test, are flush to weakly depressed and slightly arched.

The surface ornament of vertically aligned, curved ribs is not as orderly as that of

Lenticulina/Marginulina acuticosta (Reuss) subsp. restricta Magniez-Jannin (1975),

described from the Albian of France. There is perhaps also some similarity with the

Lenticulina (Marginulinopsis) sp. illustrated by Bartenstein et al. (1957: 32, pl. 6

(fig. 122a—b)) from the middle Middle to Late Barremian of the Cuche Formation of

Trinidad, but the surface ribs reach close to the aperture and are distributed equidistantly

over the surface of the final chamber, neither of which feature is evident on the Sundays

River specimen.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 149

Astacolus spp.

Fig. 47N

Remarks

Small numbers of smooth and unornamented, rather compressed Astacolus specimens

occur through most of the more normal marine Sundays River Formation. Some, such as

that illustrated, may be referable to A. grata (Reuss), and thus be comparable with the

specimen illustrated by McLachlan et al. (19765, fig. 11 (no. 19)). Others are certainly

juveniles that display insufficient diagnostic features for them to be assigned to species,

and still others are too poorly preserved to allow a full identification.

Genus Citharina d’Orbigny, 1839

Citharina sp. A

Fig. 48L

Remarks

A single specimen from Zoetgeneugd Cliff outcrop (Biozone C, Late Valanginian) 1s

distinguished by its slightly inflated chambers and weakly depressed sutures. The surface

ornamentation of distinct and sharply defined, vertically aligned ribs tend to be entirely

absent over the sutures. The dorsal margin is carinate and bladed and, for portions of its

length, it is irregularly tricarinate. The ventral margin is weakly lobate and rounded in

cross-section. The restriction of the surface ribs to the inter-sutural areas occurs, although

to a lesser degree, in Vaginulina sp. 3309 of Espitalié & Sigal (1963: 48, pl. 20 (fig. 16)).

However, the arrangement of the ribs, which spread out towards the dorsal and ventral

margins of the test in a fan, and their density are substantially different from that seen in

the Zoetgeneugd test.

Citharina pseudostriatula Bartenstein & Brand, 1951

Figs 48M-N, 49A—B

Citharina pseudostriatula Bartenstein & Brand, 1951: 298, pl. 7 (fig. 182a—b), pl. 12A

(fig. 339a—b). Sztejn, 1957: 68, 239, pl. 7 (fig. 67). Bartenstein & Kaever, 1973: 227, pl. 3

(figs 42-43).

see Vaginulina aff. pseudostriatula (Bartenstein & Brand). Espitalié & Sigal, 1963: 51, pl. 22

(fig. 15).

Citharina striatula (non Roemer): Beer, 1970: 16, pl. 3 (fig. 2a—b).

see Citharina pseudostriatula Bartenstein & Brand. Hart et a/., 1981: 159, pl. 7.6 (figs 12-13).

Remarks

The holotype of Citharina pseudostriatula (Bartenstein & Brand, 1951, pl. 12A

(fig. 339a—b)) is characterized by its numerous fine ribs ornamenting the surface of the

test. The marginally sited ribs are aligned parallel to the test periphery; additional ribs

appear, or bifurcate from earlier ribs as the number of chambers increases. This species

150 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 48.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Li

appears to be closely related to C. harpa (Roemer), which is distinguished by its ribs being

more solidly built, and by the absence of bifurcating or additional ribs. For this reason, the

illustrations of C. pseudostriatula given by Hart et al. (1981, pl. 7.6 (figs 12, 13)) appear

a little too close to C. harpa in their arrangement of ribs. Bartenstein & Brand (1951)

noted that a number of references to C. harpa in the Late Dogger and Malm of Europe

should be re-allocated to C. pseudostriatula. The South African tests compare well with

the European illustrations of this species.

Occurrence

Citharina pseudostriatula 1s widely known in the Jurassic and Early Cretaceous of

Europe: Late Dogger to latest Valanginian of north-west Germany (Bartenstein & Brand

1937, 1951); Hauterivian of Lincolnshire, England (Bartenstein 1956); Berriasian to later

Hauterivian of the Speeton Clay, Yorkshire coast, England (Fletcher 1973); Late

Hauterivian of Heligoland (Bartenstein & Kaever 1973); and Infravalanginian

(?Berriasian) to Hauterivian of central Poland (Sztejn 1957). A very similar form occurs

high in Cenozone F (?Barremian) of the Majunga Basin, Madagascar (Espitalié & Sigal

1963).

Stratigraphic range in the Sundays River Formation

This species occurs rarely, from the lowest Biozone Bb of the Late Valanginian to

mid-Biozone VI of the Late Hauterivian. There are no Early Hauterivian records, and it

seems likely that it is confined to specific intervals of short duration in the Sundays River

sequence. Citharina pseudostriatula occurs in marginal marine and middle- to outer-shelf

environments, but is absent in both hyposaline and reduced-oxygen environments.

Fig. 48 (see facing page). A-K. Astacolus explicatus Espitalié & Sigal s./. A. SAM—PQ—MF 1342, side

view, AL 1/69, 1 750 feet (VII), F456. x 83. B. SAM—PQ-MF 1343, side view, AL 1/69, 1 930 feet

(VIL), F469. x 75.C. SAM—PQ—MF 1344, side view, shallow borehole SB-8, core ?, top (III), F665.

x 74. D. SAM—PQ—MF 1345, side view, shallow borehole SB-35, core ?, top (III), F702. x 65.

E. SAM—PQ-MF 1346, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb), F236. X 68.

F. SAM—PQ-MF 1347, side view, shallow borehole SB—32, core 2, ?199 feet, ?bottom (IV), F699.

xX 48. G. SAM—PQ-MF 1348, side view, AL 1/69, 670 feet (II), F204. x 61. H. SAM—PQ-—MF 1349,

side view, AL 1/69, 670 feet (II), F203. x 41. I. SAM—PQ—MF1350, side view, shallow borehole

SB-35, core ?, top (III), F700. x 58. J. SAM—PQ—MF 1351, side view, AL 1/69, 700 feet (II), F211.

x 51. K. SAM—PQ-—MF 1352, side view, CO 1/67, 642 feet (VI), F142. x 46. L. Citharina sp. A.

SAM-—PQ-MF1353, side view, Zoetgeneugd Cliff outcrop sample 11452 (C), F254. x 65.

M-N. Citharina pseudostriatula Bartenstein & Brand. M. SAM—PQ-MF1354, side view,

Zoetgeneugd Cliff outcrop sample 11450 (Bb), F231. x 57. N. SAM—PQ—MF1355, side view,

CO Wo; 520 feet (V1); F134) x 58.

152

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 49,

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 153

Citharina austroafricana sp. nov.

Figs 49C—J

Citharina cf. C. cristellarioides (Reuss). Rigassi, 1970: pl. 83 (pars).

Citharina sparsicostata (non Reuss): McLachlan et al., 1976a: 330, fig. 16 (no. 8); 1976b: 356,

fig. 12 (nos 22-23).

Citharina cristellarioides (non Reuss): McLachlan et al., 19766: 355, fig. 12 (nos 20-21).

Diagnosis

A strongly compressed species of Citharina possessing an irregularly tricarinate dorsal

margin; ornamented over each chamber with a narrow band of closely spaced ribs,

generally vertically aligned, and with occasional more elongate ribs developed over

several chambers close to the dorsal margin and the proloculus.

Etymology

Named for its widespread distribution in the Pletmos, Gamtoos, Algoa and Mngazana

basins around South Africa.

Material

Holotype (Fig. 49F). MF1361, SOEKOR negative F215.

Paratypes (Fig. 49C—-E, G—J). MF1358 to MF1360, MF1362 to MF1365, seven

specimens, SOEKOR negatives F132, F80, F213, F140, F263, F133, and F234. Four

additional paratypes are illustrated in the work by McLachlan et al. (1976b, fig. 12

(nos 20—23)) on the Brenton Formation and borehole PB—A1.

Stratum typicum

Biozone II, Late Hauterivian, Sundays River Formation.

Fig. 49 (see facing page). A—B. Citharina pseudostriatula Bartenstein & Brand. A. SAM—PQ-—MF1356,

side view, CO 1/67, 520 feet (VI), F135. x 58. B. SAM—PQ—MF 1357, side view, CO 1/67, 642 feet

(VII), F136. x 39. C—J. Citharina austroafricana sp. nov. C. Paratype, SAM—PQ—MF 1358, side

view, CO 1/67, 520 feet (VI), F132. x 30. D. Paratype, SAM—PQ—MF 1359, side view, Uitenhage to

Graaff-Reinet Road outcrop sample 11464 (Bb), F80. X 61. E. Paratype, SAM—PQ—MF 1360, side

view, AL 1/69, 730 feet (II), F213. x 32. F. Holotype, SAM—PQ-—MF 1361, side view, AL 1/69,

760 feet (II), F215. xX 28. G. Paratype, SAM—PQ—MF1362, side view, CO 1/67, 642 feet (VII),

F140. x 40. H. Paratype, SAM—PQ—MF1363, side view, AL 1/69, 820 feet (III), F263. x 37.

I. Paratype, SAM—PQ—MF 1364, side view, CO 1/67, 520 feet (VI), F133. xX 32. J. Paratype,

SAM-—PQ—MF1365, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb), F234. x 49.

K—M. Dentalina communis dOrbigny s./. K. SAM—PQ—MF 1366, side view, shallow borehole

SB-9A, core 1, 282 feet 6 inches (II), F694. x 55. L. SAM—PQ-MF1367, side view, AL 1/69,

370 feet (1), F47. X 68. M. SAM—PQ-—MF 1368, side view, AL 1/69, 370 feet (I), F49. x 63.

N. Dentalina sp. B, SAM—PQ—MF 1372, side view, MV 1/79, 240-250 m (A), F623. xX 150.

O-P. Dentalina spp. O. SAM—PQ—MF 1373, side view, shallow borehole SB—32, core 1, 148 feet

([V) F695. x 58. P. SAM—PQ-—MF 1374, side view, AL 1/69, 520 feet (I), F162. x80.

154 ANNALS OF THE SOUTH AFRICAN MUSEUM

Locus typicus

Borehole AL 1/69, cuttings sample at 760 feet.

Description

Test strongly compressed, leaf-like, and irregularly triangular in outline. Dorsal

margin initially weakly curved, later straight; ventral margin initially concave, becoming

convex, and, in the final part of the test, weakly to strongly lobate. In cross-section, test

elongate-rectangular, long sides parallel, with dorsal margin bounded by one rather thick

rib that is continuous for most of the height of the test; the rib is low and rounded in

cross-section. Two additional ribs are present, one on either side of the thickened rib, and

are sub-parallel to it, thus forming an irregularly tricarinate dorsal margin. Ventral margin

sub-rectangular to rounded in outline, ornamented with fine rounded ribs at its margins,

but smooth and unornamented along a central band for most of its length. Chambers

uniserially arranged throughout, arcuate, increasing greatly in width as added, but little in

height. Chambers flush, not inflated. Sutures variably evident beneath the surface

ornamentation, generally flush, but often becoming weakly depressed between the last

few chambers, broad and evenly curved in form. Aperture terminal, close to the dorsal

margin of the test; in form a narrow elongate—ovate opening that sometimes shows some

indication of a margin of short radiate slits. Surface ornamentation of numerous short ribs,

arranged in a broad arc from near the dorsal margin almost to the ventral margin, each rib

roughly vertically oriented. Ribs low and rounded in form, but they are often reduced in

intensity as a result of post-depositional corrosion of tests. The arc of ribs over each

chamber is suspended from the overlying suture, so that the lower third or half of each

chamber is usually smooth and unornamented. The chambers in the final part of the test

may develop up to 18 ribs each test side. Over the proloculus, and sporadically up the

dorsal margin, more elongate ribs occur, which may extend over two chambers, rarely

more. The great majority of the surface ribs are aligned parallel to the straight portion of

the dorsal margin, wherever they are located. Apical point of test always bluntly rounded.

Remarks

Variation in the distribution of the surface ornamentation occurs in the tests from the

Sundays River Formation. Occasional Hauterivian examples develop the short vertical

ribs over almost the entire chamber height. Late Valanginian tests, and also those from

Brenton, generally display a fainter and less organized ribbing pattern and, in such tests,

the predominant ribs are the irregular, longer ones close to the proloculus and the dorsal

margin (see Fig. 49J in particular).

Examination of true specimens of both C. sparsicostata (Reuss) and C. cristellarioides

(Reuss) from the Hauterivian and Barremian portion of the Speeton Clay, Yorkshire,

England, has indicated that the South African tests previously allocated to these two

boreal species must be referred elsewhere. As figured by Reuss (1863, pl. 3 (fig. 17a—b)),

C. cristellarioides is characterized by short ribs developed over the chambers and not over

the sutures. In the early part of the Speeton tests, many of the ribs extend over two or more

chambers and, in general, a far greater proportion of the test surface of C. cristellarioides

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION [55

is ornamented with ribs than is the case with C. austroafricana. Furthermore, because the

sutures of the European species lack ribs, they are much more clearly marked than in

C. austroafricana, and are initially flush, becoming weakly depressed for the last third of

the test; the final chambers of the test are always distinctly, but lightly, inflated in

C. cristellarioides.

South African specimens of Citharina previously allocated to C. sparsicostata are

generally broken fragments of larger tests, comprising the initial part and including the

proloculus and five or six subsequent chambers. These damaged tests therefore tend to

show the longer ribs of the proloculus and dorsal margins, and possess few of the

distinctive arcs of short ribs so typical of adult tests. In addition, true examples of

C. sparsicostata from Speeton are intensely ornamented: C. austroafricana 1s

distinguished by a much lighter, more delicate ornamentation.

Citharina delicata Magniez-Jannin (1975: 209, pl. 14 (fig. 8)), from the Albian of the

Aube district, France, features a similar surface ornament to that seen on

C. austroafricana, but differences are evident. The ribs of C. delicata are located over the

chambers and not over the sutures, but the sutures are marked, in each case, by a fine rib

that extends the full length of each suture.

There are a number of references to C. sparsicostata and C. cristellarioides in

Argentina that are of interest. The C. cristellarioides tests illustrated by Simeon (1985,

pl. 1 (figs 1—3)) and Musacchio (1979, pl. 4 (fig. 19); 1981, pl. 1 (fig. 2)), although

differing in their density of ornamentation, are clearly much closer to the European

species than any Citharina specimens yet found in the Early Cretaceous of South Africa.

However, the shells of C. sparsicostata figured by Malumian & Nanez (1983, pl. |

(figs 15—16)) and by Kielbowicz et al. (1983, pl. 1 (figs 10—11)) appear to be referable to

C. austroafricana, although the preservation of these is rather variable. In contrast, the

examples of C. sparsicostata and C. cristellarioides, illustrated by Espitali¢ & Sigal

(1963) from the Majunga Basin, Madagascar, compare well with the two European

species, but C. austroafricana, as here defined, is clearly different from either (see

Espitali¢é & Sigal 1963, pl. 21 (figs 9-11 and fig. 12, respectively)).

The specimen of Citharina cf. C. cristellarioides illustrated by Beer (1970: 15, pl. 3

(fig. 1)) from borehole CO 1/67 is probably referable to C. austroafricana, but the

ornamentation shown is quite unlike any Early Cretaceous South African specimens of

Citharina encountered by the present author, and is suspected to be a misrepresentation.

The test identified as Citharina cf. C. cristellarioides by Rigassi (1970, pl. 83) is typical,

but another illustrated test, referred to Citharina cf. C. sparsicostata by Rigassi (1970), is

of a very different form, not encountered in the Algoa material available to the author.

Occurrence

Citharina austroafricana 1s widespread but never abundant. It occurs in the early Late

Valanginian (Biozone D) Brenton Formation, and ranges from Late Valanginian

Biozone D to Late Hauterivian Biozone II of Pletmos Basin borehole PB—A1 (McLachlan

et al. 19766); the Late Valanginian (Biozone B) of the Mngazana Basin, Transkei

(McLachlan et al. 1976a); and in the offshore Pletmos, Gamtoos and Algoa basins. Its full

156 ANNALS OF THE SOUTH AFRICAN MUSEUM

range appears to be early Valanginian to Early Barremian, although it is very rare in the

Barremian.

Stratigraphic range in the Sundays River Formation

Late Valanginian Biozone Bb to Late Hauterivian Biozone I. The species occurs from

marginal marine to outermost shelf environments, but appears to be commonest in

shallow marine, well-oxygenated localities affected by turbulence and with a silty or

sandy substrate. It is absent in both hyposaline and low-oxygen conditions.

Genus Dentalina Risso, 1826 s.1.

Loeblich & Tappan (1988) have promoted the subdivision of the genus Dentalina (as

understood in Loeblich & Tappan 1964) into a variety of more tightly constrained genera.

As a consequence, the genus Dentalina sensu stricto includes only species with a

longitudinally costate surface. None of the Sundays River Formation tests display this

characteristic, and thus ought to be referred elsewhere. However, since the majority are

damaged, with initial chambers often missing and apertural structures incomplete, precise

generic allocations of the relatively few specimens found are difficult, and often

impossible to achieve. For this reason, the genus Dentalina is considered herein in the

wide sense, although it seems likely that many of the specimens from the Sundays River

Formation ought to be referred to Laevidentalina (see Loeblich & Tappan 1988: 396,

pl. 439 (figs 22—24)).

Dentalina communis d Orbigny, 1826 s./.

Fig. 49K—-M

Nodosaria (Dentaline) communis @ Orbigny, 1826: 254.

Dentalina communis @Orbigny. Sztejn, 1957: 50, 225, pl. 5 (fig. 41a—b). Beer, 1970: 10, pl. 1

(fig. 6). McLachlan et al., 1976a: 330, fig. 16 (no. 9). Stapleton & Beer, 1977: 2, pl. 3 (fig. 10).

Remarks

Scattered examples referable to this species occur widely in the Sundays River

Formation. It 1s clear that this ‘species’ must be considered a plexus of similar forms, all

rather conservative in their morphology, and it is thus regarded here sensu lato. The

plexus ranges from the Lias through to the present day. None of the Sundays River tests

are complete, being usually damaged or broken in the juvenile portion of the test. None

display any indication of an initial biserial arrangement of chambers on the dorsal margin

of the test, as is typical of Enantiodentalina communis Marie (1956).

Stratigraphic range in the Sundays River Formation

Sporadic examples occur from the Late Valanginian Biozone Bb to Late Hauterivian

Biozone I.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 157

Dentalina linearis (Roemer, 1841)

Figs SOA—C

Nodosaria linearis Roemer, 1841: 95, pl. 15 (fig. 5).

Dentalina linearis (Roemer). McLachlan et al., 1976a: 330, fig. 16 (no. 10). Musacchio, 1979:

258, pl. 4 (fig. 6). Malumian & Nafiez, 1983: 378, pl. | (fig. 17).

Remarks

This species is infrequent and rather scattered through the Sundays River Formation.

Tests are often partially crushed (Fig. 50A), which tends to exaggerate the degree of

inflation of the chambers. All well-preserved specimens possess a radiate aperture

(Fig. 50C), thus distinguishing them from the otherwise morphologically similar

Lingulonodosaria nodosaria (Reuss).

Stratigraphic range in the Sundays River Formation

Ranges through most of the sequence, from Late Valanginian Biozone Bb to Late

Hauterivian Biozone I.

Dentalina sp. B

Fig. 49N

Remarks

A single specimen from Biozone A (Late Valanginian) of borehole MV 1/79 is

characterized by 10 fine vertical ribs on the proloculus, which rapidly fade on the second

chamber. The specimen is similar to one example of Lenticulina/Vaginulina sp. illustrated

by Damotte & Magniez-Jannin (1973, pl. 3 (fig. 45)) from the Aptian of the Aube district,

France.

Dentalina spp.

Figs 49O-P

Remarks

Scattered specimens of Dentalina occur throughout most of the studied boreholes.

Specimens are usually too few, or too poorly preserved for confident specific

identification. All of this group have smooth, unornamented exteriors. Two typical forms

are illustrated.

Genus Frondicularia Defrance, 1826

Frondicularia nieuwjaarskopensis sp. nov.

Figs 5|0D-G

Diagnosis

A leaf-like, lightly ornamented species of Frondicularia, characterized by maximum

test width near mid-height, a prominent apical spine, a single short rib ornamenting the

158

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 50.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 159

proloculus on each side of the test, very weak sutural ribs, and occasional short ribs

developed on the chambers, especially close to the test periphery.

Etymology

From the presence of particularly well-preserved specimens from shallow borehole

SB-—15, drilled on the area of the old farm Nieuwjaarskop, just east of the Sundays River

Valley.

Material

Holotype (Fig. 50D). MF1375, SOEKOR negative F131.

Paratypes (Fig. 5|0E-G). MF1376 to MF1378, three specimens, SOEKOR negatives

F631, F587, and F688.

Stratum typicum

Biozone VI, early Late Hauterivian, Sundays River Formation.

Locus typicus

Borehole CO 1/67, core sample at 520 feet.

Description

Test strongly compressed, leaf-like, with flat sides, and a rather foliar outline. Test

periphery irregularly lobate; with margin in cross-section being sub-angular to

sub-rounded and sub-rectangular, rather thin. Chambers uniserially arranged throughout,

with the last-formed ones faintly inflated. The proloculus is always prominent,

subglobular to pyriform. All subsequent chambers sagittate, strongly overlapping, with

the final chamber extending backwards for one-third to two-thirds of the test height.

Proloculus bordered around its lower, exposed side by a rather thick band of shell, with

rounded apex and flat sides. Sutures generally distinct, weakly depressed to flush, often

slightly limbate, and occasionally with low ribs developed along their length close to the

test margin. Aperture terminal, composed of a small circular, possibly radiate opening at

the mid-point of the last-formed chamber. Apical point of test ornamented by a short,

Fig. 50 (see facing page). A—C. Dentalina linearis (Roemer). A. SAM—PQ—MF 1369, side view,

AL 1/69, 520 feet (1), F121. X 126. B. SAM—PQ—MF1370, side view, AL 1/69, 1 000 feet (III),

F285. X 91. C. SAM—PQ-—MF 1371, apertural view, MV 1/79, 200-210 m (X), F612. Xx 250.

D-G. Frondicularia nieuwjaarskopensis sp. nov. D. Holotype, SAM—PQ—MF 1375, side view,

CO 1/67, 520 feet (VI), F131. x 33. E. Paratype, SAM—PQ—MF1376, side view, MV 1/79, 250-260,

(A), Fo3 1) x57. F) Paratype, SAM—PQ-MF1377; side view, MV 1/79, 150m (X),-F587. X 63.

G. Paratype, SAM—PQ-—MF 1378, side view, shallow borehole SB—15, core 4, 229 feet (II), F688.

x 83. H—-L. Lagena alexandria sp. nov. H. Holotype, SAM—PQ—MF 1379, side view, AL 1/69,

940 feet (III), F274. x 271.1. Paratype, SAM—PQ—MF 1380, side view, AL 1/69, 520 feet (I), F125.

xX 143. J. Paratype, SAM—PQ—MF 1381, side view, AL 1/69, 460 feet (i), F104. x 191. K. Paratype,

SAM-PQ-MF1382, side view, AL 1/69, 1 750 feet (VID, F455. x 154. L. Paratype,

SAM-—PQ-MF 1383, apertural view, AL 1/69, 1 060 feet (III), F321. x 164.

160 ANNALS OF THE SOUTH AFRICAN MUSEUM

fairly thick, terminally rounded spine: this is usually damaged or snapped off in studied

specimens. Surfaces of chambers occasionally weakly ornamented with short, vertically

aligned ribs, often most evident close to the test periphery. These ribs never extend for

more than one chamber, are low and rounded in section, and may merge with the sutural

ribs on occasion. Proloculus ornamented with one short, vertically aligned rib on each side

of the test, which often almost develops into a spine at its lower end, while gradually

fading away upwards; this prolocular ornament is the most prominent of all the surface

costation. One or two specimens also exhibit a short, vertically aligned rib immediately

above the highest point of the proloculus, that rapidly widens and subsides in intensity

upwards, away from the proloculus.

Remarks

Species of Frondicularia are everywhere very rare in the Valanginian and Hauterivian

rocks of South Africa. This may be partly due to the restriction of the genus to oxygenated

outermost-shelf and uppermost-slope locations, which have only rarely been intersected

in boreholes. Almost all records of F. niewwjaarskopensis in the Sundays River Formation

are confined to the deeper marine borehole intersections close to the present-day coast.

This Frondicularia species, like Citharina austroafricana sp. nov., 1s relatively poorly

ornamented compared to Frondicularia from the Valanginian—Hauterivian of the Majunga

Basin or north-west Europe. Frondicularia nieuwjaarskopensis shows some superficial

similarities to F. pectinatimornata of Espitalié & Sigal (1963: 56, pl. 26 (figs 11—15)),

especially in the short ribs developed on the chambers, but it lacks the spinose

terminations to the chambers and never displays more than one rib across the inflated

proloculus. No obvious similarities can be seen between F. nieuwjaarskopensis and the

many varied Early Cretaceous species of the genus known from north-west Europe.

Stratigraphic range in the Sundays River Formation

Late Valanginian Biozone Bb to Late Hauterivian Biozone I, but never common, and

usually absent in the Early Hauterivian. Typical of oxygenated middle- and outer-shelf

environments, and for this reason, rarely seen in the Valanginian and Hauterivian of the

offshore Pletmos, Gamtoos and Algoa basins.

Genus Lagena Walker & Jacob, 1798 s./.

Remarks

The genus Lagena is considered here in the wide sense. Although the species of

Lagena described here that possess an ornamentation of vertically aligned ribs still can be

referred to this genus (see Loeblich & Tappan 1988: 415), it seems that Lagena algoaensis

sp. nov. may be better placed within the genus Pygmaeoseistron. Specimens of Lagena

hauteriviana hauteriviana Bartenstein & Brand and L. h. cylindracea Bartenstein &

Brand, as understood here, may be referable to the genus Reussoolina but, although they

are smooth-walled, with an apical process, and often pyriform in outline, they completely

lack the grooves radiating from the aperture that are characteristic of that genus.

) FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 161

| Lagena alexandria sp. nov.

| Figs 50H-L

Lagena sulcata s.\. (non Walker & Jacob): Musacchio, 1979: 258, pl. 4 (fig. 23).

Diagnosis

A species of Lagena distinguished by its subglobular test ornamented with 8-14

_ vertically aligned ribs that are sharply delineated from the chamber wall, usually rounded

in cross-section, and which merge around the aperture.

Etymology

| Noun in apposition; named from its first appearance in the study in AL 1/69 borehole,

which was drilled in the magisterial district of Alexandria.

Material

Holotype (Fig. 50H). MF1379, SOEKOR negative F274.

Paratypes (Fig. 5OI-L). MF1380 to MF1383, four specimens, SOEKOR negatives

F125, F104, F455, and F321.

Stratum typicum

Biozone III, Late Hauterivian, Sundays River Formation.

Locus typicus

Borehole AL 1/69, cuttings sample at 940 feet.

Description

Test subglobular to elongate-ovate or pyriform, unilocular. Aperture terminal,

produced on a short development of the test of variable height; in form a subcircular

opening. Surface of test ornamented with 8—14 vertically aligned ribs, which are sharply

defined from the remaining, unornamented test surface. Ribs rounded in cross-section,

rarely acute, although the difference is probably due to post-depositional leaching of acute

ribs. The ribs merge at the apical point of the test, where a short, blunt, rounded apical

spine 1s developed. The ribs also merge around the short development of the test

just below the aperture, where, in most examples, a poorly developed thickening or rib

encircles the aperture and links all the vertical ribs. In occasional examples, the apertural

area lacks this encircling ornament. Test moderate in thickness.

Remarks

This species is considered to include the specimen illustrated by Musacchio (1979)

from the Late Hauterivian of Neuquén Province, Argentina, as Lagena sulcata (Walker &

Jacob) sensu lato. However, the Argentinian test seems to possess rather more bladed ribs

than the tests of L. alexandria typical of the Sundays River Formation. The difference is

regarded as being due to calcite dissolution of the peak of each rib, thus rounding a

162 ANNALS OF THE SOUTH AFRICAN MUSEUM

previously angled ornamentation. Slight differences exist in the paratypes illustrated but

the holotype (Fig. 50H) is representative of the commonest form in the Sundays River

Formation, and is closest to the Argentinian specimen. A similar form, with fewer ribs,

has been illustrated as Lagena sp. 3 by Jones & Wonders (1992: 563, pl. 2 (fig. 9)) from

the Berriasian—Valanginian Barrow Group off north-west Australia. A further, closely

related form is that illustrated as L. sulcata by Lofaldli & Thusu (1979, pl. 46 (fig. 19))

from the Valanginian—Hauterivian Nybrua Formation of Andgya, northern Norway.

There are a number of scattered references to Lagena forms resembling L. sulcata

(Walker & Jacob) in the Early Cretaceous at many widely spaced localities. However,

examination of these, and comparison with extant L. su/cata from the coastline of the

British Isles, indicate that most, if not all, can be readily separated from the living species.

Lagena sulcata, first described from the shore sands of Sandwich in Kent, England, by

Walker & Jacob (in Kanmacher 1798), is characterized by about 25 narrow-bladed costae

(Haynes 1973). The Late Hauterivian forms here described as L. alexandria differ from

the tests of Lagena cf. sulcata from the Late Valanginian Biozone B deposits of the

Mngazana Basin (McLachlan ef al. 1976a: 330, fig. 16 (nos 13—14)). The Mngazana

species 1s characterized by a prominent apertural neck and apical tube, and its ribs are

formed as a continuation of the test surface, rather than as in L. alexandria, where a

distinct groove beside each rib sharply delineates the ribs from the remainder of the test

surface (see Fig. 50H in particular). Morphologically similar forms to the Mngazana

species occur widely in the Early Valanginian of the offshore Gamtoos Basin, but

generally possess about 15 rather than the ten or so ribs of the Mngazana tests. It is clear

that the Mngazana material warrants a new name, although this aspect 1s held over for the

moment. The Mngazana species has not been found in the Sundays River Formation of the

present study area.

Stratigraphic range in the Sundays River Formation

Confined to Biozones VII to I, Late Hauterivian, and to outermost shelf environments

of the Sundays River Formation.

Lagena sp. A

Fig. SIA

Remarks

A single specimen from Biozone IV, Late Hauterivian. The test shows similarities to

the Lagena cf. L. striatifera Tappan described by McMillan (1980) from the Portlandian

Colchester Member of the Uitenhage Trough, onshore Algoa Basin. Lagena sp. A

possesses 20 vertically aligned ribs, rounded in cross-section and often almost

flat-topped, which fade and disappear towards both the aperture and the apical point. The

apical point is raised and the apertural area 1s slightly developed.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 163

?Lagena sp.

Fig. 51B

Remarks

A number of broken fragments, probably of a species of Lagena, occur in

sample 11450 from the lower part of the Zoetgeneugd Cliff outcrop (Biozone Bb, Late

Valanginian). The fragment illustrated shows the apertural area and the density of the

costate ornamentation, this density comparable in all other fragments found. No complete

specimens have been encountered, but the test appears to have been globular.

Lagena algoaensis sp. nov.

Fig. 51C-J

Lagena apiculata neocomiana (non Bartenstein & Brand): Beer, 1970: 17, pl. 3 (fig. 4).

Diagnosis

A species of Lagena characterized by an ovate test with a prominent, stout apertural

neck and a variably developed apical tube, and ornamented with a granular or tuberculate,

occasionally hispid, embellishment that shows considerable variation in intensity.

Etymology

From its occurrence in the Algoa Basin.

Material

Holotype (Fig. 51C). MF1386, SOEKOR negative F160.

Paratypes (Fig. 51D—J). MF1387 to MF1393, seven specimens, SOEKOR negatives

Proledl3 7, F238, F685, F237, F504, and F177:

Stratum typicum

Biozone Bb, Late Valanginian, Sundays River Formation.

Locus typicus

Sample 11436, Coega Brick Pits outcrop.

Description

Test ovate in outline, subglobular and unilocular in form. Aperture terminal, produced on

a stout, prominent neck, which varies from being parallel-sided to gently tapering towards

its termination. Aperture a circular opening. Surface of test roughened, ornamented with

irregularly distributed tuberculations and granulations that show considerable variation in

density over the test surface. A finer ornament of micro-rugosities is distributed between the

larger structures. The apertural neck is similarly ornamented, as in the holotype, but in other

examples the rugosities may be weakly aligned vertically up the neck. The apical point of the

test is marked by a short tubular projection which is often damaged or completely broken away.

164 ANNALS OF THE SOUTH AFRICAN MUSEUM

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 165

Remarks

Many Lagena algoaensis tests appear to be partly corroded (probably

post-depositional leaching is responsible), so that the distinctive ornamentation is almost

obliterated (Fig. 511). Other tests (Fig. 51J) seem to have suffered mechanical abrasion,

either through transportation of tests after death and before final deposition, or through the

processing methods used on these samples. Abraded tests have had many of the

tuberculations plucked out of the test surface, leaving small, irregularly shaped holes.

Lagena algoaensis can be clearly separated from Speeton Clay and north-west German

examples of Lagena cf. L. oxystoma Reuss by its much coarser ornamentation and robust

apertural neck, and by lacking the fine needle-like short spines that are parallel-sided and

rounded-tipped, as figured by Bartenstein & Brand (1951, pl. 10 (fig. 331), pl. 13

(figs 354—356)). Lagena algoaensis differs from L. hispida Reuss in possessing a more

elongate, pyriform test chamber, as well as lower, less well-developed spines (see Speeton

Clay examples illustrated by Hart et a/. 1981: 206, pl. 7.17 (figs 7-8)). Lagena algoaensis

differs from L. apiculata neocomiana Bartenstein & Brand (1951: 317, pl. 10 (figs 275—276))

in lacking both the ‘step-like’ wide apertural neck and the dense hispid ornamentation over

almost the entire exterior of the test. Examples allocated to this European species by

E. M. Beer (1970) from the Sundays River Formation are regarded as referable to

L. algoaensis. The form illustrated by Bartenstein & Bettenstaedt (1962: 255, pl. 35

(fig. 8a—b)) as L. oxystoma from the Late Hauterivian of north-west Germany features a

more granular ornament, much in keeping with L. a/goaensis, as here understood. Jones &

Wonders (1992: 563, pl. 2 (fig. 8)) illustrated a form as Lagena sp. 2 from the Berriasian—

Valanginian Barrow Group of offshore north-west Australia that 1s also very close, perhaps

identical to L. algoaensis. Lagena sp. 2 again is characterized by an irregular, rather granular

oramentation, and ‘one specimen appears to possess apertures at either end’. Lagena

algoaensis differs from the disarticulated chambers of Nodosaria apheilolocula Tappan, as

illustrated by Tappan (1955, pl. 24 (figs 6—7)) from Early Jurassic (Late Pliensbachian)

rocks of northern Alaska, in possessing a small diameter apical projection (not always

preserved) that is markedly narrower, and less robustly constructed than the apertural neck.

In contrast, chambers of N. apheilolocula display necks of much the same diameter at both

ends. The ornamentation of the two species seems similar.

Fig. 51 (see facing page). A. Lagena sp. A, SAM—PQ—MF 1384, side view, AL 1/69, 1 390 feet (IV),

F374. x 120. B. ?Lagena sp., SAM—PQ—MF 1385, fragment of apertural area, Zoetgeneugd Cliff

outcrop sample 11450 (Bb), F245. x 120. C—J. Lagena algoaensis sp. nov. C. Holotype,

SAM-—PQ-MF1386, side view, Coega Brick Pits outcrop sample 11436 (Bb), F160. x 121.

D. Paratype, SAM—PQ—MF 1387, side view, Coega Brick Pits outcrop sample 11436 (Bb), F161.

x 102. E. Paratype, SAM—PQ—MF1388, side view, CO 1/67, 642 feet (VII), F137. x 120.

F. Paratype, SAM—PQ—MF 1389, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb), F238.

x 200. G. Paratype, SAM—PQ—MF 1390, side view, shallow borehole SB—15, core 4, 229 feet (II),

F685. xX 141. H. Paratype, SAM—PQ-—MF1391, apertural view, Zoetgeneugd Cliff outcrop

sample 11450 (Bb), F237. X 166. I. Paratype, SAM—PQ—MF1392, side view, corroded test,

AL 1/69, 2 380 feet (VIII), F504. x 109. J. Paratype, SAM—PQ—MF 1393, side view, abraded test,

E6958 O0itect (i) F177 2x) 160:

166 ANNALS OF THE SOUTH AFRICAN MUSEUM

Recent examination of tests of L. apiculata neocomiana, L. hispida and Lagena cf.

oxystoma (as understood by Bartenstein & Brand 1951) from the Speeton Clay

(Hauterivian and Barremian portion) of the Yorkshire coast indicates that South African

forms previously referred to these European species must be allocated elsewhere. In

particular, this includes the L. apiculata neocomiana of McLachlan et al. (1976a: 330,

fig. 16 (no. 11)) from the Late Valanginian of the Mngazana Basin, and the L. apiculata

neocomiana of McLachlan et al. (1976b: 356, fig. 12 (no. 27)), which is very abundant in

the earliest Late Valanginian Brenton Formation and also present in the time equivalent

interval of borehole PB—A1. It should be noted that this Lagena is confined to the

Valanginian in PB—A1, and does not extend into the Hauterivian as is shown in

McLachlan et al. (19765, fig. 10). It is as yet unclear whether the Mngazana and the

Brenton/PB—A1 examples of ‘Lagena apiculata neocomiana’ are referable to the same

species, since there are differences in the arrangement of the apertural neck, but it is clear

this group warrants a new name.

Occurrence

Similar forms to Lagena algoaensis occur in the Hauterivian of borehole PB—A1 in

Pletmos Basin (discovered during re-examination of the work of McLachlan et al. 19765),

but in general the species is rare, usually absent in the offshore Pletmos, Gamtoos and

Algoa basins in rocks of Valanginian and Hauterivian age.

Stratigraphic range in the Sundays River Formation

Late Valanginian Biozone Bb to Late Hauterivian Biozone I, but generally rare or

absent in the Early Hauterivian. The species is typical of the middle and outer shelf.

Lagena hauteriviana hauteriviana Bartenstein & Brand, 1951

Figs 52A—B

Lagena hauteriviana hauteriviana Bartenstein & Brand, 1951: 317, pl. 10 (figs 277-278). Beer,

1970: 17, pl. 3 (fig. 5). Bettenstaedt & Spiegler, 1975: 11, pl: 2 (part), abb: 1 (igs ie,

36-44). McLachlan et al., 1976a: 330, fig. 16 (no. 12); 19766: 356. Stapleton & Beer, 1977: 2,

ple 3g. 15):

Lagena hauteriviana Bartenstein & Brand. Hart et al., 1981: 206, pl. 7.17 (fig. 6).

Remarks

Bettenstaedt & Spiegler (1975) examined large populations of Lagena hauteriviana

hauteriviana, L. apiculata apiculata (Reuss), L. apiculata neocomiana Bartenstein &

Brand, and L. hauteriviana cylindracea Bartenstein & Brand from the Early Cretaceous of

north-west Germany. They concluded that all four forms are closely related, and

constitute an evolutionary lineage from the Berriasian through to the Barremian. In

contrast to north-west Germany and the Speeton Clay of Yorkshire, where these species

are widespread, smooth-walled specimens of Lagena referable to this group are extremely

rare in South African deposits of the same age. The difference may well be due to the

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 167

rapidity of sedimentation through the time period in South Africa, in contrast to that of the

Speeton Clay and equivalent strata in north-west Germany.

The occasional smooth tests of Lagena in the Sundays River Formation show a variety

of morphologies, some of which accord with those accepted for L. hauteriviana

hauteriviana and L. h. cylindracea. Preservation, however, is never as good as that seen in

tests from the fine-grained, shallowly buried clays of Speeton, and since complete

specimens with the apertural and apical necks intact are never encountered in the Sundays

River Formation, some doubt must remain as to whether the South African tests are truly

referable to these European species. Since L. h. hauteriviana is a relatively conservative,

little-ornamented form, it 1s difficult to establish the true relationship of these European

and South African tests.

Occurrence

Lagena hauteriviana hauteriviana was first described from the Late Valanginian and

Hauterivian of north-west Germany (Bartenstein & Brand 1951). Later records include

the Valanginian—Hauterivian boundary to the middle Barremian of north-west Germany

(Bettenstaedt & Spiegler 1975); Late Berriasian (Ryazanian) to Early Barremian of the

Speeton Clay, Yorkshire coast (Hart et a/. 1981), although this difference in age perhaps

results from an alternative interpretation of the species in Britain; Late Valanginian

Biozone B of the Mngazana Basin, Transkei (McLachlan et a/. 1976a); and early Late

Valanginian Biozone D of both the Brenton Formation and Pletmos Basin borehole

PB—A1 (McLachlan et al. 19766). Similar forms to those illustrated here and by

McLachlan et al. (1976a) occur but rarely in the Valanginian and Hauterivian rocks of the

offshore Pletmos, Gamtoos and Algoa basins, South Africa.

Stratigraphic range in the Sundays River Formation

Occasional examples occur through most of the sequence, particularly in the Late

Valanginian (Biozones Bb to A) and the Late Hauterivian (Biozones VII to I). The species

occurs from marginal-marine to outer-shelf locations, although it is absent in hyposaline

and poorly oxygenated conditions.

Lagena hauteriviana cylindracea Bartenstein & Brand, 1951

Fig. 52C

Lagena hauteriviana cylindracea Bartenstein & Brand, 1951: 318, pl. 10 (figs 279-280).

Bettenstaedt & Spiegler, 1975: 11, pl. 2 (part), abb. 1 (figs 12-18). Bertels, 1990: 260, pl. 2

(ities 2).

Remarks

Only one specimen from the Sundays River Formation is sufficiently elongate to be

regarded as truly referable to this subspecies. One or two intermediate forms, between

subspecies L. h. hauteriviana and L. h. cylindracea occur, but these lie closer to the

former, and are included therein. See the ‘Remarks’ for L. h. hauteriviana.

ALS OF THE SOUTH AFRICAN MUSEU

ANN

168

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 169

Occurrence

Bartenstein & Brand (1951) described L. h. cylindracea from the Late Hauterivian of

north-west Germany; Bettenstaedt & Spiegler (1975) regarded its range as Early

Hauterivian to earliest Barremian. Bertels’ (1990) example is from the Hauterivian lower

Rio Mayer Formation of southern Argentina.

Stratigraphic range in the Sundays River Formation

Insufficient specimens are available to determine its full range, the single true

specimen being from Biozone II, Late Hauterivian.

Lagena spp.

Fig. 52D

Remarks

Occasional smooth-walled specimens of Lagena occur that lack the apical projection

of L. h. hauteriviana Bartenstein & Brand. These forms have, for the moment, been left in

open nomenclature, as it seems of little sense to relate them to species of other ages, such

as the extant L. /aevis (Montagu). These Lagena spp. occur scattered throughout the

Sundays River Formation sequence.

Genus Lenticulina Lamarck, 1804

Lenticulina coegaensis sp. nov.

Figs. 52E-—G

Lenticulina (Astacolus) crepidularis (non Roemer): Beer, 1970: 12, pl. 2. (fig. 3a—b) .

Lenticulina bifurcilla (non Bartenstein & Brand): McLachlan et al., 1976a: 330, fig. 16 (no. 15);

lOVOb 355 .me. 12 \(no.) 13):

Diagnosis

A species of Lenticulina typified by a flat, strongly compressed test, a peripheral keel,

Fig. 52 (see facing page). A-B. Lagena hauteriviana hauteriviana Bartenstein & Brand. A. SAM—

PQ—MF 1394, side view, AL 1/69, 1 270 feet (IV), F366. X 160. B. SAM—PQ—MF 1395, side view,

AL 1/69, 1 630 feet (VII), F444. x 120. C. Lagena hauteriviana cylindracea Bartenstein & Brand,

SAM-—PQ-—MF1396, side view, AL 1/69, 610 feet (II), F181. x 137. D. Lagena sp., SAM—PQ-

MF 1397, side view, AL 1/69, 1 060 feet (III), F324. x 180. E-G. Lenticulina coegaensis sp. nov.

E. Holotype, SAM—PQ—MF 1398, side view, Coega Brick Pits outcrop sample 11988 (Bb), F150.

x 109. F. Paratype, SAM—PQ—MF 1399, side view, Coega Brick Pits outcrop sample 11988 (Bb),

F151. x 104. G. Paratype, SAM—PQ—MF 1400, side view, Uitenhage to Graaff-Reinet Road outcrop

sample 11464 (Bb), F70. x 114. H. Lenticulina sp. A, SAM—PQ—MF 1406, side view, MV 1/79,

350-360 m (Ba), F659. x 118. I. Lenticulina ‘depressosuturalis’, SAM—PQ-—MF 1407, side view,

offshore Gamtoos Basin, Ha—-D1, 1 240-1 250 m (B: Late Valanginian), F737. x 56.

J-K. Lenticulina cf. L. saxonica Bartenstein & Brand. J. SAM—PQ-—MF1408, side view, AL 1/69,

1 630 feet (VII), F443. x 73. K. SAM—PQ—MF1409, side view, AL 1/69, 1 870 feet (VII), F461. Xx 75.

170 ANNALS OF THE SOUTH AFRICAN MUSEUM

raised limbate sutural ribs bearing irregular offshoots along their length, and one or two

circular ribs over the umbilicus.

Etymology

Named from its frequent occurrence in the Coega Brick Pits sections.

Material

Holotype (Fig. 52E). MF 1398, SOEKOR negative F150.

Paratypes (Fig. 52F—G). MF1399, MF1400, SOEKOR negatives F151, and F70.

MF1401 to MF1404 four additional specimens from sample 11988, Coega Brick Pits.

Stratum typicus

Biozone Bb, Late Valanginian, Sundays River Formation.

Locus typicus

Outcrop sample 11988, Coega Brick Pits.

Description

Test strongly compressed, flat-sided, generally not lenticular. Axial periphery

sub-circular to ovate, continuous. Equatorial periphery acutely angled and with a

narrow-bladed keel for much of its length on the dorsal margin, and flat, rectangular on the

ventral margin. Chambers arranged in an involute planispiral coil. Up to nine chambers

visible externally, enlarging rather slowly and steadily in size as added. Width of

chambers changes little in dimension through final whorl, but height of chambers is about

three times greater in the final part of that whorl than in the initial part. Many adult tests

appear to be on the verge of uncoiling but, in all examples studied, the final chamber

extends back to, or very close to the umbilicus. Sutures distinct, initially evenly curved,

later becoming almost straight for much of their length and strongly curved near to the test

periphery: all sutures markedly backward curved. Sutures defined by raised, limbate ribs,

generally rounded and broad in cross-section, but occasionally rather acute and bladed.

The sutural ribs often exhibit irregular short extensions on their leading edge which

develop on to the surface of the cameral wall. The number and intensity of the short

extensions is variable, from one simple short rib, rapidly declining, to three or four: on the

largest tests these merge into an irregular rugose pattern, and on some examples the entire

central portion of each sutural rib, midway between the umbilicus and the test periphery,

may become distinctly roughened. At the test margin the sutural ribs merge with the

peripheral keel. Over the umbilical area the sutural ribs link with either one circular, or

more usually one circular and one semicircular rib that encircle the umbilicus. Remainder

of test surface smooth and unornamented in well-preserved specimens. Aperture terminal,

a small circular opening surrounded by the merging of the peripheral keel and two ribs

which bound the apertural face of the final chamber. Apertural face smooth, flat and

unornamented, parallel-sided for most of its height in adult examples. Umbilicus narrow,

often rather deep for the genus.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 171

Remarks

Preliminary examination of the small numbers of specimens initially available from

Mngazana (McLachlan ef a/. 1976a) and borehole PB—Al (McLachlan et al. 19765)

indicated that one or two short secondary ribs were developed from each sutural rib.

Subsequent examination of much larger numbers of tests from the Late Valanginian of the

Pletmos, Gamtoos, Algoa and Mngazana basins have shown that this is an

over-simplification, and the secondary extensions of the sutural ribs may become quite

complex and markedly variable, as described above. However, the single projection

aligned at 30 degrees from the main sutural rib, which is seen in Lenticulina saxonica

bifurcilla as described by Bartenstein & Brand (1951: 284, pl. 5 (fig. 114a—b)) from

north-west Germany, is never seen 1n the South African tests.

Specimens of Lenticulina bifurcilla illustrated by Espitali¢ & Sigal (1963: 34, pl. 11

(figs 1-4)) from the ?Kimmeridgian to Hauterivian (Cenozones C to E) of the Majunga

Basin are morphologically similar to north-west German examples but are rather more

robustly built. That figured by Ascoli (1976) from the Berriasian—Valanginian of the East

Canadian continental shelf accords even closer with the type specimens.

Juvenile specimens of Lenticulina coegaensis are lenticuline in outline, as 1s the case

with the example illustrated by McLachlan et al. (1976a) from Mngazana, but with

increasing age, the tests become flatter, with a parallel-sided apertural face to the final

chamber(see Beer 1970, pl. 2 (fig. 3b)).

Occurrence

Biozone B, Late Valanginian, Mngazana Basin (McLachlan et a/. 1976a); Biozone B,

Late Valanginian, Pletmos Basin borehole PB—Al (McLachlan 19765). The species

appears abruptly, marking the base of Biozone B, and disappears (first down-hole

appearance) equally abruptly immediately above 1 Atl, marking the top of Biozone B, in

the offshore Pletmos, Gamtoos and Algoa basins. Lenticulina coegaensis 1s thus of

considerable significance in offshore Valanginian biostratigraphy.

Stratigraphic range in the Sundays River Formation

Base of Biozone Bb to the top of Biozone Ba (Late Valanginian). Lenticulina

coegaensis 1s commonest on the middle and outer shelf, and is rare in nearshore normal

marine environments, absent in hyposaline conditions.

Lenticulina sp. A

Figs 47L, 52H

Remarks

Two specimens, one badly broken, characterized by deeply incised sutures and rib-like

raised extensions of the chambers projecting into the umbilical area and often merging

around the umbilicus. Lenticulina sp. A is closely related to or even the same as an

ornamented, large-sized species, informally named Lenticulina ‘depressosuturalis’ (see

Fig. 561), which is characteristic of the Early to Late Valanginian (Biozones y to B) of the

172 ANNALS OF THE SOUTH AFRICAN MUSEUM

Pletmos, Gamtoos and Algoa basins offshore. Description of Lenticulina sp. A is left until

the detailed taxonomy of the southern offshore Berriasian and Early Valanginian

foraminifera is complete.

Stratigraphic range in the Sundays River Formation

Lenticulina sp. A 1s present only in the Late Valanginian Biozones Bb and Ba. The

species appears to be confined to the outer shelf.

Lenticulina cf. L. saxonica Bartenstein & Brand, 1951

Figs 52J-K

see Lenticulina (Lenticulina) saxonica saxonica Bartenstein & Brand, 1951: 284, pl. 5

(fig. 115a—b).

see Lenticulina saxonica Bartenstein & Brand. Hart et al., 1981: 208, pl. 7.18 (fig. 4).

Remarks

The few Sundays River specimens are similar in test morphology to Lenticulina

saxonica, but there are a number of differences. Examples of L. saxonica for comparison

have been obtained from the Hauterivian of the Speeton Clay sequence of the Yorkshire

coast. Both the European and South African forms possess a peripheral, bladed keel,

which is best developed in the early part of the final whorl, and which appears particularly

prone to damage. The sutural ribs of the Speeton Clay examples are rather low, rounded

and irregular, whereas those from the Sundays River Formation display much more

massive ribs, but they are less sharply defined in relation to the adjacent chamber

wall. The leading portion of each chamber in Lenticulina cf. L. saxonica is deeply

indented, and rises upwards rapidly towards the posterior rib of each chamber. Such

indentation does not occur on true L. saxonica. Hart et al. (1981) gave the range of

L. saxonica as Late Valanginian to Early Barremian in Britain.

Stratigraphic range in the Sundays River Formation

Rare, but Lenticulina cf. L. saxonica seems to be confined to the earliest Late

Hauterivian (Biozone VII), and is apparently restricted to the outermost shelf.

Lenticulina nodosa (Reuss, 1863) s.1.

Figs 53A—I, 54A—F

Robulina nodosa Reuss, 1863: 78, pl. 9 (fig. 6a—b).

Lenticulina (Lenticulina) nodosa (Reuss). Bartenstein, 1974: 540, pl. 1, pl. 2 (figs 5—6, 8-12,

16-17). Aubert & Bartenstein, 1976: 1, pl. 1 (figs 1-2, 4-13, 17-21), pl. 2 (figs 1, 3, 6-24), pl. 3

(figs 6-8), pl. 4 (figs 1, 4-8). Bartenstein & Kovatcheva, 1982: 642, pl. 3 (figs 6-7).

Lenticulina nodosa (Reuss). Ascoli, 1976: 686, pl. 4 (fig. 4), pl. 14 (fig. g). McLachlan et al.,

1976a: 331, fig. 16 (no. 18); 1976b; 355; fig. 12, aos 18-19), Butt, 1979: 2595 plies):

Musacchio, 1979: 254, pl. 4 (fig. 7). Malumian & Najfiez, 1983: 382, pl. 2 (figs 6, ?7).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 173

Kielbowicz et al., 1983: 326, pl. 3 (figs 1-9). Masiuk & Vifia, 19865: 33, pl. 3 (figs 1-10),

possibly pl. | (figs 7-10). Bertels, 1990: 264, pl. 4 (fig. 7).

Lenticulina Lenticulina ex gr. nodosa (Reuss). Crittenden, 1982: 26, pl. | (fig. 6).

Remarks

Bartenstein (1974) and Aubert & Bartenstein (1976) have attempted to give order to

the many forms of Lenticulina nodosa now known from the Austral, Tethyan and Boreal

provinces. This has resulted in an increasingly complex subspeciation of the L. nodosa

plexus, much of which does not seem especially justified. Michael (1967) and Crittenden

(1982: 26) have regarded the L. nodosa species-group as a representing an ‘iterative

evolutionary modification of a smooth “lenticuline” rootstock’, deriving from a species

such as Lenticulina muensteri (Roemer). If the ‘nodosa’-type of Lenticulina test has

developed repeatedly from smooth Lenticulina species (one or more) during the course of

the Early Cretaceous, then it is clear that the construction of an evolutionary tree for the

plexus is fraught with difficulties, and may never effectively represent the group.

Fortunately, the picture of the stratigraphic distribution of the group in South Africa is

relatively simple, despite much variation, from its first appearance in the Late Berriasian

to the last continuous appearance at the top of the Early Aptian. Differences exist in the

intensity of the peripheral nodes, the height and intensity of limbation of the sutural ribs,

the presence/absence and intensity of the umbilical boss, the number of chambers tn the

final whorl (and consequently the degree to which the test 1s lenticular or flat and almost

parallel-sided in cross-section), and the extent of indentation of the test periphery between

the nodes.

As discussed above (p. 140) under the ‘Remarks’ for the closely related Astacolus

gibber Espitalié & Sigal, these two species have been separated simplistically in both the

southern offshore basins and the Sundays River Formation in South Africa. All fully

coiled tests have been referred to L. nodosa, whereas all tests displaying any clear

uncoiling have been referred to A. gibber.

Two forms of L. nodosa have been recognized in the Sundays River Formation. The first

is more common and widespread, and ranges from Biozone C, earliest Late Valanginian to

Biozone I, latest Late Hauterivian. Examples of this are illustrated as Figures 53 A—I and

54A—B, E-F. Rare specimens tend to become slightly evolute (Fig. 531), but all are

lenticular in cross-section (Fig. 54E—F). Tests of this form possess eight (rarely 9—10)

chambers in the final whorl. The sutures may be strongly or weakly ribbed, and the

peripheral nodes and the umbilical infilling vary in intensity. Differences in the degree of

development of the peripheral nodes may also occur within one test (Fig. 53B).

The second form of L. nodosa is essentially confined to the Late Valanginian

(Biozones Bb to A). The occurrence of this second form in Biozone C is not certain.

Illustrated specimens are shown in Figure 54C—D. Tests are larger sized, more

compressed, with the sides almost parallel when examined in apertural view. The number

of chambers in the final whorl is nine or ten. These tests usually feature a rather larger

umbilical infilling than is seen in the first group.

Illustrations of L. nodosa by McLachlan et al. (19764, fig. 12 (no. 18)), from the

ANNALS OF THE SOUTH AFRICAN MUSEUM

174

Figure 53.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION L735

' earliest Late Valanginian Brenton Formation, and Biozone H, Late Hauterivian of

| borehole PB—A1I (fig. 12 (no. 19)) are both of the first, more common form. The

illustration of L. nodosa by McLachlan et al. (1976a, fig. 16 (no. 18)) from Biozone B,

Late Valanginian of the Mngazana Basin is of the second, larger-sized, Valanginian form.

In the southern offshore basins of South Africa, L. nodosa appears in the Late

Berriasian, initially in small numbers entirely of the first form described above. From the

later Early Valanginian the species becomes common, and the second form of larger-sized

tests appears, to disappear later at or near the top of the Late Valanginian. In shelf

environments, the first form ranges up to the top of the Hauterivian. A distinct change then

occurs, and a third form of L. nodosa appears early in the Barremian. This group 1s

characterized by a much more indented test periphery over each chamber, so that the

nodes stand out more prominently. Extreme examples of this group may be regarded as

almost spinose at the periphery; such tests are typical of the Early Aptian. The continuous

occurrence of L. nodosa ends just below the 13Atl unconformity, high in the Early

Aptian. In the Albian is a larger-sized form, with many more chambers in the final whorl,

numerous peripheral nodes and a wide opaque calcite umbilical infilling, that has been

referred to L. angulosa (Chapman). Lenticulina angulosa (see Chapman 1896a: 3, pl. |

(fig. 4a—b)) has proved to be a useful down-hole marker for the top of the Albian locally in

the southern offshore boreholes, and its extinction at the end of the Early Cretaceous

marks the termination of the sequence of nodose Lenticulina in South Africa.

Occurrence

The plexus has been regarded as ranging in the Boreal province from the Late

Berriasian to the Early MHauterivian, in the Tethyan province’ from

Kimmeridgian—Tithonian to Late Aptian, and in the Austral province from Valanginian to

Aptian—Albian (Aubert & Bartenstein 1976). As discussed above, its range in South

Africa is Late Berriasian to Early Aptian.

Stratigraphic range in the Sundays River Formation

First, normal form from Biozone C to Biozone I; second, larger form from Biozone Bb

to Biozone A. Lenticulina nodosa ranged from innermost shelf to uppermost slope and,

both in the Algoa Basin and elsewhere in the southern offshore Early Cretaceous, it

appears to have been one of the calcareous species most tolerant of low-oxygen

conditions. It is absent in marginal-marine, hyposaline environments.

Fig. 53 (see facing page). Lenticulina nodosa (Reuss) s./. Form 1. A. SAM—PQ—MF 1410, side view,

AL 1/69, 310 feet (1), F31. x 47. B. SAM—PQ—MF1411, side view, AL 1/69, 1 030 feet (III), F310.

x 43. C. SAM-—PQ-MF1412, side view, AL 1/69, 1 090 feet (III), F333. x 40.

D. SAM—PQ-MF 1413, side view, AL 1/69, 1 180 feet (IV), F342. X 86. E. SAM—PQ-—MF 1414, side

view, AL 1/69, 1 240 feet (IV), F361. x 129. F. SAM—PQ-MF1415, side view, AL 1/69, 1 510 feet

(V), F395. x 82. G. SAM—PQ-MF1416, side view, AL 1/69, 1 600 feet (VI), F439. xX 76.

H. SAM—PQ-MF 1417, side view, AL 1/69, 1 870 feet (VII), F460. x 40. 1. SAM—PQ—MF 1418, side

view, MV 1/79, 20 m (IX), F567. x 60.

176 ANNALS OF THE SOUTH AFRICAN MUSEUM

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 177

Lenticulina heiermanni Bettenstaedt, 1952

Figs 54G—J

Lenticulina (Lenticulina) heiermanni Bettenstaedt, 1952: 270, pl. 1 (figs 9, 10a—b, 1 1la—b).

Bartenstein & Bettenstaedt, 1962: 272, pl. 39 (fig. la—b). Bartenstein & Kaever, 1973: 235, pl. 6

Gigs 95).

-Lenticulina (Lenticulina) ataktos (non Espitali¢ & Sigal): Beer, 1970: 12, pl. 1 (fig. 10a—b).

Lenticulina heiermanni Bettenstaedt. Espitalié & Sigal, 1963: 39, pl. 15 (fig. 5a—b). Butt, 1979:

259, pl. 1 (fig. 15). Hart et a/., 1981: 208, pl. 7.18 (fig. 1). Malumian & Nafiez, 1983: 382, pl. 2

(fig. 4).

~ Remarks

The tests referred to Lenticulina heiermanni from the Sundays River Formation are

~ somewhat variable, particularly in the nature of the raised sutural ribs; it may well be that

- more than one species is represented here. Some differences also occur in the nature of the

raised mass in the umbilicus. The holotype figured by Bettenstaedt (1952, pl. |

_ (fig. 1 la—b)) possesses 12 chambers in the final whorl, although the largest Sundays River

tests never exhibit more than ten, rarely eleven. The sutural ribs of some specimens

(notably those of Fig. 541) are distinctly broader and less sharply defined than those of the

holotype. The specimen figured as L. (L.) ataktos Espitalié & Sigal by Beer (1970) falls

_ within the confines of L. heiermanni.

~ Occurrence

Bettenstaedt (1952) and Bartenstein & Bettenstaedt (1962) gave its range 1n north-west

_ Germany as latest Hauterivian to Early Aptian. Other records include: Late Hauterivian to

Early Aptian in the Speeton Clay (Hart ef al. 1981); Late Valanginian to ?Barremian

_ (Cenozones E and F), Majunga Basin (Espitalié & Sigal 1963); and Barremian Rio Mayer

Formation of Santa Cruz Province, (Malumidén & Najfiez 1983) and

| Valanginian—Hauterivian Pampa Rincon Formation of Tierra del Fuego, Argentina

_ (Malumian & Masiuk 1975). It is possible that some of the specimens illustrated as

_ L. muensteri (Roemer) by Kielbowicz et al. (1983, pl. 2 (especially fig. 9)) from the

_ Valanginian Springhill Formation of southern Patagonia, are referable here.

Fig. 54 (see facing page). A—-F. Lenticulina nodosa (Reuss) s.l. A-B, E-F. Form 1. C—D. Form 2.

A. SAM—PQ-MF1419, side view, AL 1/69, 4 050 feet (A), F547. x 82. B. SAM—PQ—MF 1420, side

view, Coega Brick Pits outcrop sample 11436 (Bb), F159. x 48. C. SAM—PQ—MF 1421, side view,

MV 1/79, 410-420 m (Bb), F648. x 107. D. SAM—PQ—-MF 1422, side view, MV 1/79, 370-380 m

(Ba), F644. x 90. E. SAM—PQ-—MF 1423, apertural view, AL 1/69, 520 feet (I), F192. x 80.

F. SAM—PQ-MF 1424, apertural view, AL 1/69, 490 feet (1), F113. x 52. G-J. Lenticulina

heiermanni Bettenstaedt. G. SAM—PQ—MF 1425, side view, AL 1/69, 520 feet (I), F117. x 41.

H. SAM—PQ-MF 1426, side view, AL 1/69, 580 feet (II), F168. x 68. I. SAM—PQ-—MF1427, side

view, AL 1/69, 2 590 feet (IX), F519. X 78. J. SAM—PQ-—MF 1428, side view, AL 1/69, 610 feet (II),

F183. x 34.

178 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 55.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 179

_ Stratigraphic range in the Sundays River Formation

| Very rare in the Early Hauterivian, and sporadic in the Late Hauterivian (Biozones [X

nto I).

Lenticulina subtilis (Wisniowski, 1890)

Figs SSA—-B

| Cristellaria subtilis Wisniowski, 1890: 226, pl. 9 (fig. 29a—b).

| Lenticulina subtilis (Wismowsk1). McLachlan et al., 1976a: 331, fig. 16 (no. 16); 19765: 355,

fig. 12 (nos 14-15).

_ Remarks

| Very occasional tests are referable to Lenticulina subtilis. All are characterized by a

_weakly angled periphery, sutures that are initially flush and later depressed, and the last

3-4 chambers are inflated. The specimen illustrated (Fig. 55A) is distinguished by its

_uncoiled final chamber. The holotype illustrated by Wisniowski (1890) possesses a rather

serrate margin to the test, which is presumably a damaged keel. None of the South African

forms feature a bladed keel.

Occurrence

First described from the Late Callovian clays of Grojek, near Krakow, Poland

-(Wisniowski 1890). Later records include: middle Callovian to Early Valanginian

-(Cenozones B to D) of the Majunga Basin (Espitali¢ & Sigal 1963); Late Valanginian to

| -Hauterivian (Biozones B to III) of borehole PB—A1, Pletmos Basin (McLachlan et al.

| 1976); and Late Valanginian (Biozone B) of the Mngazana Basin, Transkei (McLachlan

| et al. 1976a).

_ Stratigraphic range in the Sundays River Formation

Widespread, occasional examples occur from Late Valanginian Biozone C to Late

Hauterivian Biozone II. The species 1s confined to the inner- to outer-shelf, normal marine

portions of the onshore Algoa Basin.

Fig. 55 (see facing page). A—B. Lenticulina subtilis (Wisniowski). A. SAM—PQ—MF 1429, side view,

AL 1/69, 910 feet (III), F269. x 72. B. SAM—PQ-—MF 1430, side view, shallow borehole SB—32,

core 1, 146 feet (IV), F693. x 72. C_F. Lenticulina muensteri (Roemer) s.1. C. SAM—PQ-—MF 1431,

side view, AL 1/69, 1 360 feet (IV), F369. x 84. D. SAM-—PQ-—MF 1432, side view, shallow borehole

SB-15, core 3, 212 feet (II), F679. x 90. E. SAM—PQ-MF 1433, side view, MV 1/79, 140 m (X),

F585. x 191. F. SAM—PQ—MF1434, side view, AL 1/69, 1 780 feet (VII), F448. x 75S.

G-H. Lenticulina cf. L. cultrata (Montfort). G. SAM—PQ—MF 1435, side view, AL 1/69, 1 510 feet

(V), F403. x 123. H. SAM—PQ-MF 1436, side view, Colchester Cliff outcrop sample 12001 (IV),

F714. x 116.1. Marginulina sp. A, SAM—PQ—MF 1437, side view, shallow borehole SB—15, core 2,

210 feet (II), F674. x 130.

180 ANNALS OF THE SOUTH AFRICAN MUSEUM

Lenticulina muensteri (Roemer, 1839) s.1.

Figs 55C—F

Robulina muensteri Roemer, 1839: 48, pl. 20 (fig. 29a—b).

Lenticulina (Lenticulina) muensteri (Roemer). Beer, 1970: 11, pl. 2 (fig. la—b).

Lenticulina muensteri (Roemer). Jendryka-Fuglewicz, 1975: 149, pls 8-10, pl. 11 (figs 1-6),

pl. 19, pl. 20 (figs 1-2). Kielbowicz et al., 1983: 325, pl. 2 (figs 7-8, 10-13, ?9). Bertels, 1990: |

263, pl. 3 (fig. 14). |

Remarks

This 1s the most widespread and commonest smooth-walled Lenticulina species 1n the —

Sundays River Formation, and is regarded as a plexus in the present work. Differences

exist in the number of chambers in the final whorl (8—10), the presence or absence of slight

inflation of the final few chambers of the test, the degree to which the sutures curve —

backwards, and the extent of the calcitic infilling of the umbilicus. An extremely detailed

analysis of L. muensteri, using statistical methods, was provided by Jendryka-Fuglewicz —

Gos):

Occurrence

Described from the Early Cretaceous Hils Clays of northern Germany (Roemer 1839).

Subsequent records of this species are exceptionally numerous and rather confused.

Jendryka-Fuglewicz (1975) considered the full range of L. muensteri as Aalenian (Early

Jurassic) to Albian in Europe. Kielbowicz et al. (1983) encountered the species in the

Valanginian Springhill Formation, and Bertels (1990) noted it in the Hauterivian lower

Rio Mayer Formation of southern Argentina.

Stratigraphic range in the Sundays River Formation

Late Valanginian Biozone C to Late Hauterivian Biozone I, occurring in variable

numbers, but commonest in the Late Hauterivian. Inner to outer shelf; absent in

marginal-marine and hyposaline environments.

Lenticulina cf. L. cultrata (Montfort, 1808)

Figs 55G—H

see Robulus cultratus Montfort, 1808: 215, text-fig. on p. 214.

see Lenticulina cultrata (Montfort). Bartenstein & Brand, 1951: 281, pl. 4 (figs 101a—b, 102a—b).

Remarks

Variably carinate Lenticulina tests, with rather limbate sutures but otherwise

unornamented, are particularly typical of the Late Hauterivian. For convenience they have

been collected under this name. They show substantial differences in numbers of

chambers per whorl, and in the style of the sutures, so that it is probable that several

Species are represented here.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 181

| Stratigraphic range in the Sundays River Formation

Early to Late Hauterivian (Biozone IX to II).

Lenticulina spp.

Remarks

Specimens of smooth-walled, conservative Lenticulina tests that cannot be assigned to

the species detailed above have not been identified to specific level, and are included here.

In addition, numbers of broken or damaged Lenticulina tests have also been incorporated

under this grouping. These occur in small numbers throughout the Sundays River Formation.

Genus Marginulina d’Orbigny, 1826

Marginulina sp. A

Fig. 55]

Remarks

A single specimen from the Late Hauterivian Biozone II of shallow borehole SB—15.

?Marginulina pyramidalis (Koch, 1851)

Fig. 56A

see Nodosaria pyramidalis Koch, 1851: 169, pl. 24 (fig. 8).

| see Marginulina pyramidalis (Koch). Bartenstein & Brand, 1951: 307, pl. 9 (figs 221-223).

Bartenstein, 1959: pl. 23 (fig. 2).

Remarks

One specimen of a strongly ribbed ?Marginulina from the lowest Biozone Bb, Late

Valanginian of the Zoetgeneugd Cliff outcrop. The test possesses fully rectilinear

chambers throughout, but the foramen is somewhat excentric. The specimen thus has

characters in common with Nodosaria s.l. and Marginulina.

Genus Marginulinopsis Silvestri, 1904 s./.

Marginulinopsis parkeri (Reuss, 1863)

Fig. 56B

| Marginulina parkeri Reuss, 1863: 59, pl. 5 (fig. 14a—b). Chapman, 1898: 15, pl. 2 (fig. 8).

_Lenticulina (Marginulinopsis) parkeri (Reuss). Bartenstein & Brand, 1951: 288, pl. 6 (figs 136a—b,

137a—b).

Remarks

The few specimens available seem best referable to Reuss’s species. All specimens are

182 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 56.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 183

slightly more compressed, the dorsal margin is less lobate in the early part of the test, and

the later chambers are rather wider than high (compared to about as high as wide) than can

be seen in the holotype. In the light of the generic description of Marginulinopsis given by

Loeblich & Tappan (1988: 406), it seems likely that this species should be referred

elsewhere, perhaps to Vaginulinopsis. Authors’ earlier use has been followed in referring

the species to Marginulinopsis s.1.

Occurrence

Originally described from the upper Hils Clays of the Early Cretaceous of northern

~Germany (Reuss 1863). Bartenstein & Brand (1951) recorded the species from the middle

-and late Valanginian and Hauterivian of north-west Germany, and Chapman (1898)

described it from the Albian Gault Clay of Southern England.

_ Stratigraphic range in the Sundays River Formation

All specimens are from Shallow Borehole SB—32, probably of Biozone IV, Late

| Hauterivian age.

Genus Neoflabellina Bartenstein, 1948

Neoflabellina cf. N. malakialinensis Espitali¢ & Sigal, 1963

Fig. 56C—E

see Neoflabellina (Falsopalmula) malakialinensis Espitalie & Sigal, 1963: 56, pl. 26 (figs 7a—b,

| 8a—b, 9a—b).

_ Neoflabellina cf. malakialinensis Espitahié & Sigal. McLachlan et al., 1976b: 358, fig. 12 (no. 29).

see Palmula cf. malakialinensis (Espitali¢ & Sigal). Malumian & Naniez, 1983: 357, pl. | (figs 1-6,

10-11).

| Remarks

Few specimens of Neoflabellina occur in the Sundays River Formation. None possess

the faint surface ribs of the specimens from Mngazana (McLachlan et al. 1976a, fig. 16

_ Fig. 56 (see facing page). A. ?Marginulina pyramidalis (Koch), SAM—PQ—MF 1438, apertural view,

| Zoetgeneugd Cliff outcrop sample 11450 (Bb), F242. x 112. B. Marginulinopsis parkeri (Reuss),

SAM—PQ-MF1439, side view, shallow borehole SB—32, core 1, 148 feet (IV), F696. x 40.

C-E. Neoflabellina cf. N. malakialinensis Espitalié & Sigal. C. SAM—PQ—MF 1440, side view,

AL 1/69, 640 feet (II), F190. X 82. D. SAM—PQ—MF 1441, side view, AL 1/69, 610 feet (II), F186.

x 112. E. SAM—PQ—MF1442, side view, AL 1/69, 1 000 feet (III), F286. x 48. F. Palmula sp.,

SAM-—PQ-MF1443, side view, AL 1/69, 2 470 feet (VIII), F516. x 61. G—L. Planularia

madagascariensis Espitalié & Sigal s./. G. SAM—PQ-—MF 1444, side view, AL 1/69, 1 630 feet (VII),

F442. X 61. H. SAM—PQ-MF 1445, side view, AL 1/69, 1 180 feet (IV), F341. x 88. I. SAM-—

PQ-MF1446, side view, shallow borehole SB—-15, core 2, 210 feet (II), F678. x 100.

J. SAM—PQ-—MF 1447, side view, AL 1/69, 1 000 feet (III), F291. x 112. K. SAM—PQ—MF 1448,

side view, AL 1/69, 1 000 feet (III), F289. x 140. L. SAM—PQ-MF 1449, side view, Zoetgeneugd

Cliff outcrop sample 11450 (Bb), F239. x 91.

184 ANNALS OF THE SOUTH AFRICAN MUSEUM

(no. 20)) and from Brenton (McLachlan et al. 19766, fig. 12 (no. 28)), and they are

regarded as a separate species. The specimen illustrated here in Figure 56D, with its

strongly overlapping and enfolding final chambers, is very reminiscent of a test illustrated

by McLachlan et al. (19766, fig. 12 (no. 29)) from the Brenton Formation. The degree to

which the earlier chambers are embraced by the later ones varies greatly, and this perhaps

signifies that more than one species has been included under the name Neoflabellina cf.

N. malakialinensis. Because of the dearth of available tests, no further subdivision can be

attempted. Comparison with the illustrations of Neoflabellina malakialinensis given by

Espitali¢ & Sigal (1963) suggests that there is greater variation among the few Sundays

River tests than among the Majunga Basin tests.

Occurrence

First described from the ?Kimmeridgian to Early Portlandian (Cenozone C) of the

Majunga Basin (Espitali¢ & Sigal 1963). Similar forms are known from the Brenton

Formation (Biozone D), and Biozone IV (Late Hauterivian) of PB—A1, Pletmos Basin

(McLachlan et al. 19766). Comparable tests also occur in the Barremian Rio Mayer

Formation of Santa Cruz Province, Argentina (Malumian & Nanez 1983).

Stratigraphic range in the Sundays River Formation

Late Hauterivian Biozones III to II. It seems likely that its absence in the Late Valanginian

is due to the rather lower oxygen values on the sea-floor during much of that time period.

Genus Palmula Lea, 1833

Palmula sp.

Fig) sor

Remarks

Two fragments were found that are clearly of a species of Pal/mula from Biozone VIII,

Early Hauterivian. In each case, only the initial portion of the test 1s preserved, with an

entire initial coil, and it is not possible to identify these specimens to species level. The

fragments do not appear similar to Pa/mula sp. from the Late Hauterivian of Neuquen,

Argentina (Musacchio 1979, pl. 5 (fig. 6)).

Genus Planularia Defrance, 1826

Planularia madagascariensis Espitali¢ & Sigal, 1963 s./.

Figs 56G—-L, 57A—D

Planularia madagascariensis Espitalié & Sigal, 1963: 28, pl. 6 (figs 8-11), pl. 34 (figs 1-15).

Kuznetsova, 1974: 676, pl. 2 (fig. 3a—b).

Planularia ex gr. P. madagascariensis Espitalié & Sigal. Malumian & Masiuk, 1975: 592, pl. |

(figs 9, 10a—b).

Planularia cf. madagascariensis Espitalié & Sigal. Rigassi, 1970, pl. 83. McLachlan et al., 1976a:

33.1 fie 16; (ne, 21):

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 185

Planularia gr. madagascariensis Espitalié & Sigal. McLachlan et al., 1976b: 356, fig. 12 (no. 25,

non no. 26).

Planularia sp. cf. P. madagascariensis Espitali¢ & Sigal. Musacchio, 1979: 258, pl. 5 (figs 1-2).

Planularia madagascariensis australis Masiuk & Vina, 1986a: 11, pl. 2 (figs 1-4, 13-16), pl. 3

(figs 5—10, 17, non 11-12).

non Planularia madagascariensis madagascariensis (non Espitalié & Sigal): Masiuk & Vina

1986a: 29, pl. 5 (figs 6—7).

Remarks

Espitalié & Sigal (1963, pl. 34) considered the variation within this species sufficiently

wide to warrant it being regarded as a plexus. Later authors have often been rather

uncertain as to how to treat the plexus. The references given above provide an indication

of the difficulty that exists in attempting to establish the limits of the species and of

possible subspecies. It is considered here in the wide sense.

There is considerable variation too in the specimens of P. madagascariensis from the

Sundays River Formation. The degree to which the later chambers extend back towards the

proloculus, the extent of raised or depressed sutures, the degree to which the initial

chambers are coiled (although they never attain a complete whorl), and the extent and

intensity of the bladed keel along the dorsal margin all show substantial variation. None of

the tests from the Sundays River Formation display the short ribs close to the dorsal margin

that are seen in some examples from the Majunga Basin (Espitalié & Sigal 1963, pl. 34

(figs 1-9, 11—12)). One of these ornamented tests (pl. 34 (fig. 7)) 1s the designated holotype.

Masiuk & Vina (1986a) attempted to subdivide P. madagascariensis into two

subspecies, P. m. madagascariensis and P. m. australis. The former (illustrated as pl. 6

(figs 8-11) and pl. 34 (figs 1—6, 8—9)) and the latter (as pl. 34 (figs 10—15)) of Espitalie &

Sigal (1963), and complemented by illustrations of Argentinian Early Cretaceous

specimens by Masiuk & Vina, serves merely to reinforce the concept emphasized by

Espitali¢é & Sigal, that this species is a plexus. It is felt that, given the wide variety in

morphology exhibited by the 19 tests illustrated by Espitalié & Sigal, the subspecies

distinctions of Masiuk & Vina (1986a) are not justified, based partly as they are on

features that are not typical, and partly on features that were not effectively illustrated and

only briefly described by Espitalié & Sigal (1963). None of the 19 tests illustrated from

the Majunga Basin display an entire initial whorl. In addition, Espitalié & Sigal (1963: 28)

described the test margins, not clearly evident in any of the illustrations, as ‘bord ventral

légerement tronque, bord dorsal pourvu d’une caréne et régulierement arqué’. For these

reasons it is felt that the two tests referred by Masiuk & Vina (1986a, pl. 5 (figs 6—7)) to

P. m. madagascariensis fall outside the realm of the original description and illustrations,

and should be referred elsewhere, probably to Astacolus. They are characterized by a

marked initial coil and by an abruptly angled, wide ventral margin. Furthermore, it invites

other problems if forms with clearly different chamber arrangements are included. For

this reason, the specimens illustrated by Masiuk & Vina (1986a) as pl. 3 (figs 11 and 12)

must be referred elsewhere since they are well outside the concept of the original

description and illustrations of Espitali¢é & Sigal (1963).

186 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 57.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 187

Occurrence

_ Described from the Middle Callovian to Early Valanginian (Cenozones B to D) of the

; Majunga Basin (Espitalié & Sigal 1963). Later records include DSDP site 261 near the Java

Trench (Late Jurassic to ?Early Cretaceous) (Kuznetsova 1974); Valanginian—Hauterivian

| Pampa Rincon Formation, Tierra del Fuego (Malumian & Masiuk 1975); Late Hauterivian

of Neuquén, Argentina (Musacchio 1979); Late Valanginian (Biozone B) Mngazana Basin,

Transkei (McLachlan et al. 1976a); Late Valanginian to Late Hauterivian (Biozones D to II)

of borehole PB—A1 in Pletmos Basin and Late Valanginian (Biozone D) Brenton Formation

(McLachlan et al. 1976b). The species ranges from the Portlandian (McMillan 1980) to

Early Barremian in the southern offshore basins of South Africa.

_ Stratigraphic range in the Sundays River Formation

| Late Valanginian to Late Hauterivian (Biozones C to I), never abundant, but

widespread. Planularia madagascariensis occurs from shallow, normal marine

environments to the outer shelf, but is absent in areas influenced by lowered salinities.

Planularia formosa sp. nov.

Figs 57E-M

-Planularia gr. madagascariensis (non Espitali¢ & Sigal, 1963): McLachlan et al., 1976b: 356,

fig. 12 (no. 26, non no. 25).

_ Planularia sp. aff. P. complanata (Reuss). Bertels, 1990: 273, pl. 6 (fig. 9).

| Diagnosis

A species of Planularia characterized by a narrow-bladed peripheral keel along the

entire dorsal margin, with straight to gently curving, limbate sutural ribs that may possess

rather irregular, almost rugose margins, and by up to four chambers arranged in an initial

_half-whorl, the later chambers arranged in a gentle arc.

Fig. 57 (see facing page). A—D. Planularia madagascariensis Espitalié & Sigal s.. A. SAM—PQ-—

| MF 1450, side view, AL 1/69, 1 240 feet (IV), F362. x 96. B. SAM—PQ—MF1451, side view,

AL 1/69, 2 410 feet (VIII), F508. x 95. C. SAM—PQ-MF 1452, side view, AL 1/69, 2 330 feet (VIII),

F496. X 105. D. SAM—PQ—-MEF1453, ventral view, AL 1/69, 1 540 feet (VI), F405. x 84.

E-M. Planularia formosa sp. nov. E. Paratype, SAM—PQ—MF1454, side view, Uitenhage to

Graaff-Reinet Road outcrop sample 11464 (Bb), F77. x 102. F. Paratype, SAM—PQ—MF 1455, side

view, Zoetgeneugd Cliff outcrop sample 11452 (C), F253. x 64. G. Paratype, SAM—PQ—MF 1456,

side view, Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F74. x 102. H. Paratype,

SAM—PQ-—MF 1457, side view, Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F72.

x 126. I. Holotype, SAM—PQ—MF 1458, side view, Coega Brick Pits outcrop sample 11988 (Bb),

F152. X 63. J. Paratype, SAM—PQ—MF1459, side view, AL 1/69, 430 feet (I), F59. x 69.

K. Paratype, SAM—PQ—MF 1460, side view, AL 1/69, 2 030 feet (VII), F485. x 88. L. Paratype,

SAM-—PQ-MF 1461, side view, AL 1/69, 1 630 feet (VII), F441. x 76. M. Paratype, SAM—PQ-

MF 1462, ventral view, AL 1/69, 520 feet (1), F195. X 88. N. Planularia sp. C, SAM—PQ—MF 1466,

side view, MV 1/79, 20 m (IX), F566. X 48.

158 ANNALS OF THE SOUTH AFRICAN MUSEUM

Etymology

Adjective, named for its first occurrence in PB—A1 borehole, just off Plettenberg Bay,

an early Portuguese name for which was Bahia Formosa.

Material

Holotype (Fig. 571). MF1458, SOEKOR negative F152.

Paratypes (Fig. S7E-H, J-M). MF1454 to MF1457, MF1459 to MF1462, eight

specimens, SOEKOR negatives F77, F253, F74, F72, F59, F485, F441, and F195.

Stratum typicum

Biozone Bb, Late Valanginian, Sundays River Formation.

Locus typicus

Outcrop sample 11988, Coega Brick Pits.

Description

Test strongly compressed, flat-sided. Equatorial periphery acutely angled, with a

narrow-bladed keel along the entire dorsal margin, and sub-rounded, flattened on the

ventral margin. Axial periphery sub-circular to elongate, with dorsal margin continuous,

occasionally weakly lobate in the final part of the test, and ventral margin varying from

irregular to lobate in outline. Chambers arranged in an initial half-whorl of up to four,

followed by an arcuate sequence of up to eight. The degree to which the later chambers

extend back towards the proloculus is very variable. Later chambers about five times as

wide as high. Early chambers increase rapidly in width but less rapidly in height as added,

but in later chambers the increase is much less. Sutures generally distinct, raised, limbate,

varying from gently curved to almost curved, rarely straight, and tending to be a little

more curved close to the dorsal margin. Sutures ornamented with thick, low ribs that often

exhibit sharply defined but roughened, irregular margins; ribs low, flat and wide in cross-

section, although often rather rounded, perhaps through post-mortem abrasion. Sutural

ribs may merge with either or both the dorsal keel or the ventral margin or, more usually,

fade in intensity and almost disappear close to the dorsal and ventral margins. Occasional

specimens exhibit short, sharply defined, vertically aligned ribs close to the dorsal margin,

which often extend from one sutural rib vertically to the dorsal margin of the next. In rare

specimens with a rather more complete initial coil, a small, irregularly shaped swelling is

formed over the umbilicus. Aperture terminal, located close to the dorsal margin of the

test; a circular opening that may show a faintly radiate margin. Apertural face of the final

chamber narrow and parallel-sided. Surface of test smooth, apart from the ornamentation

along the sutures and close to the dorsal margin.

Remarks

Substantial variation is evident in the specimens assigned to Planularia formosa, but

they can easily be separated from tests of P. madagascariensis Espitalié & Sigal by their

distinctive surface ornamentation.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 189

Planularia formosa 1s morphologically close to P. complanata complanata (Reuss),

which has been described by a number of authors from the Albian of Europe: Reuss

(1863), Chapman (18945), Noth (1951) and Magniez-Jannin (1975). Magniez-Jannin

(1975: 154, pl. 9 (figs ?31, 32-36), text-figs 83c—d)) recognized P. c. complanata as the

least ornamented of four subspecies of Reuss’s species. Planularia c. complanata 1s

characterized by an initial coil of 6-7 chambers, almost of one whorl, forming one-quarter

of the total height of the shell, a non-carinate dorsal margin, the later chambers always

extend substantially far back towards the proloculus, and the surface ornamentation

consists of fine and irregular granulations, with thin parallel ribs often close to the dorsal

margin of the test; none of these features are evident in shells of P. formosa.

The specimen figured by Bertels (1990, pl. 6 (fig. 8)), under the name Planularia sp.

aff. P. complanata (Reuss) from southern Argentina, appears to fall within the confines of

P. formosa. Its sutures are raised and limbate, but less strongly defined than the sutures of

well-preserved tests from the Sundays River Formation.

Occurrence

Late Valanginian to Hauterivian (Biozones C to II) of PB—A1 borehole, Pletmos Basin

(McLachlan ef al. 1976b, and supplementary data). The species is present in small

numbers in the offshore Pletmos, Gamtoos and Algoa basins in rocks of Valanginian and

Hauterivian age. Also present in the Hauterivian of the lower Rio Mayer Formation,

southern Argentina (Bertels 1990).

Stratigraphic range in the Sundays River Formation

Widespread, but never common from the Late Valanginian Biozone C to Late

Hauterivian Biozone I. Early Hauterivian occurrences are rare.

Planularia sp. A

Fig. 538A

Remarks

A single specimen of Planularia from borehole AL 1/69, Biozone III, Late

Hauterivian. The initial part of the test consists of a coil of four chambers in three-quarters

of a whorl. The ventral margin is narrow, parallel-sided, and weakly convex to flat. The

dorsal margin is ornamented with a narrow-bladed keel. Sutures are strongly ornamented

with thickened ribs that are sharply defined, and rounded in cross-section. Close to the

dorsal margin, the ribs abruptly thin and change direction, to reach the dorsal keel close to

the dorsal end of the following suture. The thin vertical sub-dorsal ribs are almost

blade-like, and decline in height towards the dorsal keel. At the point of the change in

angle of the ribs, a low rounded swelling of the test extends straight along the remainder of

each suture to the dorsal margin.

These ornamentation features are a re-organization of the surface characters of

P. formosa sp. nov., described above. It is distinguished from that species, however, by

the more intense ornament, and the rather rectangular cross-section of the test, although

190 ANNALS OF THE SOUTH AFRICAN MUSEUM

ayn

Figure 58.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 19]

the two are evidently closely related. The specimen is also similar to Vaginulina

(Citharina) sp. 2376 Espitali¢ & Sigal (1963: 51, pl. 22 (fig. 14)) from the Hauterivian—

?Barremian Cenozone F of the Majunga Basin, but it differs in the carinate dorsal margin

and the surface ornamentation close to the dorsal margin.

Planularia sp. B

Figs 58B—-C

Remarks

Elongate tests that fall somewhere between Planularia, Vaginulinopsis, and even

Astacolus are referred to the first of these genera for convenience. P/anularia sp. B occurs

very occasionally in Biozone X, Early Hauterivian. Tests are compressed, elongate-ovate

in cross-section, with rounded to sub-rounded ventral margins and sub-rounded to acute

dorsal margins. A very weak keel may occur on the dorsal margin in the early part of the

test. The sutures are marked by raised, thick, low and rounded ribs that are at their thickest

near the dorsal margin and taper steadily towards the ventral. The sutural ribs do not

usually link with either the ventral or dorsal margin. These tests may prove to be related to

the Astacolus explicatus shell illustrated by McLachlan et al. (19765, fig. 11 (nos 20—21))

(non Espitalié & Sigal), as previously discussed in the ‘Remarks’ for that species.

However, Planularia sp. B tests are more compressed and wider, and lack the distinctive

flange of the dorsal margin of that shell.

Planularia sp. C

Fig. STN

Remarks

A single specimen from Biozone IX, Early Hauterivian. Test compressed, elongate and

parallel-sided in cross-section. Ventral and dorsal margins rounded. Sutures indistinct,

initially flush, later lightly depressed. Surface of test smooth.

Fig. 58 (see facing page). A. Planularia sp. A, SAM—PQ-—MF 1463, side view, AL 1/69, 1 090 feet (III),

F325. X 77. B-C. Planularia sp. B. B. SAM—PQ-MF 1464, side view, MV 1/79, 90 m, (X), F579.

x 64. C. SAM—PQ-MF1465, side view, MV 1/79, 90 m, (X), F578. X 68. D. Planularia sp.,

SAM-—PQ-—MF 1467, side view, AL 1/69, 2 030 feet (VII), F484. x 110. E-J. Pravoslavlevia frankei

(Ten Dam). E. SAM—PQ—-MF1468, side view, AL 1/69, 1 180 feet (IV), F320. x 88.

F. SAM—PQ-MF 1469, side view, AL 1/69, 1 570 feet (VI), F430. x 127. G. SAM—PQ-MF 1470,

side view, shallow borehole SB—15, core 2, 210 feet (II), F676. x 117. H. SAM—PQ—MF1471,

oblique side view, AL 1/69, 2 680 feet (IX), F521. X 121. I. SAM—PQ—MF 1472, side view, AL 1/69,

1 540 feet (VI), F413. X 97. J. SAM—PQ-—MF 1473, ventral view, AL 1/69, 520 feet (I), F130. x 43.

K-L. Pravoslavlevia pravoslavlevi (Fursenko & Polenova). K. SAM—PQ-—MF1474, side view,

AL 1/69, 1 480 feet (IV), F378. x 36. L. SAM—PQ-MF 1475, side view, AL 1/69, 1 870 feet (VII),

F458. x 49.

192 ANNALS OF THE SOUTH AFRICAN MUSEUM

Planularia spp.

Fig. 58D

Remarks

Scattered specimens of damaged or otherwise indeterminate P/anularia tests occur; one

example is figured that may be related to the example of Planularia formosa sp. nov.

illustrated in Figure 63L. None of these specimens have proved to be of stratigraphic value.

Genus Pravoslavlevia Putrya, 1970

Pravoslavlevia frankei (Ten Dam, 1946)

Figs 58E—J

Saracenaria frankei Ten Dam, 1946: 573, pl. 88 (fig. la—b).

Lenticulina (Saracenaria) cf. italica (non Defrance): Bartenstein & Brand, 1951: 291, pl. 6

(fig. 149a—b). Beer, 1970: 15, pl. 2 (fig. 12a—b).

Lenticulina (Saracenaria) frankei Ten Dam. Noth, 1951: 47, pl. 1 (fig. 31). Bartenstein et al., 1957:

33, pl. 3 (fig. 60a—b). Bartenstein & Kovatcheva, 1982: 644, pl. 3 (fig. 19).

Saracenaria tsaramandrosoensis (non Espitali¢ & Sigal): Malumian & Masiuk, 1975: 592, pl. 2

(fig. 10). McLachlan et al., 1976b: 355, fig. 12 (nos 16-17). Musacchio, 1978: 151, pl. 2

(fig. 21); 1979: 258, pl. 5 (fig. 4); 1981: pl. 1 (fig. 5). Kielbowicz et al., 1983: 332, pl. 4 (fig. 9).

Masiuk & Vina, 1986a: 31, pl. 6 (figs 1-2).

Saracenaria compacta (non Espitalié & Sigal): McLachlan ef al., 1976a: 331, fig. 16 (no. 22).

Remarks

Pravoslavlevia frankei was described as characterized by a small, but complete, initial

coil that accounted for a fifth of the total height, with a sharp dorsal keel, and limbate flush

to faintly depressed sutures. The species is relatively unornamented, compared with

others of the genus. Although there are a number of references to ‘Saracenaria

tsaramandrosoensis’ from Argentina and South Africa, none of the illustrated specimens

come close to the Espitalié & Sigal holotype from the Majunga Basin. All appear to be

better referred to P. frankei, as indicated in the synonymy given above.

Espitalié & Sigal (1963) defined P. tsaramandrosoensis by its small size, slender test

with parallel edges, and with the three triangular margins all strongly carinate. The gracile

nature of the test is emphasized several times in the description, and this feature is borne

out in the stereo-pair illustrations of the holotype (pl. 24 (fig. 2a—d)). The later chambers

appear more backward extending than is usual for Pravoslavlevia and Saracenaria —

species, although this feature is not so evident in their specimen illustrated as figure 3a—b.

In both the Majunga Basin specimens illustrated, the initial coil—described as containing

from three to four chambers—appears to be scarcely more than three-quarters of a whorl

in extent, but this aspect of the species is not mentioned in the description. The sutures are

described as becoming gradually depressed towards the apertural—dorsal margin, and

rather depressed on the ventral side.

None of the illustrated Argentinian and South African specimens referred to

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 193

P. tsaramandrosoensis in the synonymy above possess as strong keels along the two

margins of the ventral side as along the dorsal margin; none possess the rather elongate,

oblique chambers; none possess such a reduced initial coil; and none display the style of

sutures typical of the holotype.

The only illustrated Argentinian specimen that comes close to the true morphology of

P. tsaramandrosoensis 1s that illustrated by Malumian & Nafiez (1983, pl. 2 (fig. 11)),

although the two ventral keels appear to be weakly developed. Malumian & Naniez (1983:

380) pointed out that the illustrations of P. tsaramandrosoensis by Espitali¢é & Sigal

(1963) suggest there are ribs close to or on the sutures that appear to be especially strongly

developed in the initial part of the test, but there is no mention of these in the written

description. It is evident from the further comments of Malumian & Naniez (1983) that a

more detailed analysis of type material of P. tsaramandrosoensis from the Majunga Basin

is necessary before its full distribution in the Southern Hemisphere can be established.

Occurrence

Pravoslavlevia frankei has been widely recognized in the Barremian (Bettenstaedt

1952; Bartenstein & Kaever 1973; Bartenstein & Kovatcheva 1982), the Hauterivian (Ten

Dam 1946; Noth 1951), the middle and late Valanginian (Bartenstein & Brand 1951) of

Europe, and in the Barremian of Trinidad (Bartenstein et al. 1957). The following

Southern Hemisphere records are regarded as referable to the same species: Valanginian—

Hauterivian Pampa Rincon Formation, Tierra del Fuego (Malumian & Masiuk 1975),

Late Hauterivian of the Agrio Formation, Neuquén (Musacchio 1978, 1979, 1981;

Masiuk & Vina 1986a), and Valanginian Springhill Formation of southern Patagonia

(Kielbowicz et al. 1983), all of Argentina; Late Valanginian Biozone B of the Mngazana

Basin (McLachlan et al. 1976a), and Late Valanginian to Early Hauterivian (Biozone B to

VIII) of borehole PB—A1, Pletmos Basin (McLachlan et al. 19766) in South Africa.

Stratigraphic range in the Sundays River Formation

Small numbers occur in the Late Valanginian and Late Hauterivian with only very rare

examples from the Early Hauterivian (Biozone Bb to I). Confined to middle- and outer-

shelf environments.

Pravoslavlevia pravoslavlevi (Fursenko & Polenova, 1950)

Figs 58K—L, 59A—C

_ Saracenaria pravoslavlevi Fursenko & Polenova, 1950: 45, pl. 4 (figs 13-15). Espitalié & Sigal,

1963: 52, pl. 23 (figs 4a—d, 5a—d, 6a—d, 7a—b), pl. 24 (fig. la—b). Bielecka, 1975: 349, pl. 10

(figs 1, 2a—b, 3). Malumian & Masiuk, 1975: 591, pl. 1 (fig. 8). Kielbowicz et al., 1983: 330,

pl. 4 (figs 7-8). Bertels, 1990: 276, pl. 7 (figs 2-3).

Remarks

A stoutly built Pravoslavlevia characterized by prominent raised sutural ribs, with a

similar rib along either edge of the apertural face, and a narrow bladed keel along the

194 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 59.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 195

dorsal margin. The ornamentation 1s distinctly more intense and the test 1s more nearly an

equilateral triangle in cross-section than is seen in P. frankei (Ten Dam). The Sundays

River Formation tests compare well with those from the Majunga Basin, Madagascar

(Espitali¢é & Sigal 1963), and with those from Argentina (Malumian & Masiuk 1975;

Kielbowicz et al. 1983; Bertels 1990).

Occasional examples, illustrated as Figures 58L and 59A, possess rather wider

uncoiled adult parts of the test (when seen in side view) than 1s typical. These appear to be

intermediate between P. pravoslavlevi and P. compacta (Espitali¢é & Sigal).

Occurrence

Originally described from the early and middle Volgian of the Russian Platform, Russia

(Fursenko & Polenova 1950). Later Southern Hemisphere records include: ?Kimmeridgian—

?’Barremian (Cenozones C to F) of the Majunga Basin (Espitali¢é & Sigal 1963),

Valanginian—Hauterivian Pampa Rincon Formation of Tierra del Fuego (Malumian &

Masiuk 1975), the Valanginian Springhill Formation (Kielbowicz et a/. 1983), and the

Hauterivian lower Rio Mayer Formation (Bertels 1990), all of southern Argentina.

Stratigraphic range in the Sundays River Formation

Present only in the most distal intersections studied. Very rare in the Late Valanginian

(Biozone Bb), more common in the later Early and Late Hauterivian (Biozones VIII to I).

Known to range up into the Early Barremian in the southern offshore basins of South Africa.

Genus Psilocitharella Loeblich & Tappan, 1986

Psilocitharella arguta (Reuss, 1860)

Fig. 59D-G

Vaginulina arguta Reuss, 1860: 202, pl. 8 (fig. 4); 1863: 47, pl. 3 (fig. 13a—b). Bartenstein ef al.,

1957: 38, pl. 5 (fig. 104), pl. 6 (fig. 136). Bartenstein et a/., 1971: 147, pl. 3 (fig. 58). Bartenstein

& Kaever, 1973: 228, pl. 4 (figs 55-56). Musacchio, 1979: 254, pl. 4 (fig. 15). Hart et a/., 1981:

222 ipl 7 25 (fies 12).

Fig. 59 (see facing page). A-—-C. Pravoslavlevia pravoslavlevi (Fursenko & Polenova).

A. SAM-PQ-MF 1476, side view, AL 1/69, 2 410 feet (VIII), F507. x 91. B. SAM—PQ—MF 1477,

oblique side view, AL 1/69, 580 feet (II), F167. x 31. C. SAM-—PQ—MF 1478, apertural view,

AL 1/69, 520 feet (1), F196. x 74. D-G. Psilocitharella arguta (Reuss). D. SAM—PQ-MF 1479, side

view, CO 1/67, 660 feet (VII), F145. x 53. E. SAM—PQ-—MF1480, side view, CO 1/67, 660 feet

(VI), F144. x 37. F. SAM—PQ-MF 1481, side view, AL 1/69, 850 feet (II), F265. x 111. G. SAM—

PQ-MF1482, edge view, AL 1/69, 1 510 feet (V), F400. x 86. H-M. Vaginulina spp.

H. SAM—PQ-MF 1483, side view, AL 1/69, 2 470 feet (VIII), F515. X 78. 1. SAM—PQ-—MF 1484,

side view, AL 1/69, 640 feet (II), F197. X 72. J. SAM—PQ-MF 1485, side view, AL 1/69, 1 120 feet

(II), F337. x 77. K. SAM—PQ—MF1486, side view, AL 1/69, 1 540 feet (VI), F406. x 61.

L. SAM—PQ—MF 1487, side view, AL 1/69, 460 feet (I), F105. x 80. M. SAM-PQ-MF 1488, side

view, AL 1/69, 520 feet (I), F118. X 129. N. Vaginulinopsis sp. A, SAM—PQ—MF 14839, side view,

Zoetgeneugd Cliff outcrop sample 11450 (Bb), F241. x 64.

196 ANNALS OF THE SOUTH AFRICAN MUSEUM

Vaginulina kochii (non Roemer): Beer, 1970: 15, pl. 2 (fig. 14).

Remarks

Test with wide, flat dorsal and ventral margins, a prominent globular proloculus that

protrudes above the flat surface of the test (Fig. 59G), a peripheral rib on either side of the

test that includes the proloculus, and low sutural ribs that extend for most of each straight

to weakly arcuate suture. Test is rectangular in cross-section. Dorsal margin weakly

convex to straight, ventral margin variably lobate, straight or faintly concave.

This is the first Psi/ocitharella to be found in the Valanginian and Hauterivian rocks of

biostratigraphic use in the Early Cretaceous of western Europe. Kindred species are known

also in the Barremian and Early Aptian of South Africa, but the group is commonest in this

region in the Late Aptian to Cenomanian. However, the number of species in the group is

substantially fewer in South Africa than are recognized in the Early Cretaceous of Europe. A

similar situation appears to hold true for Argentina, based on published data, and it would

seem that the genus Psi/ocitharella 1s mainly boreal in distribution.

Albers (1952) examined Psilocitharella assemblages in the Barremian of the Hanover

region of Germany, and separated P. kochi (Roemer) and P. arguta essentially on the

absence or presence, respectively, of the sutural ribs.

Occurrence

Psilocitharella arguta was first described from the Albian higher Gault (Minimus

clays with greensand) and ?Cenomanian of Westphalia, Germany (Reuss 1860). Later

records include: upper Hils Clays (?Barremian) of northern Germany (Reuss 1863); Late

Hauterivian to Middle Barremian of Heligoland (Bartenstein & Kaever 1973); Barremian

and Aptian of Bulgaria (Bartenstein et a/. 1971); Barremian of Trinidad (Bartenstein et al.

1957); Early and Late Hauterivian of Neuquén, Argentina (Musacchio 1979); and base

Hauterivian to Early Barremian of the Speeton Clay, England (Fletcher 1973; Hart et al.

1981).

Stratigraphic range in the Sundays River Formation

Restricted to the more distal, outer-shelf localities, and confined to the Late

Hauterivian (Biozones VII to II). The species is present in small, scattered numbers only.

Genus Vaginulina d’Orbigny, 1826

Vaginulina spp.

Figs S9H—-M

Remarks

Occasional examples of Vaginulina occur scattered through the Sundays River

Formation. A wide variety of simple forms, lacking surface ornamentation, have been

encountered—sufficiently wide that it is difficult to determine any species boundaries

within the plexus. For the moment, no attempt has been made to separate this group into

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 197

species. Vaginulina spp. range from the Late Valanginian (Biozone Bb) to Late

Hauterivian (Biozone I).

Genus Vaginulinopsis Silvestri, 1904

Vaginulinopsis sp. A

Fig. SON

Remarks

Six specimens are referred to Vaginulinopsis from the lower part of the Zoetgeneugd

Cliff outcrop (basal Biozone Bb, Late Valanginian). These tests possess an initial coil of

well over one whorl, but otherwise are reminiscent of Astacolus calliopsis (Reuss).

Vaginulinopsis cf. V. matutina (d’Orbigny, 1850)

Figs 60A—C

see Cristellaria matutina d’Orbigny, 1850a: 242. Macfadyen, 1936: pl. 1 (fig. 264).

see Lenticulina (Vaginulinopsis) matutina (d’Orbigny). Bartenstein ef al., 1957: 31, pl. 6

(fig. 120a—b).

Vaginulinopsis matutina (non d’Orbigny): McLachlan et al. 1976b: 353, fig. 12 (nos 5—7).

Remarks

Although superficially similar to D’Orbigny’s Liassic species, these tests exhibit

distinct differences, and probably warrant a new name. The specimen of V. matutina from

the D’Orbigny collection described by Macfadyen (1936), is characterized by a straight

_ dorsal margin and a markedly lobate ventral margin. In cross-section this specimen 1s

_ strongly compressed toward the dorsal margin, which is acute but not keeled. The ventral

- margin is broad and rounded. Comparison may also be made to some of the ‘Form F’ tests

illustrated by Barnard (1960) from the English Lias.

In contrast, the South African specimens manifestly lack a lobate ventral periphery, the

cross-section of the adult test 1s elongate-ovate, and both ventral and dorsal margins are

broad and rounded, although the latter may be slightly pinched in the initial uncoiled part of

the test. Vaginulinopsis cf. V. matutina is evidently closely related to the following species.

~ Occurrence

| Vaginulinopsis cf. V. matutina ranges from Late Valanginian Biozone B to Late

_ Hauterivian Biozone III in Pletmos Basin borehole PB—A1 (McLachlan et al. 19765).

| Stratigraphic range in the Sundays River Formation

| Late Valanginian Biozone Bb to Late Hauterivian Biozone I, where it is rather rare,

_ but the species is particularly abundant in the upper part of Biozone VII. This abundance

in the earliest Late Hauterivian is sufficiently consistent that it can be traced across most

_ of the boreholes intersecting this part of the section, and it has been used to define the top

_ of Biozone VI.

198 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 60.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 199

Vaginulinopsis cf. V. prima (dV Orbigny, 1850)

Figs 60D-G

see Cristellaria prima @Orbigny, 1850a: 242. Macfadyen, 1936: pl. | (fig. 266a—b).

see Lenticulina (Vaginulinopsis) prima (d’Orbigny). Bartenstein et al., 1957: 31, pl. 3 (fig. 59a—b),

pl. 4 (figs 89-90).

Lenticulina (Vaginulinopsis) prima (non @ Orbigny): Beer, 1970: 13, pl. 2 (fig. 10a—b).

Vaginulinopsis gr. prima (non d Orbigny): McLachlan et al., 1976: 353, fig. 12 (nos 8-10).

Remarks

A similar situation holds true for this species as was discussed above for

Vaginulinopsis cf. V. matutina (d’ Orbigny). Originally recognized from the Liassic rocks

of France by D’Orbigny (1850a), more complete descriptions and the first illustrations

were given by Macfadyen (1936). Macfadyen (1936: 151) described the species as: ‘In

section the tests appear to be flattened-lenticular; the sutures are well marked, rather broad

and slightly depressed. The umbilicus of the larger specimen 1s excavated. The outer

margin varies from being lightly keeled to sharp edged.’ D’Orbigny’s original (1850qa)

description was confined to: ‘Espéce carénée, comprimeée, lisse, pourvue de nombreuses

loges non saillantes’.

Both the PB—A1 and Brenton examples (McLachlan et a/. 19765) and the present

forms show marked differences from D’Orbigny’s species. Particular differences exist in

the broadly rounded dorsal and ventral margins of the South African tests, the flush to

faintly raised sutures, the elongate-ovate cross-section in the adult part of the test, and the

relatively small initial coil and long uncoiled portion in all tests studied. The Lias

specimens, in contrast, display a large initial coil and a small uncoiled portion. For the

moment, these South African tests have been referred to Vaginulinopsis cf. V. prima, but it

seems increasingly likely that a separate name is warranted.

The distinction of Vaginulinopsis cf. V. prima from Vaginulinopsis ct. V. matutina

Fig. 60 (see facing page). A—-C. Vaginulinopsis cf. V. matutina (d’Orbigny). A. SAM—PQ—MF 1490,

side view, AL 1/69, 640 feet (II), F200. x 55. B. SAM—PQ-—MF1491, side view, AL 1/69, 2 680 feet

(IX), F520. x 54. C. SAM—PQ-MF1492, side view, AL 1/69, 1 540 feet (VI), F415. x 65.

D-G. Vaginulinopsis cf. V. prima (d’ Orbigny). D. SAM—PQ—MEF 1493, side view, CO 1/67, 642 feet

(VII), F141. x 52. E. SAM—PQ—MF 1494, Side view, shallow borehole SB—35, core ?, top (III),

F703. X 48. F. SAM—PQ—MF1495, side view, AL 1/69, 820 feet (III), F262. x 55.

G. SAM-PQ-MF 1496, side view, AL 1/69, 820 feet (III), F261. x 60. H-K. Pseudonodosaria

humilis (Roemer). H. SAM—PQ—MF1497, side view, AL 1/69, 1 000 feet (III), F295. x 73.

I. SAM—PQ-—MF1498, side view, AL 1/69, 400 feet (I), F52. x 69. J. SAM—PQ—MF 1499, side view,

AL 1/69, 340 feet (1), F40. x 85. K. SAM—PQ—MF 1500, apertural view, AL 1/69, 1 060 feet (III),

F318. X 160. L—N. Lingulonodosaria nodosaria (Reuss). L. SAM—PQ-—MF1501, side view,

AL 1/69, 460 feet (1), F111. X 825. M. SAM—PQ—MF1502, side view, AL 1/69, 370 feet (I), F50.

X 128. N. SAM—PQ—MF1503, side view, Coega Brick Pits outcrop sample 11988 (Bb),F156. x 82.

O-P. Paralingulina hexacarinata (Espitali¢ & Sigal). O. SAM—PQ—MF 1504, side view, AL 1/69,

640 feet (II), F187. x 53. P,. SAM—PQ-MF1504, close-up of apertural area of O, F188. X 373.

200 ANNALS OF THE SOUTH AFRICAN MUSEUM

employed during the Sundays River Formation study is the same as that of McLachlan et

al. (19766), with the added comment that the maximum width of the uncoiled portion of

the former species is adjacent to the initial coil, whereas in the latter species it is at the

level of the final chamber. Nevertheless, the two are very closely related, and it may well

be that they are tests from different generations of the same species.

Occurrence

Late Valanginian Biozone D to Late Hauterivian Biozone II of borehole PB—A1,

Pletmos Basin, and in the Late Valanginian (Biozone D) Brenton Formation (McLachlan

et al. 19765).

Stratigraphic range in the Sundays River Formation

Rare in the Late Valanginian and Early Hauterivian, more common in the Late

Hauterivian (Biozones Bb to I).

Family Ichthyolariidae Loeblich & Tappan, 1986

Genus Lingulonodosaria A. Silvestri, 1903

Lingulonodosaria nodosaria (Reuss, 1863)

Figs 60L—N

Lingulina nodosaria Reuss, 1863: 59, pl. 5 (fig. 12a—b). Magniez-Jannin, 1975: 217, text-fig. 112.

Musacchio, 1979: 258, pl. 4 (fig. 13). Malumian & Nanfiez, 1983: 378, pl. 1 (fig. 18).

Remarks

Occasional examples of Lingulonodosaria occur in the Sundays River Formation.

Most are as illustrated in Figure 66L—M, but scattered tests as in Figure 66N that are rather

corroded seem referable here also. The height of the chambers 1s a little lower than in the

holotype illustrated by Reuss (1863) and in the examples figured by Magniez-Jannin

(1975). The aperture of the Sundays River shells is often rather damaged but, where

visible, appears to be of the same dimensions as that illustrated by Reuss (1863). A

number of Algoa Basin tests show signs of crushing caused by post-depositional

compaction, which tends to accentuate the degree of compression of the test and the

inflation of the chamber margins.

Occurrence

First described by Reuss (1863) from the ‘Speeton Clay’ of northern Germany. Later

records include: Gault Clay (Albian) of Folkestone (Chapman 1894a); latest Berriasian

and Late Hauterivian of the Speeton Clay, Yorkshire (Fletcher 1973); Albian of the Aube

region, France (Magniez-Jannin 1975); Cenomanian Grayson Formation of northern

Texas (Tappan 1940); Late Hauterivian of Neuquén (Musacchio 1979) and the Barremian

Rio Mayer Formation, Santa Cruz Province (Malumian & Nafiez 1983), both of

Argentina; and Portlandian Colchester Member of the Uitenhage Trough, Algoa Basin

(McMillan 1980).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 201

Stratigraphic range in the Sundays River Formation

Rare in the Late Valanginian Biozones Bb and Ba, and in the Late Hauterivian

Biozones VI to I.

Genus Paralingulina Gerke, 1969

Paralingulina hexacarinata (Espitali¢ & Sigal, 1963)

Figs 600-P, 61A

Frondicularia hexacarinata Espitahé & Sigal, 1963: 60, pl. 28 (fig. 3a—b). Beer, 1973: 9. Bertels,

1990; 259, pl. 2 (fig? 19).

Remarks

A distinctive species of Paralingulina characterized by inflated, chevron-shaped

chambers, a bladed peripheral keel, and two sub-peripheral sharply-defined ribs per side.

The sub-peripheral ribs almost merge beneath the proloculus near the apical point of the

test, and again in a distinct manner around the apertural neck. The aperture in well-

preserved specimens 1s an elongate slit set at the top of a short, wide compressed neck.

Neither Espitali¢é & Sigal (1963) nor Bertels (1990) provided details of the nature of the

apertures of their specimens, either written or illustrated, so that their allocation of the

species to Frondicularia cannot be confirmed without examination of their material.

None the less, the distinctive test morphology is more similar to the Paralingulina tenera

(Bornemann) plexus than to typical Frondicularia species. Thus, with some hesitation,

the species is referred to the genus Paralingulina. The specimen illustrated by Bertels

(1990) is rather wider than either those from the Majunga Basin (Espitalié & Sigal 1963)

or the Algoa Basin (present study).

Paralingulina tenera is known from the European Lias (Barnard 1956; Copestake &

| Johnson 1981, 1989; Bartenstein & Brand 1937; Norvang 1957) and a similar form,

_ within the plexus, occurs as late as the Early Oxfordian in Southern Poland (Bielecka

1960). Tests of the P. tenera plexus in general lack inflated chambers, except perhaps for

_ the last-formed one, the proloculus is not especially prominent, the vertical ribs usually

_ fade away over the final chamber, and there is no well-defined apertural neck.

| Bartenstein & Brand (1951: 301, pl. 8 (fig. 194a—b)) recognized Lingulina tenera in

_ the Valanginian of north-west Germany, similar in all respects to the European Liassic

| forms. It is not possible from the descriptions and illustrations given by Bartenstein &

_ Brand to determine if this middle to late Valanginian example can be regarded as

— conspecific with the Southern Hemisphere species P. hexacarinata, although Espitali¢ &

| Sigal (1963: 60) regarded it as ‘without doubt very near, if not identical’.

— Occurrence

: Described from Biozones E and F (Late Valanginian—?Barremian) of the Majunga

_ Basin, Madagascar (Espitalié & Sigal 1963). Bertels (1990) encountered the species in the

_ lower Rio Mayer Formation (Hauterivian) at Lago San Martin, Patagonia, Argentina.

202 ANNALS OF THE SOUTH AFRICAN MUSEUM

Stratigraphic range in the Sundays River Formation

Restricted to the most distal parts of the Upper Sundays River Formation (Late

Hauterivian Biozone III to basal Biozone I). Beer (1973) too reported it from the highest

Sundays River Formation (her Biozone A). The species has not been encountered in South

Africa outside the northern Algoa Basin.

Family Lingulinidae Loeblich & Tappan, 1961

Genus Lingulina @ Orbigny, 1826 s./.

Lingulina trilobita sp. nov.

Figs 61B—F

Lingulina ?denticulocarinata (non Chapman): McLachlan et al. 19766: 358, fig. 13 (no. 5).

Lingulina denticulocarinata (non Chapman): Bertels, 1990: 278, pl. 7 (fig. 10).

Diagnosis

A species of Lingulina distinguished by vertically aligned indentations of the test wall

close to both margins of the test, by horizontal sutures with marked downward-angled

perimeters, and by a narrow, elongate slit-like aperture at the termination of a tapering,

graceful test, often arthropodal in appearance.

Etymology

Adjective, from the morphology of the series of chambers being reminiscent of the

segmental arrangement of a trilobite.

Material

Holotype. MF1506, SOEKOR negative F978 (see McLachlan ef al. (1976b), fig. 13

(no. 5)).

Paratypes (Figs 61B—F). MF1507 to MFI1511, five specimens, SOEKOR negatives

FO/3, F288 )8382. F 309s and h320)

Stratum typicum

Biozone B, Late Valanginian, borehole PB—A1, Pletmos Basin.

Locus typicus

Borehole PB—A1, cuttings sample at | 528 feet.

Description

Test compressed, elongate, with maximum width of test usually at the level of the

penultimate chamber, or the base of the final one. Test graceful, tapering and, in

cross-section, lenticular. Test periphery initially acutely rounded, becoming broad and

rounded; in side view periphery initially straight or weakly curved, becoming a little

lobate in the later part of the test. Chambers arranged in a uniserial, rectilinear sequence,

increasing regularly and steadily in size as added. Initial chambers flush, last-formed

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 203

2-3 chambers weakly inflated. Chambers display marked backward-angled peripheries

throughout the test; chambers initially about three times as wide as high, later slightly

wider than high; up to 10 chambers in the adult test. Sutures distinct throughout,

horizontal, straight, becoming strongly backward-angled towards the test periphery;

initially flush, later becoming weakly depressed. Aperture terminal, centrally placed on

the last-formed chamber; in form an elongate slit, very narrow, aligned parallel to the

plane of compression of the test; test wall inturned, smooth and rounded around the

opening. Surface of test smooth, unornamented for the most part, but with distinct,

vertically aligned indentations on the lower part of each chamber, close to the test

margins, developed on both sides of test. Indentations rise from the marginal change in

angle of each suture, and develop for about three-quarters of the height of each chamber.

In some specimens, a horizontally aligned groove or ‘double suture line’ extends just

above and parallel to the true suture, around the test.

Remarks

| McLachlan et al. (1976b) tentatively referred this species to Lingulina

| denticulocarinata, originally described (as Frondicularia) from the Albian Gault Clay of

Folkestone by Chapman (1894a). Although there is some similarity in the chamber shape

and suture form, L. trilobita lacks the distinctive thorns ranged along the test margin of

_ Chapman ’s species, and its aperture 1s never produced ona slight development of the final

| chamber. Magniez-Jannin (1975: 220, pl. 12 (fig. 17—18)) illustrated L. denticulocarinata

_ from the Albian of the Aube region, France; these specimens are a little different from that

_ figured by Chapman from Folkestone, particularly in the form of the sutures, but the

| peripheral thorns are well developed.

— Occurrence

| Re-examination of the PB—Al foraminifera first described by McLachlan et al.

- (1976b) has shown that L. trilobita is present in Biozone B in the Late Valanginian, and in

_ Biozones IV and III in the Late Hauterivian. The species occurs only rarely in the Late

_ Valanginian and Hauterivian of the offshore Pletmos, Gamtoos and Algoa basins, South

_ Africa. It also occurs in the Hauterivian lower Rio Mayer Formation of southern

_ Argentina (Bertels 1990).

Stratigraphic range in the Sundays River Formation

| Early to Late Hauterivian (Biozones X to earliest I). It appears to avoid

| the oxygen-poor environments of the Late Valanginian in the Sundays River Trough.

. Lingulina trilobita ranges from the inner to outermost shelf, but avoids all marginal

- marine facies.

ANNALS OF THE SOUTH AFRICAN MUSEUM

204

Figure 61:

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 205

Lingulina bettenstaedti (Zedler, 1961)

Figs 61G—H, N

Frondicularia bettenstaedti Zedler, 1961: 44, pl. 8 (figs 21a—b, 22a—b), text-fig. 5.

Lingulina bettenstaedti (Zedler). McLachlan et al., 1976a: 331, fig. 16 (no. 25). Kielbowicz et al.,

19833332 pl. 2(fie: 4).

~ Remarks

The interpretation and differentiation of this species from Lingulina simplicissima

(Ten Dam) is based essentially on the comments and illustrations given by Zedler (1961).

She separated L. bettenstaedti on the basis of its more numerous, lower chambers, its

arched, poorly chevron-shaped chambers, and its weakly lobate test margins. The

| majority of the specimens referable to this species from the Sundays River Formation

display rather stronger, backward-curving chambers than is typical in the north-west

- German tests, as shown in Figure 61G. Occasional specimens (e.g. Fig. 61N) possess

rather more broadly rounded sutures, and these forms seem to be morphologically closer

— to the European tests.

~ Occurrence

Originally described from the Hildesiense-zone of the middle Late Hauterivian of

north-west Germany (Zedler 1961); later records are sparse: Late Valanginian

_ (Biozone B) of the Mngazana Basin (McLachlan ef a/. 1976a), and the Valanginian

_ Springhill Formation of southern Patagonia, Argentina (Kielbowicz et al. 1983).

_ Stratigraphic range in the Sundays River Formation

Very occasional specimens occur in the Late Valanginian and Late Hauterivian

_ (Biozones Ba, A, VII, HI) but are insufficient to determine the full stratigraphic range.

Fig. 61 (see facing page). A. Paralingulina hexacarinata (Espitali¢ & Sigal). SAM—PQ—MF 1505, side

view, AL 1/69, 520 feet (1), F127. X 98. B-F. Lingulina trilobita sp. nov. B. Paratype, SAM—

PQ—MF 1507, side view, shallow borehole SB—15, core 2, 210 feet (II), F673. X 110. C. Paratype,

SAM—PQ—MF1508, side view, AL 1/69, 1 000 feet (II), F288. x 112. D. Paratype, SAM—PQ-

MF1509, side view, AL 1/69, 1 480 feet (IV), F382. X 111. E. Paratype, SAM—PQ-—MF1510, side

view, AL 1/69, 1 030 feet (III), F309. x 143. F. Paratype, SAM—PQ—MF1511, apertural view,

AL 1/69, 1 090 feet (III), F329. x 320. G—-H, N. Lingulina bettenstaedti (Zedler).

G. SAM—PQ-MF1512, side view, CO 1/67, 915 feet (VII), F149. x 123. H. SAM—PQ-—MF1513,

apertural view, shallow borehole SB—9A, core 1, 282 feet 6 inches (II), F670. x 430.

N. SAM—PQ-MF1514, side view, MV 1/79, 240-250 m (A), F618. X 167. I-K. Lingulina

praelonga Ten Dam. I. SAM—PQ—MF 1515, side view, Coega Brick Pits outcrop sample 11988 (Bb),

F154. x 102. J. SAM—PQ—MF1516, side view, Coega Brick Pits outcrop sample 11988 (Bb), F155.

xX 121. K. SAM—PQ-MF1517, side view, shallow borehole SB—9A, core 1, 282 feet 6 inches (II),

F668. X 135. L—M. Lingulina simplicissima (Ten Dam). L. SAM—PQ—MF1518, side view, shallow

borehole SB—9A, core 1, 282 feet 6 inches (II), F672. 171. M. SAM—PQ-MF1519, side view,

shallow borehole SB—9A, core 1, 282 feet 6 inches (II), F669. x 126.

206 ANNALS OF THE SOUTH AFRICAN MUSEUM

Lingulina praelonga Ten Dam, 1946

Figs 61I-K

Lingulina praelonga Ten Dam, 1946: 576, pl. 88 (fig. 12a—b); 1948: 183. Espitalié & Sigal, 1963:

Gl ple2s Gigs 9).

Remarks

A small number of specimens appear referable to Ten Dam’s species, but they are

distinguished by possessing rather more broadly rounded margins to the test than is

typical. Tests studied exhibit up to nine chambers. The sutures are either low arched

(Fig. 611), more rounded (Fig. 61J), or more chevron-shaped (Fig. 61K). In terms of the

sutural shape, the specimen in Figure 61K seems closest to Ten Dam’s original illustrated

specimen. The South African examples do usually feature an ovate proloculus, as noted

by Ten Dam (1946).

Occurrence

First described from the Hauterivian of the Netherlands (Ten Dam 1946, 1948). One of

the few additional records to the species is that of Espitalié & Sigal (1963), from the Late

Portlandian to Early Valanginian (Cenozone D) of the Majunga Basin, Madagascar.

Stratigraphic range in the Sundays River Formation

Rare examples occur in the Late Valanginian (Biozones Bb and Ba) and in the Late

Hauterivian (Biozones VI to IT). Because of the thin elongate test, with depressed sutures,

it is probable that many specimens are damaged or destroyed in sample processing, and

that broken fragments are perhaps referred to other species, particularly L. simplicissima

(Ten Dam).

Lingulina simplicissima (Ten Dam, 1946)

Figs 61L—M

Frondicularia simplicissima Ten Dam, 1946: 576, pl. 88 (fig. 1 la—b). Bartenstein, 1956: 519, pl. 2

(fig. 39). Zedler, 1961: 45, pl. 8 (figs 23a—b, 24a—b, 25a—b, 26a—b, 27a—b), text-fig. 6.

Bartenstein & Kaever, 1973: 228, pl. 3 (fig. 45). Kielbowicz et al., 1983: 324, pl. 2 (fig. 5). Lott

et al., 1986: 44, fig. SD-E.

Lingulina simplicissima (Ten Dam). McLachlan et al., 1976b: 358, fig. 13 (nos 3-4). Simeon,

1985220 ol. Giese)

Remarks

The specimens illustrated by Zedler (1961) from the German Hauterivian possess an

elongate-ovate to slit-like aperture. Unfortunately, the original description and

illustrations given by Ten Dam (1946) provide no indication (slit-like or circular) of the

style of the aperture. This has led to allocations to either Frondicularia or Lingulina by

various authors. Zedler’s (1961) interpretation of the species has been followed here, and

for this reason, it is referred to Lingulina. Features that distinguish L. simplicissima from

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 207

the similar L. bettenstaedti (Zedler) are the generally lobate test periphery and the

- distinctly chevron-shaped chambers, but gradations of these characters are evident in the

_ Sundays River tests, indicating that the two species are very closely related.

| Occurrence

Widespread in the Hauterivian of north-west Europe (Ten Dam 1946, 1948;

- Bartenstein 1956; Bartenstein & Kaever 1973; Lott et a/. 1986); in Argentina known from

the latest Valanginian to Early Hauterivian of the Agrio Formation, Neuquén (Simeoni

1985) and the Valanginian Springhill Formation of southern Patagonia (Kielbowicz et al.

1983). Re-examination of the foraminifera of Pletmos Basin borehole PB—A1 (see

~ McLachlan et al. 19766) shows it to range from Late Valanginian Biozone B to Late

Hauterivian Biozone III.

_ Stratigraphic range in the Sundays River Formation

~ Occasional examples occur in the Late Valanginian Biozones Bb and Ba, and in the

_ Late Hauterivian Biozones VII to I. The full range is certainly greater than this suggests.

Lingulina mngazanaensis sp. nov.

Figs 62B-I

| Lingulina sp. McLachlan et al., 1976a: 333, fig. 16 (no. 26).

| Lingulina sp. B Riegraf, 1989: 1054, pl. 1 (fig. 12).

Diagnosis

A species of Lingulina distinguished by rapid increase in chamber size, inflated

_ chambers, ovate cross-section to the test, an elongate, slit-like aperture of variable length,

and very weakly arched sutures.

| Etymology

| From its first record in the Mngazana Basin of the Transkei, South Africa.

- Material

~ Holotype (Fig. 621). MF1527, SOEKOR negative F613.

Paratypes (Figs 62B—H). MF1520 to MF1526, seven specimens, SOEKOR negatives

F303, F432, F474, F681, F336, F273, and F593.

_ Stratum typicum

Biozone X, Early Hauterivian, Sundays River Formation.

_ Locus typicus

Borehole MV 1/79, cuttings sample 200-210 m.

208 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 62.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 209

Description

Test lightly compressed, elongate but rather squat, with maximum width at the level of

_ the last-formed chamber or the penultimate one. In cross-section, test ovate, with broad

rounded margins. Test periphery lobate, especially in the later part of the test. Chambers

: arranged in a uniserial, rectilinear sequence, increasing rapidly in size in the early part of

the test, later more slowly, as added. Proloculus globular, occasionally prominent, with

the following chambers flush, becoming distinctly inflated in the later part of the test.

Juvenile chambers usually about twice as wide as high, later becoming about

- one-and-a-half times as wide as high, although significant variations occur, even in the

same test; up to eight chambers in adult tests. Sutures initially flush, indistinct, later

distinct, depressed, varying from almost horizontal to weakly and uniformly arched.

_ Aperture terminal, centrally sited, orientated parallel to the plane of compression of the

test; in form, an elongate narrow slit of variable length, with the test wall incurved along

_ the margin of the opening. Surface of test smooth, unornamented.

_ Remarks

Tests assigned to this species from the Sundays River Formation and the Mngazana

Formation appear to constitute a plexus that cannot be easily divided. The typical form of

_ the group is regarded as that illustrated by McLachlan er al. (1976a, fig. 16 (no. 26)), and

_as Figure 62C, E-F and I in the present study.

No previously recorded Early Cretaceous species of Lingulina 1s characterized by such

_ arapid increase in chamber size, by inflated chambers and by an ovate cross-section to the

_ test. The specimen illustrated as Figure 62G shows some similarity to Lingulina sp. 2824

of Espitali¢ & Sigal (1963, pl. 28 (fig. 8)) from the Kimmeridgian to Early Portlandian

-(Cenozone C) of the Majunga Basin, but this is rather atypical for L. mngazanaensis.

There is also some similarity between L. mngazanaensis and Lingulina sp. 3 of

Bartenstein & Brand (1951, pl. 8 (fig. 193a—b)), but it differs in its inflated chambers,

_lobate test periphery and more rapid increase in test size 1n the early part of the test. Some

Fig. 62 (see facing page). A, J. Lingulina spp. A. SAM—PQ—MF1531, side view, AL 1/69, 520 feet (1),

F124. x 115. J. SAM—PQ-MF1532, side view, MV 1/79, 240-250 m (A), F625. X 137. B—-I. Lingulina

mngazanaensis sp. nov. B. Paratype, SAM—PQ—MF 1520, side view, AL 1/69, 1 000 feet (III),

F303. X 176. C. Paratype, SAM—PQ-MF1521, side view, AL 1/69, 1 570 feet (VI), F432. x 172.

D. Paratype, SAM—PQ-—MF 1522, side view, AL 1/69, 1 960 feet (VII), F474. x 177. E. Paratype,

SAM-—PQ-MF1523, side view, shallow borehole SB—15, core 3, 215 feet (II), F681. x 102.

F. Paratype, SAM—PQ—MF 1524, side view, AL 1/69, 1 120 feet (III), F336. x 176. G. Paratype,

SAM-—PQ-MF1525, side view, AL 1/69, 940 feet (IID), F273. x 151. H. Paratype, SAM—PQ-

MF 1526, side view, MV 1/79, 160 m (X), F593. X 175. I. Holotype, SAM—PQ—MF 1527, side view,

MV 1/79, 200-210 m (X), F613. X 167. K. Lingulina sp. A, SAM—PQ—MF 1528, side view, Coega

Brick Pits outcrop sample 11988 (Bb), F153. x 73. L—M. Lingulina cf. L. furcillata Berthelin.

L. SAM—PQ—-MF 1529, side view, AL 1/69, 460 feet (I), F110. x 112. M. SAM-—PQ-MF1530, side

view, shallow borehole SB—15, core 4, 229 feet (II), F687. x 113. N—-O. Eoguttulina anglica

Cushman & Ozawa s./. N. SAM—PQ-MF1533, side view, AL 1/69, 670 feet (II), F206. x 123.

O. SAM—PQ-MF 1534, side view, AL 1/69, 790 feet (III), F257. < 77.

210 ANNALS OF THE SOUTH AFRICAN MUSEUM

of the shells of LZ. furcillata Berthelin illustrated by Magniez-Jannin (1975, text-fig. 113)

are also close to this species, but again the South African tests develop more inflated

chambers and a more lobate periphery. :

Occurrence

Late Valanginian Biozone B of the Mngazana Basin, Transkei (McLachlan et al.

1976a), and Barremian (not Valanginian—Hauterivian) of DSDP site 249, Mozambique

Ridge, Indian Ocean (Riegraf 1989). Occasional specimens also occur in the Valanginian-

Hauterivian of the offshore Gamtoos and Algoa basins, but L. mngazanaensis is absent in

the offshore Pletmos Basin.

Stratigraphic range in the Sundays River Formation

Late Valanginian to Late Hauterivian Biozones Bb to II. Widespread, but always rare,

and only very occasional tests occur in the Early Hauterivian.

Lingulina sp. A

Fig. 62K

Remarks

A single specimen from Biozone Bb, Late Valanginian of the Coega Brick Pits outcrop.

It shows some similarity to the specimens incorrectly allocated to Lingulina loryi

(Berthelin) by McLachlan et al. (19765, fig. 13 (nos 1—2)), from the early Late Valanginian

Brenton Formation, and probably caved from the same stratum in borehole PB—A1.

The Sundays River Formation test differs from the Brenton and PB—A1 species 1n its

more inflated chambers and correspondingly depressed sutures. The aperture is ovate,

rather intermediate between the accepted aperture outline of Lingulina (a slit) and of

Frondicularia (circular).

As a supplementary note on the Brenton/PB—A1 species, it may be added here that

these South African specimens are distinct from true Albian Lingulina loryi (see

Magniez-Jannin 1975: 219, pl. 12 (fig. 16)) in their wider, more squat, and more

compressed test, generally flush sutures, the occasional vertically aligned short ribs

developed peripherally in the early part of the test, and the broad-bladed peripheral keel.

The Brenton/PB—A1 species appears to be new, and it is hoped to formally describe it in a

future re-examination of the Brenton foraminifera.

Lingulina cf. L. furcillata Berthelin, 1880

Figs 62L—M

see Lingulina furcillata Berthelin, 1880: 65, pl. 4 (fig. 6a—c). Said & Barakat, 1957: 43, pl. 1

(fig. 10-11).

Remarks

Two specimens with low-arched, depressed sutures, inflated chambers, and a narrow

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 211

elongate aperture. These tests lack the backward curving peripheries to the chambers of

Berthelin’s illustrated test, and the sutures of the South African examples are not as

strongly and evenly curved. The two illustrated tests are from Biozones II and I, later Late

Hauterivian.

Lingulina spp.

Figs 62A, J

Remarks

Occasional tests of Lingulina that lie outside the limits of the species described above,

and are poorly preserved or broken, have been allocated here. Lingulina tests tend to be

thin-walled and particularly prone to corrosion damage induced by deterioration of pyrite

infillings within chamber cavities. The specimen illustrated as Figure 62A lacks the

vertically aligned peripheral indentations over the sutures that are typical of Lingulina

trilobita sp. nov., aS well as possessing more regularly arched sutures, markedly inflated

chambers throughout the test and a rather wider test than 1s typical of that species.

Family Polymorphinidae d’Orbigny, 1839

Subfamily Polymorphininae d’Orbigny, 1839

Genus Eoguttulina Cushman & Ozawa, 1930

Eoguttulina anglica Cushman & Ozawa, 1930 s./.

Figs 62N—O, 64A—B

Eoguttulina anglica Cushman & Ozawa, 1930: 16, pl. 1 (fig. 3a—c). McLachlan et al., 1976a: 333,

fig. 16 (no. 28). Musacchio, 1979: 258, pl. 4 (fig. 24).

Remarks

This 1s the commonest and most conservative species of Eoguttulina in the Late

Jurassic and Early Cretaceous of South Africa. Its full range in the South African offshore

basins is probably Kimmeridgian to Early Aptian. A range of morphologies is evident in

the Sundays River tests but, in general, maximum test width is below mid-height,

indicating rather embracing and overlapping later chambers, the chambers are moderately

inflated, and the sutures correspondingly depressed and distinct for most of the test. The

chambers of the holotype (Cushman & Ozawa 1930; refigured by Loeblich & Tappan

1964, fig. 415 (no. 2a—c)) are more uniformly inflated and more pyriform than those seen

in the South African tests, and the initial chamber is of a distinctly larger size. Because of

these differences, and because of the variation in the South African tests, it seems wisest to

regard this species sensu lato in its usage here.

Occurrence

Described by Cushman & Ozawa (1930) from the Cambridge Greensand (earliest

Cenomanian) of England. Subsequent records include: Hauterivian (Ten Dam 1948) and

Albian (Ten Dam 1950) of the Netherlands; Albian of Romania (Neagu 1965);

Kimmeridgian (Lloyd 1962) of England; Valanginian—Hauterivian Pampa Rincon

ZZ ANNALS OF THE SOUTH AFRICAN MUSEUM

Formation (Malumian & Masiuk 1975) and Late Hauterivian of Neuquén (Musacchio

1979), Argentina; and Late Valanginian Biozone B of the Mngazana Basin, Transkei

(McLachlan et al. 1976a).

Stratigraphic range in the Sundays River Formation

Ranges throughout the sequence, Biozone C to Biozone I. The species is often most —

frequent in rather poorly oxygenated environments where agglutinated foraminifera

predominate and few other calcareous foraminifera occur. Its environmental range is |

innermost shelf to slope, but it is absent in littoral, high-energy environments and —

hyposaline, estuarine conditions.

Eoguttulina cf. E. inovroclaviensis (Bielecka & Pozaryski, 1954)

Figs 63A—C

see Sigmomorphina inovroclaviensis Bielecka & Pozaryski, 1954: 63, 192, pl. 9 (fig. 47a—c).

Foguttulina cf. inovroclaviensis (Bielecka & Pozaryski). McLachlan et al., 1976a: 333, fig. 17

(no; 1):

non Eoguttulina cf. inovroclaviensis (non Bielecka & Pozaryski) McLachlan et al., 1976b: 358,

fig 3 (mo, 9).

Remarks

One or two specimens compare closely to the test illustrated by McLachlan ef al.

(1976a), in their strongly lobate margins and abrupt basal terminations to the later

chambers. Such differences enable them to be easily distinguished from Loguttulina

anglica Cushman & Ozawa s.l. The later chambers of South African Eoguttulina cf.

E. inovroclaviensis are rather narrow and elongate. Because of poor preservation, the

chamber arrangement of the early part of the tests is often obscured or obliterated, so that

they are referred to Bielecka & Pozaryski’s species with great reservations.

Occurrence

First described from the Kimmeridgian to Portlandian of Poland (Bielecka & Pozaryski

1954). Later records include Kimmeridgian of England (Lloyd 1962). The similar South

African forms occur in the Late Valanginian Biozone B of the Mngazana Basin (McLachlan

et al. 1976a). These have also been found, very rarely, in the offshore Gamtoos and Algoa

basins in the Valanginian, but appear to be absent everywhere in the generally

shallower-water environments of the Valanginian succession of the Pletmos Basin.

Stratigraphic range in the Sundays River Formation

Confined to the Late Hauterivian (Biozones VI to II). There are signs that the species

prefers outer-shelf environments, and it is never found in shallow or marginal marine

conditions, but too few specimens are available to determine its full range. In contrast, in

the Colchester Member of the Uitenhage Trough, Eoguttulina cf. E. inovroclaviensis 1s

found in shallow marine facies (McMillan 1980).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 213

Figure 63.

Eoguttulina cf. E. inovroclaviensis (Bielecka & Pozaryski). A—B. Side views. C. Apertural

view. All SAM—PQ—MF1537, AL 1/69, 940 feet, (III). x 135.

Eoguttulina cf. E. liassica (Strickland, 1846)

Figs 64C—E

see Polymorphina liassica Strickland, 1846: 31, text-fig. b.

_ see Eoguttulina liassica (Strickland). Lloyd, 1962: 370, pl. 1 (figs la—d, 2a—c, 3a—c), text-fig. 2.

Winter, 1970: 39, pl. 4 (fig. 135).

_ Eoguttulina cf. liassica (Strickland). McLachlan et al., 1976a: 333, fig. 16 (no. 27).

| non Foguttulina cf. liassica (Strickland): McLachlan et al., 19766: 358, fig. 13 (no. 8).

_ Remarks

| South African specimens from the Valanginian and Hauterivian compare closely with

the more globular, megalospheric tests illustrated by Lloyd (1962) from the English

-~Kimmeridge Clay. Lloyd has shown in detail the variation of this plexus in the

Kimmeridgian, but it is clear that his interpretation of the species is wider than accepted

by most authors, who have followed Strickland’s (1846) original illustration more

closely. Forms similar to Strickland’s example are scarcely distinguishable from

Foguttulina anglica Cushman & Ozawa.

| It is not clear whether the South African specimens are properly referable to

_ Eoguttulina liassica, bearing in mind the differences in authors’ interpretations of the

species, so for the time being they have been referred to Eoguttulina cf. E. liassica.

Occurrence

Widespread in the Jurassic of north-west Europe.

Stratigraphic range in the Sundays River Formation

| Eoguttulina cf. E. liassica occurs in small numbers from the Late Valanginian

_ Biozone Bb to Late Hauterivian Biozone I.

214 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 64.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION ZU)

Eoguttulina cf. E. polygona (Terquem, 1864)

Figs 64F—G

see Polymorphina polygona Terquem, 1864: 305, pl. 14 (figs 16, 19-21, 23a—b, 35, 39).

— see Eoguttulina polygona (Terquem). Lloyd, 1962: 372, pl. 1 (fig. 4a—c), text-fig. 3.

Remarks

Small numbers of tests show the elongate shell and distinctive chamber arrangement

characterized by slight overlap that are typical of Jurassic Eoguttulina polygona. Too few tests

have been obtained to permit detailed analysis of the form in the Sundays River Formation.

Stratigraphic range in the Sundays River Formation

Confined to the latest Valanginian and Early Hauterivian (Biozones A to IX) of the

- most distal borehole intersections.

Eoguttulina sp. B

Figs 64H-I

Remarks

An elongate, fusiform, large-sized species of Eoguttulina, with weakly depressed

_ sutures and strongly overlapping chambers, that shows some resemblance to Eoguttulina

_oolithica (Terquem). The Algoa Basin tests differ from that species, however, in

possessing rather less-overlapping chambers than is typical (see Lloyd 1962, pl. |

_ (fig. 8a—c), text-fig. 5). The Sundays River Formation tests are easily distinguished from

other species of the genus, initially on the size of the test and, although often crushed

(Fig. 641) or otherwise damaged, the species occurs widely enough to warrant its use as a

_ zone marker in a part of the Sundays River sequence that is difficult to subdivide.

Stratigraphic range in the Sundays River Formation

Late Valanginian to Early Hauterivian (Biozones C to IX).

Fig. 64 (see facing page). A-B. Eoguttulina anglica Cushman & Ozawa s./. A. SAM—PQ-—MF1535,

side view, AL 1/69, 2 710 feet (IX), F522. x 166. B. SAM—PQ—MF1536, side view, AL 1/69,

2 710 feet (IX), F523. x 124. C-E. Eoguttulina cf. E. liassica (Strickland). C. SAM—PQ—MF 1538,

side view, AL 1/69, 3 450 feet (X), F538. 173. D. SAM—-PQ—MF1539, side view, AL 1/69,

1 540 feet (VI), F418. x 173. E. SAM—PQ-MF1540, side view, AL 1/69, 520 feet (I), F122. x 160.

F-G. Eoguttulina cf. E. polygona (Terquem). F. SAM—PQ—MF1541, side view, MV 1/79, 90 m (X),

F573. x 114.G. SAM—PQ-MF1542, side view, MV 1/79, 90 m (X), F575. X 142. H—I. Eoguttulina

sp. B. H. SAM—PQ—MF 1543, side view, MV 1/79, 90 m (X), F580. x 72. I. SAM—PQ-MF 1544,

side view, MV 1/79, 200-210 m (X), F610. xX 78. J-N. Globulina prisca Reuss s.l.

J. SAM—PQ-MF1545, side view, Zoetgeneugd Cliff outcrop sample 11452 (C), F255. x 137.

K. SAM—PQ-MF1546, side view, AL 1/69, 1 480 feet (IV), F391. x 128. L. SAM—PQ— MF1547,

side view, AL 1/69, 490 feet (I), F115. x 164. M. SAM—PQ—MF1548, side view, MV 1/79, 20 m

(IX), F568. x 140. N. SAM—PQ-MF1549, side view, AL 1/69, | 480 feet (IV), F389. x 148.

216 ANNALS OF THE SOUTH AFRICAN MUSEUM

Genus Globulina d’Orbigny, 1839

Globulina prisca Reuss, 1863 s.1.

Figs 64J—N

Polymorphina (Globulina) prisca Reuss, 1863: 79, pl. 9 (fig. 8a—b).

Globulina prisca Reuss. Beer, 1970: 18, pl. 3 (fig. 8a—b). McLachlan et al., 1976a: 333, fig. 17

(no. 2); 1976b: 358, fig. 13 (nos 6—7). Stapleton & Beer, 1977: 2, pl. 3 (fig. 14a—b). Malumian &

Nafiez, 1983: 379, pl. 1 (figs 19-20). Bertels, 1990: 278, pl. 7 (fig. 12).

Remarks

Tests from South Africa possess rather broader, rounded apical ends, with maximum

width of test in the lower half, than was originally illustrated by Reuss (1863). The acute

apical termination of the test figured in Figure 64K 1s atypical.

Occurrence

Widely reported from the Early Cretaceous. First described from the upper Hils Clays

(Barremian to Early Aptian) and the Minimus Clays (Late Albian) of northern Germany |

(Reuss 1863). Later records include: Late Valanginian Biozone B of the Mngazana Basin, |

Transkei (McLachlan ef al. 1976a), earliest Late Valanginian (Biozone D) of the Brenton |

Formation (McLachlan et al. 1976b; Stapleton & Beer 1977), and the Late Valanginian |

(Biozones B and A) of Pletmos Basin borehole PB—A1 (McLachlan et al. 19766). The

species 1s widespread in South Africa, ranging at least from the Portlandian to the Early

Aptian.

Stratigraphic range in the Sundays River Formation

Occurs in small, variable numbers throughout the sequence, from Biozones D tol. The |

species tolerates a wide range of environments, from innermost shelf to upper slope,

including those with reduced oxygen conditions on the sea-floor, but is absent from |

hyposaline locations.

Genus Pseudopolymorphina Cushman & Ozawa, 1928

Pseudopolymorphina colchesterensis sp. nov.

Figs 65A—H

Diagnosis

A species of Pseudopolymorphina distinguished by a compressed test with a broad,

rounded periphery, flush to weakly depressed sutures, and a smooth, unornamented test

surface.

Etymology

From its abundance at several horizons in the Colchester Cliff outcrop, close to

Colchester railway halt.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 217

Material

Holotype (Fig. 65E). SAM—1554; SOEKOR negative F350.

Paratyoes (rie. 65A—D;, F, Gi). MFI550 to MF1553, MF1555, MF1556, six

specimens, SOEKOR negatives F706, F709, F708, F705, F343, and F344/F345.

Stratum typicum

Biozone IV, Late Hauterivian, Sundays River Formation.

Locus typicus

Borehole AL 1/69, cuttings sample at | 240 feet.

Description

Test compressed, elongate, with maximum width at the level of the final pair of

chambers. Maximum depth of test, in initial portion, close to proloculus. In cross-section,

adult portion of test elongate-ovate, with broad rounded margins and roughly parallel

sides. Test periphery initially continuous, straight or weakly convex, later distinctly lobate

in megalospheric tests; continuous and straight or slightly convex in microspheric tests.

Chambers initially arranged in a polymorphinid manner, about four in number; later

chambers biserially arranged, attaining up to four pairs. Chambers increase slowly and

steadily in size as added, becoming about as wide as high in megalospheric tests and

almost twice as wide as high in microspheric tests in the final part. Sutures initially flush,

indistinct, becoming distinct and depressed, especially in megalospheric tests; declining

at an angle of about forty-five degrees to the horizontal in the adult portion, straight to

slightly curved. Aperture terminal, sited at the apical point of the last-formed chamber:

radiate in form, composed of about 18 narrow slits that occasionally merge to form larger,

more irregular openings. Apical point of test broad, rounded, unornamented. Surface of

test smooth, unornamented.

Remarks

Two major types of test can be recognized, which appear to be referable to the

megalospheric (Fig. 65A—C) and microspheric (Fig. 65D—G) generations. Pseudo-

polymorphina_ colchesterensis lacks the peripheral keel and apical spine of both

P. martinezi (Canon & Ernst), described from the Esperanzian and Rinconian (?Oxfordian

to Hauterivian) of the Magallanes Basin of southernmost Chile (see Cafion & Ernst 1974:

75, pl. 2 (fig. 8a—b); Malumian & Masiuk 1975: 594, pl. 1 (fig. 2a—c), pl. 2 (fig. 1)), and of

the informal species P. ‘carinata’, present in the Early Barremian of South Africa (see

‘Introduction’ on DSDP site 249, p. 24).

Pseudopolymorphina_ roanokensis, described by Tappan (1940) from the

mid-Cenomanian Grayson Formation of Texas, tends to become uniserial in the final part

of the test, a feature not seen in the Sundays River species. The test outline of

Pseudopolymorphina sp. from the Valanginian—Hauterivian Pampa Rincon Formation

(Malumian & Masiuk 1975, pl. 2 (fig. 2)) of Argentina is different from that of

P. colchesterensis.

218 ANNALS OF THE SOUTH AFRICAN MUSEUM

ae Brut

Figure 65.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 219

Although not reported by McLachlan ef al. (1976b), P. colchesterensis occurs in

-Pletmos Basin borehole PB—A1, and aids in correlating the Hauterivian sequences of the

Pletmos and Algoa basins. It ranges there through the Late Hauterivian Biozone IV, and

possibly into the top of Biozone V.

Stratigraphic range in the Sundays River Formation

Apparently confined to the Late Hauterivian Biozone IV, where it often occurs in

considerable numbers. Typical of inner- to outer-shelf conditions, and seems to be able to

tolerate some reduction in salinity, as it occurs in the top of the NA 3/70 section.

Genus Pyrulina d@ Orbigny, 1839

Pyrulina cylindroides (Roemer, 1838)

Figs 66C—D

Polymorphina cylindroides Roemer, 1838: 385, pl. 3 (fig. 26).

Pyrulina cylindroides (Roemer). Tappan, 1940: 114, pl. 18 (fig. la-c). Dailey, 1973: 71, pl. 10

(fig. 11). McLachlan et al., 1976a: 333, fig. 17 (no. 4).

Remarks

Rare specimens occur in the Sundays River Formation that are strongly fusiform, with

the two last-formed chambers generally occupying most of the test. They are more

elongate and narrower than the examples illustrated by Tappan (1940) and are closer to

the test figured by Dailey (1973). It is difficult to determine how genetically close these

Early Cretaceous individuals are to the original form described by Roemer (1838), which

_was from the Cainozoic of northern Germany. The degree of chamber overlap in authors’

illustrations often differs greatly from that of the type illustration. For these reasons, no

worldwide distribution of this species in the Early Cretaceous is given here, since it is

clear the ‘species’ warrants a detailed investigation.

Fig. 65 (see facing page). A-H. Pseudopolymorphina colchesterensis sp. nov. A. Paratype,

SAM—PQ-—MF1550, side view, Colchester Cliff outcrop sample 12001 (IV), F706. x 44.

B. Paratype, SAM—PQ—MF1551, side view, Colchester Cliff outcrop sample 12001, (IV), F709. x

>. C. Paratype, SAM—PQ—MF1552, side view, Colchester Cliff outcrop sample 12001 (IV),

F708. X 55. D. Paratype, SAM—PQ—MF1553, side view, Colchester Cliff outcrop sample 12001

(IV), F705. x 54. E. Holotype, SAM—PQ-—MF 1554, side view, AL 1/69, 1 240 feet (IV), F350. x 57.

F. Paratype, SAM—PQ-—MF1555, side view, AL 1/69, 1 210 feet (IV), F343. x 73. G. Paratype,

SAM—PQ-—MF 1556, apertural view, AL 1/69, 1 210 feet (IV), F344. x 127. H. SAM—PQ—MF1556,

close-up of aperture of G, F345. xX 521. I-J. Webbinella subhemisphaerica Franke. I. SAM—PQ-—

MF1559, free test, AL 1/69, 520 feet (1), F193. x 45. J. SAM—PQ—MF1560, free test, AL 1/69,

460 feet (1), FI08. x 64. K—L. Bullopora laevis (Sollas). K. SAM-PQ—MF1561, attached to

Ammobaculites subaequalis fragment, shallow borehole SB—32, core 2, 2 feet below ?top (IV),

F698. X 67. L. SAM—PQ-MF1562, attached to Ammobaculites subaequalis, AL 1/69, 1 540 feet

(VI), F404. x 31.

ANNALS OF THE SOUTH AFRICAN MUSEUM

Stratigraphic range in the Sundays River Formation

Apparently confined to the early Late Hauterivian (Biozones VII and VI).

Subfamily Webbinellinae Rhumbler, 1904

Genus Webbinella Rhumbler, 1904

Webbinella subhemisphaerica Franke, 1936

Fig. 65I-J

Webbinella subhemisphaerica Franke, 1936: 11, pl. 1 (fig. 4). McLachlan et al., 1976a: 333, fig. 17 _

(no. 5); 1976b: 359; fig. 13 (no. 10), Kielbowiez er al 19832 333, pl. 3 Gigs)!

Remarks |

Similarities to and differences from other closely related genera are given in the ~

emended description of Webbinella by Loeblich & Tappan (1957: 226). In the South —

polymorphinid portion of the test and the final flanged chamber. The final chamber is

often severely damaged. All South African tests recognized so far, including those of

McLachlan et al. (1976a), with the single exception of that illustrated by McLachlan et al.

(19765, fig. 13 (no. 10)), are found separated from the surface to which they were attached —

in life. The single exception, from borehole PB—A1, is attached to a shard of oyster shell.

Haynes (1981: 181, 198) considered the genera Webbinella, Bullopora and Ramulina —

to be ‘form genera’, reflecting possible growth stages in much the same way as fistulose

growth chambers occur in some adult polymorphinids. Haynes regarded Webbinella as an —

attachment form produced by different polymorphinids. However, little difference can be —

seen in the initial chamber arrangement of South African examples, most of which would —

probably be assigned to Eoguttulina species if the final flanged chamber was absent. The —

three genera are here regarded as formal taxonomic units, bearing in mind that other ‘form —

genera’ have had a long and respectable taxonomic history (Orbulina, Tretomphalus).

Occurrence |

Described from the Lias of northern Germany (Franke 1936). Southern Hemisphere —

records include: Valanginian Springhill Formation of southern Patagonia, Argentina ~

(Kielbowicz et al. 1983); Late Valanginian (Biozones B and A) of Pletmos Basin borehole —

PB-—A1 (McLachlan et al. 19766) and Late Valanginian (Biozone B) of the Mngazana —

Basin, Transkei (McLachlan ef a/. 1976a), as well as the Portlandian Colchester Member —

of the Uitenhage Trough (McMillan 1980). In the southern offshore basins, —

W. subhemisphaerica ranges from Portlandian to Hauterivian, but it is always rare and is

of no clear biostratigraphical value through the period.

Stratigraphic range in the Sundays River Formation

Occasional specimens occur from the Late Valanginian Biozone Bb to the Late —

Hauterivian Biozone I. It may prove to be associated with shell accumulations of the —

middle and outer shelf: it is usually absent closer to shore.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 221

Genus Bullopora Quenstedt, 1856

Bullopora laevis (Sollas, 1877)

Figs 65K—L, 66A—B

| Webbina laevis Sollas, 1877: 103, pl. 6 (fig. 1-3).

Vitriwebbina laevis (Sollas). Chapman, 1896b: 585, pl. 12 (fig. 12).

Bullopora laevis (Sollas). Tappan, 1940: 115, pl. 18 (fig. 6).

Remarks

Much confusion has existed over Bullopora laevis in the past, as authors subsequent to

_Sollas (1877) have included several different attached forms under this name. Adams

| (1962: 153-155) gave detailed comments on the genus Bullopora, regarded by him as

| possessing a ?radial hyaline test wall, which is ‘adherent, consisting of a linear or

' curvilinear series of chambers that are variable in shape but commonly subglobular or

_pyriform. Proloculus separate from, or partially embraced by, the second chamber. There

is no initial coil. Wall calcareous, vitreous in appearance when well preserved, probably

perforate; in thin section showing its radiate fibrous structure’. It is evident that poly-

'morphinid forms with a final spreading chamber (vide Bullopora cf. laevis of Bartenstein

| & Brand 1951, pl. 11 (figs 303a—b and 304a—b)) should be transferred to Webbinella.

) The morphology of the chambers of Sundays River Formation tests compare well with

the illustrated specimens of Sollas (1877). Chambers vary from circular to pyriform to

elongate-ovate in outline. In all cases the stoloniferous necks are either short, or not

visible if the chambers are closely appressed. Most B. /aevis in the Sundays River

Formation are found clinging to tests of Ammobaculites, especially A. subaequalis

Mjatliuk, comparatively few are adhering to shell fragments, and none embrace

| individual quartz grains.

Occurrence

Bullopora laevis was described from the Cambridge Greensand (Cenomanian) of

England (Sollas 1877). Other records include: Gault Clay (Albian) of Folkestone,

England (Chapman 1896)),; Aptian (Damotte & Magniez-Jannin 1973) and Albian

(Magniez-Jannin 1975) of the Aube region, France; Hauterivian (Ten Dam 1948) and

Albian (Ten Dam 1950) of the Netherlands; middle and late Valanginian of north-western

J Germany (Bartenstein & Brand 1951); middle Cenomanian Grayson Formation (Tappan

1940) and Late Albian Duck Creek Formation (Tappan 1943, pars) of Texas and

Oklahoma, U.S.A.; and Portlandian Colchester Member of the Uitenhage Trough, Algoa

_ Basin (McMillan 1980).

Stratigraphic range in the Sundays River Formation

| Present in small numbers in the Late Valanginian (Biozones Bb and Ba); more

} common, especially in sandstone intervals where A. subaequalis predominates, in the

_ Early and Late Hauterivian (Biozones VIII to II). Ranges from marginal-marine to

-outermost-shelf environments, but is more common on the deeper parts of the shelf.

ANNALS

OF THE SOUTH AFRICAN MUSEUM

Figure 66.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 223

Subfamily Ramulininae Brady, 1884

Genus Ramulina T. R. Jones, 1875

Ramulina fusiformis Khan, 1950

Fig. 66E

— Ramulina fusiformis Khan, 1950: 272, pl. 2 (figs 1-2). Seibold & Seibold, 1960: 371, text-fig. 7h.

Magniez-Jannin, 1975: 230, pl. 15 (fig. 21), text-fig. 122.

Ramulina tappanae Bartenstein & Brand, 1951: 322, pl. 11 (figs 305-307).

Remarks

A few specimens referable to Ramulina fusiformis occur in the Zoetgeneugd Cliff

| outcrop samples. The finely acicular ornament of these tests is variably affected by

secondary calcite crystallization in all studied tests. All examples are composed of one

-chamber with long, rather tubular stoloniferous necks. Magniez-Jannin (1975) has

' illustrated the variations evident in chamber outline and neck morphology in her Albian

- material. This species differs from R. aculeata (d’ Orbigny) (see Loeblich & Tappan 1964:

| C537, fig. 420 (no. 8)) in its finer, denser hispid ornament and much narrower

| stoloniferous necks.

Occurrence

First described from the Gault Clay (Albian) of England (Khan 1950). Other records

include: Late Berriasian to latest Hauterivian of the Speeton Clay, north-east England

| (Fletcher 1973); Albian of the Aube district, France (Magniez-Jannin 1975); middle

| Cenomanian Grayson Formation of Texas (Tappan 1940, as Ramulina sp.); Valanginian

of north-west Germany (Bartenstein & Brand 1951, as R. tappanae); Oxfordian of

southern Germany (Seibold & Seibold 1960); and Portlandian Colchester Member of the

_ Uitenhage Trough, Algoa Basin (McMillan 1980).

_ Stratigraphic range in the Sundays River Formation

Occurs in small numbers in the basal Biozone Bb, Late Valanginian. Apparently

_ restricted to innermost-shelf environments.

Fig. 66 (see facing page). A-B. Bullopora laevis (Sollas). A. SAM—PQ—MF1563, attached to

| Ammobaculites subaequalis, AL 1/69, 1 270 feet (IV), F365. X 50. B. SAM—PQ—MF 1564, attached

to Ammobaculites subaequalis, shallow borehole SB—32, core 2, 2 feet below ?top (IV), F697. x 26.

C-D. Pyrulina cylindroides (Roemer). C. SAM—PQ—MF 1557, side view, AL 1/69, 1 540 feet (VI),

F407. x 99. D. SAM—PQ-MF1558, side view, AL 1/69, 1 780 feet (VID), F449. x 143. E. Ramulina

fusiformis Khan, SAM—PQ-—MF1565, side view, Zoetgeneugd Cliff outcrop sample 11450 (Bb),

F240. X 96. F-—G. Ramulina spp. F. SAM—PQ—-MF1566, side view, MV 1/79, 150 m (X),

F588. X 126. G. SAM—PQ-—MF 1567, side view, MV 1/79, 150 m, (X), F589. X 127. H-K. Tristix

acutangula (Reuss). H. SAM—PQ—MF1568, side view, AL 1/69, 640 feet (II), F189. x 67.

I. SAM—PQ-MF1569, side view, AL 1/69, 1 090 feet (IIT), F331. X 129. J. SAM—PQ—MF1570, side

view, AL 1/69, 790 feet (IIT), F225. x 76. K. SAM—PQ—MF1571, apertural view, AL 1/69,

1 090 feet (III), F330. x 249.

224 ANNALS OF THE SOUTH AFRICAN MUSEUM

Ramulina spp.

Figs 66F—G

Remarks

A number of crushed, damaged specimens probably of separated Ramulina chambers.

The two specimens illustrated, from Biozone X (earliest Early Hauterivian) appear to be

either smooth-walled or slightly rugose. These may be identical to the R. aculeata —

(d’Orbigny) Wright of Kielbowicz et al. (1983, pl. 4 (fig. 11)) from the Valanginian

Springhill Formation of southern Patagonia.

Family Glandulinidae Reuss, 1860

Subfamily Glandulininae Reuss, 1860

Genus 7ristix Macfadyen, 1941

Tristix acutangula (Reuss, 1863)

Figs 66H-K, 67A

Rhabdogonium acutangulum Reuss, 1863: 55, pl. 4 (fig. 14a—b).

Tristix acutangula (Reuss). Damotte & Magniez-Jannin, 1973: 37, pl. 4 (figs 14-15). Magniez-

Jannin, 1975: 222, pl. 12 (figs 2-6). Bartenstein & Kovatcheva, 1982: 646, pl. 3 (figs 29-30).

Tristix acutangulus (Reuss). Beer, 1970: 16, pl. 3 (fig. 6a—b). McLachlan et al., 1976a: 334, fig. 17

(no. 6); 1976b: 359, fig. 13 (no. 11). Musacchio, 1979: 258, pl. 4 (fig. 21). Kielbowicz et al.,

1983: 333, pl. 5 (figs 4-5).

Tristix sp. Malumian & Masiuk, 1975: 593, pl. 2 (fig. 16).

Remarks

Widely recorded, especially in the boreal and austral Early Cretaceous. The specimen

figured by Reuss (1863) and many of those illustrated by later authors (e.g. Damotte &

Magniez-Jannin 1973; Magniez-Jannin 1975) contain up to 11 chambers, but the

maximum number in South African tests is about eight, with five or six being usual.

Individuals with fewer chambers also seem to be the norm in Argentina (Malumian &

Masiuk 1975; Musacchio 1979; Kielbowicz et al. 1983). There are differences too in the

intensity and form of the peripheral margins amongst authors’ illustrated tests, which vary

from sub-angular and entirely lacking any peripheral ornamentation, to angular with a

thickened and raised margin, to fully carinate.

In South Africa, Tristix acutangula is the longest ranging and commonest species of —

the genus, and 1s the only one to be found in strata later than the Hauterivian. Its full range

is Early Portlandian to Middle Cenomanian, although it is usually absent in the poorly

oxygenated environments of the Barremian to Early Aptian sequence. No South African

specimens of the quadrate variety have been found at any level in the Late Jurassic or

Early Cretaceous.

Occurrence

This species was described by Reuss (1863) from the middle and upper Hils Clays

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION

(Barremian—Aptian) of northern Germany. Most records are from the Early Cretaceous:

Aptian (Damotte & Magniez-Jannin 1973) and Albian (Magniez-Jannin 1975) of France;

Berriasian to Early Barremian of the Speeton Clay sequence, north-east England (Fletcher

1973); Late Barremian to Early Albian of north-west Germany and Late Barremian to

Late Aptian of Bulgaria (Bartenstein & Kovatcheva 1982); Late Hauterivian of Neuquen

(Musacchio 1979), Valanginian—Hauterivian Pampa Rincon Formation, Tierra del Fuego

(Malumian & Masiuk 1975), and the Valanginian Springhill Formation, southern

Patagonia (Kielbowicz et a/. 1983), all of Argentina. In South Africa the species occurs in

the Late Valanginian (Biozone B) of Mngazana Basin, Transkei (McLachlan ef al.

1976a), the earliest Late Valanginian (Biozone D) Brenton Formation of the southern

Cape coast (McLachlan et al. 19765) and in the Portlandian Colchester Member of the

Uitenhage Trough, Algoa Basin (McMillan 1980).

Stratigraphic range in the Sundays River Formation

Present in small numbers throughout the sequence, from Biozone Bb to Biozone I, but

occurs most frequently in the Late Hauterivian (Biozones VII to I). Although the species

tolerates shallow marine, oxygenated conditions, as at Brenton and in the Colchester

Member, it appears to have avoided reduced salinity and poorly oxygenated conditions.

Its full environmental range seems to be innermost to outer shelf.

Tristix excavata (Reuss, 1863)

Figs 67B—-E

Rhabdogonium excavatum Reuss, 1863: 91, pl. 12 (fig. 8a—c). Chapman, 1894a: 160, pl. 4

(fig. 9a—b). Noth, 1951: 81, pl. 2 (fig. 41a—b).

Tristix excavata (Reuss). Neagu, 1965: 24, pl. 5 (figs 14-15). Dailey, 1973: 66, pl. 9 (fig. 11).

Magniez-Jannin, 1975: 224, pl. 12 (figs 7-11). Bertels, 1990: 279, pl. 7 (fig. 14).

Remarks

Four Sundays River Formation tests only are referable here. Two are weakly carinate

along the margins (Fig. 67B—C); this feature is not evident in Reuss’s original

illustrations, but can be seen to a slight degree in some of the Late Albian individuals

figured by Magniez-Jannin (1975). However, the South African tests display a stronger,

more continuous carina than that seen in the French Albian examples, and perhaps are

closest to that illustrated by Bertels (1990). The remaining two Sundays River tests exhibit

broadly rounded, non-carinate margins.

Of more critical importance is the nature of the aperture and the presence or absence of

an entosolenian tube in the chamber cavity. Loeblich & Tappan (1988) reinstated the

genus Tricarinella Ten Dam & Schijfsma on the basis of the description and illustrations

of Van Voorthuysen (1947), and emphasized these features in the distinction of

Tricarinella from Tristix. Thus Tricarinella possesses an entosolenian tube and Tristix

does not; Tricarinella has a triradiate aperture whereas that of Tristix is multiradiate; and

tests of Tricarinella are deeply excavated whereas those of Tristix are more nearly

226 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 67.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION

flat-sided. However, examination of the Sundays River material reveals the presence of

deeply excavated tests with both simple circular and triradiate apertures (Fig. 67C, E).

None of these tests is as deeply excavated or as lobate as that illustrated by Van

Voorthuysen (1947). Multiradiate or simple circular openings are typical of many tests

referred to this species (Bertels 1990, description; Magniez-Jannin 1975; Chapman

1894a; Neagu 1965; Noth 1951; and, seemingly, Reuss 1863). Some concern must exist

that the specimens figured and described by Van Voorthuysen (1947) may be

morphologically somewhat different from Reuss’ type specimen, particularly with regard

to the nature of the margins of the chamber lobations (more nearly rounded or more acute)

and to the aperture form (triradiate or simple, circular). Recognition of the genus

Tricarinella (as amended by Loeblich & Tappan 1988) can only be warranted if the

distinctive features of the genus (entosolenian tube, triradiate aperture) are identified in

Reuss’s holotype of Rhabdogonium excavatum or in a designated replacement test. No

clear connection has been proven between presence of triradiate aperture, entosolenian

tube and deeply excavated sides of the test. Until a more detailed study of the Tristix group

has been undertaken, it seems premature to separate particular tests to Tricarinella on the

basis of the amended generic description given by Loeblich & Tappan (1988). The few

specimens available from the Sundays River Formation preclude a detailed thin section

analysis; in external view none permit examination of the test interior or identification of

any entosolenian tube because of the opacity of the test.

Occurrence

Described by Reuss (1863) from the Gault Clay (Albian) of Folkestone, England. Later

records in Europe tend to be of the same age: Albian of Romania (Neagu 1965); Albian of

France (Magniez-Jannin 1975); Albian of the Netherlands (Ten Dam 1950); Albian of

Austria (Noth 1951); Albian of California (Dailey 1973), middle Cenomanian Grayson

Formation (Tappan 1940), and late Albian Duck Creek Formation (Tappan 1943) of

Texas and Oklahoma, U.S.A.; and the Hauterivian of southern Argentina (Bertels 1990).

Stratigraphic range in the Sundays River Formation

Late Valanginian Biozone Bb and the Late Hauterivian Biozones VI to II only. Its

environmental range seems to be similar to that of Tristix acutangula (Reuss).

Fig. 67 (see facing page). A. Tristix acutangula (Reuss), SAM—PQ-—MF 1572, apertural view, AL 1/69,

1 600 feet (VI), F436. x 63. B-E. Tristix excavata (Reuss). B. SAM—PQ—MF1573, side view,

shallow borehole SB—15, core 4, 229 feet (II), F686. x 103. C. SAM—PQ-MF1574, apertural view,

AL 1/69, 1 570 feet (VI), F431. xX 78. D. SAM—PQ—MF1575, side view, Uitenhage to Graaff-Reinet

Road outcrop, sample 11464 (Bb), F78. x 111. E. SAM—PQ—MF1576, apertural view, AL 1/69,

610 feet (II), F180. x 169. F—G. Spirillina tenuissima Giimbel. F. SAM—PQ-MF 1577, side view,

shallow borehole SB—15, core 3, 215 feet (II), F682. x 245. G. SAM—PQ—MF 1577, close-up of test

perforations of F, F683. x 909. H. Conorboides sp. A, SAM—PQ—MF 1578, side view, MV 1/79,

360-370 m (Ba), F643. x 294.

228 ANNALS OF THE SOUTH AFRICAN MUSEUM

Family Spirillinidae Reuss, 1862

Genus Spirillina Ehrenberg, 1843

Spirillina tenuissima Gumbel, 1862

Figs 67F—G

Spirillina tenuissima Gumbel, 1862: 214, pl. 13 (fig. 2). Seibold & Seibold, 1955: 125 (fig. 5n).

Espitalié & Sigal, 1963: 65, pl. 30 (figs 19-20). Hanzlikova, 1965: 93, pl. 9 (figs 19, 23a—b).

Winter, 1970: 42, pl. 4 (fig. 144a—b). McLachlan et al., 1976a: 334, fig. 17 (no. 10). Barnard et

al., 1981, 428, pl. 4 (figs 4, 8). Gregory, 1989: 188, pl. 1 (fig. 23).

Remarks

A single specimen from the Late Hauterivian (Biozone II) is clearly referable to

Spirillina. The genus, so well represented at Mngazana on the Transkei coast, is generally

absent throughout the Kimmeridgian to Hauterivian of the nearshore Pletmos, Gamtoos

and Algoa basins. Occasional examples occur in the more distal Late Valanginian of the

Gamtoos Basin, and it appears that the genus 1s commonest on the continental slope

during the latest Jurassic and earliest Cretaceous in South Africa. The Sundays River and

Mngazana tests compare closely in terms of the number and size of the whorls, and the

density of the test perforations.

Occurrence

Described by Gumbel (1862) from the Oxfordian of southern Germany. Most

subsequent records are from the Jurassic of Europe; later Jurassic records including latest

Oxfordian to Kimmeridgian Klentnice Beds, Czech Republic (Hanzlikova 1965);

Kimmeridgian of south-eastern Germany (Winter 1970); Callovian—Oxfordian of

England (Barnard et a/. 1981); and Kimmeridgian of north-east Scotland (Gregory 1989).

In Madagascar, Espitalié & Sigal (1963) reported it from the Kimmeridgian to Early

Valanginian (Cenozones C and D); and McLachlan et al. (1976a) recognized it in the

Late Valanginian (Biozone B) of the Mngazana Formation, Transkei, South Africa.

Family Conorboididae Thalmann, 1952

Genus Conorboides Hofker, 1952

Conorboides sp. A

Figs 67H, 68A

Remarks

Occasional specimens of a high-spired, aragonitic-walled form, with just over two

chambers per whorl in the adult part of the test, and a closed umbilicus. Sutures flush to

weakly depressed, generally only faintly visible unless the test is moistened. The aperture

is not well preserved in any of the tests studied, but would seem to be a low elongate slit

extending from the umbilicus out towards the test periphery. The absence of a clear

aperture, the high trochospiral coiling and the closed umbilicus suggest this species is

better referred to Conorboides than to Pseudolamarckina, but more, well-preserved tests

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 229

are necessary before this identification can be confirmed.

Conorboides sp. A compares closely with an undescribed species mainly occurring in

the latest Valanginian to Early Barremian off the south coast of South Africa, and the two

may prove to be conspecific. Conorboides sp. A has not been found at time-equivalent

horizons in the earlier Late Valanginian in the offshore Pletmos, Gamtoos or Algoa basins

off South Africa.

Stratigraphic range in the Sundays River Formation

Confined to Biozone Ba of the Late Valanginian, only on the middle and outer shelf.

Family Epistominidae Wedekind, 1937

Genus Epistomina Terquem, 1883

Epistomina hechti Bartenstein, Bettenstaedt & Bolli, 1957

Figs 68B—H

Epistomina (Brotzenia) hechti Bartenstein et al., 1957: 46, pl. 7 (fig. 170a—c).

Epistomina hechti Bartenstein, Bettenstaedt & Bolli. Ohm, 1967: 138, pl. 18 (fig. 6a—b).

Bartenstein ef al., 1971: 149, text-fig. 3 (nos 61-65). Ascoli, 1976: 674, pl. 4 (fig. la—d). Butt,

19792259. pl, 2 (tie. 4°57).

Epistomina sp. McLachlan et al., 1976b: 359, fig. 13 (nos 20-21, non nos 17-19).

see Epistomina cf. ornata (non Roemer): Musacchio, 1979: 258, pl. 5 (fig. 8).

see Epistomina hechti (non Bartenstein, Bettenstaedt & Bolli): Hart et al., 1981: 188, pl. 7.8

(fig. 5—7).

Remarks

Variably preserved, ornamented Epistomina tests occur at two horizons in the upper

Sundays River Formation, and are used to mark the tops of Biozones V and II. The lower

part of the later of these also occurs near the top of the Pletmos Basin borehole PB—A1

(McLachlan et al. 1976b). These tests possess a distinctive sutural ribbing pattern that

extends also around the old, secondarily infilled sub-peripheral apertures and is at its most

complex over the umbilical area of the ventral side. Sutural ribs on the ventral side are

very weakly curved and tend to thin significantly from the umbilicus towards the

test periphery. The dorsal intercameral sutural ribs curve gently and obliquely to the test

margin. The Biozone V and Biozone II tests are similarly ornamented, but can be easily

distinguished by their different states of preservation.

The original description and illustrations of Epistomina hechti by Bartenstein et al.

(1957) give few details of the nb patterning. The South African examples possess similar

oblique dorsal sutures to those of Bartenstein et al. (1957), but their ventral sutures are not so

curved. Comparison with the Canadian tests figured by Ascoli (1976) shows a close similar-

ity, although the detail of the ribbing pattern over the ventral umbilicus shows differences.

The shells identified as Epistomina sp. by McLachlan et al. (1976b) that derive from

the Late Valanginian are referable to another species, E. australis Masiuk & Vina (see

below). The sutural ribs of £. hechti are more delicate, less limbate and more sharply

230 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 68.

~—

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION

defined, and the tests more strongly biconvex than seen in EF. australis. A similarly

ornamented Epistomina has been reported by McMillan (1990a), as Epistomina cf. hechti,

from probable Late Barremian black silty claystones in Core 2 of borehole Kudu 9A—2,

southernmost offshore Namibia. It has proved very difficult to confirm if the Algoa Basin

and Kudu forms are the same, since the ornamentation of the latter is very poorly

preserved in all specimens due to their subsequent deep burial (over 4 000 m).

Ornamented Epistomina of this type, however, are absent in the Barremian to Early

Aptian (6AtI to 13Atl) of the Bredasdorp, Pletmos and Zululand basins.

Occurrence

Originally from the early and middle Barremian of north-west Germany, as

Epistomina D7 (Hecht 1938) and described from the middle Barremian of Trinidad

(Bartenstein et a/. 1957). Other records include: Barremian of Atlantic offshore Canada

(Ascoli 1976); latest Early to earliest Late Barremian of north-west Germany and Late

Barremian of Bulgaria (Bartenstein et a/. 1971); Late Hauterivian and Early Barremian of

DSDP site 397 off Cape Bojador, north-west Africa (Butt 1979); middle Barremian of the

Speeton Clay, north-east England (Fletcher 1973); probably the Early and Late

Hauterivian of Neuquéen, Argentina (Musacchio 1979); and Late Hauterivian (Biozone V

to Biozone II) of PB—A1 borehole, Pletmos Basin, South Africa (McLachlan et al. 19765).

Stratigraphic range in the Sundays River Formation

Restricted to Biozones VII to top V, and Biozone II, all Late Hauterivian. Confined to

middle- and outer-shelf localities.

Epistomina australis Masiuk & Vina, 1986

Figs 681, 69A

Epistomina sp. McLachlan et al., 1976b: 359, fig. 13 (nos 17-19, non nos 20-21).

Epistomina caracolla caracolla (non Roemer): Stapleton & Beer 1977: 2, pl. 3 (figs 13a—b).

Epistomina australis Masiuk & Vina, 1986a: 17, pl. 1 (figs 10-14).

Remarks

Numerous, although usually poorly preserved, ornamented Epistomina specimens

Fig. 68 (see facing page). A. Conorboides sp. A. SAM—PQ-MF 1579, side view, MV 1/79, 350-360 m,

(Ba), F658. X 271. B—-H. Epistomina hechti Bartenstein, Bettenstaedt & Bolli. B. SAM—PQ-MF 1580,

ventral view, AL 1/69, 550 feet (II), F165. x 102. C. SAM—PQ-MF1581, dorsal view, AL 1/69,

550 feet (ID), F164. x 99. D. SAM—PQ—MF 1582, ventral view, AL 1/69, 1 510 feet (V), F397. x 113.

E. SAM-PQ-MF1583, side view, AL 1/69, 1 510 feet (V), F399. x 188. F. SAM—-PQ-MF1584,

dorsal view, AL 1/69, 1 510 feet (V), F398. x 176. G. SAM—PQ-MF1585, ventral view, AL 1/69,

2 110 feet (VIII), F492. x 126. H. SAM—PQ—-MF1586, dorsal view, AL 1/69, 1 930 feet (VII),

F468. x 135. I. Epistomina australis Masiuk & Viiia, SAM—PQ-MF 1587, dorsal view, Zoetgeneugd

Cliff outcrop sample 11450 (Bb), F243. x 148.

232 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 69.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 233

occur in the Late Valanginian that appear best referred to FE. australis Masiuk & Vina.

/However, it is not clear whether all Masiuk & Vifia’s specimens are referable to

-E. australis or E. hechti Bartenstein, Bettenstaedt & Bolli, as here understood, since test

preservation is very variable. Tests closest to E. australis are confined to the Late

Valanginian in the Sundays River Formation sequence.

Sutures are ornamented by low, limbate ribs on both sides of the test. There 1s an area

of fine reticulations over the ventral umbilicus in well-preserved tests. The dorsal sutures

are straight or weakly curved, oblique; and the ventral sutures radiate, straight or weakly

curved. The sutural ribs tend to be broader and more substantial than those of E. hechti,

and the tests are more plano-convex, with a nearly flat dorsal side in many cases. The

generally poor preservation has prevented a detailed analysis of this species. It is almost

always found in association with abundant FE. caracolla (Roemer) s.l., in the strata

affected by the lowered-oxygen conditions of Biozone Bb and Ba.

Occurrence

Epistomina australis was described from the Upper Agrio Formation (Late

Hauterivian) of Neuquén, southern Argentina. It also ranges from Biozone C to early

Biozone A in the Late Valanginian of Pletmos Basin borehole PB—A1 and 1s present in the

Brenton Formation (Biozone D) (McLachlan et a/. 19765) in South Africa.

Stratigraphic range in the Sundays River Formation

Confined to Biozone C to top Ba (Late Valanginian). Ranges from well-oxygenated

innermost shelf to poorly oxygenated middle- and outer-shelf environments.

Epistomina caracolla (Roemer, 1841) s./.

Figs 69E-I, 70A—I, 72A—E

see Gyroidina caracolla Roemer, 1841: 97, pl. 15 (fig. 22).

see Epistomina caracolla caracolla (non Roemer): Beer, 1970: 18, pl. 3 (fig. 9a—c).

Epistomina ex gr. caracolla (Roemer). Rigassi, 1970: pl. 83 (pars).

see Epistomina caracolla (Roemer). Ascoli, 1976: 684, pl. 3 (fig. 10a—c), pl. 14 (fig. b). Butt, 1979:

259, pl. 2 (figs 2-3, 5). Lott et al., 1986: 44 (fig. 4G—H).

see Epistomina (Hoeglundina) caracolla (Roemer). Espitalié & Sigal, 1963: 68, pl. 32 (fig. 6a—c).

Fig. 69 (see facing page). A. Epistomina australis Masiuk & Vina, SAM—PQ—MF 1588, ventral view,

| MV 1/79, 360-370 m (Ba), F645. X 87. B—D. Epistomina caracolla (Roemer) s.s. B. SAM—

| PQ-MF1589, ventral view, Late Hauterivian (C5/C4), Speeton Clay, Filey, Yorkshire coast,

| England, F98. x 72. C. SAM—PQ—MF1590, side view, Late Hauterivian (C5/C4), Speeton Clay,

| Filey, Yorkshire coast, England, F100. x 66. D. SAM—PQ-—MF 1591, dorsal view, Late Hauterivian

(C5/C4), Speeton Clay, Filey, Yorkshire coast, England, F99. x 78. E-I. Epistomina caracolla

(Roemer) s./. E. SAM—PQ—MF1592, ventral view, AL 1/69, 460 feet (1), F109. x 117.

F. SAM—PQ—MF 1593, side view, AL 1/69, 760 feet (II), F218. x 84.G. SAM—PQ—MF 1594, ventral

view, AL 1/69, 1 240 feet (IV), F357. x 129. H. SAM-—PQ—MF1595, side view, AL 1/69, | 240 feet

(IV), F355. x 141. I. SAM—PQ—MF 1596, dorsal view, AL 1/69, 1 240 feet (IV), F354. x 132.

34 ANNALS OF THE SOUTH AFRICAN MUSEUM

‘

eek eee

Figure 70.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Oe)

| Epistomina caracolla (non Roemer): McLachlan et al., 1976a: 336, fig. 17, (nos 18-19); 1976b:

359, fig. 13 (nos 13-16). Masiuk & Vina, 1986a: 18, pl. 1 (figs 8a—b, 9). Jones & Wonders,

1992: 564, pl. 2 (fig. 22).

see Hoeglundina caracolla (Roemer). Hart et al., 1981: 204, pl. 7.16 (figs 10-12).

see Epistomina caracolla caracolla (Roemer). Malumian & Nafiez, 1983: 387, pl. 3 (figs 1-5).

~ Remarks

Examination of tests of Epistomina caracolla from the Hauterivian and Barremian of

“the Speeton Clay of the Yorkshire coast, England (Fig. 69B—D), as well as other authors’

scanning electron microscope photographs (Hart et a/. 1981; Lott ef al. 1986), indicates

that north-west European forms of this species are much more massively constructed,

more strongly biconvex, and with significantly more chambers in the final whorl (usually

9-11) than is typical in South African specimens referred to this species. The limits of

Roemer’s species have become greatly widened, both in the Northern and Southern

hemispheres, by the inclusion under this name of a considerable variety of forms with

| smooth-walled tests, perhaps with weakly raised, limbate sutures, from the Early

Cretaceous. The name has tended to become a catch-all for most morphologies of this

type. If the north-west European tests are considered as Epistomina caracolla sensu

stricto, then it seems probable that the South African specimens should be referred

_ elsewhere, as the morphological ranges of the two groups are substantially different and

do not overlap. However, there is no other appropriate available name that effectively

- encompasses their morphology. Since the Southern Hemisphere form clearly occupied a

similar niche to Epistomina caracolla s.s. of the Northern Hemisphere, and often occurs in

floods like its northern counterpart, the name Epistomina caracolla s.1. has been used here

for the austral group. Morphometric analysis of the group (s.s. and s.I.) on a fine scale is

| probably the only means of separating the many lineages of this complex, little-studied

_ plexus.

An attempt has been made here to show a range of Epistomina caracolla s.\. tests from

throughout the Sundays River Formation. However, they tend to be poorly endowed with

surface features, and the resulting scanning electron microscope photographs are

_ frequently rather bland, although better illustrations, using light microscope photography

or drawings, are difficult to obtain without a confusion of internal and external details, ora

projection of internal details to the exterior, respectively. Hauterivian tests tend to be more

strongly biconvex, especially ventrally, whereas Late Valanginian shells are generally

Fig. 70 (see facing page). Epistomina caracolla (Roemer) s.1. A. SAM—PQ—MF1597, ventral view,

AL 1/69, 1 540 feet (VI), F421. x 132. B. SAM—PQ—-MF1598, ventral view, AL 1/69, 1 930 feet

(VII), F467. x 112. C. SAM—PQ-—MF1599, side view, AL 1/69, 1 930 feet (VII), F470. x 115.

D. SAM—PQ-MF1600, ventral view, AL 1/69, 1 960 feet (VII), F473. x 101. E. SAM—PQ—

MF1601, ventral view, AL 1/69, 2 360 feet (VIII), F501. X 175. F. SAM—PQ—MF 1602, side view,

AL 1/69, 2 360 feet (VIII), F502. x 160. G. SAM—PQ—MF 1603, dorsal view, AL 1/69, 2 410 feet

(VII), F510. x 145. H. SAM—PQ—MF1604, dorsal view, AL 1/69, 2 830 feet (IX), F524. x 114.

I. SAM—PQ-MF 1605, ventral view, MV 1/79, 180-190 m (X), F607. x 251.

ANNALS OF THE SOUTH AFRICAN MUSEUM

236

(he

sie

{y)

iu)

WwW

DEPTHS

STUDIED

(FEET)

NO. CHAMBERS IN

FINAL WHORL

(AVERAGE 20 SPECIMENS

PER SAMPLE)

TO% LEFT

82-1 % LEFT

%o LEFT

94-2% LEFT

86° 2%. LEFT

1630!

eee

85 % LEFT

90 % LEFT

85% LEFT

83-3 % LEFT

Figure 71:

Numbers of chambers in the final whorl and coiling direction in Epistomina caracolla (Roemer) s./.,

in the Hauterivian of borehole AL 1/69 (A—see above) and the Late Valanginian to Early

Hauterivian of borehole MV 1/79 (B—see alongside).

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION

NO. CHAMBERS IN PERCENTAGE OF LEFT

FINAL WHORL ANDO RIGHT COILING

(AVERAGE 20

SPECIMENS PER

SAMPLE)

8 T 6

LEF T ( %e)

100 90 60 79

(Ud )

ianis

SHid3d

9 10 20 30 RIGHT (°%e)

©} a3

EPISTOMINA CARACOLLA 5.1.

X |BIOZONE Ix

HAUTERIVIgAN

$2°0%. LEFT

83-3 %. LEFT

81-0 % LEFT

93:3 % LEFT

$3°O% LEFT

85°0 %e LEFT

86-O%. LEFT

85-0 % LEFT

; A ON HEARLY

B1O2ZONE BbI|BIOZONE Ba |BIOZONE A

86-0 % LEFT

=TOO FEW SPECIMENS —=

-6os

TOP KIRKWOOD

Fim.

Figure 71 (CONTINUED).

238 ANNALS OF THE SOUTH AFRICAN MUSEUM

more compressed, often with an almost bicarinate periphery angled on either side of the

sealed marginal apertures. The distribution of Epistomina caracolla s.\. through the

Sundays River Formation shows considerable fluctuations in abundance. The species is —

absent in Biozone D, is rare in Biozone C, but becomes abundant from the base of —

Biozone Bb to the top of Biozone A in the Late Valanginian, where the species

predominates in most samples, almost to the exclusion of other species. The species is |

rare, but usually persistent, throughout the Early Hauterivian, and although more common —

in the Late Hauterivian and present in most samples, it remains a minor element of these —

nodosarid-dominated assemblages. This distribution through the Sundays River .

Formation tends to fade towards the margins of the basin, to the west, north and east, and

is clearly best developed where middle- and outer-shelf environments prevailed.

Because of the frequency of Epistomina caracolla s.\. through the Sundays River —

Formation, tests were counted at regular intervals throughout, and the ratio of left to nght

coiled individuals determined. This technique was first attempted by Ohm (1968) on —

Epistomina caracolla s.s. of the Valanginian of north-west Germany. Numbers of |

chambers in the final whorl were also counted, using about twenty or twenty-five

well-preserved tests per sample. In order to avoid contamination due to down-hole caving, —

the Hauterivian (Biozones I to base IX) of borehole AL 1/69 and the Late Valanginian and ~

earliest Hauterivian (Biozones top X to C) of borehole MV 1/79 were studied (Fig. 71).

No substantial changes in either parameter have been recognized throughout the Sundays

River Formation, although minor fluctuations do occur, which perhaps may be of

stratigraphic value. However, the generally poor quality of adjacent cuttings boreholes,

and the more erratic distribution of the species through cored borehole CO 1/67, hinders —

any attempts at correlating these features on a wider scale. Most assemblages contain 90 —

to 95 per cent sinistrally coiled tests with from six-and-a-half to seven-and-a-half —

chambers in the final whorl. |

Variation in the morphology of the Epistomina caracolla s.\. tests can be seen in the —

test periphery, which may be sub-angular to carinate, and occasionally serrated carinate

(Fig. 70H). Sutures are generally flush to weakly depressed but, particularly in the Late —

Valanginian, shells with weakly raised sutures occur. Occasional examples feature —

irregular inverted L ‘glyphs’ on the dorsal side of the chambers in the final whorl

(Fig. 72E). The ventral umbilicus is always flush, infilled and unornamented.

Tests of Epistomina caracolla s.1. illustrated by Malumian and Nafiez (1983) from the —

Barremian Rio Mayer Formation of Santa Cruz Province, Argentina, are very different —

from those of the Sundays River Formation, notably in the sutural ribs on both ventral and

dorsal sides of the test. The whole assemblage detailed by these authors, with the

dominance of suturally ribbed Epistomina caracolla s.\., closely resembles Early

Barremian assemblages from poorly oxygenated, organically enriched, high-gamma,

grey or black shelf claystones in the Bredasdorp, Pletmos and Zululand basins: these

assemblages remain to be described.

The only illustrated tests from elsewhere with which our specimens compare at all

closely in their finer morphological features are those of Masiuk & Vina (1986a), from the —

Late Hauterivian portion of the Upper Agrio Formation, Neuquén, Argentina. These tests

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 239

appear to be plano-convex or biconvex, with the dorsal side strongly convex and the

ventral side weakly so, the final whorl displays 8, rarely 6 chambers, and all tests are

sinistrally coiled, with a weakly polygonal and carinate periphery.

Occurrence

- Described from the Early Cretaceous of northern Germany (Roemer 1841). Later

records include: Early Berriasian to mid-Barremian of the Speeton Clay sequence,

north-eastern England (Hart et a/. 1981; Lott et a/. 1986); Late Valanginian to Early

Barremian of north-west Germany (Bartenstein & Bettenstaedt 1962); Early Berriasian to

Early Barremian off the south coast of South Africa, including the records of McLachlan

et al. (1976a, 1976); and Late Hauterivian Upper Agrio Formation, Neuquén, Argentina

\(Masiuk & Vina 1986a).

| Stratigraphic range in the Sundays River Formation

_ Late Valanginian to Late Hauterivian (Biozones C to I). Widespread, but absent in

hyposaline conditions along the northern fringe of the Sundays River Formation.

Family Ceratobuliminidae Cushman, 1927

Subfamily Reinholdellinae Seiglie & Bermudez, 1965

Genus Reinholdella Brotzen, 1948

Reinholdella valendisensis (Bartenstein & Brand, 1951)

Figs 72F—I, 73A—F

Conorbis valendisensis Bartenstein & Brand, 1951: 326, pl. 11 (figs 321la—c, 322a—c, 342-343).

i Beer, 1970: 18, pl. 3 (fig. 7a—c).

Reinholdella_valendisensis (Bartenstein & Brand). McLachlan eft al., 1976a: 336, fig. 17

| (nos 22—23); 1976b: 359, fig. 13 (nos 22—23), non fig. 14 (nos 1-2)).

Conorboides valendisensis (Bartenstein & Brand). Ascoli, 1976: 684, pl. 3 (fig. 2a—c) (see also

pl. 14 (fig. h)). Bartenstein, 1976b: 256, fig. 1.

see Conorboides valendisensis (Bartenstein & Brand). Hart et al., 1981: 186, pl. 7.7 (figs 6-8).

| Lofaldli & Thusu, 1979: 420, pl. 47 (fig. 27). Jones & Wonders, 1992: 564, pl. 2 (fig. 21).

Remarks

' More detailed examination of the PB—A1 borehole section subsequent to the work of

McLachlan et al. (1976), together with study of many additional borehole sections in the

Pletmos, Gamtoos and Algoa basins, has shown that tests of the ‘Reinholdella

valendisensis group’ range for a longer period of time than was thought. They first appear

in the Portlandian in abundance in parts of the offshore Algoa Basin, disappear in the

Early Berriasian, then reappear in small numbers in the Late Berriasian and Early

Valanginian. They are again in abundance in the Late Valanginian, are absent in the

earliest Hauterivian, present locally in the mid- and later Hauterivian, and occur finally in

the mid-Barremian.

_ This group has been divided into five taxa, all of which are clearly closely related. The

240 ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure. 72.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 241

earliest and latest of the five, found in the Portlandian of the offshore Algoa Basin, and in

- the Barremian of the Bredasdorp Basin and in Zululand, are not considered further here.

~ Comments on the remaining three, given the names R. valendisensis, R. v. plettenbergia

subsp. nov. and R. platterugensis sp. nov., follow below.

It has proved difficult to determine if the South African specimens from the Late

Berriasian to the top of the Valanginian are conspecific with Bartenstein & Brand’s

species from north-west Germany, and to which genus these forms should be referred.

Conorboides (a replacement name for Conorbis Hofker) has been used for this species by

_ Northern Hemisphere workers, but the presence of a slightly convex ventral side, often

| with an umbilical plug, and an extra-umbilical foramen and a possible similarly placed

aperture too, are not typical of this genus (see Loeblich & Tappan 1964: C769). These

forms seem to compare more closely with the genus Reinholdella in their external

_ morphology. The original description of Conorbis valendisensis by Bartenstein & Brand

(1951) gave no details on the structures within the chamber cavities, but the style of recess

| development along the ultimate suture in their illustrations is very reminiscent of

| Reinholdella species. No indication is made as to whether the sutural recess remains

' evident on earlier sutures, or whether it is absent, or concealed by the calcification

developed over the ventral side of the test. Subsequent scanning electron microscope

_ photographs of this species provide little additional data, because of poor preservation

| (Ascoli 1976) or damage (Hart et a/. 1981). Until subsequent, more detailed work on

— European Reinholdella valendisensis 1s completed, some doubt remains as to whether the

| South African Berriasian and Valanginian tests are truly referable to that species.

Late Valanginian tests from the Sundays River Formation assigned to R. valendisensis

possess the following features: almost all tests encountered are dextrally coiled (as are all

illustrated Northern Hemisphere tests), the test 1s plano-convex, with the dorsal side

| strongly convex and the ventral side usually weakly convex and somewhat thickened or

| ‘calcified’; test periphery circular, occasionally weakly lobate in the final part; in

cross-section test margin is rounded in juveniles, becoming sub-angular in adults.

Chambers arranged in a high trochospiral coil, with from six to seven-and-a-half in the

final whorl. Dorsal sutures generally distinct in the later part of the test, weakly raised,

limbate, curved to almost straight, oblique; ventral sutures initially indistinct, generally

with the last two or three becoming distinct, radiate, weakly depressed, curved or sinuous.

About one-third to half-way along their length from the umbilicus, all ventral sutures

|. Fig. 72 (see facing page). A-E. Epistomina caracolla (Roemer) s.1. A. SAM—PQ—MF 1606, oblique side

view, MV 1/79, 180-190 m (X), F609. x 240. B. SAM—PQ—MF1607, dorsal view, MV 1/79,

180-190 m (X), F608. x 180. C. SAM—PQ—MF1608, ventral view, Uitenhage to Graaff-Reinet

Road outcrop sample 11464 (Bb), F66. x 114. D. SAM—PQ-—MF1609, ventral view, Uitenhage to

Graaff-Reinet Road outcrop sample 11464 (Bb), F67. x 114. E. SAM—PQ—MF1610, dorsal view,

Uitenhage to Graaff-Reinet Road outcrop sample 11464 (Bb), F68. x 120. F-I. Reinholdella

valendisensis (Bartenstein & Brand), adult tests. F. SAM—PQ—MF1611, ventral view, MV 1/79,

250-260 m (A), F630. X 80. G. SAM—PQ-MF1612, ventral view, MV 1/79, 330-340 m (Ba),

F656. X 89. H. SAM—PQ—MF1613, ventral view, MV 1/79, 270-280 m (A), F653. x 69.

I. SAM—PQ-MF 1614, side view, MV 1/79, 250-260 m (A), F632. xX 88.

242

et ‘ \

ANNALS OF THE SOUTH AFRICAN MUSEUM

ath

‘\

Hicune: 73.

ee ee Ee Oe ee oe Pe vee SY

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 243

feature a narrow indentation into the following chamber, although this 1s only clear in the

early sutures when tests are moistened. The aperture is interio-marginal, umbilical to

extra-umbilical, at the base of the terminal face of the final chamber, although this is rarely

clearly evident in Sundays River Formation tests. The umbilicus is almost entirely infilled

with a solid plug of shell, although the size of the plug and its prominence at the surface

vary. Apart from the limbate dorsal sutures, the exterior of the test is smooth and

unornamented. A partition 1s developed within each chamber cavity, associated with the

externally visible sutural indentations. Unfortunately, all tests of R. valendisensis from the

Sundays River Formation are calcite or pyrite infilled, and it has not yet proved possible to

establish the structure of the partition. However, on tests with the final chamber broken

away, a fragment of the base of the partition 1s evident along the inner side of the ovate

foramen, extending from near the floor of the chamber up to, and joining with the roof

(that is, the ventral test wall).

Examination of assemblages of R. valendisensis from the Sundays River Formation

indicates that there is a marked difference in morphology between the juvenile and adult

tests. Juveniles (Fig. 73C—F) are characterized by lower, more nearly biconvex tests with

broadly rounded margins. Adults (Figs 72F—-I, 73A—B) develop rather more bowl-shaped,

almost plano-convex tests with a high trochospire and subangular margins.

- Occurrence

First described from the middle Valanginian of north-west Germany (Bartenstein &

_ Brand 1951). Other records include: middle Valanginian (Khan 1962) and Berriasian to

latest Valanginian (Fletcher 1973; Hart et a/. 1981) of the Speeton Clay sequence, north-

east England; Berriasian to Valanginian of eastern offshore Canada (Ascoli 1976;

_ Bartenstein 19765), although later work (Jansa et al. 1980) indicates the species ranges to

late in the Hauterivian; Late Valanginian Biozone B of the Mngazana Basin, Transkei

| (McLachlan et al. 1976a); and the earliest Late Valanginian (Biozone D) Brenton

_ Formation and Late Valanginian (Biozones B to top A) of Pletmos Basin borehole PB—A 1

(McLachlan et al. 19766). Note that the range given for this species by McLachlan et al.

(1976b, fig. 10) 1s incorrect; its first down-hole appearance coincides with that of

R. hofkeri (Bartenstein & Brand).

Reinholdella valendisensis occurs extensively in the offshore Pletmos, Gamtoos and

_ Algoa basins off the south coast of South Africa. It appears in small numbers in the Late

. Fig. 73 (see facing page). A-F. Reinholdella valendisensis (Bartenstein & Brand). A-B. Adult tests.

| A. SAM-—PQ-MF1615, ventral view, MV 1/79, 260-270 m (A), F635. X 92.B. SAM—PQ-MF 1616,

dorsal view, MV 1/79, 260-270 m (A), F636. x 72. C—F. Juveniles. C. SAM—PQ-—MF1617, side

view, MV 1/79, 260-270 m (A), F641. X 215. D. SAM-PQ—MF1618, ventral view, MV 1/79,

260-270 m (A), F639. X 146. E. SAM—PQ-MF 1619, ventral view, MV 1/79, 260-270 m (A), F638.

x 222. F. SAM—PQ—MF1620, dorsal view, MV 1/79, 260-270 m (A), F651. xX 250.

G-I. Reinholdella sp. D. G. SAM—PQ—MF 1621, dorsal view, AL 1/69, 1 240 feet (IV), F352. x 251.

H. SAM—PQ-MF 1622, side view, AL 1/69, 1 240 feet (IV), F353. x 300. I. SAM—PQ-MF 1623,

ventral view, AL 1/69, 1 240 feet (IV), F351. x 265.

“=

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 74.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 245

Berriasian, ranges similarly through the Early Valanginian, and becomes abundant in the

' Late Valanginian. Because of major facies changes at the level of the seismic 1At]

| unconformity, lying at a level very near the top of Biozone B, R. valendisensis is often

_ missing in the latest Valanginian in these three basins. Where shallower marine conditions

prevailed across the 1Atl unconformity, R. valendisensis ranges up to the top of the

Valanginian in some numbers, as is the case in the Sundays River Formation.

Stratigraphic range in the Sundays River Formation

Base of Biozone Bb to the top of Biozone A, Late Valanginian. Depositional

- environments in Biozones C and D appear to have been too shallow for the species’

_ preferences, and it is not found in the estuarine and hyposaline facies in the northern

i Algoa Basin. In Biozone A, numbers are very variable in different borehole sections: the

species 1s always more common in clayey sequences than in silty or sandy ones.

Reinholdella sp. D

Figs 73G—I

| Remarks

| This is one of several small-sized Reinholdella species recognized over short intervals

in the Late Hauterivian. Only seven specimens of Reinholdella sp. D have been found, six

_ of which are from the middle of Biozone IV in borehole AL 1/69 and the remaining one

from Colchester Cliff outcrop (also Biozone IV). Tests are low trochospiral, compressed,

_ with about seven chambers in the final whorl and a sub-rounded to broadly rounded test

periphery. Sutures on both ventral and dorsal sides are flush: oblique on the dorsal, radiate

on the ventral.

Tests of this and the other rare species of Reinholdella (species A to C), although

_ confined to short stratigraphic intervals, are usually poorly preserved and are not widely

distributed, and until now have thus proved of little use in correlation studies. For these

reasons, the even rarer Reinholdella sp. A and sp. B are not discussed further in the present

_ work.

| Fig. 74 (see facing page). A-H. Reinholdella platterugensis sp. nov. A. Holotype, SAM—PQ—MF 1624,

ventral view, AL 1/69, 460 feet (I), F102. x 56. B. Paratype, SAM—PQ—MF 1625, ventral view,

AL 1/69, 370 feet (I), F44. x 129. C. Paratype, SAM—PQ—MF 1626, side view, AL 1/69, 400 feet (1),

F55. x 84. D. Paratype, SAM—PQ-—MF 1627, dorsal view, AL 1/69, 370 feet (I), F45. < 148. E. Paratype,

SAM-—PQ-MF 1628, side view, AL 1/69, 400 feet (I), F53. x 129. F. SAM—PQ—MF 1628, close-up

of foraminal area of E, F54. x 646. G. Paratype, SAM—PQ—MF 1629, showing tubercles on floor of

final chamber, AL 1/69, 790 feet (III), F222. x 227. H. SAM—PQ—MF 1629, close-up of perforated

tubercle of G, F223. xX 5915. I. Reinholdella valendisensis plettenbergia subsp. nov. Paratype,

SAM-—PQ-MF 1630, ventral view, AL 1/69, 2 470 feet (VIII), F517. x 86.

246 ANNALS OF THE SOUTH AFRICAN MUSEUM

Reinholdella platterugensis sp. nov.

Figs 74A—H

Diagnosis

A species of Reinholdella characterized by a biconvex to plano-convex test with six or

seven chambers in its final whorl, ventral sutures flush to depressed, dorsal sutures flush

to weakly raised, limbate, and an internal tuberculate ornamentation developed over the

floor of the final chamber between the internal partition and the aperture.

NO. CHAMBERS IN PERCENTAGE OF LEFT

FINAL WHORL AND RIGHT COILING

(AVERAGE 20 SPECIMENS LEFT (%e)

PER SAMPLE) 20 10

6 , , iodo RIGHT (es)

AL1/69) IR. PLATTERUGENSIS

| UPPER

|ALGOA GROUP | |

i roo! iIFEw

| SPECIMENS

4370} — @ 100% RIGHT

@ 100%. RIGHT

14.00

M100 %e RIGHT

460 | |

4580

BIOZONE

[85 %e RIGHT |

195% RIGHT

4640 |92-9°%. RIGHT

cate =Ie —

{700 \gi00% RIGHT

BIOZONE

/ 4 | e T

Figure 75:

Numbers of chambers in the final whorl and coiling direction in

Reinholdella platterugensis sp. nov. in the Late Hauterivian of borehole AL 1/69.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 247

| Etymology

| Named for its presence in the highest Sundays River Formation of borehole AL 1/69,

_ which was drilled on the lands of the old farm Platterug (“Flat Ridge’).

_ Material

Holotype (Fig. 744A). MF 1624, SOEKOR negative F102.

: Paratypes (Figs 74B—H). MF 1625 to MF 1629, five specimens, SOEKOR negatives F44,

| F55, F45, F53/F54, and F222/F223.

Stratum typicum

Biozone I, Late Hauterivian, Sundays River Formation.

) Locus typicus

| Borehole AL 1/69, 460 feet.

_ Description

Test plano-convex to biconvex, with ventral side less convex, dorsal side more

strongly convex. Test periphery circular in outline, acutely rounded to sub-rounded in

cross-section; never carinate, but showing a faint thickening around the dorsal margin.

Almost all tests are dextrally coiled. Chambers arranged in a moderately high trochospiral

coil, with six or seven in the final whorl. Chambers wedge-shaped in ventral view,

- semicircular to lunate in dorsal view. Last-formed one or two chambers weakly inflated,

_ especially on the ventral side. Sutures indistinct to distinct; on the ventral side initially

flush, later weakly depressed, radiate and slightly curved; marked at one-third of their

| length from the umbilicus by a distinct, perpendicular incision into the following

~ chamber: incision visible on the final few sutures, but is present on them all, previous ones

- apparently being secondarily infilled. Dorsal sutures initially flush or weakly raised,

_ limbate, becoming weakly raised, oblique and gently curved. Aperture interio-marginal, a

low elongate slit developed from the final sutural incision, past the umbilicus to an extra-

umbilical position some distance from the test periphery. The upper margin of the aperture

_ 1s bordered by a thin, blade-like, slightly out-turned lip. Umbilicus infilled by a low, rather

poorly developed swelling.

_ Within the chamber lumen a short partition is developed from the inner, umbilical side

_ of the foramen, which thins and declines rapidly in height as it extends and curves into the

_ chamber cavity. The partition thus partly separates the main body of the chamber cavity

_ with the foramen from a small, umbilically located portion with the aperture; the addition

of a further chamber seals most or all of the previous aperture. It is clear that the

_ elongate-ovate foramen must be secondarily formed at the time of adding the next

_ chamber, since its shape and areal position are radically different from the construction

and location of the aperture. The floor of the inner portion of the final chamber, between

_ the partition and the aperture is secondarily ornamented by up to a hundred or so small

_ rounded-topped tubercles or crater-like prominences. These may also be present in small

numbers above the foramen, close to the ventral side of the test. This internal

248 ANNALS OF THE SOUTH AFRICAN MUSEUM

ornamentation is unique to the final chamber, and is removed from the floors of earlier

chambers. Surface of test smooth, unornamented; no secondary calcification on the

ventral side.

Remarks

Reinholdella platterugensis is clearly closely related to R. valendisensis (Bartenstein

& Brand) as here understood, but it differs in a number of respects. Adult tests of

R. platterugensis are never so strongly convex on the dorsal side, being generally more

nearly biconvex; dorsal sutures are not as raised nor as limbate; the test periphery is

acutely rounded rather than sub-angular; the secondary thickening of the ventral surface

does not occur; and there are tuberculations within the final chamber. However, similar

tuberculations do occur in the Early Hauterivian R. valendisensis plettenbergia

subsp. nov. (see below). |

Reinholdella platterugensis shows little similarity to Jurassic species of the genus.

Reinholdella dreheri (Bartenstein in Bartenstein & Brand 1937) exhibits a broad, rounded

test periphery; R. media (Kaptarenko-Chernousova) is similar in outline but displays a

distinctly larger and more prominent umbilical boss (Kaptarenko-Chernousova 1959);

R. crebra Pazdro (1969) possesses fewer chambers, about five, in the final whorl, and the

coiling is generally sinistral, according to Coleman (1981).

Coiling of R. platterugensis tests (Fig. 75) in the topmost part of borehole AL 1/69 is

predominantly dextral, with 6—7 chambers in the final whorl. No clear trends can be seen

in AL 1/69, and the poor quality of KE 1/71 section—the only other one in which this

species occurs—precludes identification of changes in these two test characteristics that

may be of stratigraphic value.

Stratigraphic range in the Sundays River Formation

Restricted to the later Late Hauterivian (Biozones II and I). This species has as yet not —

been found offshore 1n time-equivalent strata in the Pletmos, Gamtoos or southern Algoa

basins, partly because of the widespread erosion of Hauterivian rocks during the latest

Hauterivian to earliest Barremian, and partly because of the rather narrow continental

shelf that, in combination with anoxic slope facies at this time, restricted the distribution

of R. platterugensis considerably, when compared with the widespread Late Valanginian

distribution of R. valendisensis. In unpublished reports on the foraminifera of the Sundays

River Formation, onshore Algoa Basin, this distinctive species has been identified as

Lamarckina sp. (Beer 1973), Pseudolamarckina cf. P. rjaesanensis (Venter 1971) and

Reinholdella sp. and R. valendisensis (Bagnall et al. 1971d, 1972c).

Reinholdella valendisensis (Bartenstein & Brand) plettenbergia subsp. nov.

Fig. 741

Reinholdella valendisensis (non Bartenstein & Brand): McLachlan et al., 19766: 359, fig. 14

(nos 1—2), non fig. 13 (nos 22—23).

—

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 249

Remarks

Tests of Reinholdella valendisensis plettenbergia differ from R. valendisensis

_ valendisensis in South Africa in their lower umbilical filling and the strong tuberculate

ornamentation within the final chamber. However, in the general test morphology, the

nature of the dorsal and ventral surfaces, the sutures, chamber shape and trochospire

height, no distinct differences between the two can be ascertained.

| Reinholdella valendisensis plettenbergia occurs only in small numbers in the northern

Algoa Basin, in the most distal borehole sections, especially AL 1/69. Only a few tests are

: sufficiently well preserved to merit photography. However, preservation is very much

_ better in Pletmos Basin borehole PB—A1, and the test illustrated by McLachlan et al.

_ (19766, fig. 14 (no. 2)) is designated the holotype, deriving from | 260 feet in that

) borehole, from high in Biozone IX. The subspecies is known from a number of other

: offshore boreholes of the Pletmos and Gamtoos basins. Its stratigraphic extent in PB—A1

_ and in the Sundays River Formation in AL 1/69 is from late in Biozone IX to early in

_ Biozone VIII in the Early Hauterivian. It appears to range into deeper waters (upper

- continental slope) than is typical for the other species of Reinholdella from the

Valanginian and Hauterivian rocks of South Africa.

The subspecies is named for its first occurrence 1n borehole PB—A1, sited just off the

coast from Plettenberg Bay (adjective).

Reinholdella sp. C

Fig. 76A

_ Remarks

Four specimens, most of which are damaged. Tests are relatively small for

- Reinholdella, and with their rather inflated chambers, show some similarity to R. hofkeri

_ (Bartenstein & Brand, 1951). They differ, however, in their angled test periphery. The

| dorsal side is more strongly convex than the ventral. See also Reinholdella sp. D.

_ Stratigraphic range in the Sundays River Formation

Restricted to one horizon in the middle of Biozone III, Late Hauterivian. Too few

| specimens occur for this species to be considered stratigraphically significant at present.

Reinholdella hofkeri (Bartenstein & Brand, 1951)

Figs 76B—G

_ Conorbis hofkeri Bartenstein & Brand, 1951: 325, pl. 11 (fig. 320a—c).

- Conorboides hofkeri (Bartenstein & Brand). Bartenstein, 1976b: 256 fig. 1. Ascoli, 1976: 722

| (tig5 27):

| Reinholdella hofkeri (Bartenstein & Brand). McLachlan et al., 1976a: 336, fig. 17 (nos 20-21);

1976b: 361, fig. 14 (nos 3-4). Masiuk & Vina, 1986a: 20, pl. | (fig. 7).

?Reinholdella sp. aff. R. hofkeri (Bartenstein & Brand). Masiuk & Vifia, 1986qa: 21, pl. 1 (fig. 6).

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 76.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 25

Remarks

Tests from South Africa possess peripheries that are rather more rounded in

cross-section than the somewhat angled periphery of the holotype figured by Bartenstein

& Brand (1951). As with the other species of Reinholdella discussed here, the sutural

incisions projecting into the following chamber on the ventral side of the test can be seen

on all of the sutures of the final whorl, although the earlier ones are only evident if the test

is moistened, and appear to have been secondarily infilled. From the presence of the

incisions and the umbilical to extra-umbilical aperture, this species seems better referred

to Reinholdella than Conorboides.

It is felt that insufficient differences exist between the tests referred by Masiuk & Vina

(1986a) to R. hofkeri and those referred to ?Reinholdella sp. aff. R. hofkeri from the Late

Hauterivian part of the Agrio Formation. The height of the trochospire, the degree of

inflation of the final chambers and the corresponding depression of the sutures all display

variation in the present material, some of which is doubtless due to distortion of tests

induced by compaction of the host rock. Thus both of the Argentinian tests (only dorsal

views are illustrated) seem to fall within the morphological range of the species, as

understood in South Africa.

Because of the generally greater depth of burial of the lower Sundays River Formation

| beds, tests of R. hofkeri from the Algoa Basin are not as well preserved as those from

_ borehole PB—A1I (McLachlan er a/. 19766). Most examples are juveniles.

_ Occurrence

| Originally described from the Late Valanginian of north-west Germany (Bartenstein &

Brand 1951); Bartenstein (19764) regarded its full range there as mid-Berriasian to Late

| Valanginian. Ascoli (1976) reported it to range from the Early Berriasian to the Late

_ Barremian of the eastern continental margin of Canada. A closely comparable form,

_ “Conorboides hofkeri’, was reported from the Late Hauterivian of the type Barremian

_ section in France (Guillaume & Sigal 1965). Masiuk & Vifia (1986a) obtained specimens

_ from the Late Hauterivian part of the Agrio Formation, Neuquén, southern Argentina. In

South Africa it has been recorded from Late Valanginian Biozone B of the Mngazana

— Basin (McLachlan et al. 1976a) and Late Valanginian Biozones B and A in Pletmos Basin

| borehole PB—A1 (McLachlan et al. 19766). Reinholdella hofkeri occurs widely off the

south coast of South Africa in the Pletmos, Gamtoos and offshore Algoa basins, where it is

_ generally confined to Biozones C and B in the Late Valanginian, being absent in

_ Biozone A because of low oxygen values on the sea-floor.

_ Fig. 76 (see facing page). A. Reinholdella sp. C, SAM—PQ—MF 1631, dorsal view, AL 1/69, 1 030 feet

(If), F314. x 124. B-G. Reinholdella hofkeri (Bartenstein & Brand). B. SAM—PQ—MF 1632, ventral

view, MV 1/79, 240-250 m (A), F617. X 186. C. SAM—PQ-MF1633, ventral view, MV 1/79,

240-250 m (A), F616. X 217. D. SAM—PQ-MF 1634, side view, MV 1/79, 240-250 m (A), F621.

x 195. E. SAM—PQ—MF1635, dorsal view, MV 1/79, 240-250 m (A), F615. X 230. F. SAM—PQ-

MF 1636, dorsal view, MV 1/79, 240-250 m (A), F620. x 171. G. SAM—PQ—MF 1637, dorsal view,

MV 1/79, 240-250 m (A), F619. X 158. H-I. ?Colomia sp. H. SAM—PQ—MF1638, side view,

AL 1/69, 1 480 feet (IV), F384. x 256. I. SAM—PQ—MF 1638, apertural view of H, F392. x 283.

Royh ANNALS OF THE SOUTH AFRICAN MUSEUM

Stratigraphic range in the Sundays River Formation

Confined to the Late Valanginian, from Biozone Bb to top Biozone A. There are one or

two possible in situ records also in Biozone C. The species is absent in reduced salinity

and other marginal marine environments, as well as in substantially reduced oxygen facies

as seen in borehole CK 1/68.

Family Robertinidae Reuss, 1850

Genus Colomia Cushman & Bermudez, 1948

?Colomia sp.

Figs 76H-I

Remarks

A single specimen with a test wall, although damaged, of the same visual type as

Reinholdella and Epistomina, 1s very reminiscent of tests of Colomia. The shell consists

of about seven uniserial, roughly rectilinear chambers. In apertural view the test is faintly

trilobate in outline. The elongate opening with rounded ends, sited centrally on the

terminal face, lacks the curved ends of the typical Co/omia aperture.

The presence of the single poor test has precluded any attempt to confirm the wall as

either aragonite or calcite, or to establish if the distinctive Colomia style of internal

columella is developed between aperture and foramen in the final chamber cavity.

Other Early Cretaceous Co/omia tests appear to be confined to the Albian Gault Clay

(see Bolivina subcretacea Khan, 1950) of England, and the Late Aptian and Albian of

South Africa (undescribed species), and earlier forms are not known. These

Aptian—Albian species are predominantly biserial in chamber arrangement, becoming

cuneate only in the latest part of the test, and never rectilinear and uniserial. Only in the

Late Cretaceous do almost fully uniserial Co/omia tests occur. This apparently entirely

uniserial test from the Late Hauterivian, if referable to Colomia, is thus morphologically

rather anomalous. There are perhaps relationships between Early Cretaceous

(Aptian—Albian) Colomia and high-spired Conorboides with just over two chambers per

whorl; different associations may exist for the Late Cretaceous rectilinear forms, and the

genus may well be polyphyletic in origin.

OTHER MICROFOSSIL GROUPS

Radiolaria (Figs 77A—J)

All Radiolaria obtained from the Sundays River Formation are preserved as pyrite

casts, and show little of the original structure. Two major morphotypes can be recognized:

spheres and conical segmented forms. The spherical forms may be referable to many

genera, but the latter are probably assignable to Dictyomitra and its allies.

The spherical Radiolaria (Fig. 77A—E) casts are all composed of masses of minuscule

pyrite crystals and/or microframboidal pyrite spheres. They can be easily distinguished

from non-radiolarian framboidal pyrite masses by their near-spherical outline, which is

rare in true framboids, in the distinctly smaller size of the particles of pyrite that constitute

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 253

the cast, and in the presence of definite dimples in the surface of each visible particle

(Fig. 77E). The last characteristic presumably reflects internal positive features of the

original silica test. The dimples give the surface of the spherical cast an ornamentation

rather reminiscent of a pineapple when viewed in close-up.

Radiolaria are confined to the most distal intersections through the Sundays River

Formation, such as MV 1/79 and AL 1/69. They are never common, and are restricted to

the clayier intervals of the sequence, principally between Biozone Bb to I, Late

Valanginian to Late Hauterivian. The two major morphotypes show no restricted

stratigraphic range within this interval.

It is probable that Radiolaria are more common in the sequence than 1s apparent. Their

absence in a number of the distal boreholes is evidently due to differences in drilling and

sample quality from hole to hole, a feature that has been discussed previously with regard

to the foraminifera distributions. Their absence in nearly all outcrop samples, even those

from distal localities, is due to a combination of their natural absence close to shore

combined with the susceptibility of pyrite to percolating oxygenated groundwater.

A re-examination of samples from the Mngazana outcrop described by McLachlan er

al. (1976a) has revealed far greater numbers and variety of Radiolaria than was originally

thought, as noted previously. The sampled section is regarded as being of Biozone B, Late

Valanginian age. It is clear this section 1s substantially richer in Radiolaria than any

borehole interval or outcrop of equivalent age in the Pletmos, Gamtoos or Algoa basins

off the south coast of South Africa, even allowing for some post-depositional destruction

of tests. The Mngazana outcrop thus represents the locality most intimately influenced by

true oceanic conditions yet known from the mid-Late Valanginian in South Africa.

Bivalves (Fig. 78A) and gastropods

Bivalve fragments are widespread throughout the Sundays River Formation, and in

shelly sands or silts are especially common. The last comprehensive review of the

Bivalvia of the Algoa Basin was by Kitchin (1908) and the trigonioids have been more

recently re-appraised by Cooper (1991). In the borehole samples, because of the styles of

drilling, substantial bivalve fragments are commonest in core samples, but even in the

cuttings boreholes, scattered juvenile shells occur. These are usually those that are

robustly constructed, such as the 7rigonia illustrated. Gastropods also occur widely, but

are seldom dominant, and none seen in the boreholes to date are particularly distinctive or

stratigraphically useful; again, Kitchin (1908) last reviewed this group.

Mysid statoliths (Figs 78B, D)

Small golden-brown sub-spheres occur intermittently in small numbers through much

of the sequence. All possess an indentation on one side, which exposes, to a variable

degree, concentric layers. These spheres are considered to be mysid statoliths—‘stones’

of calcium fluorite secreted in the balance organs of the shrimp-like Mysidae (Crustacea).

The most recent study and review of statoliths is by Voicu (1981), who has concentrated

on those from the Miocene to Recent.

CH mee

ees

sit

Aan

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 77.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION Pie)

Arthropod fragments and ‘shrimps’ (Figs 79A—D)

Occasional microscopic portions of arthropod claws occur. These are disarticulated,

hollow elements reminiscent of crab and lobster pincers. They appear present mainly in

more proximal, littoral environments. Too few examples occur in the Sundays River

Formation for them to be of stratigraphic value.

In the basal Sundays River Formation cored in borehole CO 1/67, several samples (see

Fig. 81) yielded microscopic ‘shrimps’, tiny segmented isopod-like forms. The form of

the dorsal plating of these is particularly well preserved, but the nature of the numerous

limbs of the ventral side has been lost.

Echinoid spines and skeletal plates (Fig. 78C)

Echinoid skeletal components that can be identified as such usually comprise spines

and disarticulated attachment plates. The plates to which spines attach feature a prominent

subglobular boss and are pentagonal in outline. The spines may be spiny, as illustrated, or

ribbed rods, or spatulate at their free end.

Echinoid debris is perhaps more common in shallow marine environments of the

Sundays River Formation than in deeper-water localities, but 1t never predominates

macrofaunal assemblages. Perhaps because of the calcite crystal structure of the spines,

these are invariably broken, probably as a result of differential compaction of the

surrounding sediment.

Crinoid ossicles (Figs 78E—G)

Present in small numbers throughout the Sundays River Formation, but commonest in

shallow marine environments, as in Biozone C, Late Valanginian, as well as in the

marginally sited outcrops such as Zoetgeneugd Cliff.

A wide variety of skeletal ossicles, derived from the arms and possibly the stem, have

been encountered. All the skeletal elements are disarticulated, and seem to be commonest

in shallow marine sands, so that post-mortem disaggregation of crinoids by swell or wave

activity, coupled with bacterial activity and predation by larger animals appear to be

Fig. 77 (see facing page). Radiolaria. A. Microframboidal pyrite infilling, spherical morphotype,

SAM—PQ-—MF 1644, MV 1/79, 150 m (X), F590. X 260. B. Microframboidal and microcrystalline °

pyrite infilling, spherical morphotype, SAM—PQ—MF 1645, MV 1/79, 180-190 m (X), F601. x 356.

C. Microcrystalline pyrite infilling, spherical morphotype, SAM—PQ—MF 1646, CO 1/67, 915 feet

(VII), F148. x 154. D. Microframboidal and microcrystalline pyrite infilling, spherical morphotype,

SAM—PQ—-MF 1647, MV 1/79, 180-190 m (X), F604. x 280. E. Close-up of pyrite surface, spherical

morphotype, SAM—PQ-—MF 1648, MV 1/79, 180-190 m (X), F603. X 2612. F. Microcrystalline

pyrite infilling, dictyomitrid morphotype, SAM—PQ-MF1649, AL 1/69, 1 900 feet (VII),

F463. x 172. G. Microcrystalline pyrite infilling, dictyomitrid morphotype, SAM—PQ—MF 1650,

MV 1/79, 250-260 m (A), F628. xX 122. H. Microcrystalline pyrite infilling, dictyomitrid

morphotype, SAM—PQ-—MF1651, AL 1/69, 1 000 feet (III), F301. X 187. I. Microcrystalline pyrite

infilling, dictyomitrid morphotype, SAM—PQ—MF1652, AL 1/69, 790 feet (III), F259. x 155.

J. Microcrystalline pyrite infilling, dictyomitrid morphotype, SAM—PQ-—MF1653, MV_ 1/79,

260-270 m (A), F640. x 143.

ANNALS OF THE SOUTH AFRICAN MUSEUM

256

Figure 78.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 257

responsible for their dispersal. Occasional ‘Pentacrinus '—five-pointed star ossicles—are

seen, similar to that figured by McLachlan et al. (197654, fig. 16 (no. 26)) from the Late

Valanginian Brenton Formation. However, the commonest ossicles are similar to that

illustrated here in Figure 78E.

Indeterminate echinoderm debris (Fig. 78H)

Many skeletal echinoderm elements seen in the Sundays River Formation cannot be

distinguished further. Many of these are in the form of a curved plate, with an acutely

angled periphery around three sides, and attachment nodes and sockets on the fourth.

These may prove to be from asteroids, but present evidence 1s not conclusive.

Ophiuroid ossicles (Fig. 80B)

Again widespread throughout the sequence, and commonest in shallow marine

environments. The width and length of the ossicles appears to reflect their original

position within the arms of the ophiuroid. Wide, shallow and complex ossicles derive

from the bases of each arm, whereas the longer, thinner, less-ornamented ones are from

the free ends of each arm. All possess the distinctive vertebra-like arrangement (see also

McLachlan et al. 19765, fig. 16 (no. 24)).

Holothurian sclerites (Figs 781, 80A)

These occur rarely, but widely, through the sequence. Two forms occur. Most are as

illustrated (Fig. 781) and appear to be referable to Achistrum (Achistrum) (see Hampton

1958). All examples of this form are broken at some point along the shank, and lack the

presumably hook-like spear termination. Similar forms, with much the same incomplete

preservation, are known from the Late Valanginian of the offshore Gamtoos Basin in

particular.

At one horizon only, sieve-plate sclerites (Fig. 80A) are seen in the Sundays River

Formation. These are confined to the top of the Late Hauterivian Biozone III, but occur

only in the cleanly drilled AL 1/69. Based on Frizzell & Exline (1966), these would seem

best referred to Calclamnella or a similar genus.

Fig. 78 (see facing page). Miscellanea. A. Trigonia juvenile, SAM—PQ-—MF 1654, AL 1/69, 4 470 feet (A),

F557. X 120. B. Mysid statolith, SAM—PQ—MF1655, edge view, AL 1/69, 2000 feet (VII),

F477. X 342. C. Echinoid spine, SAM—PQ—MF 1657, side view, AL 1/69, 4 470 feet (A), F559. X 68.

D. Mysid statolith, SAM—PQ—MF1656, view of scalloped side, AL 1/69, 1960 feet (VID),

F472. X 300. E. Crinoid ossicle, SAM—PQ—MF1658, terminal view, AL 1/69, 4470 feet (A),

F558. X 105. F. Crinoid ossicle, SAM—PQ—MF1659, terminal view, AL 1/69, 4200 feet (A),

F552. X 84. G. Crinoid ossicle, SAM—PQ—MF 1660, side view, AL 1/69, 4 200 feet (A), F553. x 64.

H. ?Asteroid skeletal component, SAM—PQ—MF1661, AL 1/69, 4200 feet (A), F554. x 94.

I. ?Achistrum (Achistrum) sp., SAM—PQ-—MF 1662, holothurian sclerite, AL 1/69, 4 050 feet (A), F549.

xa133%

‘n

ANNALS OF THE SOUTH AFRICAN MUSEUM

Figure 79:

Figure 80.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 259

Terrestrial plant remains (Figs 80C—D)

Beside lignite and carbonized plant fragments, which are widespread and often

abundant, throughout the Sundays River Formation, megaspores, hexagonal incertae

sedis (‘hexiseds’), and one possible charophyte oogonium occur. It is generally the case

that samples rich in lignite and plant debris are poor in foraminifera, with the genera

Ammobaculites and Haplophragmoides usually predominant, and calcareous forms are

usually rare. In samples with excessive quantities of lignite, no microfauna is preserved.

In general, lignite increases in abundance towards the north of the basin, and this is also

reflected by the distribution of megaspores and ‘hexiseds’. Least lignite occurs in

shallow-marine, wave-influenced and oxygenated environments, as at Zoetgeneugd Cliff

and the Uitenhage to Graaff-Reinet Road cuttings.

Despite intensive study, we have been unable to discover the origin of the six-sided

forms we have named ‘hexiseds’. They are solid, composed of carbonized plant matter,

and generally possess a dimpled ?attachment point at one end. The height, and the degree

of taper from the wider basal to narrower upper end varies considerably, but they are

always six-sided. These forms have been found in proximal environments where rapid

deposition of sediment occurred. They are seen in the South African stratigraphic record

from the Valanginian to the top of the Early Aptian in abundance, are less common in the

Late Aptian to Cenomanian, occur rarely in the Santonian—Campanian of the Mzamba

Formation, Transkei, and are widespread in Turonian to Late Santonian marginal marine

rocks off the west coast of South Africa. They are clearly derived from land-plants.

Charophyte oogonia are absent in most of the Sundays River Formation, and the

pyritized form illustrated (Fig. 80D) is the only possible oogonium found. Larger numbers

are known from the transition beds at the top of the Kirkwood Formation along with

associated non-marine ostracods, as at Mfuleni (McLachlan & McMillan 1976, fig. 7,

site 15).

Fig 79. (see facing page). Two shrimp-like arthropods from the hyposaline basal Sundays River

Formation. A—B. Specimen 1, SAM—PQ—MF1667, dorsal and side views, respectively, CO 1/67

3 352 feet (D). X 51. C—D. Specimen 2, SAM—PQ—MF1668, dorsal and side views, respectively,

CO 1/67 3 352 feet (D). X 61. Ventral sides of these and all other specimens recovered from CO 1/67

core samples lack any clear detail and are infilled with cemented sediment.

Specimen | (A—B) displays a few fragments of appendages; these are missing or not visible

in all other examples studied.

Fig. 80. (see facing page). Miscellanea. A. ?Calclamnella sp., holothurian sclerite, SAM—PQ—MF 1663,

AL 1/69, 790 feet (III), F224. x 99. B. Ophiuroid ossicle, SAM—PQ—MF 1664, side view, AL 1/69,

4 200 feet (A), F555. X 71. C. Carbonized hexagonal incertae sedis, SAM—PQ-—MF 1665, ‘hexised’,

AL 1/69, 3 900 feet (X), F545. xX 67. D. Pyritized ?charophyte oogonium, SAM—PQ—MF 1666,

PONVO9: 790 treet (IN), F260; xX 155.

260 ANNALS OF THE SOUTH AFRICAN MUSEUM

REPRESENTATIVE SECTIONS

Three borehole sections (Figs 81—84, see fold-outs at back of volume) are included as

representative sections of the foraminifera and miscellaneous microfossil assemblages of

the Sundays River Formation. The fully-cored section across the Kirkwood—Sundays

River transition (Fig. 81A and B) in borehole CO 1/67 reveals this interval far more

clearly than in any of the rotary cuttings boreholes. Cavings, and mud and drilling

problems variably afflict many of the rotary boreholes, as previously described, but the

sections intersected in borehole MV 1/79 through the Late Valanginian (Fig. 82), and in

borehole AL 1/69 through the Late and Early Hauterivian (Figs 83 and 84, respectively),

are regarded as the cleanest and most representative.

ACKNOWLEDGEMENTS

This paper was prepared by the author while in the full-time employment of SOEKOR

(Pty) Ltd (now the two organisations, PetroSA and the Petroleum Agency of South

Africa). It represents the culmination of studies undertaken by SOEKOR that were started in

1971. It has benefitted by the involvement of a number of geoscientists over the past

two-and-a-half decades and their contribution is acknowledged here.

Permission to publish by SOEKOR (Pty) Ltd is gratefully acknowledged. The author is

greatly indebted to Mr I. R. McLachlan (consultant: SOEKOR) for initiating and

encouraging this study, and for numerous discussions over the years on the geology and

stratigraphy of the Algoa Basin and its associated Late Jurassic—Early Cretaceous basins

in the southern Cape. Outcrop samples were collected by Mr C. Reabow, formerly of

SOEKOR in Port Elizabeth, and Mr I. R. McLachlan. Many thanks are also due to

Mr V. H. Valicenti (Head: Palaeontology) of SOEKOR for encouragement, discussion and

for comments on the manuscript. Diagrams were fair drawn by Mr Gordon Rigg and

draughted by the SOEKOR drawing office. Scanning electron microscopy was undertaken

by Dr M. Witcomb of the University of the Witwatersrand, Johannesburg. The arduous

task of typing the manuscript was tackled and completed by Miss Cyd Wolfaardt with

help from Mrs J. du Toit, and final corrections were made by Miss Rugaya Abrahams.

Checklist II range charts were kindly constructed by C. Wolfaardt and Mr H. Petrie. The

author wishes to thank Dra. Alwine Bertels (Buenos Aires, Argentina), Dr Steven

Crittenden (Chagford, Devon, United Kingdom), and Dr Wolfgang Riegraf (Munster,

Germany) for their critical appraisal of the manuscript, and their constructive comments.

Views held herein are not necessarily those of SOEKOR (Pty) Ltd, either in its internal or

external dealings, and are those of the author alone.

FORAMINIFERA OF THE SUNDAYS RIVER FORMATION 261

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274 ANNALS OF THE SOUTH AFRICAN MUSEUM

IN MEMORIAM PETER WALTER BRENNER

SYSTEMATIC papers must conform to the International code of zoological nomenclature (particularly Articles 22

and 51).

Names of new taxa, combinations, synonyms, etc., when used for the first time, must be followed by the appropriate

Latin (not English) abbreviation, e.g. gen. nov., sp. nov., comb. nov., syn. nov., etc. The name of the taxon should be

followed, without intervening punctuation, by the author’s(s’) name(s) (not abbreviated) and the year of publication; a

comma must separate author’s(s’) name(s) and year. The author’s(s’) name(s) and date must be placed in parentheses if

a species or subspecies is transferred from its original genus. The name of a subsequent user of a scientific name must

be separated from the scientific name by a colon.

Synonymy arrangement should be either according to chronology of names, 1.e. all published scientific names by

which the species previously has been designated are listed in chronological order, with all references to that name

following in chronological order (see example 1), or according to chronology of bibliographic references, whereby the

year is placed in front of each entry, and the synonym repeated in full for each entry (see example 2). The author should

adopt one style or the other throughout a paper.

Family Nuculanidae

Nuculana (Lembulus) bicuspidata (Gould, 1845)

Figs 14-15A

Example |

Nucula (Leda) bicuspidata Gould, 1845: 37.

Leda plicifera A. Adams, 1856: 50.

Laeda bicuspidata (Gould) Hanley, 1859: 118, pl. 228 (fig. 73). Sowerby, 1871, pl. 2 (fig. 8a—b).

Nucula largillierti Philippi, 1861: 87.

Leda bicuspidata (Gould): Nicklés, 1950: 163, fig. 301; 1955: 110. Barnard, 1964: 234, figs 8-9.

NOTE punctuation in the above example: comma separates author’s name and year; semicolon separates more than one

reference by the same author; full stop separates references by different authors; figures of plates are enclosed in

parentheses to distinguish them from text-figures; dash, not comma, separates consecutive numbers.

Example 2

1845 Nucula (Leda) bicuspidata Gould, p. 37.

1856 Leda plicifera A. Adams, p. 50.

1859 Laeda bicuspidata (Gould) Hanley, p. 118, pl. 228 (fig. 73).

1861 Nucula largillierti Philippi, p. 87.

1871 Laeda bicuspidata (Gould): Sowerby, pl. 2 (fig. 8a—b).

1950 Leda bicuspidata (Gould): Nickles, p. 163, fig. 301.

1955 Leda bicuspidata (Gould): Nickles, p. 110.

1964 Leda bicuspidata (Gould): Barnard, p. 234, figs 8—9.

In describing new species, one specimen must be designated as the holotype; other specimens mentioned in the original

description are to be designated allotype (if applicable) and/or paratypes; additional material not regarded as paratypes

should be listed separately. The complete data (registration number, depository, description of specimen, locality,

collector, date) of the holotype and paratypes must be recorded, e.g.:

Holotype. SAM—A13535 in the South African Museum, Cape Town. Adult female from mid-tide region, King’s Beach,

Port Elizabeth (33°51'S 25°39’E), collected by A. Smith, 15 January 1973.

Note standard form of writing South African Museum registration numbers and date.

SPECIAL HOUSE RULES

Capital initial letters

(a) The Figures, Maps and Tables of the paper when referred to in the text, e.g. ‘... the Figure depicting C. namacolus ...’, or

*,.. nC. namacolus (Fig. 10) ....’

(b) The prefixes of prefixed surnames in all languages, when used in the text, if not preceded by initials or full names: e.g. Du

Toit, but A. L. du Toit; Von Huene, but F. von Huene

Punctuation should be loose, omitting all not strictly necessary. Reference to the author should preferably be expressed

in the third person. Roman numerals should be converted to arabic, except when forming part of the title of a book or

article, e.g. ‘Revision of the Crustacea. Part VIII]. Amphipoda.’. A specific name must not stand alone, but be preceded

by the generic name or its abbreviation to initial capital letter (except at the beginning of a sentence or paragraph),

provided the same generic name is used consecutively. The name of new genus or species should not be included in the

title; it should be included in the abstract, counter to Recommendation 23 of the Code, to meet the requirements of

Biological Abstracts.

GENERAL. Once referees’ reports have been received by the editor, these will be discussed by the editorial

committee. If the paper is considered acceptable after minor or major revision, the reports will be forwarded to the

author who must then thoroughly revise in accordance with the referees’ suggestions. Final acceptance of the revised

manuscript will be considered by the editorial committee. In the case of major revision being necessary, the committee

reserves the right to consult one or more referees regarding the revised manuscript.

I. K. McMILI

THE FORAMINIFERA OF

LATE VALANGINIAN TO HAUTERIV

(EARLY CRETACEOUS) SUNDAYS RIN

FORMATION OF THE ALGOA BA:

EASTERN CAPE PROVINCE, SOUTH AFR

ISBN 0 86813 17

9 "780868" 1317:

I. K. McMILLA

THE FORAMINIFERA OF TH

LATE VALANGINIAN TO HAUTERIVIA

(EARLY CRETACEOUS) SUNDAYS RIVE

FORMATION OF THE ALGOA BAS

EASTERN CAPE PROVINCE, SOUTH AFRIC

SBN 0 86813 178

MCZ ERNST MAYR LIBRARY

3 2044 128 408 101

COMPOSITED

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