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ANNALS OF THE

SOUTH AFRICAN MUSEUM

VOLUME 79

ANNALE VAN DIE

SUID-AFRIKAANSE MUSEUM

BAND 79

ANNALS OF THE SOUTH AFRICAN MUSEUM

ANNALE VAN DIE SUID-AFRIKAANSE MUSEUM

VOLUME 79 BAND

THE TRUSTEES OF THE DIE TRUSTEES VAN DIE

SOUTH AFRICAN MUSEUM SUID-AFRIKAANSE MUSEUM

CAPE TOWN KAAPSTAD

1979-1980

& SET, PRINTED AND BOUND IN THE REPUBLIC OF SOUTH AFRICA BY

THE RUSTICA PRESS (PTY.) LTD., WYNBERG, CAPE

209

LIST OF CONTENTS

Cook, P. L. see HAYWARD, P. J.

GENTRY, A. W.

Fossil Bovidae (Mammalia) from ee South Africa. (Published April

1980.) é He su me be

GRIFFITHS, C. L.

A redescription of the kelp curler Ampithoe humeralis (Crustacea, Amphipoda)

from South Africa and its relationship to eg es (Published

September 1979.) Me cee oe a

HAYWARD, P. J. & Cook, P. L.

The South African Museum’s Meiring Naude cruises. Part 9. Bryozoa. (Published

September 1979.) Me ae iy an er st ue i

KENSLEY, B.

A second genus in the marine isopod family Bathynataliidae. (Published July 1979.)

Mies, G. A. see SIESSER, W. G.

SALMON, D. see SIESSER, W. G.

SANTA Luca, A. P.

The postcranial skeleton of Heterodontosaurus tucki (Reptilia, Ornithischia) from

the Stormberg of South Africa. (Published February 1980.) ..

SIESSER, W. G. & MILES, G. A.

Calcareous nannofossils and planktic foraminifers in Tertiary limestones, Natal

and eastern Cape, South Africa. (Published December 1979.) ..

SIESSER, W. G. & SALMON, D.

Eocene marine sediments in the pee South West Africa. (Published July

1979.) a ; : a8 a me s iy

SIMPSON, G. G.

Tertiary penguins from the Duinefontein site, Cape Province, South Africa.

Published July 1979.)

Page

213

131

159

139

NEW GENERIC NAMES PROPOSED IN THIS VOLUME

Page

Damalacra Gentry, 1980 age ‘ zi oa aye Ee me a un. 2264

Inversiscaphos Hayward & Cook, 1979 ae are mr ee = = ag 76

Leiosalpinx Hayward & Cook, 1979 se ae abe ay SH ss oe 66

Naudea Kensley, 1979 a : ae 2 ae se aS if ae 36

Notocoryne Hayward & Cook, 1979 ee aie ae an a te be 54

Nucleornis Simpson, 1979... ae on ar pe oa aie ae a: 2

VOLUME 79 PART 1 JULY 1979

S 907. 63

OF THE SOUTH AFRICAN

MUSEUM

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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 le vitalité des mollusques. J. Conch., Paris 88: 100—140.

FIsCcHER, P.-H., DuvAL, M. & Rarry, A. 1933. Etudes sur les échanges respiratoires des littorines. Archs

Zool. exp. gen. 74: 627-634.

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

Ann. Mag. nat. Hist. (13) 2: 309-320.

Konn, A. J. 19606. Spawning behaviour, egg masses and larval development in Conus from the Indian Ocean.

Bull, Bingham oceanogr. Coll. 17 (4): 1-51.

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

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(continued inside back cover)

ANNALS OF THE SOUTH AFRICAN MUSEUM

ANNALE VAN DIE SUID-AFRIKAANSE MUSEUM

Volume 79 Band

July 1979 Julie

Part 1 Deel

TERTIARY PENGUINS FROM THE DUINEFONTEIN

Behe, CAPE PROVINCE, SOUTH AFRICA

GEORGE GAYLORD SIMPSON

Cape Town Kaapstad

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TERTIARY PENGUINS FROM THE DUINEFONTEIN SITE,

CAPE PROVINCE, SOUTH AFRICA

GEORGE eee SIMPSON

The Simroe Foundation, 5151 East Holmes Street, Tucson, Arizona 85711

(With 3 figures and | table)

[MS. accepted 17 May 1979}

_ ABSTRACT

Penguin bones of possible Miocene age were found in excavations for a nuclear power

plant about 25 km north of Cape Town. At least two species are present, but the smaller

species cannot be more precisely identified than as spheniscid. The larger species is represented

by tarsometatarsi with a single metatarsal foramen between the second and third metatarsals,

an arrangement hitherto unknown among penguins. A new genus and species Nucleornis

insolitus is based on these specimens.

CONTENTS

PAGE

Introduction . 1

Systematics . 2;

Acknowledgements 6

References F

INTRODUCTION

In 1978 penguin bones were found in excavations for the Koeberg Nuclear

Power Station on the farm Duinefontein a few kilometres north of Melkbos

(or Melkbosstrand), which is about 25 km north of Cape Town. These bones

came from two excavations, one for the reactor and one for a pump station.

The stratigraphic section is essentially the same in the two excavations. Between

about 5 and 9,4 metres above mean sea-level there are fine quartzose dune sands

and a palaeosol calcrete of late Pleistocene age from which vertebrate fossils and

Palaeolithic artefacts were recovered (Hendey 1968; Klein 1976). From about

three metres above sea-level down to Precambrian bedrock at eleven metres

_ below that level there is a complex of marine deposits. In this complex at about

8,2 to 8,5 metres below sea-level there is a bed of coarse quartzose sand in which

were found whale debris, sharks’ teeth and other fish debris, and the penguin

bones described in this paper. The age of this bed has not yet been determined,

but Hendey (pers. comm.) suggests that it may correlate with late Tertiary

deposits elsewhere in the general vicinity and tentatively considered Miocene in

age, for example at Ysterplaat, where penguin bones were also found (Simpson

1973).

The specimens here described are in the South African Museum and they

are designated as in that museum’s catalogue, prefixed by SAM-PQ.

Measurements are in millimetres.

Ann. S. Afr. Mus. 79 (1), 1979: 1-7, 3 figs, 1 table.

Ds ANNALS OF THE SOUTH AFRICAN MUSEUM

SYSTEMATICS

Order SPHENISCIFORMES

Family Spheniscidae

Nucleornis gen. nov.

Etymology

Nucle- is a reference to the serendipitous association of this discovery with

a nuclear power station. Ornis is the common neo-Latin use of the Greek word

for ‘bird’. The generic name is masculine.

T ype-species

Nucleornis insolitus sp. nov.

Included species

Type only.

Known distribution

?Miocene at the Koeberg Nuclear Power Station, Cape Province, South

Africa.

Diagnosis

Tarsometatareus short and stout. A single intermetatarsal foramen

between the second and third metatarsals, plantar opening immediately distal

to the inner calcaneal ridge.

Discussion

This position of a single intermetatarsal foramen is not known to occur in

any other penguin, living or fossil. In all six living genera there are usually two

such foramina, one inner or medial foramen between the second and third

metatarsals, and one outer or lateral between the third and fourth metatarsals.

In Aptenodytes and Pygoscelis the two are approximately equal and both open

on the plantar surface, the medial foramen just distal to the inner calcaneal

ridge, and the lateral foramen at the same level and below the less salient outer

prominence or ridge. In the other living genera, Megadyptes, Spheniscus,

Eudyptes, and Eudyptula, the inner foramen is smaller than the outer foramen

and is a small, comparatively long canal that does not open on the plantar

surface, strictly speaking, but on the medial surface of the bone and, here,

between the inner calcaneal ridge and the shaft of the second metatarsal.

According to Watson (1893) the small inner foramen or canal is sometimes

absent in Spheniscus, and according to Marples (1952) it is also sometimes

absent in Eudyptula. There is then only one such foramen, the outer or more

lateral of the two. (This variant does not occur in specimens of those genera that

have been examined.)

In the two genera named from the late Tertiary of Cape Province, Inguza

TERTIARY PENGUINS FROM SOUTH AFRICA 3

has the foramina about as in Pygoscelis, and Dege has it intermediate in position

between those of Pygoscelis and of Spheniscus (Simpson 1975, 1979). Among

older known fossil penguins some have two foramina differing only in detail

from those of Aptenodytes and Pygoscelis. That is true, for instance, of

Paraptenodytes from the early Miocene of Argentina (Simpson 1946) and

Archaeospheniscus from the early Oligocene of New Zealand (Simpson 1971a),

and the probable late Eocene of Seymour Island, Antarctica (Simpson 19716).

Others, however, have a lateral foramen present and the medial or inner foramen

small or, more commonly, absent, notably Palaeeudyptes from the early

Tertiary of New Zealand (Marples 1952; Simpson 1971a) and Palaeospheniscus

from the early Miocene of Argentina (Ameghino 1905; Simpson 1972). Until

now no spheniscid tarsometatarsus was known to have a single medial or inner

foramen. Some fossil genera have been named on the basis of bones other than

the tarsometatarsus, usually the humerus, and for some of those the tarso-

metatarsus is not known. It is possible that some had a single medial foramen,

but no such occurrence has been known hitherto.

The presence of such an unpenguin-like character in what is clearly a

penguin tarsometatarsus seemed almost unbelievable on beginning this study.

The possibility that a lateral foramen had been mistaken for a medial one had

to be considered. That would be possible if a left tarsometatarsus were taken for

a right or if the plantar face were taken for the dorsal or anterior face, but in this

case that is not possible. In other respects the tarsometatarsus of Nucleornis is a

mere variant of a completely spheniscid pattern. The shaft of the second meta-

tarsal is curved, that of the fourth straight. The prominent inner calcaneal ridge

is medial, and the much less prominent ridge is lateral. There are deep grooves

between the metatarsals on the dorsal or anterior face, none on the plantar face.

The proximal articulation for the tibiotarsus is also asymmetrical exactly as on

the right tarsometatarsus of other penguins. The holotype of the type-species is

certainly a right tarsometatarsus and its single foramen is certainly medial. The

possibility that this is an unusual variant or perhaps teratological is also

effectively ruled out by the fact that there are two specimens surely of different

individuals and exactly alike in this remarkable character. The functional

significance, if any, is unknown.

The type-species Nucleornis insolitus may be within the possible size range

of Palaeospheniscus ? huxleyorum Simpson 1973, also from the Cape Province

and possibly of about the same geological age. The latter species was based on

humeri and its tarsometatarsus is unknown. The humerus of Nucleornis insolitus

_ is unknown. Thus the possibility that the species are synonymous cannot be

entirely ruled out. That does not affect the validity of the genus Nucleornis,

which cannot be synonymous with Palaeospheniscus or any other genus in which

the tarsometatarsus is known. The clearly valid generic name must be linked

with a type-species known to have its generic characters. Under these circum-

stances a new specific name must be proposed despite the slight possibility that

it could be synonymous with P. ? huxleyorum.

4 ANNALS OF THE SOUTH AFRICAN MUSEUM

Nucleornis insolitus sp. nov.

Etymology

Insolitus, Latin, ‘unusual’, ‘strange’, because of the unusual presence of a

single medial intermetatarsal foramen.

Holotype

MBD4, right tarsometatarsal lacking the distal ends of the second and

third metatarsals (Fig. 1).

Fig. 1. Nucleornis insolitus, type, tarsometatarsus SAM—PQ-MBD4.

Proximal, dorsal and plantar views.

Hypodigm

The holotype and MBD3, right tarsometatarsal lacking the part proximal

to the fourth metatarsal and the distal end of the second metatarsal (Fig. 2).

Known distribution 7

As for the genus.

Diagnosis

Only known species of the genus. Measurements as in Table 1.

TABLE |

Measurements of Tarsometatarsi of Nucleornis insolitus

MBD4,

holotype MBD3

Width across proximal end : : : ; eS Z 19,9 —

Width about one-fourth of distance from proximal end . ; : 19,9 21,6

Width of distal end of third metatarsal : 2 ; : é 4 —— 9,0

Length of third metatarsal to distal groove : : : : —

Length of fourth metatarsal to distal groove. , : ; ‘ 31,3 —

TERTIARY PENGUINS FROM SOUTH AFRICA 2)

Fig. 2. Nucleornis insolitus, tarsometatarsus SAM—PQ-MBD3.

Dorsal and plantar views.

Discussion

Although MBD3 is somewhat more nearly complete, MBD4 has crucial

structure better preserved and is therefore selected as the holotype. MBD4 is

slightly smaller than MBD3 but the morphology is almost identical in the two

and the difference in size is well within the expected size range of this bone in a

single species of penguins.

MBD7 from the same deposit is a right radius of size appropriate for this

species and probably belonging to it. It lacks the distal end. The part preserved

is characteristically spheniscid but does not clearly show any particularly

distinctive features. As reference to the species is not certain and it would add

no diagnostic characters, it is not included in the hypodigm.

Gen. et sp. indet.

Material

MBD70, left humerus, proximal and distal ends incomplete. This bone is

from the excavation for the reactor and all the others are from that for the pump

station, but as noted above all are from the same bed (Fig. 3).

MBD10, right humerus, so badly abraded as to have little remaining

character.

MBD1, left tibiotarsus, lacking proximal end.

MBD2, left coracoid, lacking posterior end.

Discussion

These bones could all belong to a single species, although there is no

assurance that they do so. None can be confidently identified to genus or species.

They are all definitely too small to belong to Nucleornis insolitus.

6 ANNALS OF THE SOUTH AFRICAN MUSEUM

MBD70 is a short, relatively light humerus, probably with a bipartite

tricipital fossa, with a gently but definitely curving shaft distinctly wider toward

the distal end and without a preaxial angulation. This specimen falls just short

of permitting identification but suggests that it represents a distinct species. It is

not referable to Palaeospheniscus? huxleyorum, based on a humerus and of

possibly near the same age at Ysterplaat, MBD70 being somewhat smaller, with

shaft more distinctly curved and with a greater difference between proximal and

distal widths. The very poorly preserved humerus MBD10 might be of the same

species as MBD70.

Fig. 3. Spheniscidae indet., humerus SAM

Medial view.

The coracoids of penguins are often characteristic at a generic or even a

specific level. This is seldom of diagnostic use for fossil penguins because

articulated or associated skeletons of fossil penguins are extremely rare, almost

all named taxa are based on the humerus or the tarsometatarous, and few fossil

coracoids are definitely referable to a defined genus or species. It has frequently

been noticed (e.g. Marples 1952; Zusi 1975) that in living penguins there are two

quite distinct patterns of coracoids, one, in Pygoscelis and Aptenodytes, without

a fenestra, and one, in the other living genera, with a fenestra. Although because

of breakage this is not quite certain, MBD2 seems to have had a fenestra.

As with many other spheniscid characters it is not yet clear which, if either, of

these states was primitive and which is derived or whether both are.

There are three other specimens in the collection that are probably bre

ments of penguin bones but are entirely unidentifiable: MBD8, MBD9, and

MBD11.

ACKNOWLEDGEMENTS

Once more I am greatly indebted to the South African Museum and to

Dr Q. B. Hendey who arranged the loan of the fossil specimens for my study,

provided the locality and stratigraphic data, and reviewed the manuscript of this

paper. The field data include a geological section by Dr J. Rogers of the

Geological Survey of South Africa. Study was carried out at the Simroe

Foundation with support from the Department of Geosciences of the University

of Arizona, Tucson, U.S.A.

TERTIARY PENGUINS FROM SOUTH AFRICA ¥

The illustrations were prepared by Miss J. Nolte of the South African

Museum.

REFERENCES

AMEGHINO, F. 1905. Enumeracién de los Impennes fosiles de Patagonia y de la Isla Seymour.

Buenos Aires: Juan A. Alsina.

HENDEY, Q. B. 1968. The Melkbos site: an upper Pleistocene fossil occurrence in the south-

western Cape Province. Ann. S. Afr. Mus. 52: 89-119.

KLEIN, R. G. 1976. A preliminary report on the ‘Middle Stone Age’ open-air site of

Duinefontein 2 (Melkbosstrand,. south-western Cape Province, South Africa). S. Afr.

archaeol. Bull. 31: 12-20.

Marp Les, B. J. 1952. Early Tertiary penguins of New Zealand. Palaeont. Bull., Wellington

20: 1-66.

Simpson, G. G. 1946. Fossil penguins. Bull. Am. Mus. nat. Hist. 87: 1-100. :

Simpson, G. G. 197la. A review of the pre-Pleistocene penguins of New Zealand. Bull. Am.

Mus. nat. Hist. 144: 319-378.

Simpson, G. G. 19716. Review of fossil penguins from Seymour Island. Proc. R. Soc. (B) 178:

357-387.

Simpson, G. G. 1972. Conspectus of Patagonian fossil penguins. Am. Mus. Novit. 2488: 1-37.

Simpson, G. G. 1973. Tertiary penguins (Sphenisciformes, Spheniscidae) from Ysterplaats,

Cape Town, South Africa. S. Afr. J. Sci. 69: 342-344.

Simpson, G. G. 1975. Notes on variation in penguins and on fossil penguins from the Pliocene

of Langebaanweg, Cape Province, South Africa. Ann. S. Afr. Mus. 69: 59-72.

SIMPSON, G. G. 1979. A new genus of late Tertiary penguin from Langebaanweg, South Africa.

Ann. S. Afr. Mus. 78: 1-9.

WATSON, M. 1893. Report on the Spheniscidae collected during the voyage of H.M.S.

*“Challenger’’. Challenger Rep. Zool. 7.

Zusi, R. L. 1975. An interpretation of skull structure in penguins. Jn: STONEHOUSE, B., ed.

The biology of penguins: 59-86. London and Basingstoke: Macmillan.

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Nuculana (Lembulus) bicuspidata (Gould, 1845)

Figs 14-15A

Nucula (Leda) bicuspidata Gould, 1845: 37.

Leda plicifera A. Adams, 1856: 50.

Laeda bicuspidata Hanley, 1859: ee pl. 228 (fig. 73). Sowerby, 1871: pl. 2 (fig. 8a—b).

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GEORGE GAYLORD SIMPSON

TERTIARY PENGUINS FROM THE DUINEFONTEIN

SITE, CAPE PROVINCE, SOUTH AFRICA

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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 le vitalité des mollusques. J. Conch., Paris 88: 100-140.

FISCHER, P.-H., DuvAL, M. & Rarry, A. 1933. Etudes sur les échanges respiratoires des littorines. Archs

Zool. exp. gen. 74: 627-634.

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

Ann. Mag. nat. Hist. (13) 2: 309-320.

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

Bull. Bingham oceanogr. Coll. 17 (4): 1-51.

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

und anthropologische Ergebnisse einer Forschungsreise im westlichen und zentralen Siid-Afrika 4: 269-270.

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(continued inside back cover)

ANNALS OF THE SOUTH AFRICAN MUSEUM

ANNALE VAN DIE SUID-AFRIKAANSE MUSEUM

Volume 79 ~~ Band

July 1979 Julie

Part 2 Deel

EOCENE MARINE SEDIMENTS IN THE

SPERRGEBIET, SOUTH WEST AFRICA

WILLIAM G. SIESSER

DAVID SALMON

Cape Town Kaapstad

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EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET,

SOUTH WEST AFRICA

WILLIAM G. SIESSER

South African Museum, Cape Town

' DAVID SALMON

Geological Survey, Cape Town

(With 15 figures)

[MS. accepted 5 June 1979]

ABSTRACT

Twelve taxa of calcareous nannofossils and twenty-one of benthic foraminifera have been

identified from calcareous marine siltstones near Bogenfels, South West Africa. These taxa

establish the sediments as upper Eocene. It is equally correct to assign them either to Martini’s

NP 19-NP 20 nannofossil zones (37,2—39,5 m.y.B.P.) or to Bukry’s Jsthmolithus recurvus

subzone (38-41 m.y.B.P.). The sediments were deposited in a shallow, near-shore environment;

the overlying watermass was cool-temperate and had normal marine salinity.

The informal name ‘Langental beds’ is suggested for the low-lying, fossiliferous rocks in

the area, at least some of which are upper Eocene. The informal name ‘Buntfeldschuh beds’ is

suggested for the topographically higher, essentially unfossiliferous units. The Buntfeldschuh

beds may be upper Paleocene—lower Eocene.

CONTENTS

PAGE

Introduction . : ; ; ‘ : : : ‘ ea aS)

Tertiary marine deposits. : : : : seo as ee ALO

Buntfeldschuh . ; : : A : . 10

Lithology . F : p : é : . 10

Palaeontology : f : : , : ce eek

Bogenfels : ; ; ; ; 4 é Cena

Lithology . , ; 3 é ; ‘ ie? © 6)

Palaeontology . , : : . : cw als

Palaeoecology : , ; , : : oe OO

Stratigraphic status of the Tertiary deposits . : ne 50

Acknowledgements . ; : : : : : LS

References . : . 3 ; : f : : 33

INTRODUCTION

Study of the Tertiary Period in southern Africa is severely constrained by

the scarcity of outcrops. This is especially true along the western coastal margin

of the subcontinent. Scattered outcrops occur in the southern coastal zone

between Cape Town and Hondeklip Bay, but between Hondeklip Bay and the

Ann. S. Afr. Mus. 79 (2), 1979: 9-34, 15 figs.

10 ANNALS OF THE SOUTH AFRICAN MUSEUM

Kunene River—a distance of more than 1 200 km—the only known marine

Tertiary beds are a few small exposures in the Sperrgebiet (Fig. 1). It is therefore

imperative to extract as much geological information as possible from these

outcrops, since they are the only positive record left of Tertiary marine incursion

along this long stretch of coastline. |

The main purpose of this paper is to present an account of the microfossils

in these rocks, although aspects of the lithology, depositional environment and

stratigraphic status are discussed as well.

TERTIARY MARINE DEPOSITS

All the Tertiary deposits occur in the ‘Sperrgebiet’. The name means ‘the

forbidden area’, and was applied by the German government a few months after

diamonds were discovered (1908) in the northern part of the area. General

prospecting was forbidden in the region lying between the coast and the Great

Escarpment and extending from the Orange River northwards to latitude 26°S—

the area originally defined as the Sperrgebiet (Stocken 1962).

Tertiary marine deposits occur sporadically as small outcrops from

Buntfeldschuh in the south to Liideritz Krater in the north, a distance of about

40 km (Fig. 1). The best-preserved and most-studied outcrops occur at two

localities: Buntfeldschuh, and a few kilometres north and north-east of

Bogenfels. Smaller outcrops occur at or near Eisenkieselklippenbake, Liideritz

Krater, Advokat Bake and in a few other patches (see Beetz 1926, and the

geological map in Kaiser 1926).

BUNTFELDSCHUH

LITHOLOGY

_At Buntfeldschuh there is a surf-cut platform at 120-140 m (Martin 1973).

About 45 m of marine sediments lie on this platform. The marine unit consists

of a sporadically occurring pebble conglomerate at the base, overlain by clayey,

mostly fine-grained sandstones. Occasional pebble lenses dominated by

chalcedony, agate and jasper cut through the sandstones (Fig. 2). These lenses

are known to be diamondiferous; Beetz (1926) reports the finding of gemstones

as large as 2,5 cts.

The sandstones are predominantly greyish green (5 GY 7/2), although

dusky yellow (5 Y 6/4), dark greyish orange (10 YR 6/6) and very pale orange

(10 YR 8/2) colours are also common (colours from the GSA Rock Color

Chart). Most units are fine-grained in texture; quartz is the most abundant

component grain, with minor, variable amounts of feldspar, rock fragments and

Opaque minerals. Only a few calcareous layers are present, and in these the

CaCO, occurs as cement. The sandstones are mostly poorly to moderately

indurated. Figure 3 shows a thin section cut from a more indurated sample.

Overlying the marine rocks is a thick (over 40 m) sequence of cross-bedded

brown aeolian sandstone (Fig. 4). This aeolian sequence is capped by about | m

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET

SOUTH WEST AFRICA

(NAMIBIA)

PAE LUDERITZ

2 >-

. Liideritz Krater

\. ° Granitberg @

Elizabeth Bay

Fe Pomona

\.Bogenfels m

\- eEisenkieselklippenbake

\.-Advokat Bake ©

\.-*Buntfeldschuh = —

a om

Fig. 1. Map showing the locations of Tertiary marine outcrops mentioned in the text.

i2 ANNALS OF THE SOUTH AFRICAN MUSEUM

Fig. 2. Pebble lens in Buntfeldschuh sandstones. Pebbles are predominantly vein quartz,

chalcedony, agate and jasper.

Fig. 3. Photomicrograph of a greywacke sandstone from Buntfeldschuh. Groundmass is

comminuted mica and clay; grains are mostly quartz, with some altered feldspar and

rock fragments.

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 13

Fig. 4. Cross-bedded aeolian sandstones overlying ?upper

Paleocene-lower Eocene marine beds at Buntfeldschuh.

‘Diagenetic’-ooid-bearing calcrete caps the section.

of calcrete, containing the same unusual diagenetic ooids and intraclasts (Fig. 5)

first reported by Siesser (1973) from ?Pliocene—Pleistocene calcretes of the Cape

Province.

Further details of the Tertiary section at Buntfeldschuh are given by Beetz

(1926). Unpublished work by geologists of Consolidated Diamond Mines,

South West Africa suggests that the Buntfeldschuh-escarpment section may be

more stratigraphically complex than previously realized. Local faulting and

tilting in the section allows recognition of at least two marine members. The

lower member overlies a remnant of the Pomona beds (here capped by Tafelberg

Quartzite) in a small depression at the northern end of the escarpment

(C. G. Stocken pers. comm. 1979).

ANNALS OF THE SOUTH AFRICAN MUSEUM

ye Tis Wim.

‘Diagenetic’ ooids and intraclasts set in an intergranular fabric of microspar and

micrite at Buntfeldschuh (see Fig. 4).

“SS SS S

SAGs

Fig. 6. Burrow in sandstone at Buntfeldschuh.

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET itp)

PALAEONTOLOGY

The only macrofossils found in the marine section were burrows (Fig. 6).

Fish teeth have been reported by B6hm (1926) and C. G. Stocken (pers. comm.

1979).

All samples collected were barren of microfossils.

BOGENFELS

Tertiary remnants are preserved 3-5 km north and north-east of Bogenfels

village in two depressions on either side of the Langental (Fig. 7). The larger

exposures are south and east of the Langental. The smaller, but better-known

deposits, are on the northern side of the Langental, adjacent to Wanderfeld IV

(Fig. 7). Most attention in the past has focused on the smaller exposure, which

will be referred to here as the Wanderfeld IV locality, since it is the most

fossiliferous exposure and also overlies the only known marine Cretaceous

deposit between the southern Cape Province and the Kunene River. The

following lithological and micropalaeontological descriptions of this section

refer specifically to the Wanderfeld IV outcrops.

LITHOLOGY

Tertiary outcrops rest on a platform carved into the late Precambrian

Bogenfels Formation (mostly dolostone and phyllitic schists in this area), at an

elevation of about 70 m. Beetz (1926) gives general characteristics for the

Tertiary beds. Klinger (1977) presents a diagrammatic stratigraphic section, and

the following description is taken partly from his section, and partly from our

own observations.

The marine beds are only about 4 m thick. They consist of a pebble layer

at the base, which is overlain by concretionary calcareous sandstones and marly

sandstones and siltstones. At least one layer of light-brown (5 YR 5/6)

ferruginous calcirudite occurs near the bottom of the section. This layer contains

_ pebbles, but is predominantly composed of neomorphosed mollusc fragments

set in micrite and microspar (Fig. 8). The marly sand- and siltstones are mostly

pale greenish yellow (10 Y 7/2), poorly consolidated, and calcareous. The

calcareous concretionary layers are greyish yellow (5 Y 7/4) to pale greenish

yellow (10 Y 7/2) and are moderately well indurated. All layers contain occasional

macrofossils and agates. This section is generally much more calcareous than

the Buntfeldschuh section.

PALAEONTOLOGY

Klinghardt discovered the first fossils at Bogenfels (Haughton 19306).

Reuning and Lotz collected from the locality in 1909, and supplied the original

fossils studied by BOhm & Weissermel (1913). A Miocene age was initially

assigned, based mainly on the molluscs and fish teeth. BOhm (1926) later

revised the age to middle to upper Eocene, after obtaining a more extensive

collection of fossils made by Kaiser and Beetz during 1914-19 (Haughton 19305).

16 ANNALS OF THE SOUTH AFRICAN MUSEUM

However, doubt remained in some quarters as to the age of these beds (see

Siesser 1977 for a review). Siesser (1977) eventually confirmed the age as upper

Eocene, based on calcareous nannofossils.

Macrofossils

Bohm & Weissermel (1913), B6hm (1926), and Weissermel (1926) provide

an extensive list of the macrofossils found near Bogenfels. Bryozoans, bivalves,

ES WF Wil

SA WR

\ SASS

Be Dated Tertiary section (kK) Upper Cretaceous inlier

\! Precambrian

Quaternary & Tertiary

BS) thin sand & gravel

Tertiary sand & 1:= 30 000

siltstones

Tw N

Fig. 7. Map showing location of upper Eocene rocks north and north-east of

Bogenfels (from Kaiser 1926; Klinger 1977).

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 17

Fig. 8. Photomicrograph of the upper Eocene mollusc calcirudite at Wanderfeld IV

(Fig. 7). Groundmass is micrite and microspar; light grains are quartz; large elongate

grains are mollusc fragments neomorphosed te pseudospar.

gastropods, a nautiloid, cirripeds, a crab, corals, hydrozoans, fish teeth and

Callianassa burrows are all present. Bivalves and gastropods are the most

abundant fossils: B6hm (1926) named 9 new species in the former class and 13

in the latter from this locality; fish teeth are also numerous and diverse: Bohm

(1926) named 13 new species here.

The abundance and diversity of the gastropod Turritella is especially

_ striking. This genus litters the ground (Fig. 9) in the area, and prompted

Haughton (1930a) to coin the term ‘Turritella-beds’ for the Tertiary outcrops.

Microfossils

Calcareous nannofossils

Moderately to poorly preserved calcareous nannofossils (Figs 10-11) occur

in the clayey siltstones. A list of the species identified follows. The relative

_ percentage of each species, based on specimen counts in smear slides, is also

listed. (These species are all well known and their taxonomy is not controversial ;

therefore a systematic palaeontology section is not included.)

Braarudosphaera bigelowi (Gran & Braarud) Deflandre . . . . i

Braarudosphaera discula Bramlette & Riedel . . . . . ~~. trace

2 LES DIDS SU ee nae rem a eee ey a 1

18 ANNALS OF THE SOUTH AFRICAN MUSEUM

Coccolithus eopelagicus (Bramlette & Riedel) Bramlette & Sullivan . 28

Coccolithus formosus (Kamptner) Wise s,s 6

Discoaster saipanensis Bramlette & Riedel lo. i 5

Discoaster tani Bramlette & Riedel . : ; : : : ; é 3)

isthmolithus recurvus Weflandre ©: 54 . 3. = ea 3

Reticulofenestra bisecta (Hay, Mohler & Wade) Roth . . . . 37

Reticulofenestra coenura (Reinhardt) Roth 2 ny A ee eee

Reticulofenestra umbilica (Levin) Martini & Ritzkowski. . . . 12

Lygrhablithus bijugatus (Dellandre)-Dellandre a 4

The age can be narrowly defined by the range overlap of Discoaster

saipanensis and Isthmolithus recurvus. The former ranges from middle to upper

Eocene and the latter from upper Eocene to lower Oligocene. They co-occur

only in the NP 19 and NP 20 zones of Martini’s (1971) biostratigraphic zonal

scheme, and only in the J. recurvus subzone of Bukry’s (1975) zonal scheme.

Fig. 9. Various species of Turritella weathered out of

the upper Eocene rocks at Wanderfeld IV (Fig. 7).

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET

Gr. .., Fas eee

Fig. 10. Calcareous nannofossils from the upper Eocene rocks at Wanderfeld IV (Fig. 7).

Light photomicrographs. A. Braarudosphaera bigelowi, crossed nicols, scale = 6u.

B. Coccolithus eopelagicus, crossed nicols, scale = 9u. C. Coccolithus formosus,

crossed nicols, scale = 5u. D. Discoaster saipanensis, plane polarized light, scale = 6p.

E. Discoaster tani, plane polarized light, scale = 4u. F. Isthmolithus recurvus, plane

polarized light, scale = 5u. G. Reticulofenestra bisecta, crossed nicols, scale = Sp.

H. Reticulofenestra cf. R. coenura, crossed nicols, scale = 3u. I. Reticulofenestra

umbilica, crossed nicols, scale = 6p.

20 ANNALS OF THE SOUTH AFRICAN MUSEUM

Vail et al. (1977) show the estimated time boundaries of NP 20-NP 19 as

37,2-39,5 m.y.B.P.; Bukry (1975) estimates the boundaries of the J. recurvus

subzone as 38-41 m.y.B.P.

Benthic foraminifera

Poorly preserved benthic foraminifera occur in small numbers in the clayey

siltstones at Wanderfeld IV. This is the first report of in situ upper Eocene

benthic foraminifera on the mainland of South or South West Africa. (The

‘upper Eocene’ deposits recorded by Chapman (1930) in the eastern Cape

Province are now known to be lower Eocene (Siesser & Miles in press).) The

fauna is dominated by Glandulina sp. and Lenticulina spp. Most of the other taxa

are represented by only a few specimens, or in some cases, a single specimen.

Rather formidable taxonomic problems plague the study of benthic

foraminifera under the most favourable conditions (Boltovskoy & Wright 1976;

Boltovskoy 1978). These difficulties are accentuated here, since specimens are

relatively scarce and have been affected by diagenesis (Fig. 1 1c—f). All specimens

have been variously affected by mechanical breakage, solution, recrystallization

or test infilling. The variation noted among specimens of some of the better-

known species suggests that there may be new species present. However,

insufficient numbers of specimens available for study precludes describing them

as new species.

Because there is little previously published information on southern

African Palaeogene benthic foraminifera, and because of the taxonomic

problems involved, a section on systematics follows, together with illustrations

of the taxa identified at Wanderfeld IV (Figs 11-15). Generic assignments have

been made following the classification of Loeblich & Tappan (1964). The

preferred modern species name is given, followed by a brief synonymy.

Family Textulariidae

Textularia sp.

Fig. 12A

Remarks

A single arenaceous specimen from which the initial portion of the test is

partly missing and the remainder indistinct; therefore the generic position is

somewhat uncertain. The test is slightly elongate, biserial and rhomboidal in

section. It is finely agglutinated and fourteen chambers are visible. Apertural

details are obliterated.

Family Nodosariidae

Astacolus sp.

Fig. 12B

Remarks

A solitary specimen with slightly compressed planispiral test, the final

chamber of which breaks away to become uniserial. The last chamber is shorter

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 21

E | | F

=—— ——

Fig. 11. Calcareous nannofossils and benthic foraminifera from the upper Eocene rocks at

Wanderfeld IV (Fig. 7). Scanning electron micrographs. A. Coccolithus formosus, scale = 2.

B. Reticulofenestra bisecta, scale = 24. Note dissolution effects on C. formosus and accretion

of secondary calcite in the central area of R. bisecta. C-—F. Test infilling and test dissolution

in Lenticulina. Differential test dissolution is displayed in C (SAM-K5538) and D (SAM-—

K5539). The umbo and sutures are more resistant to dissolution and remain prominent.

Dissolution eventually produces an internal mould as shown in E (SAM-K5540) and

F (SAM-KS5541). Scale = 100z.

aD ANNALS OF THE SOUTH AFRICAN MUSEUM

in height, but broader than the previous chambers. Twelve chambers are

visible and the sutures are flush to very slightly raised.

Lenticulina simplex d’Orbigny, 1839

Fig. 12C—D

Robulus simplex (d’Orbigny) Cushman & Laiming, 1931: 98, pl. 10 (fig. 5a—b).

Remarks

A few well-preserved specimens occur, with thick, prominent umbos and

keels.

Lenticulina cf. L. pseudo-mamilligerus (Plummer, 1926)

Fig. 12E-F

Robulus pseudo-mamilligerus (Plummer) Cushman, 1951: 13, pl. 4 (figs 1-5).

Remarks

The illustrated specimen resembles the species figured by Cushman (1951)

in test outline and in suture and chamber disposition.

Lenticulina cf. L. oblonga (Coryell & Howe, 1930)

Lenticulina cf. L. oblonga (Coryell & Howe) fide Fairchild, Wesendunk & Weaver, 1969:

42, pl. 6 (fig. 4a—b).

Remarks

A poorly preserved eight-chambered specimen was found. The keel is

present on the early chambers only, the remainder unpreserved.

Lenticulina subalata Reuss, 1854

Fig. 13A-B

Cristellaria subalata Reuss, 1854: 68, pl. 25 (fig. 13). Chapman, 1926: 65, pl. 4 (igs 19a—b,

25a—b, 26a—b).

Remarks

Two specimens of this species were found. This form has been noted from

the Aptian by Reuss and from the upper Eocene of New Zealand by Chapman

(1926).

Lenticulina spp

Remarks

Twelve very badly preserved specimens were found. None could be

definitely identified to species level.

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 23

c gies

Fig. 12. Benthic foraminifera from the upper Eocene at Wanderfeld IV (Fig. 7). Scanning

electron micrographs. All scales = 100u, unless otherwise noted. A. Textularia sp. SAM-—

K5520. B. Astacolus sp. SAM-K5521. C. Lenticulina simplex, side view, SAM-K5522,

scale = 300u. D. Lenticulina simplex, peripheral view, SAM-K5522. E. Lenticulina cf.

L. pseudo-mamilligerus, side view, SAM-K5523. F. Lenticulina cf. L. pseudo-mamilligerus,

peripheral view, SAM-K5523.

24 ANNALS OF THE SOUTH AFRICAN MUSEUM

Family Glandulinidae

Siphoglobulina ? sp.

Fig. 13C-D

Remarks

A single specimen appears referable to this genus, but the state of preserva-

tion does not allow an accurate diagnosis. The test is subfusiform and circular in

cross-section. Chambers are strongly overlapping, the sutures depressed and the

specimen has a terminal radiate aperture. In side view the specimen appears

similar to Marginulina, a distinguishing feature of this genus noted by Parr

(1950) in his description of the genoholotype Siphoglobulina siphonifera. The

genus ranges from lower Tertiary to Holocene.

Family Polymorphinidae

Glandulina sp.

Fig. 13E

Remarks

The most abundant form present in the Bogenfels section. Chambers and

sutures are indeterminate because of poor preservation. The terminal, radiate

aperture, however, is often preserved. |

Family Elphidiidae

Elphidium cf. E. crispum (Linné, 1758)

Fig. 13F

Nautilus crispus Linné, 1758: 709.

Polystomella crispa (Linné) Brady, 1884: 736, pl. 110 (figs 6-7).

Elphidium crispum (Linné) Barker, 1960: 220, pl. 110 (figs 6-7).

Remarks |

A single, broken specimen was found. Although broken, the features of the

central boss, chambers and sutures suggest E. crispum, rather than the closely

related form E. macellum.

Elphidium sp. A

Fig. 14A—-B

Remarks

A small Elphidium with subcircular outline has twelve chambers and raised.

sutures bridged by retral processes. The retral processes (four or five present)

of the earlier parts of the whorl are confused, giving a pitted appearance to the

test. The aperture consists of a number of pores at the base of the apertural face.

This specimen is very similar to E. saginatum Finlay, but differs in not having a

depressed central area.

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 25

E ess F cones,

Fig. 13. Benthic foraminifera from the upper Eocene at Wanderfeld IV (Fig. 7). Scanning

electron micrographs. A. Lenticulina subalata, side view, SAM-K5524. B. Lenticulina

subalata, peripheral view, SAM—K5525. C. Siphoglandulina? sp., side view, SAM-—K5526.

D. Siphoglandulina? sp., front view, SAM-K5526. E. Glandulina sp. SAM-K5527.

F. Elphidium cf. E. crispum side view, SAM--K5528. All scales = 100z.

‘

;

}

26 ANNALS OF THE SOUTH AFRICAN MUSEUM

Elphidium sp. B

Fig. 14C—D

Remarks

This well-preserved specimen has a flattened test with near-parallel sides.

Numerous chambers with raised sutures and retral processes are present, but

detail of the earliest chambers of the whorl is confused because the specimen is

broken. The umbilical area is slightly depressed and filled with calcareous

nodules. Small papillae cover the chambers and the apertural face. The aperture

consists of four pores in a circular position at the base of the apertural face and

three pores in the areal position in the lower half of the apertural face. The

specimen appears somewhat similar to Discorotalia tenuis, but trochospiral

coiling cannot be confirmed as the specimen is broken. It also differs from

D. tenuis by having the typical circular apertures of Elphidium.

Family Nonionidae

Nonion costiferum (Cushman, 1900)

Fig. 14E-F

Nonion costiferum (Cushman) fide Rau, 1964: 16, pl. 5 (fig. 5).

Remarks

Three specimens of this species were identified. The species is notable in

having raised sutures and a depressed umbilical region. The specimens from

Wanderfeld IV differ from those illustrated by Rau (1964) in possessing fewer

chambers. The previously reported occurrence of this species in the U.S.A. is

near the Oligocene-Miocene boundary (Rau 1964).

Nonion sloanii (d’Orbigny, 1839)

Fig. 15A

Nonionina sloanii d’Orbigny, 1839: 68, pl. 6 (fig. 18).

Nonion sloanii (d’Orbigny) Cushman, 1930: 9, pl. 3 (figs 6-8).

Remarks

This species is represented by a single specimen. It has been recorded in

sediments of Eocene to Holocene age.

Family Discorbidae

Valvulineria aegyptina Le Roy, 1953

Fig. 15B

Valvulineria aegyptina Le Roy, 1953: 53, pl. 9 (figs 21-23).

Remarks

The specimen found differs from the type by having dorsal chambers

which overlap strongly, making only eight chambers visible. Apertural features

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET oi |

SE |

Fig. 14. Benthic foraminifera from the upper Eocene at Wanderfeld IV (Fig. 7). Scanning

electron micrographs. All scales = 100u, unless otherwise stated. A. Elphidium sp. A, side

view, SAM-K5529. B. Elphidium sp. A, peripheral view, SAM-—K5529, scale = 30u.

C. Elphidium sp. B, side view, SAM-—K5530. D. Elphidium sp. B, peripheral view, SAM-K5530.

E. Nonion costiferum, side view, SAM-—-K5531. F. Nonion costiferum, peripheral view,

SAM-K5532.

;

28 ANNALS OF THE SOUTH AFRICAN MUSEUM

are not distinct as the apertural flap is broken; therefore the full extent of the

aperture is not known. Other features are typical of this species. A coarsely

punctate wall occurs on both dorsal and ventral sides. A typically imperforate

area occurs on the lower ventral part of the final chamber. The final chamber is

inflated and extends over, and covers part of, the central umbilical region. The

dorsal side is flat, the ventral side convex and umbilicate. This species is

recorded from the Eocene in Egypt.

Family Rotaliidae

Ammonia cf. A. beccarii (Linné, 1767)

Nautilus beccarii Linné, 1767: 1162.

Rotalia beccarii (Linné) Cushman, 1928: 104, pl. 15 (figs 3-7).

Ammonia beccarii (Linné) Cifelli, 1962: 119, pl. 21 (figs 1-6).

Remarks

This genus occurs in two forms at Bogenfels. A. beccarii has a ventral

umbilical area which lacks an umbilical boss, but this is not unusual in this

species.

Ammonia sp.

Remarks

Broken specimens occur which were impossible to identify because of poor

preservation. The features visible are typical of the genus. The umbilical area is

closed but a small protruding plug is present. This is not the typical plug found

in A. beccarii; the plug appears as a nodule of material on the umbilical

covering.

Pararotalia inermis (Terquem) emend. Le Calvez, 1949

Fig. 15C-D

Rotalia inermis Terquem, 1882: 68, pl. 6 (fig. la—c).

Pararotalia inermis (Terquem) emend. Le Calvez, 1949: 32, pl. 3 (figs 54-56).

Remarks

Badly broken specimens of this species were found. The tests are eroded

into the typical mushroom shape in side view. Perforate chambers are separated

by flush, oblique, imperforate sutures, and an imperforate central area occurs

on the dorsal side. The umbilical plug has been eroded out by removal of some

or all the chamber flaps. This species was originally described by Terquem (1882)

from the middle Eocene of the Paris Basin. McMillan (1974) described a closely

related form, Pararotalia cf. P. inermis, from Holocene sediments on the

Agulhas Bank.

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 29

‘ § 2. :

t J ES

Fig. 15. Benthic foraminifera from the upper Eocene at Wanderfeld IV (Fig. 7). Scanning

electron micrographs. A. Nonion sloanii, side view, SAM-—K5532. B. Valvulineria aegyptina,

dorsal view, SAM-—-K5533. C. Pararotalia inermis, dorsal view, SAM-—K5534. D. Pararotalia

inermis, ventral view, SAM—K5535. E. Cibicides pseudoungerianus, dorsal view, SAM—K5536. .

F. Cibicides sp., peripheral view, SAM—-K5537. All scales = 100u. .

30 ANNALS OF THE SOUTH AFRICAN MUSEUM

Family Cibicididae

Cibicides pseudoungerianus (Cushman, 1922)

Fig. 1SE

Truncatulina pseudoungeriana Cushman, 1922: 97, pl. 20 (fig. 9).

Cibicides pseudoungerianus (Cushman) Cushman, 1931: 123, pl. 22 (figs 3-7).

Remarks

A species that ranges from the Eocene to Holocene; only a single specimen

was found.

Cibicides sp.

Fig. 15F

Remarks

This specimen is not well preserved, but has features similar to the form

Cibicides sp. illustrated by Van Hinte (1963), viz. a central raised area on the

dorsal side.

Cibicides spp

Remarks

A number of poorly preserved forms were found which fit the basic

description of this genus. .

PALAEOECOLOGY

Members of the nannofossil genus Braarudosphaera are virtually absent in

open-ocean deposits, and are thus strong indicators of nearshore environments;

Zygrhablithus bijugatus is also most common in nearshore waters. These taxa

make up a small percentage only of the nannoflora in the samples studied, but

their presence in even minor amounts suggests deposition in a shallow-water

environment. The benthic foraminifera also suggest a normal marine, shallow-

water environment.

The nannoflora may in general be considered a temperate-water assemblage.

However, Isthmolithus recurvus is a cool-water nannoplankter. Miliolid and

peneropolid foraminifera, which are normally common, are conspicuously

absent among the benthic foraminifera, and this also suggests that ‘cool—

temperate’ may be the most appropriate designation for the water mass

overlying this site during the upper Eocene.

The benthic foraminifera are not closely age diagnostic, but do corroborate

a Palaeogene age for the Wanderfeld IV beds.

STRATIGRAPHIC STATUS OF THE TERTIARY DEPOSITS

Early workers assumed age equivalency among the scattered Tertiary rocks

cropping out between Buntfeldschuh and the Bogenfels—Granitberg area.

Haughton (1930qa) first expressed doubt, on palaeontologic grounds, noting that

the fish teeth reported at Buntfeldschuh do not prove these beds are con-

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 3]

temporaneous with the Bogenfels exposures. Bohm (1926: 55), refers to abundant

fish remains at Buntfeldschuh in the introductory remarks to his paper on the

Bogenfels fossils. But he does not designate any teeth specifically from Buntfeld-

schuh in the text of his paper, and his summary table on p. 86 lists teeth from

Bogenfels only. Based on published reports, the numerous geologists who have

subsequently visited Buntfeldschuh have failed to find a single marine body

fossil (e.g. Haughton 1930a; Stocken 1962; Ziegler 1969; Martin 1973; Siesser

1977), although C. G. Stocken (pers. comm. 1979) has confirmed the presence of

fish teeth in the pebble layers. The Buntfeldschuh section is therefore considered

to be essentially unfossiliferous, and in marked contrast to the highly fossiliferous

sections near Bogenfels.

Nor can the two localities be correlated on lithologic grounds: dissimilarities

are as apparent as similarities (cf. Beetz 1926; Klinger 1977; and the descriptions

in this paper). In fact, the chief basis for age correlation seems to be that both

contain lenses of agates and other pebbles (Beetz 1926; Kaiser 1926; Martin

1973). Against this, Haughton (1930a) points out that the Buntfeldschuh beds

contain pebbles and boulders of the Pomona beds (pre-Oligocene, possibly

Cretaceous (Stocken 1962)), whereas the exposures near Wanderfeld IV do not

(Haughton 1930a). Descriptions by Beetz (1926) also suggest lithologic

similarity among the various non-fossiliferous outcrops in the area, and among

the fossiliferous outcrops, but less similarity between the two. A significant

point is the relative elevations of the fossiliferous and non-fossiliferous beds. The

base of the exposures at Buntfeldschuh lic 65 m above those at Wanderfeld IV,

and those at Advokat Bake and Eisenkieselklippenbake lie up to 100 m above

Wanderfeld IV (Kaiser 1926; Haughton 1930a; Stocken 1962).

Haughton (1963) has already suggested that there may be an age difference

between the higher and lower Tertiary deposits in this area. He suggested that

the higher deposits may be Eocene and the lower may be Miocene, presumably

believing, with Du Toit (1954), that the original age (Miocene) assigned by

Bohm & Weissermel (1913) to the lower deposits was more likely to be correct.

The writers also think the higher, non-fossiliferous deposits are probably older

than the lower, fossiliferous deposits. But there is now an unequivocal date for

the lower deposits: upper Eocene. Therefore the higher deposits may be upper

Paleocene-lower Eocene. This suggestion is based on evidence for a late

Paleocene—early Eocene transgression of the Cape Province south coast recently

documented by Siesser & Miles (1979). Moreover, Siesser & Dingle (1979) have

suggested that this transgression was higher and more extensive than the late

Eocene transgression around the coast of southern Africa.

The writers frankly admit that assigning the Buntfeldschuh outcrops to the

upper Paleocene—lower Eocene is based on circumstantial evidence. But it is no

more speculative than to assign them to the middle or upper Eocene, or to the

Miocene for that matter, as has been done in the past. In fact, what little evidence

there is for the age of these unfossiliferous beds (viz. topographically higher than

the known upper Eocene deposits; known major late Paleocene-early Eocene

32 ANNALS OF THE SOUTH AFRICAN MUSEUM

transgression in southern Africa) supports the age assignment suggested here.

Whatever the age relationship of these two units, their lithologic dis-

similarity precludes their inclusion in a single lithostratigraphic unit. The

generally higher, and essentially non-fossiliferous beds are best exposed at

Buntfeldschuh, and this can be regarded as the type locality for this unit.

A ‘Buntfeldschuh Formation’ is thus potentially available, but is not herein

proposed. SACS (1977: 21) has set out strict requirements for establishing a

formal lithostratigraphic unit, and the writers do not have sufficient data on this

unit to describe a stratotype. However, the 1977 South African Stratigraphic

Code makes clear provision for the erection of informal lithostratigraphic units

in such cases. Thus it is proposed that this unit be informally termed the

‘Buntfeldschuh beds’. This name can be upgraded to the ‘Buntfeldschuh

Formation’ if and when the requirements for formal status can be met.

Topographically lower and richly fossiliferous outcrops occur near

Bogenfels, with the best-known exposures at Wanderfeld IV. This unit is also a

potential formation, but again cannot be formally proposed in this paper for the

same reason: insufficient data available to satisfy requirements for erection of a

formal stratotype. It is proposed that this unit also be given informal status.

As with a formal unit, an informal unit should carry a geographic name.

‘Bogenfels’ is unsuitable, as it already is used for the Precambrian dolostone

formation in the area. Similarly, “Wanderfeld IV’ has already been pre-empted

for the Cretaceous informal lithostratigraphic unit occurring in the same area

(Klinger 1977).

The writers suggest that this unit be informally called the ‘Langental beds’,

referring to the long valley adjacent to which the best exposures occur. This name

can later be upgraded to the ‘Langental Formation’.

ACKNOWLEDGEMENTS

Consolidated Diamond Mines of South West Africa Ltd kindly granted

permission and provided facilities for one of us (WGS) to visit and sample the

outcrop areas. Dr C. G. Stocken and Mr D. Minney of Consolidated Diamond

Mines are thanked for their efforts in making the trip a success. The senior

author is grateful to the South African Committee for Stratigraphy who

provided funds for his flight to Oranjemund. The South African Geological

Survey also provided additional samples, which were originally collected by

Dr H. C. Klinger, from the area.

The senior author began this project while a member of the Department of

Geology, University of Cape Town and completed it after he joined the

Palaeontology Department, South African Museum. Both organizations are

thanked for their support. We wish to thank the Director of the Geological

Survey for permission for one of us (DS) to publish.

Scanning electron micrographs were taken in the Electron Microscope

Unit, University of Cape Town. Dr C. G. Stocken read the manuscript and

offered useful comments.

EOCENE MARINE SEDIMENTS IN THE SPERRGEBIET 33

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