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Jean-François Deconinck (USTL, Lille)

Patrick De Wever (MNHN, Paris)

Jean Marcoux (U. Denis Diderot, Paris)

Christian Ravenne (IFP, Paris)

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geodiversitas

InterRad VIN, Paris/Bierville 8-13 septembre 1997

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Introduction

The first meeting of radiolarian micropaleonto-

logists was organi/.ed in 1978 by R De Wever

(Lille, France). Most participants being from

European universities, the name o( “EuroRad”

was coined to designatc this meeting and the fol-

lowing ones. EuroRad II was held in 1980

(Basel, Swilzerland), EuroRad Ilî in 1982

(Bergen, Norway), and EuroRad IV in 1984

(Leningrad, USSR). More and more radiolarists

from ail continents joining the EuroRad group, a

formai international association ol radiolarian

micropaleontologists was created and its First

meeting (InterRad V) was held in 1988 at

Marburg (Gcrmany) followcd by InterRad VI in

1991 (Firenze, Italy), and Interrad VII in 1994

(Osaka, Japan).

The last InterRad VIII meeting (almost twenty

years after Eurorad I) was held Iront September

8th to 13th (1997) at the Château de Bicrville, a

meeting centre locaied 50 kilometers South of

Paris (France). 85 participants from 17 councries

attended 8 workshops and presented 144 oral

communications or posters. The abstracts of the

communications were published in a spécial

volume before the meeting, and furrher distribu-

ted to a total of 200 scientists. A one day spécial

excursion was organized during InterRad VIII

including a wcll-apprcciated visit of a winery in

the Loire area including somc wine tasting, and a

visit of the Château de Chambord, a gorgeous

Renaissance castle.

During the meeting, 23 papers were offered for

publication in a spécial issue of Geodiversitas. A

grand total of 21 manuscripts were received by

the éditorial committee and submitted to a pair

review. Finally, 14 publications were selected and

are presented in this volume.

Two years after InterRad VIII, this spécial issue

ol Geodiversitas cannot reflect the wide scope of

the communications that encompassed ail the

geological record from Cambrian to Présent.

Original information Is, however, given about

significant advances in radiolarian biosrratigra-

phy of Mesozoie formations of the Aritartic and

Pacific domains. New taxonomie descriptions of

Paleozoic and Mesozoie forms arc presented. A

single paper is devoted to the radiolarians of the

Messinian diatomites of the Mediterranean area.

As usual, publication delay was longer rhan

expected due to scveral reasons: some authors

were lare submitting their manuscript, some

reviewers took a lengthy time to review manus¬

cripts and answer successive requests from the

editor. Modifications requested by reviewers took

some extra time to bc completed.

Support from the CNRS, the Muséum national

d’Hisioire naturelle, the Ministère des Affaires

étrangères and the Total Company is gratefully

acknowledged.

Patrick De Wever and Jean-Pierre Caulet

GEODIVERSITAS • 1999 • 21 (4)

501

Non-Tethyan Triassic Radiolaria from

New Zealand and northeastern Siberia

Yoshiaki AITA

Department of Geology, Faculty of Agriculture, Utsunomiya University,

350 Mine, Utsunomiya 321-8505 (Japan)

aida@cc.utsunomiya-u.ac.jp

Nikita Yu. BRAGIN

Geological Institute, Russian Academy of Sciences,

Pyzhevsky 7, 109017 Moscow (Russie)

bragin@ginran.msk.su

Aita Y. & Bragin N. Yu. 1999. — Non-Tethyan Triassic Radiolaria from New Zealand and

northeastern Siberia, in De Wever P. & Caulet J.-P. (eds), InterRad VIN, Paris/Bierville 8-13

septembre 1997, Geodiversitas 2^ (4) : 503-526.

KEY WORDS

Radiolaria,

non-"l’ethyan,

Middic Triassic,

New Zealand,

Siberia,

new species,

Glomeropyle n. gen.

ABSTRACT

We!Upresei*vcd Middle Triassic radiolarian faunas hâve been documented

from phosphatic nodules collected from the Waipapa Terrane, New Zealand

and the Omolon Massif, northeastern Siberia, respectively. Both New

Zealand and northeastern Siberia faunas include many species that are well-

known from European Tethys area, including Silicarmtger costatus costatus

Dumitrica, Kozur & Mostler, 1980 which indicates an early Ladinian âge.

These Tethyan species occur with abondant non-Tethyan l adiolarians that

are characteristic of these faunas. Distinctive pylomate spumellarians are des-

cribed herein as a new genus Glomeropyle Kwa &c Bragin. This genus bas not

been recognized in Middle Triassic sequences of Europe, Japan, Southeast

Asia or North America. Seven new Middle Triassic species are described:

Glomeropyle atirora, Glomeropyle horeale, Glomeropyle poinuiy Glomeropyle (?)

galagalay Glomeropyle grantiruickiei, Glomeropyle mahinepunensis-, Glomeropyle

waipapaensis. They do not hâve Tethyan affinities and are only known from

northern and Southern high latitudes. They are Triassic Radiolaria with a

bipolar distribution pattern.

GEODIVERSITAS • 1999 • 21 (4)

503

Aica Y. & Bragin N. Yu.

MOTS CLÉS

radiolaires»

non-Téthys.

Trias moyen»

Nouvelle-Zclandc,

i)jbérie,

nouvelle espèce,

Glomeropyle n. gen.

RÉSUMÉ

Radiolaires triasi^ues non téthysiens de Nouvelle-Zélande et dti Nord-Est de la

Sibérie.

Des radiolaires bien conserves du Trias moyen ont été découverts dans des

nodules phosphatés provenant des formations Waipapa, en Nouvelle-

Zélande c( du massif Omolon, au Nord-I£st de la Sibérie. Les deux faunes

comprennent de nombreuses espèces bien connues en Europe de la zone

téthysienne, incluant Silinirmiger costatus costatus Dumitiica, Kozur &

Mosticr» 1980 qui indiquent un age Ladtnien inférieur. C'es espèces téthy-

siennes existent avec de nombreux radiolaires non-téchysiens, caractérisliques

de CCS fituries. Parmi eux des spumellaires i pylome sont décrits dont le nou¬

veau genre Glomeropyle Aira & Bragin. Ce genre n'avait pas encore été trouvé

dans les séries du Trias moyen d’Europe» du J.apon, d'Asie du .Sud-Est et

d’Amérique du Nord. Sept nouvelles espèce.s du Trias moyen sont décrites :

Glomeropyle aitrora, G. horcaU\ G. poinw^ G. (?) galagitLu G. g>’ant7?iackieK

G. intthiriepuaensis-i G. ivaipapuensis. Elles n’ont pas d’afFinités téthysiennes et

sont seulement connues dans les hautes latitudes (Nord et Sud). Ces faunes

triasiques ont donc une distribution bipolaire.

INTRODUenON

In récent year.s radiolarians bave provided

valuable information on the âge of previously

undated strata» improvements to corrélation both

within terranes and between terranes, and in the

assessrnenr of paleobiogcographic aiTinities (Aita

bc Spbrü 1992» 1994). Recendy, distinctive non-

Tethyan rudiolarian faimas bave been fbund in

Middle Triassic strata in both New Zealand and

northeastern Siberia (Fig. 1), (Aiia in MaLsuoka

et ai 1996: 204-206; Bragin in Matsuoka et al.

Fig. 1. — Paleogeographic map of the Middle Triassic (Ladinian-Anisian) at 237 million years ago (Ma), showing localities cited in

this study in New Zealand, northeastern Siberia and northern Italy (modified from Scotese 1997; Smith étal. 1994).

504

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

1996: 209). Alrhou^i gcographically distant, the

fimnas of büth areas art* very similar and almost of

corrélative âge. They both include distinctive spu-

meJlarians wirh pylome. These taxa hâve never

bccn reported from Tethyan areas (Dumitrica et

al 1980; Ko 2 ur ô£ Mostler 1994; Kozur ei al.

1996; Dumitrica pets, comm.), Japan (Yao 1982;

Sugiyama 1997; Ohtaka et al. 1998). or the

Philippines (Yeh 1990). In this paper, we describe

and illastratc these high-latitude ta.xa^ including

one new gcniis and seven new species. In addi¬

tion, we briefly summarizc the lichostratigraphy

of the radiolarian-beanng séquences in New

Zealand and in northeastern Siberia.

TRIASSIC RADIOLARIA IN WAIPAPA AND

CAPLES TERRANES, NEW ZEALAND

Waipapa 'I’errane, Mahinepua Peninsula,

Northiano

The Waipapa Terrane is one of rive Meso/oic ter-

rancs recogni/ed in the North Island, New

Zealand (l'ig. 2). It lies in the northeastern and

central part of the North Island and consists of

spihtic basalts, radiolarian cherts, green argillites,

and terrigenous clastics (Aifa & Sporli 1992).

Although these rocks are metamorphosed to

Fig. 2, — Map showing basement terranes of New Zealand and

location of Whangaroa area (squared area) In the Waipapa

Terrane, modified from Aita & Spôrü (1992) and Poser et al.

(1993). *, Bull Creek in the Caples Terrane.

Whangaroa Bay

Arrow Rocks

Whangaihe Bay

xjÿfxp

Pacific Océan

Mahinepua Section

Kairawaru

Mahinepua Bay

Tauranga Bay

massive sandstone

green siliceous argillite

bedded chert

spilitic basait with limestone |

Xp,xt fossil locality

P: Permian, T: Triassic

0 500 1000m

Fig. 3. — Geological map of the Whangaroa area, Northland, New Zealand and location of the Mahinepua Section (squared area) in

the Waipapa Terrane. and fossil localities. Xp, Permian âge; Xt, Triassic âge.

GEODIVERSITAS • 1999 • 21 (4)

505

Aita Y. & Bragin N. Yu.

Green argillite & siliceous sandstone

with phosphatic concrétions _

Green argillite

radiolarian-bearing

samples

Grey chert & black siliceous argillite

Fig. 4. — Geoiogical sketch map showing wave-cut bench exposures on Mahinepua Peninsula, Northland, New Zealand. Five strati¬

graphie units are recognized. Measured sections from A lo K and location of radiolarian samples are indicated. Sample PO4/f103 (=

fleld No. MAH-3.5); Grid reference P04/88618928. Whangaroa sheet P04. New Zealand 1:50.000 topographical map sériés NZMS

260.

prehnilc-pumpcilyite faciès (Black 1994), phos¬

phatic concrétions hosted wichin green argillite

hâve yi'cldcd well'prescrvcd radiolarian faiinas

(Sakai et al. 1998).

In general, the âges ol the radiolarian faunas in

the Waipapa Icrrane show that an older

Permian-Triassic complex occurs in the north

and a youngen Jriassic-Jura.ssic complex is in the

South (Aita & Sporli 1992; Sporli et ni 1989; sce

also Black 1997). Borh complexes consist ol very

similar lithologie scqucnccs charactcrizcd by

radiolarian chert. green argillite and terrigenous

mudstotîc and sandstone although the older

complex also has some spiliric basait with asso-

ciated limestonc Icnses.

In the Whangaroa area, located in the northern

part oi the Waipapa Terrane, the older Waipapa

rocks are well exposed in sections at Arrow

Rocks, Marble Bay, Orua Bay, Kairawaru Bay,

and Mahinepua Peninsula (Fig. 3).

Beddcd cherts in tins area arc of Late Permian âge

(Aita & Sporli 1992) whilc Latc Triasslc radiola-

rians from phosphatic concrétions within green

argillire at Mahinepua hâve been repcirted by Aita

in Matsuoka et tti (1996), Detailed investigations

of the Waipapa Terrane h\' a Japanese and New

Zealand collaborative research projcct in 1995

and 1996 revcaled that the hemipelagic green

argillite at Mahinepua ranges from Middie to

Late Tria.s.sic in âge (Takernura et ni 1998),

A rc-cxaniiivation of the Permian fusulinid liines-

tones from Orua Bay by Leven ôc Grant-Maclde

(1997) re.sulted in the identification of Yttheina

globosa (Yabe, 1906) and Leptdolîna shimiwaensis

O/.awa, 1925, and establishcd corrélation with

the Yabeinn-Lepidolina zone of the Midian Stage.

Leven & Grant-Mackie (1997) attribuie the

Midian to the Late Permian, but fbllowing Jin et

506

GEODIVERSITAS • 1&99 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

40'

39H

37-

36-

35-

34-

33-

32-

ibH

16 i

12-1

^ Stratigraphie Columns of Mahinepua Section

Bluish grey mudstone

with turbldites

-1

yc6

H76

h75

h74

T-C-2

MAH-63-

'73

71.72

vhite tuff layer

» brown chéri

%in white laye^

I cherty bed

Unit 4

•Fault

• Fault

brownish tuff

-D-5

white tuff layer

Unit 3

I Green argillite and siliceous

thin bedded unit sandstone with

^ phosphatic concrétions

^8-3

cherty bed

MAH-5.15

Green argillite

Unit 2

Ff103(=MAH-3.5) 9^®®" ^''9'*''^® with

phosphatic concrétions

^MAH-1.0

A, B,C

grey chert and black

siliceous argillite

Unit 1

Fig. 5. — Stratigraphie columns in the Mahinepua Section, Waipapa Terrane, New Zealand. Composite columns show lithologie

composition of four units and horizons of radiolarlan-bearing samples.

al. (1997), the Midian îs correlated with the Late

Middle Permian Capitanian Stage. More recent-

ly, the lithostratigraphy and radiolarian biostrati-

graphy of the Late Permian to Middle Triassic

succession at Arrow Rocks has been described

(Takemura étal. 1998, 1999 in this volume).

GEODIVERSITAS • 1999 • 21 (4)

507

Aita Y. & Bragin N. Yu.

Table 1 . — Radiolarian faunal list for Mahinepua, Bull Creek (New Zealand) and Dzugadzak River (Northeast Siberia) and occurren¬

ce of radiolarians from Buchenstein Limestone, Recoaro (Northern Italy).

NEW

NE SIBERIA

N ITALY

ZEALAND

Waipapa

Caples

Omolon

Vicentinian

Terrane

Massiv

Alps

Locality

Mahinepua

Bull Creek

Dzugadzak

Recoaro

River

Sample or Unit

PO4/t103

H45f074

7438-89-1

Buchenstein

Field No.

MAH-3.5

YABC-26

Unit 10

Limestone

Spongopallium confortum Dumitrica, Kozur & Mostler

Spongopaltium aff- kappi (Lahm)

Spongopallium sp.

Cryptosîephanidium iongispinosum (Sashida)

Hindeosphaera sp.

Pseudostylosphaera sp.

Eptingium sp.

Kahlerosphaera sp.

Plafkerium (?) sp.

Stauracontium (?) sp.

Archaeosemantis sp.

Parentactinia inerme Dumitrica

Parentaotinia pugnax Dumitrica

Pentactinorbis mostieri Dumitrica

Pentactinorbis sp.

Glomeropyte nurora Aita. n. sp.

Glomeropyle boreale Bragin, n. sp.

Glomeropyte poinui Aita. n. sp.

Gfomeropyl9 ('') gaiagala Aita, n. sp.

Glomerupytë giantmacKitii Aïia, n. sp.

Glomeropyle mahhepuaensis Ma, n. sp.

Glomeropyle waipapaensis AWa, n. sp.

Silicarmiger cosiaîus costatus Dumitrica,

Kozur & Mostler

Silicarmiger ci. laïus Kozur & Mostler

Silicarmiger sp.

Foremanellina aranea Dumitrica

Foremanellina expansotabrum Dumitrica

Foremaneliina sp.

Recoaroella sp.

Triassospongocyrîis sp.

Hozmadiaci retreu/ata Dumitrica. Kozur & Mostler

Hozmadia sp.

Goestlingella sp.

Pouipus sp.

Pachus (?) sp.

Laxtorum (?) sp.

Simple multicyrtoids

MAHfNFPiiA Section

Mahinepua section is located on the northern

side of Mahinepua Peninsula (Fig. 3), east of the

Whangaroa area, North Island, New Zealand.

The fossil locality is PO4/fl03 (= field

No. MAH-3.5), grid référencé P04/886892 in

the archivai New Zealand Fossil Record File

maintained by the Gcological Society of New

Zealand, i.e. locality No, 1103 in map sheet P04

of the 1:50,000 sériés NZMS260. It lies in the

lower part of Unit 2 (Fig. 4).

The complété section consists of red bedded

508

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

chère (20 m thick). green siliceoüs argillite

(25.5 m), bluish grey mudstone with turbidites

(30 m), and massive sandstone (> 100 m) in

ascending order (Figs 4, 5). This is a typical

“chert-green argillite-clascics” sequence which is

considered tt? rcpicscnc a suaiigraphically conti¬

nuons accrctionary scqucnce From pelagic (bed-

ded chert) and hcmipclagic (green argüiire) faciès

to terrigenous Faciès (b!ue-grey nmdstone and

massive sandstone). Black phosphatic concré¬

tions from many horizons vvithin the green argil¬

lite yielded diverse, well-prcserved radiolarian

faunas of Middlc co Late Triassic âge.

The Mahinepua Section is subdivided into five

unies as follows (Figs 4, 5):

Unit 1. Grey chert and black siliceoüs argillite ..

. 5 m.

Unit 2. Green argillite with lenticular phosphatic

bands . 10 m.

Unit 3- Well bedded green argillite and siliceoüs

sandstone with phosphatic concrétions and inter-

calated thin white tuff. 15 m.

The lower 4 m is thïn bedded.

Unît 4. Bluish grey mudstone with turbidites ....

.30 m.

Many turbidites layers of 10-20 cm thickness are

intercalated with mudstones.

Unit 5- Massive sandstone . 100 m.

The radiolarian fauna in the basal part ol Unît 2

includes Pseridostylosphaera spinuJosa (Nakascko

& Nishimura, 1979), Glomeropyle atirora n. sp.,

Hozrnadiû aff. pyntmidulis Gorican, 1990 in

Gorican Ruser, 1990. Sample fl 03 (= field

No. MAH-3.5) is a black phosphatic concrétion

taken from 3.5 m above the base of tlils unît and

contains well-preserved Middle Triassic radiola-

rians. The launa îs doniinated by abundant

Spumellaria including Spongopallium contortnni

Dumitricaï Koyur & Mostler, I9S0, Plafkcriurn

(?) sp., Eprinpum (?) sp.» Parcinactinia inerme

Dumirrica, P. pugnax Dumitrica, 1978,

Pentactinorbls mosderi Dumitrica, 1978, and

Cryptostephanidiuni longispinosum (Sashida,

1991). In addition, Glomeropyle aurora n. sp.,

G. poinui n. sp., G. (?) galagala n. sp., G. grant-

stage

Unit

Lllhology

Carnian

jgBggggjjgg

Ladinian

Anisian

Olenakian

0t1

injmj

Induan

ES3

mudslone sritstone

limestone phosphatic

concrétions

Fig. 6. — Géographie location (A. B) and stratigraphie column

Dzugadzak River (Oniulon Mae»if noftheaslern Sibeda).

Location map D showmg the sludied section (squared area.

Fig. 7). Synibote ûit IhH luit aide ot me stratigraphie column are;

(1) stngo and substage: 1?, probably Induan, ol1.

Olenekinn: ol2. late Olcnekian; a2. middle Antsian; «3. iat«

Anisian, (2. laie Lariinien. kl. esrly Carnidn: k2?. probably

middle Carnian; (2| numbejr of stratigraphie unii as deactibed

herein.

mackiei n. sp., G. mahineptiaensis n. sp. and

6’ waipapaensis n. sp. are présent. The nassella-

rians include Silicarmiger costatus costatus

Dumitrica, Kozur & Mostler, Foremanellina ara-

nea Dumitrica, 1982, Hùzmadia cl. reticulata

Dumitrica, Kozur 6l Mostler, 1980, Hozmadici

aff. pyramidalis Gorican and an lindescribed

form oF PoitlpKS, This assemblage is con.sidered tp

be oF early Ladinian âge.

The first appcarance ol Capnmhùsphaerti inclu¬

ding C, colernani Blome, 1983, is recorded iii the

middlc part of Unit 3. Nunierous undescribed

spumellarians bclonging lo the gênera CapnU'-

chosphitera De Wever, 1979, Dumitricasphacru

Koziu & Mostler, 1979, KarfwspongclLi Kozur ik.

Mo.silcr. 1981, Pantatidlmn) IVssagno, 1977,

Siirki Fessagno, 1979, Wclirdla Dumitrica, Kozur

& Mostler, 1980. Xenorurn Blome, 1984 are al-so

présent in this unir, and a Late l'riassic age is

inferred.

GEODIVERSITAS • 1999 • 21 (4)

509

Aita Y. & Bragin N. Yu.

Quaternary alluvial deposits

Cretaceous dolerite dykes

Cretaceous granitoids

Late Triassic (Norian)

sandstone and slltstone

Middie to Late Triassic

(Anlsian-Carnian)

mudslone and siitslone

Early Tnassic

limestone and

mudslone

Late Permtan

li'mestone and siitslone

Devonian granitoids

Oevonian basic

volcanics and tuffs

Ai'Chaean melamorphic

basement

Geological boundaries

a; stratigraphie

b; faulls

Triassic section

Fig. 7. — Geological map of the study area, left bank of Dzugadzak River.

CaPLES TPUIUNE, RlH-I CKIU'K, O i ago

An additional fo.ssil locality, FÎ45/r074 (= field

No. YABC-26; grld rctcrcnce H45/884437) lies

500-600 m South ot ihe mouth ol Bull Creek on

the Otago coast, southeast ot Milton, South

Island, New Zcaland,

The localiiy i.s wiihin Caples Terrane (Fig. 2).

Some workers consider the Caples Tt rrane to be

the Southern extension ol the Waipapa Terrane

bascd on spatial relations and tectonic recons¬

tructions pf basement terranes fSporli 1978).

Radiolarians of Triassic and possible Middle-Late

Jurassic âges kave been reported froin the

“Chrystalls Beach Coinplex'' along this section oi

the Ôtago Coast (l lada et al. 1988). DetaÜcd

examination (by Y, Aita) of radiolarians from

phosphatic nodules in argillitc Iront the Tuapeka

Group exposed at Bull Creek hâve established

that the faunas are of Middie Triassic âge and

thar there are no Jurassic faunas. The Tuapeka

Group rocks are best exposed on the South

Otago coast between Chrystalls Beach and Taieri

Mouth and are characterised by non-schistose

sandstone and argillite wich minor chert and

phosphatic concrétions. et al (19*13), from

trace eicment analysis, showed rhat the ea.stcrn

lliapeka Group rocks on the (3tago coast display

active continental margin lelsic provenance,

contain more of Forlesse-like sandstones and less

mafic sandstone. On the other hand> Adams &

Graham (1997) analysed Rb-Sr whole-rock 5o-

chrons and K-Ar whok rock âges of metagrey-

waeke seqiiences in the Torlesse and Caples

Terranes. According to rheir data, Bull Creek

satnples h.ive an initial isotopic ratio of

0.70568 snggesîing a provenance of “uncertain”

terrane aifmity corresponding to the “Waipapa-

type” zone, but different Irom truc Caples and

Torlesse-type zones fAdams & Graham 1997).

"(Tus geochronological and géologie data from

Bull Creek samplcs show a similarity between

Caples and Waipapa Terrane rocks.

RADJOLARLAN CORRELATION AND FAUNAI. AFFINITY

The radiolarian fauna from the basal part of the

Mahinepua Section, Waipapa Terrane, is remar-

510

GEODIVERSITAS * 1999 • 21 (4)

Non-Tethyan Triassîc Radiolaria from New Zealand and Siberia

kably similar to rhe early Ladinian assemblages

from Bull Crcek. Early Ladiniân species in corn-

mon to both Mahinepua and Bull Creek faunas

includc Silicarnüger costatm costatus Duinitrica,

KozLir Mcisiler, htrentacikna inervie Dumi-

trica, /? pugnax Oumitrica, and Spougopallium

contorturn Dumitrica. Kozui & Mostlcr

(Table 1). Recent work by Black (1994) suggescs

that the rocks in the type area (Omahucâ-l’iiketi

in Southwest Northland) of the Waipapa Tcrranc.

arc different froni oihcr Waipapa rocks and may

bc a Norih Island extension or corrélative tïf the

Caples Terrane, Howcvcr» radiolarian fâunal

similantics suggcst that the northern Waipapa

Terrane has dose paleobiogcographic affiniiies

with the casternmost Caples Tcrranc.

In addition, both Mahinepua and Bull Creck

faunas contain many speciçs (labié 1) known

from the early Ladinian (Fassanian) part of the

Buchenstein Limestone fn the Southern Alps of

Europe (Dumitrica, Koziir & Mo.sricr 1 9H();

Gorican & Buscr 1990; Ko/ur ôr Mostler 1994;

Kozur et al 1996) The Recoaro Limestone, of

rypical Tethyan affinity (Vicencinjan Alps, north¬

ern Italy) is known to yield more than 250 radio-

larian species (l.ahm 1984; Baumgariner et ai

1997). However, it Indudes no forms of the ne^v

genus (jloniernpyk (Table 1), vvhereas Mahinepua

and Bull Creek Faunas incliide abundanr spéci¬

mens and J number of forms of the new genus

Glomeropyle (described herein) This genus may

bc rcstricted to hlgh latitude aHmicy. Ihc com-

inon occurrence ol this gcnti.s, including cspecial-

ly G. g^antmackiei n. sp. and G. (?) galagala

n. sp. is charactcristic of the early Ladinian Bull

Creck fauna of the Caples Tcrranc, South Island.

Undescribed spccics ol the gcncra Poutpus De

Wever, 1979, Hozmadia Dumitrica, Kozur &c

Mostler, 1980, and PLifkerium Pessagno, 1979,

are aiso présent. The presence of simple multi-

cyrtüids and the absence of the genus Ladino-

campe Kozur, 1984 may characterize the

Southern Heniisphere high latitude fauna in

ternis of paleobiogcographic affinity.

TRIASSIC RADIOLARIA IN SIBERIA

Dzugadzak River Section, Omolon Massif

Radiolaria are présent in the Dzugadzalc Section

of the Omolon Massif (uortheastern Siberia).

The Omolon Massif is regarded as a microconti-

nent with Pre-Cambrian metamorphic basement

and a sedimentary cover of Paleozoic and

Mesozoic âge (Fig. 7). Triassic rocks in this

région vvere deposired in oceanic conditions as

hcmipelagites. lliey are represented predomi-

nantly by claystones and mud.stones wiih rare

limeïïtûncs and contâin ammonoids, pseudo-

planktonic bivalves, foraminifers and radiola-

rians. Betirhic fossils are relatively rare (Dagys et

al. 1979; Egorov et al. 1987; Dagys étal 1991,

Dagys & Konstaminov 1995; Egorov bc Bragin

199S).

The IViassic section is located on rhe left bank of

Dzugadzak River in its middle reaches. The fol-

lowing unies arc exposed as follows (Figs 6, 7):

la. Power Triassic, Jndaan Stage (?)

Unit I, Pale-grey claystones with poorly preser-

ved brachiopods .10 m.

Ik Lower TriassiCy Power Olenekian

Unit 2. Pale-grey bitumiaotLs platy and massive

limestone with rareintcrcalations of grey mud-

stonc .7 m.

Unît 3. Grey, dark-grey and brownish-grey mud-

stone with intercalations (0.1 m) of grey limesto-

nc and brownish-grey clavstone .3 m.

Unît 4. Grey and dark-grey thin-beddeci mud-

Stone with intercalations (0.1-0.2 m) ol black

caustülïioHthic shale with rare phosphoritic

concrétions containing poorly preserved

Radiolaria .6.5 m.

Units 2-4 are characterized by conodonts and

bivalves confîrming the présence of the early

Olenekian: hedensrroerni and tardas zones.

Je. Upper Olenekian Stage

Unit 5. Dark-grey mudstone with Claraia aranea

Tozer .4 m.

2a. Middle Triassic, Middle Ânisian

Unit 6. Dark-grey and black thin-bedded mud-

GEODIVERSITAS • 1999 • 21 (4)

511

Aita Y. & Bragin N. Yu.

stone with ammonoid Czekanowskites decipiens

(Mojsisovics). Lower contact uf th'is bed erosio-

nal with a stratigraphie gap representing carly

Anisian tinte.8 m.

2b. Middle TrUissic, Upper Anisian

Unit 7. Dark'grey and black mudstone with

numeroiis phosphoritic concrétions, with the

ammonoid Amphipopanoceras dzenginense

Archipov and radiolarians Triassothamnulus (?)

sp., Entactinia sp., Pstudmtylosphaera (?) sp. ex gr.

P. fragilis (Bragin, 1991), P. (?) sp.> Spongo-

discoidca (?) gcn. indet., SpongopalVmm (?) sp.,

Stauracontium (?) .sp., Truusocampc (?) sp. ..9 m.

Unît 8. Datk'grey and black mudstone and silt-

stone with phosphoritic concrétions and beds of

grey fine sandstonc, black caustobioliihic shale

and brownish'grey biruminous limestonc with

the ammonoid Para fre ch i tes s u b la quea ta s

(Bytschkov, 1968) . 8 m.

2c. Ladinian

Unit 9. Black thin-bedded mudstone interbed-

ded with grey, yellow and whice claystone and

dark-grey biiuminotis limcstone with Daonella

prima Kiparisova, 1937 ...».5.5 m.

Unit 10. Dark-grey and black mudstone and

caustobiolitic shale with numerous phosphoritic

concrétions conraining the ammonites

Arctoptychites omolojemis Archipov, 1974 (lower

2.5 m), Arctogymnites cf. spectori Archipov, 1974,

Indigiraphyllites oimebonensis Popov, 1946 (5-

5.5 m above has'e), algac Tasmanites sp., and

Radiolaria: Anhaeocenosphacm sp., Entactinia sp.,

Ferresium (?) sp., Hindeosphaera (?) sp.,

Hozrnadia (?) sp., Laxtorum (?) sp., Paebus (?) .sp.,

Parentactinia ptt^iax Dumitrica, P. cf. inerrne

Dumitrica, 1978, Praenausna Pottlpus

Glomeropyle horeale n. sp., Silicarmtger costatiis

costatus Dumitrica, Kozut Ôc Mostler, 1980,

5. cf latus Kozut &: Mostler, 1994, Spongo-

discoidea gcn. sp. indet., Spongopallium affi

koppi (Lahm, 1984), Stauracontium (?) sp.

.....6.5 m.

Unit 11. Black platy siltstone interbedded with

yellow and white claystone, with rare phosphori-

ric concrétions containing ccphalopods Arcto¬

ptychites sp,, Indigirophylliies sp.. Giyponaiitilus

sp. ex gr. G. kegalensis Sobolev. 1989 (1-1.2 m

above ba.se), Nathorstites sp. cl. N. melearni

Tozer, 1961, Aristoptychites kolymensis Kipari.sova,

1961 (13-3 m above base) .15 m.

Unit 12. Black thin-laminated mud.stone with

abundant phosphoritic concrétions containing

cephalopods- Nathorstites melearni Tozer,

Arïstoptychitcs kolymensis Kiparisova, 1961 (1-

2 m above base), Sphaeroclndiscites omolojemis

Bytschkov, 1968, Indigirophylliies oimekonensis

Popov, Nathorstites mecornudli (Whitcaves, 1889),

Sintipltcorhynchia kegalensis Dag)'s. 1965 (2.8-

9.7 m above base), Nathorstites lindstroemi

(Boehm, 1903), Sphaerocladisvites omolojemis

Bytschkov (9.7-10.3 m above base), and Radio¬

laria: Archaeocenosphaera sp.. Pseudostylosphaera

sp , Ferresium (?) sp.10.5 m.

Unit 13. Black mudstone with abundant phos¬

phoritic concrétions with ccphalopods

Nathorstites lindstroemi Bohm, Sphaerocladiscites

omolojensis Bytschkov (1.3-2.3 m above base),

Proclydonautilus aniarnemis (Sbimansky, 1957)

(4.1-6 m above base) .11.6 m.

J. Late Triassic, Carnian

Unit 14. Dark-grey bituminous siltstone with

abundant phosphoritic concrétions with

Disi'ophyllîtes sp., Stolleyiies et. tennis (Stolley,

191 i), Proclydonautilus dniamensis (Shimansky),

Cenoceras horeale Dagys àc Sobolev, 1989 (0-

0-3 m above base), Proclydonautilus anidniensis

(Shimansky), Pennospiriferina papovi Dagys,

1965, Pennospiriferina {llentospirijerina) costata

Dagys, 1965, P (D.) pepidiaevi Dagys, 1965 (1.1-

3 m above base), Holcothyuchia tibetica (Bittner,

1899) (4.5 m above base), and Radiolaria:

Pseudostylosphaera sp., ferresium sp.2 m.

Unit 15. Black placy siltstone with rare phospho¬

ritic concrétions and macrofossils: Discophyllites

tairnyrensis Popov, 1961, Cenoaras horeale Dagys

de Sobolev, Pennospiriferina {Dentospiriferind)

costata Dagys, Planirhynchia ydkutica Dagys,

1965 (4.5-4.9 m above base) .10 m.

512

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

Unit 16, Dark'grey massive and platy bioturba-

ted siltsrone with rare carbonate concrétions

containing Discophyllites taimymisis Popov, and

Pennospinferina (Dentospiriferirm) cmtnta Dagys

(5.3 ni above b.ase) .8 m.

Unit 10 of this section contains the most diverse

radiolarian assemblage including Glomeropyle

horeale n. sp. and ammonoids which are com-

mon in norchcastcrn Siberia, but not présent in

the low-latitude régions. This scquencc was ori-

ginally interpreted as carly Ladinian (Dagys et ai

1979) but has been redetertnined as the lowcr

part of the latc Ladinian (Dagys et al. 1991;

Dag)'s ôc Konstantinov 1995), This conclusion

was based on animonoid data. However, radiola-

rian faunas have doser alünity wrth carly

Ladinian assemblages, based on the présence of

such taxa as ParenUictinia puguax Dumitrica,

P. cf. inermr Dumitrica, SiUianiaiger cosTatus

costatiis Duttiirrka, Ko^ur ôt Mosiler, cf. latus

Kozur & Mostler, Spongopallium aff. koppi

(Lahm).

The variance of these two âge interprétations

require further research.

The âge ranges of the key radiolarian taxa may be

longer than presently understood and rhere is as

yet poor corrélation between ammonoid zones of

high- and low-paleolatitude Ladinian sections.

CONCLUSIONS

Radiolarian faunas of Middie Triassic âge from

New Zealand and northeastern Siberia have been

documented. They are characterized by abon¬

dant occiurences of non-Tethyan species inclu¬

ding seven new species of Glomeropyle n. gen.

(dcscribcd heretn) Alihough the faima includes

many species known from the European Tethyan

sequences>. the pnesence of Glomeropyle n, gen. is

only known from souitiern and northern high

latitudes during Middie IViassic time. In terms of

Triassic paleohiogeography these radiolarian lau-

nas appcar to rcflcct a bipolar latitudinal pattern.

Furrher examioatlon of New Zealand and Sibe-

rian radiolarian faunas are required in order to

csrablish Boréal and Austral launal différentia¬

tion from Tethyan forms.

In New Zealand, the Mabinepua early Ladinian

fauna in the WaipapaTerrane has a non-Tethyan

affiniry and is similar to that in the Capics

Terratie. Furthermore, the Mahinepua Section

ofVers great potential for establLshment ofa stan¬

dard radiolarian biostratigraphy for Middie and

Late Triassic successions that acctimulated in

Southern high latitudes along the margin of

G O n dwan aland.

SYSTEMATIC PALEONTOLOGY

Type specimens of species authored by Aira are

deposited at the Geology Department,

Utsunorniya University (UTU), and of species

authored by Bragin are deposited at the

Geological Institiite (GIN), Russian Academy of

Sciences.

Suborder SPUMELLARIA Ehrenberg, 1875

Glomeropyle A\i^ & Bragin, n. gen.

TyPÊ species. — Glomeropyle atirora Aita n. sp.

EtymoIOCY. — Làùn, glomero- form into a bail;

Greek fyk~ gâte, orifice, opening.

OccuRKtNCE. — Middie Triassic. Anisian to

Ltdinian. Waipapa l'err.tne, Norih Bland and Caples

Terrane. South Island, New Zealand, Omolon Massif,

northeiiMcrn Siberia.

DïaGNOSIS. — Shell of variable small to large size,

subspherical, with upen subcircular uperture and pylo-

me, wirli or without primar)' spincs; wall very iltick,

muiti-layercd, with internai cavity, with or without

internai spicnic, without mcdu|)ar>'shclls,

Remarks

Glomeropyle n. gen. differs from the Tertiary

Prunopyle Dreyer, 1889, emend Kozlova in

Kozlova & Gorbovetz, 1966 by having a heavy

thick-walled sheJl without mcdullary shells. It

differs from Sphaeropyle Dreyer, 1889 by having

a Icss spherical outer shell with pores irregularly

arranged, and variable in size, and without

medullary shells.

Although tlierc arc a number of species known

from the Middie Triassic of New Zealand and

GEODIVERSITAS • 1999 • 21 (4)

513

Aita Y. & Bragin N. Yu.

Fig. 8. — Glomeropyle aurora Aita. n. sp.; A-C, holotype (photo Nos 31101, 31102 & 31107); A, B. stereograph, C. latéral view; D,

E, paratype (photo Nos 31123, 31125), stereograph: F. paratype (photo No. 31106); G. H, photo Nos 31109, 31110. Sample MAH-

3.5, Unit 2. Mahinepua Peninsula. North Island, New Zealand. Scale bar: 100 pm.

Russia, however, no record of forms resembling

any species of Glomt^rùpyle n. gcii. bas been

found from Middle Triasslc séquences in the

Europe, japan, Southeast Asia or North yVmcrica.

Thus, this genus appears to be restricted to nortli-

ern and Southern high latitude areas, suggesting a

bipolar biogeographic distribution.

Glomeropyle aurora Aita, n. sp.

■(Fig. 8A-H)

Tvte material. — Hulon^pc: UTUlOl (Fig. 8A-C).

Paratypes: UTU102 (Fig. 8D, E), UTIJ103 (Fig. 8F).

Type locality. — Al! specimens from sample

PO4/fl03 (= MAH-3.5), Mahinepua Peninsula.

514

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

Fig. 9. — Glomeropyle boreale Bragin, n. sp.; A, holotype; B-F, paratypes. Northeastern Siberia, Omolon Massif, Dzugadzak River,

Middie Triassic, Ladinian, Unit 10. Scale bar: 100 pm.

Age. — Middie Triassic (Anisian to early Ladinian).

Etymoiogy. — Latin, nurora, dawn, morning.

OccuRRENCf. — Lovvcf grceii argillite (sample

MAH-3.5)) Mahinepuu Pcninsula. Whaiigaroa area.

Waipapa Terrane, North Lland, New Zealand.

Measuremen ri. — Miaimum widili- 180-250 pm,

height; 200-305 pm, thickness of shell wall: 10-15

(max. 20) pm.

Description

Relatively small, ovoidal shell with a few spines

or clusters of short spines at one pôle and with a

short pyiome at the orher pôle. Cortical .shell

usually thin-walled; upper part hemisphcrica!,

lower hall part tapering, inverted conicaJ with an

aperturc. Pores suhcircular lo irrcgular in shape,

widi or wîthout pore Irames, Idiome Icss develo-

ped, with a few short spines. Aperture narrow,

GEODIVERSITAS * 1999 • 21 (4)

515

Aita Y. & Bragin N. Yu.

rwo to three rimes as wide as rhickness of shell

Wall. No mcdullary shells recognized.

Remarks

This species difFers from Gbmeropyle poinui Aita

n. sp. in irs smaller size and thinner shell, and by

having a few spines or clusters of short spines at

one pôle.

Glorneropyle boreale Bragin, n. sp.

* (Fig. 9A-F)

Pylentonemidac (?) gen. indet. — Egorov & Bragin

1995,%. 2 {] 0-12).

Type material. — Holoypc GIN No. 7438-89-1

(Fig. 9A).

Type LOCALITY. — Omolon Massif, Dzugadzak River.

Age. — Middie Triassic (Ladinian).

EtymoIOGV. — Greek, boreios, god of thc north

wind.

Occurrence. — Middie Triassic, Ladinian. Omolon

Massif, northeastern Siberia.

MeasuREMENTS. — Maximum width of shell: 230-

330 pm, heighl wirh pylome tube: 310-385 pm, dia-

meter of aperture: 55-75 pm, length of spines:

50-120 pm.

Description

Large subspherical or roughiy ellipsoidal shell

with well-developed .subcircidar aperture fonning

short pylome. Small short rod-like spines are pré¬

sent around aperture, three of them longer than

others. Outer shell with rwo visible layers; outer

layer with polygonal (trigonal to pentagonal)

commonly irnegular pore frames with apophyses

and massive nodes ar vertices. Inner layer with

small irregular pore frames.

Shell wall vtry rhick, inner cavity small, inner

structure unclear. One or more primary spines

présent, each with triangular in cross-section

proximally, rod-like distally. Sometimes primary

spines are absent.

Remarks

Glorneropyle boreale Bragin, n. sp. differs from

G. mahinepuaensis Aita, n. sp. in having a rou-

gher shell surface, and in its larger and more

clearly defined polygonal pore frames with massi¬

ve nodes at vertices.

Glorneropyle poinui Aita, n. sp.

(Fig. lOA-F)

Type material. — Holotype: UTU104 (Fig. lOA,

B). Paratypes: UTU105 (Fig. lOC, D), UTU106

(Fig. lOE),

Type LOCALHY, — AU specimens from sample P04/

fl03 (= MAH-3.5), Maliinepua Peninsula.

Age. — Middie Triassic (early Ladinian).

En'MüLüGV. — Maori, poinui, a large bail.

Occurrence. — Lowci grcen argillitc (.sample

MAH-3.5), Mahinepua Peninsula, Whangaroa area,

Waipapa Tetrane, North bland, New Zealand.

Mfasurememt.S, — Maximum width: 265-310 pm,

height: 310-355 pm, thickness of shell wall: 25-30

(max. 40) pm.

Description

Large spherical lo subspherical shell with a short

pylome. Cortical shell thick-walled with nume-

rous subcircular tü irregular small pores. Pores

variable in size usually withour distinct pore-

frames, bur rarely wiih polygonal pore-frames.

Overall outline smooth, but area around pylome

rough. Aperture narrow. No mcdullary shells

recognized.

Remarks

Glorneropyle poinui Aita n. sp. resembles Glo-

meropyte aurora Aita n. sp. in overall shape, but it

is disdnguishcd by its large size (> 265 pm in

maximum width) and chicker shell wall com¬

monly with smooth surface.

Glorneropyle (?) galagala Aita, n. sp.

(Fig. 1 lA-C)

Type material. — Holotype: UTU107 (Fig. IIA,

B).

Type locality. — Sample PO4/fl03 (= MAH-3.5),

Mahinepua Peninsula.

Age. — Middie Triassic (early Ladinian).

516

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

Fig. 10. — Glomeropyle po/nu/Aita, n. sp.; A, B, holotype, stereograph {photo Nos 31104, 31105); C, D, paratype stereograph

(photo Nos 31126, 31127); E, paratype (photo No. 31128); F, photo No. 31135. Sample MAH-3.5, Unit 2, Mahinepua Peninsula,

North Island, New Zealand. Scale bar: 100 pm.

GEODIVERSITAS • 1999 • 21 (4)

517

Aita Y. & Bragin N. Yu.

Fig. 11. — A-C, Glomeropyle (?) galagafa Aita, n. sp.; A. B. holotype, stereograph (photo Nos 31075, 31076); C, c!ose-up view,

holotype (photo No. 31077); D*F, Glomeropyle grantmackiei Aita, n. sp.; holotype (photo Nos 31089. 31090, 31092); D, E, stereo¬

graph; F. oblique basal view. Sample MAH-3.5. Unit 2. Mahinepua Peninsula, North Island. New Zealand. Scale bars; A. B, D-F,

100 pm; C. 50 pm.

Etymolugv. — galagala^ a rattle.

OCCURRHNCF. — Ijowtrr preeri argillitc (sampie MAH-

3.5). Mahinepua Peninsula, ^C'Tiangaroa area, Waipapa

Terrane, Norrh Island; Bull Creek (sample YABC-26),

Caples 'l'crranc, South Island, New Zealand.

MeasuREMENTS. — Maximum widrh of shell:

210 pm (holotype 194 pm), height of shcll: 220 pm

(holotype 188 pm), length ofspines: 70, 50 pm (holo¬

type 62.5, 50 pm), length of pylomc:100 pm (holo¬

type 150 pm).

Description

Spherical shell with two conical spines at one

518

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

Fig. 12. — Glomeropyle grantmackiei Aita, n. sp.; A, B, paratype, stereograph (photo Nos 31066, 31067); C, D, stereograph (photo

Nos 31098, 31097); E, {photo No. 31072); F, paratype (photo No. 31073). Sample YABC-26, Bull Creek, Caples Terrane, Otago,

South Island. Scale bar: 100 pm.

GEODIVERSITAS • 1999 • 21 (4)

519

Aita Y. & Bragin N. Yu.

end and a developcd pylome at the other end.

Cortical -shell double layered with rough ridged

surface; outer layer with rriangular to polygonal

coarse mesh consisting of interconnecring bars;

Inner layer fine meshed but unclear in detail,

Two distinct conical .spines forming angle of 60®.

Angles between onc pôle and cach .spine asym-

metric, 20® and 40®. Pylome wcll-developed,

with long spincs, sometimes forming a long per-

forate hoUow tube. Usually two or three minute

spines fused at ends, forming a rod-like stout

spine.

Remarks

This species is questionably assigned to the genus

Glomeropyle AsKTi ôc Bragin, n. gen. because it has

approximateJy spherical shell and has two dis¬

tinct horn like spines.

Glomeropyle grantmackiei Aita, n. sp.

(Figs 1ID-F, 12A-F)

Type MATERIAL. — Holotype: UTU108 (Fig. IID-F).

Paratypes: UTU109 (Fig. 12A, B), UTUllO

(Fig. 12F).

Type locality. — Holotype: saniplc PO4/fl03 {=

MAH-3.5)* Mahinepua Peninsula. Paraiypes: sample

H45/fô74 (= tield No. YABC-26), Bull Creek.

Ace. — Middle Triassic (early Ladinian).

EtymoLOGY. — This spccies is named for Professor

Jack A. Crant-Mackie, Department of Geology, The

University oi Auckland, in honour of his significant

contribution lu paleontology in New Zeaknd.

Occurrence. — Rare in the lower green argillire

(sample MAH-3.5), Mahinepua Peninsula,

Whangaroa area, Waipapa Tcrranc, Norrh Island;

common ro abundant in Bull Crcck (sample YABC-

26), Capics Tcrrane, South Island, New Zcaland.

Measurement-S. — Maximum widih of shell: 200-

345 pm, heigbt of shell: 21 5-325 pm, length of pyio-

me: 38-70 prn, width of aperture; 40-70 pm,

rhickness of shell: 40-60 pm, length of spines: 70-

120 pm.

Description

Large hemispherical, thick-walled shell with a

well-developed pylome. Cortical shell consisting

of a thick outer layer with coarse spongy mesh-

work and a thin inner spongy layer. Pores nume-

rous, irregular in shape, variable in size, closely

spaced, separared by intervening bars. Rarher

long, stout, rod-like slender spines are sparsely

distributed; four or five spines recognized on the

visible side. Each spine three-bladed up to midd-

Iç ol basal portion and with grooves only at base.

Aperture wcD-defined, medium-sized, (•orniing a

cylindrical to sometimes lubular pylome, with

two to thrcc dcscending spines.

Re.makks

Glomeropyle grantmackiei Aita n. sp. has a relati-

vcly broad morphological variation. It includes

such morphotypes as thosc ornamented with rid¬

ged, and lîodose surfaces on the inflatcd sub-

sphcrical shell. Very heavy massive rod-like

spines arc developcd on many spécimens from

the phospharic nodule sample of Bull Creek,

Caples Terrane.

Glomeropyle mahineptmensis Aita, n. sp.

(Fig. 13A-J)

Type materiai. — Holotype; UTUlll (Fig. 13A,

B). Paratypes: UTU1I2 (Fig. 13D, E), UTU113

(Fig. 13H,l).

Type locality. — Ail specimens from sample

PO4/fI03 (= MAH-3.5), Mahinepua Peninsula.

Ace. — Middle Triassic (early Ladinian).

ETYMOLüCY, — This species is named for Mahinepua

Peninsula, Whangaroa area, Northland, New

Zealand, as the type locality.

Occurrence. — Common in the lower green argilli-

tc (sample MAH-3.5), Mahinepua Peninsula,

Whangaroa area, Waipapa Terrane, North Island,

New Zealand.

Measurements. — Maximum width of shell: 144-

250 pm, heighr of shelh 138-280 pm, length of

spines; 25-55 pm. length of pylome: 18-50 pm.

Description

Cortical shell pyriform with an opening at one

end bcaring a short pylome. Pores small, subeir-

cular to subangular, irregularly arranged. Overall

shell with rough surface of numerous small

nodes at vortex of pore-frames. Slender, cylindri-

520

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberîa

Fig. 13. — Glomeropyle mahinepuaensis Alla, n. sp. ; A. B, holotype, stereograph {photo Nos 3111 1 , 31112); C. photo No. 31119;

D, E, paratype, stereograph (photo Nos 31113, 31114); F, G, paratype, stereograph (photo Nos 31129, 31130); H. I, paratype, ste¬

reograph (photo Nos 31116, 31115); J, photo No. 31117. Sample MAH-3.5, Unit 2, Mahinepua Peninsula, North Island, New

Zealand. Scale bar; 100 pm.

cal, short spines widely spaced and developed RKMARKS

from ihe shcll surface. Berween two and five C/omeropyle 7mihniepuaemis Aiï3L, n, sp, resemblcs

spines rise upwnrd and at least two spines exiend Glomeropyle grofittnaebiei Aita, n. sp. in overall

downwards. Pylome well-developed with a .short shapc, but is distinguished from the latter in

stout descending spine and many minute spines. having a smaller shell, thinner shell wall and

No medullary shell recognized. shorter, more slender spines. This spccies differs

GEODIVERSITAS • 1999 • 21 (4)

521

Aita Y. & Bragin N. Yu.

522

GEODIVERSITAS • 1999 • 21 (4)

Non-Tethyan Triassic Radiolaria from New Zealand and Siberia

from Glomeropyle aurora Aita, n. sp. by having

rather rough, pointed nodes on the shell surface

and more frequcndy arranged shorr spines.

Glomeropyle waipapaemis n. sp.

(Fig. 14A-D)

Type material. — Holotype; U'FUlH (Fig. 14A,

B).

Type locaiity. — Sample PO4/fl03 (= MAH-3.5),

Mahinepua Peninsula.

Age. — Middic Triassic (carly Ladinian).

EtymoloOY. — This specLes is named for the

Waipapa Tcrrane. a typical accretionary complex of

Triassic ro Jurassic agc, including spilitc, chcrt, grccn

argillite, sandsrone, and minor limcstone, Norch

Island, New Zealand.

OccURRENtT. — Lowcr green argillite (sample

MAH*3.5), Mahinepua Peninsula. VCliangaroa area,

Waipapa Terranc. North Island. New Zealand.

MeASUREMENTS. — Holotype: maximum widch of

shell: 269 pm, height of shell: 313 pm, lengrh of

spines: 25 pm, length of pylome: 31 pm.

Description

Large thick-walled shell, upper half dome-shaped

and lower funncl-shapcd, wirh rather ridged sur¬

face. Very shorr, pointed spines are spiusely dis-

tributed at apex between four facets; four spines

recognizcd on the visible side. Shell probably

double-lavered: inner layer is unclear, but inter-

vcning bars are visible. Pores closely-spaced, cir-

cular ro iubcircular, variable in size, irregularly

arranged with rectangular, pentagonal ro hexago¬

nal pore-frames. Ridges or small knobs are deve-

loped from apex of pore-fraraes. Pylome

well-developed, with teeth-like spines.

Remarks

This species resembles Glomeropyle grantmackiei

Aita, n. sp. in having a similar shapc and size.

Fig. 14. — A'D G\omeropy\e wa/papaens/y Aita, n. sp.;

A, B. holotype. steraograph (photo Nos 31079. 310785);

C, D, stereograph (photo Nos 31081, 31084). E-G. Glomeropyle

cf. grantmackiei Ma. n. sp. (photo Nos 31087. 31088, 31091);

E. F. stereograph. G. basai view. Sample MAH'3.5, Unit 2,

Mahinepua Peninsula, North Island, New Zealand. Scale bar:

100 pm.

However, it differs from the laiter in having

more circular to subcircular pores on the shell, is

less spinose, and has very short pointed spines.

Acknowledgements

We are gratefui co ProL Toyosaburo Sakai for

valuable advice and encouragement on an aspect

of radiolarian study. We thank Chris Hollis

(Geological Survey of Japan) and Jack A. Grant-

Mackie (The University of Auckland) for impro-

veraent of the early draft of this paper.

Dr Paulian Dumitrica kindly provided corn-

ments on the taxonomy and information on

Tethyan species- At$u.shi Takemura (Hyogo

Teacher’s Univcrsiiy), Rie S. Horl (Hhinie

Univcrsity)î Kazuto Kodama (Kochi University),

Bernhard Sporli (Llniversiry of Auckland) and

Toyosaburo Sakai (Utsunomiyu Universir)4 assis-

ted with sampling at the Mahinepua Section in

New Zealand. Hamish Campbell (Instirutc of

Geological Nutlear Sciences) greaily improved

the manu-script. We rhank P. Dumitrica and

A. Ollier for reviews. This work was partly sup-

ported by grant.s from the Minlstry ot Education

Grants-in-Aid International Scicntific Research:

1995 and 1996 to Prof. T. Sakai (Project

No. 07041085).

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526

GEODIVERSITAS • 1999 • 21 (4)

Corrélation of the early Albian-late Turonian

radiolarian biozonation with planktonic and

agglutinated foraminifera zonations in the

Pieniny Klippen Belt (Polish Carpathians)

Marta B/^K

Institute of Geological Sciences, Jagiellonian University,

Oleandry 2a, 30-063 Krakôw (Roland)

bak@ing.uj.edu.pl

Krzysztof BP^K

Institute of Geography, Cracow Pedagogical University,

Podchor^zych 2, 30-084 Krakôw (Roland)

kbak@cyf-kr.edu.pl

B^k M. & B^k K. 1999. — Corrélation of the early Albian-late Turonian radiolarian biozona¬

tion with planktonic and agglutinated foraminifera zonations in the Pieniny Klippen Belt

(Polish Carpathians), in De Wever P. & Caulel J.-P. (eds), InterRad VIII, Paris/Bierville 8-

13 septembre 1997. Geodiversitas 2^ (4) : 527-537.

ABSTRACT

Marine pelagic deposits of the lower AJbian to upper Turonian inter\'al in

the Polish part of the Pieniny Klippen Belt are relativcly rich in radiolarian

fauna as well as in planktonic and agglutinated foraminifera. The proposcd

radiolarian zones (Holoayptocanium barbui^ Hemiayptocapsa prepolyhedra

and Hemicryptocapsa polyhedra) hâve been correlated with planktonic forami¬

nifera biozonarion (from TidnelUt primula to Dicarinella prhnitiva zone.s),

and with agglutinated foraminifera biozonation (from Haplophragmoides

nonioninoides to Vvigerinarnmma ex ^r.jankoi zones).

RÉSUMÉ

Corrélation des biozones à radiolaires de l'Albien inférieur- furonien supérieur

avec celles à foraminifères planctonicjues et agglutinés dans la région des klippes

piénines (Carpathes polonaises).

Les dépôts marins pélagiques de PAlbien inférieur-Turonien supérieur de la

zone dc.s klippc.s piénines sont relativement riches en faune de radiolaires,

ainsi que de foraminifères planctoniques et agglutinés. Les zones de radio¬

laires proposées (Holocryptocanium barbais Ifvniicryptoctipsa prepolyhedra cr

Hemiciypwcapsa polyhedra) sont en corrélation directe avec les biozones de

foraminifere.s planctoniques (de la zone Ticinelln primula à la zone

Dicarineüa primitiva) et celles des foraminif^res agglutinés (de la zone

Haplophragmoides nonioninoides à la zone Uvigerinammina ex jankoï).

MOTS CLÉS

Crétacé,

Radiolaria,

Foraminifera,

biostratieraphie intégrée,

zone des klippes piénines,

Carpathes.

KEYWORDS

Cretaceous,

Radiolaria,

Foraminifera,

integrated biostraiigraphy,

Pieniny Klippen Belt,

Carpathians.

GEODIVERSITAS • 1999 • 21 (4)

527

B^kM. &B^k K.

INTRODUCTION

Detailed micropalaeontological studies of marine

pelagic Cretaceous deposirs hâve been carried out

in rhe Picniay Klippen Belt during the last 15

years. A part of thcse concerncd bioscracigraphy,

based on differejic groups oFmîcrofauna; forami-

nifera (Birkenmajcr & Jednorowska ]987i

Gasihski 1988i Kostka 1993; K. Bi^k 1998), nan-

noplankton (Dudziak 1985)» dinoq'srs (Jamihski

1990) and radiolaria (M. B^k 1995, 1996a, b).

However, only very few studies comprise an intc-

grated biostraiigraphy of rhese deposirs

(Birkenmajer Z*/ 1979; K. BtjkfY^ïZ. 1995).

The Crccaccous dcposits ol thc Picniny Klippen

Bclt providc ihc bcst marctial lor iTc intcgratcd

biostraiigraphical studies in the whole

Carparhians, because rhey represenr pelagic and

hemipelagic calcareous-marly faciès, and contain

abundant micmfauna. These depos’us hâve been

formed în the Pieniny Klippen Basin

(Birkcnmajer 1977), a pari of the Penninic

Ocean-northcrn part of Western Tethys

(Fourcade étal. 1993) (Fig. lA). The sédimenta¬

tion during Albian thtough Campanian rook

place iindcr deep-water conditions, ar outer shelf

through Jower bathyal/abyssal depths, above or

near CCD (Birkenmajcr & Gasihski 1992;

K. B^k 1995a, b). l'hcy crop oui in a highiy tcc-

tonically deformed zone, known as the Pienîny

Klippen Belt, rhat séparâtes the Innct ftom rhe

Outer Carparhians (Fig. IB, C)'.

The présent aurhors propose here an integrated

local biostrarigraphy based on planktonic Fora-

minifera, agglutinaicd l'uraminifera and Radio-

laria for early Albian rhrough laie Turonian lime

span. rhe corrélation is based on studies of

microfauna from the sanie samples wirhin the

same sections. Foraminifera and Radiolaria are

relativcly abundant in the studied deposirs.

GEOLOGIC^\LSETTING AND

RADIOLARIAN HORIZONS

Twenty five sections locaced at Niedzica,

Kroscienko, Szczawnica, Jaworki, Sromowce,

Dursztyn, Szaflary and State Byscre hâve been

chosen for integrated micropalaeontological ana¬

lyses. A detailed description of profiles, sample

location, and lithology is given in papers by

HL (1992, 1993» 1998) and M. B^k (1995,

1996a, b, 1997). In 18 of these sections, radiola-

rian skelctons hâve been foimd together with

forarninifera. and thc best sections (15) were

used lierc for corrélation purposes (Figs 1,2).

In thc sections examined, the microfauna has

been recovered from rhe deposirs of the

Kapusnica and Jaworki formations. Liihological

features, thickness and âge of these lithostratigra-

phical unies, distinguished by Birkenmajer

(1977, 1987), and Birkenmajer 6c Jednorowska

(1984) and presented below, concern only the

studied sections.

KaPIISNTCA l-OrU'tATKlN

This formation is subdivided in two members,

the Brodno Member and the Rudina Member,

both represented in the sections investigated.

The Brodno Member. Ir has been identified

only in the one section as a 40 cm thick layer of

black maris, ? upper Aprian in âge. The radiola-

rian launa is présent burver)’^ rare in these depo-

sits.

The Rudina Member. (1-20 m thick; lower-

upper Albian) It is represented by green-grey and

black maris and inarly shales with niarly liniesto-

ne imercalaiions, with red maris appearing in the

upper part. Abundant and well-prcserved radio-

larian skeletons are présent in green and black

maris and niarly shales.

JAWOKKI POKMAI'ION

Deposits of the Jaworki Formation hâve been

examined in sections belonging to ail Klippen

successions (Fig. 2).

The Brynczkowa Mari Member. (2-22 m thick;

Vraconian-middle Cenomanian) it consists of

green or grey-green maris with thin scarce red

mari inrercalation. Moderarely to poorly preser-

ved radiolaria are rare.

The Skalski Mari Member. (4-15 m thick;

middie-upper C^cuonvanian) It consisis of varie-

gaced maris, iniercalated with green, red and grey

maris. Hxcept of thc Altana Shale Bed, thc radio-

larians are présent in this member but are rare

and mosily poorly preserved.

The Altana Shale Bed. (0.4-3 ni thick;

528

GEODIVERSITAS • 1999 • 21 (4)

Radiolarian and foraminiferal biozonation in the Pieniny Klippen Belt

Fig. 1. — Location of the study ârea: A, In the Western Tethys {rectangle B) (map of late Cenomanlan palaeoenvironments after

Fourcade et ai 19&3; simplîfied); B. C. in the Carpathians (Pieniny Klippen Bell in black). D. in lhe Pieniny Klippen Belt. Legend. 1.

investigated outcrops; 2. symbols ot outcrops; 3. more important dislocations. List ot outcrops (from west to east): Sb, Stare Bystre;

Ki. Kietowy stream: Sz, Szaflary quarry, Lor Lorencowe Klippes: Csk, Czerwona Skaia, Zt, Ztobowy Creek; Nd. Niedziczanka

slream; Kos, Kosarz.yska Valley; McO Macelowa-Osice; Pg. Podskalnia Gôra ML Mag. Magierowa Klippe; Or. Orlica Hlll: Bw.

Bukowiny Valley: Bd. Bukowiny Hill.

Cenomanian/Turoniaiî boundary) h consists of

black-blue, grecnish and black shales and marly

shales. Radiolarians are abundant bur low-diver-

sified and poorly preservcd. Their pyritized ske-

Ictons are mostly found within the Czorsztyn

Succession deposits.

The Magierowa Mari Member. (9 m;

Cenomanian/Turonian boundar)^ Il is reprcscn-

icd by shales, marly shales, maris, and thin-bcd-

ded marly ümestonc of grey to green colour with

black alternations. Radiolarian fauna is abun-

GEODIVERSITAS • 1999 - 21 (4)

danc: wcll-preserved siliceous specimens are pré¬

sent in green and grcy shales and marly shales.

The radiolarians arc also abundant in black

shales but are often diftlcult to déterminé, becau-

sc of Fe-oxide coating and pyritization.

The Trawnc Menibcr. (5 m, lowcr-middle

Cenomanian) It consists of gre>'-grccn maris and

shaly maris with sandstonc intercalations.

Radiolarian fauna is scarce: only a few poorly

preserved specimens bave been found.

The Sneznîca Siltstone Member. (3-? 40 m;

529 I

B^k M. & B^k K.

Fig, 2. — Lithological columns of the studied sections in relalion lo the âge of deposits (dashed Itne cortesponds \o the

Cenomanian/Turonian boundary) and tbeir atlnbutton to Klippen successions and sedimenlary zones (Pieniny Klippen Basin recons¬

truction after Birkenmajer (1977)]. Lithological units invesligated |llthoslratlgraphy aller Birkenmajer (1977, 1987), Birkenmajer &

Jednorowska (1984)]: 1, Lorencowe Chert Bed; 2. Osice Siltslone Member; 3, Macelowa and Pusteinia Mari rnenibers 4, Trawne

Member; 5, Sneznica Siltslone Member, 6, Altana Shale Bed; 7, Magierowa Member; 8, Skalski Mari Member; 9, Brynczkowa Mari

Member; 10. Rudina Member: 11, Brodno Member; 12, Pieniny Limestone Formation. Scale bars: 5 m. except of Branisko

Succession sections, 1 m.

530

GEODIVERSITAS • 1999 - 21 (4)

Radiolarian and foraminiferal biozonation in the Pieniny Klippen Belt

middlc Cenomanian-middle Turoiiian) It is rcpre-

scntcd by altcrnating bright blue-grey and green

shaly maris widi thin-bcddcd slltstone and sand-

stone, and bright-grccn pclitic Ümcstonc intercala¬

tions. Radiohiriims arc raie in this nicmbcr, but

the upper Cenomanian deposirs arc cnriched in

wcll-preser\’cd, pyi iri/.ed radiolruian skclcron.

The Macelowa Mari Member. (15-70 m; lower

Cenomanian-iSantonian) Ir corisists nnjstly of red

maris and marly Jimesronc vvith thin intercala¬

tions of greenish or bltiish siltstones and sand-

stones which appcar in its lower and upper parts.

Poorly preserved and mainly calcified radiola-

rians are présent in this member. They are diver-

sified, especially those lound in a horizon

corresponding to the lower-middle Turonian.

The Pustelnia Mari Member. (6-45 m; middle

Cenomanian-Santonian) Ir consists of pure

brick-red, strongly lectonized maris wïthout clas-

ric intercalations. Radiolarian skcletons are vciy

scarcct poorly preservedt and maixily calcified.

The Lorencowe Chéri Bed. (3 m; upper

Santonian-lower Campanian) h is represented by

a two-meter-thick complex consistiiig of altema-

ting variegated maris (mostly red) wirh rhin

intercalations of lighr-green limestone.

Radiolarian skeletons are also scarce, poorly pre-

ser\’'ed, mostly calcified.

RADIOLARIAN ASSEMBLAGES

Seventy seven radiolarian species hâve been

determined from the Cretaceous deposics ran-

ging from lower Albian to Santonian of the

Pieniny Klippen Bclt. 20 gênera and 53 spedes

of Nassellaria, and 11 généra and 24 species of

Spumellaria were recognised (M. Bqk 1997).

The assemblages, in ail Klippen successions

mvestigated, are dominated by cryptoccphalic

and cryptothoracic Nassellaria belonging ro the

gênera Holocryptoaviiuni^ Hepiicryptocapsa^

Cryptainphorella. Dorypyle. Hiscocapsa^

Trisyringium and Squirtabollum, Multiscgmcntcd

Nassellaria arc also common being represented

by the gênera Dictyomitra, Thanarla,

Pseudodictyomitm^ Stichomitm, Xrtus, Obeliscoites

and Torculum. Spumellaria are less common; the

most abundant are the specimens belonging to

the familles Actinommidac, Pracconocar)'om-

midac, Xiphostylidac (gênera Staurosphaeretta

and Tviaciomii) y and Dactyliosphaeridae

{Diictyiîodisciis^ Godia and Dactyliosphaera).

Other Spumellaria bclong to the généra

Ilexapyrûniis^ Cavdspongla., Pseudoaulophacus,

Patellulû^ Paroniiella and CrucelLi.

Within the Klippen successions investigated, the

radiolarians are most abundant and diversificd in

the Czorsztyn Succession deposits (ourer shelf-

upper barhyal environment), becoming generally

scarce in the deposits of the Pieniny Succession

(lower bathyal environments, close to Calcium

Compensation Depth).

The radiolarian specimens are most abundant

and diverse in green and black marly shalcs,

maris and limestones ol the Kapusnica and

Pomied/nik formations, rhe Magierowa Member

and ihe Aliana Shale Bed of rhe Jaworki

Eorination. Thcy arc scarce in red and variegated

maris and shales of the Macdowa Mari,

Brync/kowa Mari and the Skalski Mari members

ol the Jaworki Formation. This itilght he dépen¬

dent on lirhology and iliagenesis factors respon-

sible for préservation of siliceous microfossils;

however, radiolarian fauiias radiarion and turn¬

overs could be also taken inro account. Both

causes might reflecr an ecological response of

marine biota to global cUmace and sea level

changes during mid-Crctaceous rimes.

Two great changes in the radiolarian assemblages

hâve been retorxied within the srudied deposirs:

1. Beginning of an important first radiation of

Radiolaria occurred during the middle Albian

{Ticmella priwula foraminiferal zone» K. Bijk

1992)' as maiiy new species had rheir first appea-

rance in the middlc and rhe lare Albian, The

maximum of différentiation in the radiolarian

assemblage is obsers^ed in the Vraconian deposits

(Rotalipara tidnensis through the Rotalipora

appennhiica-Plevwm<tlina huxtorfi foraminiferal

zones, K. Bijk 1998). Starting from the upper

part of the It appennimat-P. hiixtorfi foraminitc-

ral zone towards the Cenomanian/Turonian

boundary, a relative decrease in the number of

species occurred. As a rcsult, the radiolarian làu-

nas in the Czorsztyn, Branisko and Niedzica suc¬

cessions show great similarities. The same

GEODIVERSITAS • 1999 • 21 (4)

531

B^k M. & B^k K.

characteristic taxa from rhe Riborder Nassellaria

(both cryptorhoracic and cryptocep halle forms)

represented by the généra Holocryplocanium,

Hemicryptocapsa, Squinclbollum and Cryptam-

phorella arc the most abundant, svhilc the gênera

Dictyornitray Pseudodictyomiiray Thanarla,

Stichomitrity Toradumy atul Xitm arc also com-

mon.

2. The nexr change in radiolarlan assemblages

took place around ihe Cenomanian/Turonlan

boundary, Ir surted during the latc Cenomanian

(Rotalipora aishniani loraminiferal 7one, K. B;^k

1998). At that time, dic radiolarlan assemblages

from tire Picniny Succession becamc similar to

those from rhe Czorsztyn, Niedzica and Branisko

successions. Moreover, ir was enriched in formvS

described so iar only from the Silesian and the

Skole units of the Outer Flysch Carpathians

{Praeconnearyomma lipmanae^ Godia sp.,

Diacanthocapsa sp. — sec M. B^k 1994; Corka

1996).

FORAMINIFERAL ASSEMBLAGES

The early and middle VVlbian Foraminifera in the

Pieniny KJippcn Bcit represent a well-diversified

assemblage. Planktonk forms prcvail, being

represented by hedbergellids (//. dtdrioensisy

H. planispira and H. mnplcx)^ Glohgerinelloides

bentoneusis^ and ticincllids (Tidnella primnliiy

T robeni) (k. Bak 1992). Benthos fs dominated

by cakâreous forms with the most frequent

Gyroidimida inJhureMceay Gavcl/nella cenomam-

ca and G, interniedia^ and accompanied by

Denîalina sp., Nodosuria sp. and Latticidhja sp.

Agglutinated foraminifoa {predominantly infau-

nal forms) are infrequent in rhese deposirs, with

Dorothia gradata, Xpiroplecfinaîa annectemy

Tritaxüt gatdtma and Textularia foeda prevaillng.

The upper Albian planktonlc Foraminifera are

very numerous and more div'crsified. Besicles the

most frequent hedbetgellids, Bitidnella hreggien-

sisy PlanornitUna huxtfjrfiy Glabigerinelloides bento-

nesisy G, ultramicrciy praegiobotruncanids and

rotaliporids occur there. Bctuho.s i.s very rare,

dominated by calca^eou^s■ forms, similar to those

présent in the older assemblage.

A very similar assemblage is also characteristic of

the Cenomanian deposits; planktonic Foramini-

fera prcvail there. with dominating rotaliporids,

associated with représentatives of the généra

Pmeglo ho tru Haï fua Hedbergelht^ Wbile in ella ,

Glvbiga inellûidtSy HcteroheUx and Shuckoina.

Ratio of calcareous to agglutinated bcnihic forms

is different in pelagic and hemipelagic deposits of

this stage. Agglutinated taxa prcvail (more than

80% of benthos) in the scaglia rossa-type

(Macelowa Mari Member) and fivschoid deposits

(Trawne Member, Sneznica Siltstonc Mentber).

being dominated by Plectorecurvoides tiheruanSy

Recurvoides sp., Bidbohitcidites sp.. Trochamniina

sp., Haplophragtnoides sp.. Spiroplecuimminn

naparroanriy Arcmlndimina predii, Dorodva sp.,

Triittda sp., Glomospira sp., and by tubular fi^rms.

Calcareous forms are more frequent in variegated

and red pelagic maris (Brynczkowa Mark Skalski

Mari and Fustelnia Mari membets). However,

they are represented by single specimens only.

Agglutinated foraminifers indude the généra

Dentalindy Nodosariay Triitix, Lenticulina,

MarginulinopnSy Mnrginulinay SaYUcenariUy

AsîiUùlus. Planulariity Globulinay OolinUy

Pyridimu Rantfdimy huebulimmay P/eurostorneP

la y ValvH U n e ria , Pu lU n ta » (ha ng u la riuy

GyroidinoideSy Gavelinellay Lingulognvelindla and

Fpnnides.

A quilc different foraminiteral assemblage

appears in black shale faciès close to the

Cenomatiian/Turonian boundary. Planktonic

Foraminifera are still frequent in the lower part

of the shales, being represented predominantly

by Rotalipora cushmanh they are accompanied by

whiteinellids, praegiobotruncanids, hedbergeilids

and single form.s from the généra Globigerinel-

loules and Heterohflix. In a higher pari ol the

shales, only single forms’ of Praeglohotruncana

delrioensis and Hedbergella detrioensis bave heen

found. Benthonic forms are dominated by very

frequent Lenticulina gaultiria. Tliis form is

accompanied by single specimens of agglutinated

foraminifera from the généra BulhobaculiteSy

'['rochamminta HarmosinUy Glomospira, Ammo-

disais and Rhizammhia.

The middlc-laïc Turoniaii foraminifcral assem¬

blage considcrably difters from the Cenomanian

one. Middle furonian was the acme of Helveto-

glohotruncana helvetica and H. praehelvetica

532

GEODIVERSITAS • 1999 • 21 (4)

Radiolarian and foraminiferal biozonation in the Pieniny Klippen Belt

which characterise this assemblage, while ben-

ihonic forms are almost absent. Durlng che late

Turonian, bcnihonic forms bccorae more fre¬

quent, and they prcvail in the latest Turonian

deposiis. rhc bcnthos is dominatcd by aggluti-

nated taxa (more than 90%) with vcty characte*

ri.stic Uvigertnammina jankoi^ Recurvoides

gnduleytsis. GerochitJnmina Cütivena, Kiirrerul'tna

canijonnis, Huplophragmoides c£ bulloides and

Bulhohamlites problematims. Calcarcous benthos

is represented predominantly by the généra

Eponides^ Stensioema and Gyroidinoides.

RADIOLARIAN BIOSTRATIGRAPHY

Radiolarian spccics wcrc idenufied in more than

200 samples from 18 sections in the deposits of

the Pieniny, Branisko, Nicdzica and Czorsznm

successions of the Pieniny Klippen Belt (M. B^k

1997). Scvcntccn horizons containing abundanr

and well-prcscrvcd Radiolaria hâve been chosen

for doser analysis (M. B^k 1999); the Bio-

Graph 2.02 computer program (Savary & Guex

1991) based on the Unitary A-Ssociations Method

was applied. This program produced a scqucnce

of 1 1 U. A. (Hig. 3), which wcrc used for

construcring a radiolarian zonal standard

(M. Bqlc 1999). Three radiolarian zones and five

subzones were proposed for the early Albian

dtrough late Turonian rime span (Fig. 3). These

arc: (1) the Holoayptocttnium barbui zone wilh

Stichornitra Tosilen.sis^ Squinahollum fossile,

Thauitrlü veneUi^ Torcubon dengoi and Oheliscoises

maximus subzones; (2) the Hemicryptoatpsa pre-

polyhedra zone; (3) die Hemwryptoaipsa palyhedm

zone, The top of each zone and subzone is defi-

ned by the FAD of ihe index taxon and aiso by

the base of the overlying zone.

FORAMINIFERAL BIOSTRATIGRAPHY

Extensive biostratigraphical studies based on

planktonic foraminifera were carried out in

Cretaceous deposirs of the Polish pan of the

Pieniny Klippen Belt (Alexandrowicz 1966;

Alexandrowicz er 1968a, 1968b; Jednorowska

1979; Gasihski 1983, 1988; Birkenmajer &

Fig, 3. — Occurrence range chan ot index radiolarian apecies

recorded In the Albian to Coniacian deposits in the Pieniny

Klippen Bell successions, based on their first and the last

appearances. and their co-occurrence based on the Unitary

Associations. Abbreviations ot zones: S. tosaensis. Stichomitra

fosaensrs; S. fos., Squinabollum fossile; T. pulch., Thanajia

pulchra, O. maxim,, Obeliscoites rnaximus. 1, local planktonic

foraminiferal zonation atter Robaszynski & Caron (1985) modi-

fied by K. t3a> (1992,1998),

Jednorowska 1987; Kostka 1993). The local bio¬

zonations hâve been tied to the zonal standards

of the Western Tethys.

GEODIVERSITAS • 1999 • 21 (4)

533

B^kM. &B^k K.

The local planktonic biozonation hcre présentée!

(K. B^îk 1992, 1998), is based on studies of

18 field secrion.s (more than 270 samples) repre-

senting deposits from ail sedirnentary zones ol

the Pieniny KÜppen Basin in Roland. The zones

distingnished and their chmnostratigraphic cali¬

bration, correspond very well with the Medi-

terranean zona! standard as pioposcd by

Robaszynski Sc Caron (1995), with only minor

révision (for more details, see K. B^k 1998).

The biozonation based on agglutinaced foramini-

fera foUows that proposed for Outer Carparhians

by Geroch & Nowalc (1984), and applied aiso to

the Pieniny Klippen Bclt (K, B^k ei al. 1995).

CORRELATION OF RADIOLARAN

ZONATION WITH PLANKTONIC AND

AGGLUTINATED FORAMINIFERA ZONES

Varions radiolarian zonations for the latc Cieta-

ceoLis deposits were proposed depending on the

area concerned. Tw'O proposed standards calibra-

ted with chronostrâtigraphy in the western part

of the Tethys deserve spécial aaention. d’he first

standard was proposed by Llumitricâ (1975) for

the Romanian C'arpachians. Hc rccognised two

radiolarian assemblages, the oldei assemblage

and the younger one correlatcd with planktonic

foraminifcr-a. The Holoçryptocaniam barbui-

H. tuberadiitum assemblage corresponds, accor-

ding to L'iiimitrica (I975}> to the Rotalipora

reicheli-R. ci^diwaai7.ont (latest Cenomanian).

O’Dogherty’s (1994) standard was more dctailcd

and compriscd a calibration with the Northern

Apeninnes and Beric Cordillera. l'hLs calibration

bas been based on planktonic Foraminifera par-

tially following the zonal standard as proposed by

Caron (1985), with some modifications.

O’Dogherry (1994) recognised five radiolarian

zones correlated with the HedbergeUa

(Barremiari) through the Marginommeana sigali

(late Turonian) foraminiferal zones.

In this study, wc propose a corrélation of radiola¬

rian zones with planktonic and agglutinaced fora¬

miniferal zones for the early Albian rhrough late

Turonian time span, for the PoHsh part of the

Pieniny Klippen Belc (Fig. 4).

d'he définition ol the Holocryplocanium barhui

zone used in this zonation lollows that of

Schaaf’s (1985)., with some modification of its

upper limit. The lower boundary of H. hnrbui

zone {- lowcr boundary of the Stichornitra

tûsaensh subzone) is not wcil defined, because the

eailicst iAlbian and larest Aptian ( Ticinella wbeni

planktonic loraminifetal zone and Haplo-

pbritgnioldes nonioninoides agglutinated loramini-

leral zone) deposits arc not well represented in

the sections investigated, their radiolarian fuuna

is rare and poorly preserved. d'he upper bounda-

t)'- ot the H. barhui zone hdls wirhin a lower part

of the Rotalipora reicheli planktonic foraminiferal

zone and tbc Bulbohaadite^ problrmaticus agglu-

tinafed foraminiteraJ zone (middle Ceno¬

manian). The Sipdnahollum fossile radiolarian

subzone coiucîdes with the Biticinella bfrggiensis

foraminiferal zone (Late Albian). The Thanarla

pulthra subzone coincide.s with the Rotalipora

tkinemis-R. subtidnertsis forajninifcral zone (laie

Albian). ITc lower limit of the Toradnw deiigoi

subzone correlates with the upper boundary of

the Ratalipora tiànvnsiS'R. suhtiçinemis foramini¬

feral zone. Its upper limit correlates with the

upper boundary ot the Rotalipora appenaimea

foraminiferal zone (Albian/Cenoinanian bounda¬

ry), and also coïncides with the lower limit of the

Obeliscoües maximus subzone.

The lower boundarv' of ihe Hemicryptocapsa pre~

polyhedra zone corresponds to a lower part of the

Rotalipora reicheli planktonic foraminiteral zone

(middle Cenomanian). Its upper boundary

(= lower boundary of tlîc Pîtrnscrypîovapsa poly¬

hedra zone) corresponds to an upper pan of the

R, cushmani planktonic foraminiferal zone (latc

Cenomanian). I be upper boundary of the

H. polyhedra zone bas not been defined within

the deposits itwestigated because the Radiolaria

from the latest Turonian and the Coniacian are

very poorly preserved (mosrly calcified). This

zone correlates with the Rotalipora cn^hrnani

through Dicarinella y>r;w/oW planktonic fbrami-

niferal zones (■= upper part ol Bulhohaculites pro-

hlematicus and lowcr parc of Uvigerinarmnsna ex

gf. jankoi agglutinated foraminiferal zones; late

Cenomanian through late Turonian).

It îs hoped that the proposed radiolarian zonal

standard will bccome a calibration tool to whicb

534

GEODIVERSITAS • 1999 • 21 (4)

Radiolarian and foraminiferal biozonation in the Pieniny Klippen Bell

STAGES

LOCAL PLANKTONIC

FORAMINIFERAL

ZONES (1)

LOCAL

BENTHONIC

FORAMINIFERAL

ZONES (2)

RADIOLARIAN

ZONES AND SÜBZONES

M. Bak, 1999

!9oH

Turonian

Cenomanian

iooH

■ 110 ^

Albian

Dicarinella primitiva

Marginotruncana sigali

Helvetogtobotruncana

helvetica

Praeglobotrvncana delrioensis

Rotalipora cushmani

Roi.ilipora giùü!ihr4fr,eii^s

Uvigerinammina

ex gr. jankoi

Bulbobaculites

problematicus

Rotalipora reichell

Rotalipora

globotruncanoides

R appenninica —

- R.appen.^ P.buxt.

R buxtorfi-R. ticinensis _

R.ticinensis-R.subticinensis

Biticinella breggiensis

Plectorecun/oides

alternans

Ticinella

primula

Haplophragmoides

nonioninoides

Ticinella

roberti

Hemicryptocapsa

polyhedra

zone

Hemicryptocapsa

prepolybedra zone

Obeliscoites maximus

Torculum dengoi

Thanarla pulchra

Squinabollum fossile

Stichomitra tosaensis

Fig. 4. — Corrélation of radiolarian biozones and subzones with planktonic and agglutinated Foraminifera zonations in the Pieniny

Klippen Belt. PoHsh Carpalhians (chronologicat scale after Robaszynski & Caron (1995)]. 1, local planktonic foraminiferal zonation

after Robaszynski & Caron (1985) modified by K. B^k (1992. 1998): 2. local benthonic foraminiferal zonation after Geroch & Nowak

(1984) modified by K. Bak étal. (1995). K Bak (1995a).

local zonations from orher Carpathian régions

could bc correlated.

Acknowledgements

The authors are greatly indebted to Prof. K.

Birkenmajer (Institute of Geological Sciences,

Polish Academy of Sciences, Krakow) for

vainable éditorial commcnts. Particular thanks

are due to Prof M. Caron (Institut de Géologie

de rUniversité, Fribourg) and Dr. P. Dunikrica

(Institut de Géologie et Paléontologie^ Université

de Lausanne) who tcvised the manuscript. Mrs

1. Chodyri (Institute of Geological Sciences,

Jagiellonian University, Krakow) helped us in the

laboratory part of the work. This research is a

GEODIVERSITAS * 1999 • 21 (4)

535

B^kM. &B^k K.

contribution of the IGCP 362 Project, Tethyan

and Boréal Cretaceous.

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Submitîed for publication on 1 April 1998;

accepted on 18 February 1999.

GEODIVERSITAS • 1999 • 21 {4)

537

Early Norian Radiolaria from Cyprus

Nikita Yu. BRAGIN

Geological Institute, Russian Academy of Sciences

Pyzhevsky 7, 109017 Moscow (Russia)

bragin@ginran.msk.su

Kirill A. KRYLOV

Geological Institute, Russian Academy of Sciences

Pyzhevsky 7, 109017 Moscow (Russia)

krylov@ginran.msk.su

kirka@geo.ifaran.ru

Bragin N. Yu. & Krylov K. A. 1999. — Early Norian Radiolaria from Cyprus, in De Wever P.

& Caulet J.'P. (eds), InterRad VIII, Paris/Bierville 8-13 septembre 1997, Geodiversitas 2^

(4) : 539-569.

KEYWORDS

Radiolaria,

systemacics,

1 riassic,

Norian,

Cyprus.

ABSTRACT

Lower Norian limestones from the Mamonia Complcx, sourhwcstern

Cyprus, are characterized by diverse radiolarian assemblages. New taxa are

described: Bulbocyrtium famm n. sp., Caphtorocyrtium tenerum n. gen., n. sp.,

Capnuchosphâera theloides minor n. ssp., Haeckelicyrt'mm (?) carterae n. sp.,

Kinyrosphaera trispinosa n. gen., n. sp., K. heücata n. gen., n. sp., Naholella

trispinosa n. sp., Whalenella robusta n. sp., and Xiphotheca (?) spinellifera

n. sp.

MOTS CLÉS

Radiolaires,

systématique,

Trias,

Norien,

Chypre.

RÉSUMÉ

Radiolaires du Norien inférieur de Chypre.

Des calcaires du Norien inférieur de la formation de Mamonia, sud-ouest de

Chypre, sont caractérisés par divers assemblages de radiolaires. De nouveaux

taxons sont décrit.s : Bulbocyrtium latum n. sp., Caphtorocyrtium tenemm

n. gen., n. sp., Capnuchosphaera theloides minor n. ssp., Haeckelicyrtium (?)

carterae n. sp., Kinyrosphaera trispinosa n. gen., n. sp., K. heücata n. gen.,

n. sp., NabolelLi trispinosa n. sp., Whalenella robusta n. sp. et Xiphotheca (?)

spinellifera n. sp.

GEODIVERSITAS • 1999 • 21 (4)

539

Bragin N. Yu. & Krylov K. A.

INTRODUCTION

The presence of Radîolaria in the Triassic sedi-

mentan' rocks of Cyprus was indicated by many

previous investigaiors (Lapierre 1975; Robertson

ik Woüdcock 1979: Swarbrick & Robertson

1980). Altfiough these fossÜs are abondant and

well preserved, there is no systematic study of

thcm. Assemblages of the upper Norian were

only illustraced before (Bragin & Krylov 1996).

This Work deals with the diverse lower Norian

fauna, which includes many undescribed taxa.

Previous investigaiors described diverse Carnian

and Norian radiolarian assemblages from Sicily,

Greece and Turkey (De Wever er ni 1979),

Austria (Kozur & Mostler 1972; 1979; 1981;

Lahm 1984), Croacia (Halamic & Gorican

1995), Japan (Yao 1982; Yoshida 1986;

Sugiyama 1997), -western North America (Blomc

1984; Yeh 1989), l’hilippincs (Yeh 1990), castern

Russia (Bragin 1991). The Carnian to Norian

stratigraphie Litterval was subdividcd inco radio¬

larian zones and subzones in the régions of

Circum-Pacific belt (Yao 1982; Blome 1984;

Bragin 1991; Sugiyama 1997), There are still no

such subdivisions for the Mediterranean région

and the stratigraphie ranges of numeroiis taxa

remain uncerrain. The description of well-dated

and extremely diverse radiolarian assemblages

from Cyprus will givc supplemcntary data for

further rcscarch in the Triassic bioscratigraphy as

well as in tlie taxonomy and évolution of the

Triassic Radiolaria.

GEOLOGICAL SETTING

The Triassic of Cyprus was subdivided into rwo

units: sedimentary and volcanogenous with sedi-

mentary intercalations (Lapierre 1975).

Swarbrick & Robertson (1980) defined two

important parts ol the Mamonia Allochtiionous

Complex-scdimcntary Ayos Photios Group

(MiddJe Triassic-Early Cretaccous) ;md volcano¬

genous Dhiarizos Group (Upper Triassic-

Jurassic) (Fig. 1). Borh these groups arc

incorporared into complicated allochthonous

structures. The detached blocks of the Ayos

Photios and Dhiarizos groups are common in the

varlous mélangés of the Mamonia Complex.

The formations of the Mamonta Allochthonous

Complex hâve wide disiribuiion acar Agia

Varvara Village, southwestern Cyprus (Fig. 1).

T’his area bas an imbricated structure complica¬

ted by a .System of sublatitudinal and NW-tren-

ding srrike-slip fruits. The lowetmost structural

unit is composée! uf the terrigenous mélangé

with blocks derived both from the Troodos

Complex and Mamonia Complex. They are

overthrusted by sériés of allochthonous unies that

are represenred by (Fig. 1 );

1, SerpcncinUe mélange with blocks of Troodos

lavas;

2, Nappe composed of Agia Varvara mecamor-

phics: amphibühtes and quartz-mica shists;

3, Serpentinire mélangé with blocks derived both

from the Mamonia Complex and Troodos

Complex;

4, Nappe composed of Dhiarizos hasic lavas with

limestone intercalations (Upper Triassic to Lower

Cretaccous),

3. Nappe of Ayos Photios sedimentary group

represenred by the Upper Triassic clastics (Bragin

k Krylov 1996) and the Middle Jurassic to

Cretaccous cherts, mudstones, calcarenites and

sandstoncs.

The blocivs of sedimentary rocks were studied in

the field ol terrigenous mélangé located at

34°45’N, 32°30’E. One of such blocks consists

ol white and pink plary niicritic limestones with

intercaUtion.s of grcy and ycTlowish-pink cherts

with observed thicknes.s 14 m (Fig l).This

limestone block is interpreted as a sedimentar)'^

Icasc derived from the Triassic part ol Dhiarizos

Group. This conclusion oui bc supported by rhe

fact that thèse limestones did noc contain clastic

intercalations that are commun for the carbonate

sédiments of the Ayos Photio.s Group (Swarbrick

& Robertson 1980; Bragin & Krylov 1996).

Lirnesrones and cherts contain abundanr radiola-

rians replaccd by ealcuc and recrysiallizcd. Only

onc sample yicldcd radioiariaos replaccd by pyri¬

te. The pyrirized radiolaaians exhibit well-preser¬

ved morphological featurcs. The radiolarian

assemblage is characterized by high taxonomie

diversity. Radiolaria are represenred by tlic iollo-

wing taxa: Annulotriassocampe sp. cf. A. sulovensis

540

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cypms

Fig. 1. — Geological position of the Upper Trlassic radiolarian-bearing limestones in the southwestern Cyprus. I, map showing

generalized geological position of the Mamonia Allochthonous Complex in the southwestern Cyprus; II. geological map of the Agia

Varvara area (Loc.. position of studied limestone block); 111, geological section A-B. Legend; 1, Troodos Complex; 2. Mamonia

Allochthonous Complex; 3. Cer\ozoic sédiments; 4, Ayos Photios Group (Upper Triassic^lretaceaus]; 5. serpentinite mélangé with

Troodos blocks; 6, Agia Varvara metamorphics; 7, Dhiarizos Group (volcanics with limestone intercalations, Upper Triassic-Lower

Cretaceous); 6, serpentinite mélangé with Mamonia blocks; 9, terrigenous mélangé; 10, boundaries; a, stratigraphie; b, tectonic.

GEODIVERSITAS • 1999 • 21 (4)

541

Bragin N. Yu. & Krylov K. A.

(Kozur & Mock, 1981). Archaeacenosphaera sp.,

Biilbocyrtium latum Bragin n. sp., Caphtorocyr-

tium tenerum Bragin n. gtn., n. sp., Capnodoce

ruesti Kozur & Mock, 1981, Cuptutchosphaera

deweveri Kozur & Mostler, 1979. C sp. cf.

C. deweveri Kozur hc Mosrlcr, 1979. C theloides

minor Bragin n. ssp., C sp. cl. C theloides De

Wever, 1979, C. sp. aff. C. curpathica Kozur &

Mock, 1981. Capnuchosphacridac n. gen.. sp,

indet., Citrinaheliosomd carinatd (Kozur Ôc

Mostler, 1979), Entdctimnphaerü sp. aft. E. simo-

ni Kozur ^ Mostler, 1979. E. (?) sp. 1. E. (?)

sp. 2, Ferresiitm sp. afh E vonclusum Carter,

1993, Forenuineltina (?) sp., Haeckelicyrtium car-

terae Bragin n. sp., Heliosoma (?) riedeli Kozur &

Mostler, 1981, Heliosoma (?) sp., lcrioma remtn-

cistrum De Wever. 1979, L sp. aff. /. ictrands^

trum De Wever. 1979. KahUrosphuera aspinosrt

Kozur & Mock, 198!, K. nortca Kozur àc

Mostler. 1979, Ktmnnpongetlej hhphiosa Kozur &:

Mostler, 1981, KinyTcnphaeyd trispinosa Bragin

n. gen., n. sp., K, hdkatu Bragin n. gcn., n. sp.,

Kinyrosphaera (?) sp., Laxtomm (?) sp., Liasso-

saturnalis pttrvus Kozur & Mosrlcr, 1990, Loffa

(?) sp., MuhmortilispulehcrYchy 1989, Nabolella

trispinosa Bragin n. sp , Napora (?) sp. \,N. sp. 2,

Neopylentouemn sp. aff N. prneera Sugiyama,

1997, Palaeosatiirnalis triassicus (Kozur &

Mostler, 1972), î\ laiiannulatus Kozur &

Mostler, 1983, E rnneki Kozur & Mosrier, 1983,

Paronaeila nortca Kozur & Mock, 1981,

Paronaella sp,, PrntactjnocarpHs sp. aff P tetrO'

canthus Dumirrica, 1978, Pentactinocarpus sp.y

Praemesosaturnalh sp. cf. P. multidematus (Kozur

& Mostler, 1972), Pentaspon^disens 1, P sp.

2, Poulptis piahyx De Wever, 1979, Pseudo-

saturniforrna carnica Kozur & Mostler, 1979,

Praenanina veghne ]LtyL\x\y 1994, Praenrhiculi-

formella goestlingensis Kozur 6l Mostler, 1978,

Pseudostylosphacra (?) sp., Sürla (?) sp.. Sepsagon

sp., Sethticapsû sp., Spongostylus carnicus Kozur &

Mostler, 1979, S. tortilis Ko/.wx ôc Mostler, 1979,

Sulovella constricta Kozur 6c Mock, 1981,

Syringocapsa batodes De Wever, 1979,

Syringocapsa sp., Trialatus robtisUts (Nakaseko &

Nishimura, 1979), Triassohipedis (?) sp.,

Triassocampidac n. gcn., sp. indet., Triassocru-

cella triaisica (Kozur & Mostler, 1978),

Veghicyclia sp. cf. V. robusta Kozur & Mostler,

1972, Vinassaspongus transitas Kozur 6i Mock,

1981. Whalenella sp. alf. U'( perfecta (Blojne,

1984), W. robusta Bragin n. sp., Xiphotheca rugo-

sa Bragin, 1991, X. longa Kozur & Mock, 1981,

X. (?) spineltifera Bragin n. sp.. Xiphotheca sp.,

Xiphotheca (?) sip., Zhamojdasphaeraproceruspino-

sa Lahm, 1984. AU rhesc radiolatians corne trom

a single samplc,

l’Iic early Norian age ol thîs assemblage is confir-

med by tlic présence of conodoiits Epigondolella

spatulata (Hayashi) and such radioJariao taxa as

Capnodoce rucsli, Sulovella constricta and

Vinassaspongus transitas. Radiolarian assemblage

is typical For dte Capnodoce ruesti (Kozur &

Mo.stler 1994) wiih .somc cxccpiioits. Sonic .spe-

cics wcrc known only from Carnian or older

deposits: Karnospongella bispinostu Praenanina

veghae^ Spotigostylus carnicus. T he locality from

Cyprus may represent a latcst occurrence of these

taxa.

SYSTEMATICS

Subclass IIADIOLARIA Millier, 1858

Order POLYCYSTINA Ehrenberg, 1838

Suborder SPUMELI ARIA Ehrenberg, 1875

Superfamily HFXASTY1.ACKA Haeckel, 18(S2

Family En lACnNllDAE Ricdcl, 1967a

Geniis Entactinosphaera Foreman, 1963

Type SPECIES. — Entactinosphaera esostrongyla

Foreman, 1963.

Entactinosphaera sp. aff E» simoni

Kozur & Mostler, 1979

(Fig. 30

alT. Entactinosphaera ’i simoni Kozur & Mostler, 1979:

72, pl. 4, fig. 5; pl. 7, fig. 2; pl. 8, fig. 1. - Lahm

1984: 17, pl. 1, fig. 10.

Occurrence. — Lower Norian of Cyprus.

Descri prroN

Small sphericaJ shell with six symetrically arran-

ged spines, four of them in the same plane.

Spines long, robust, Y-shaped. Cortical shell one-

542

GEODIVÊRSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

layered, with prominent pores in irregular hexa¬

gonal to pentagonal pore frames.

Rf.marks

This form differs from E. simoni Kozur &

Mostler by more spherical cortical shell with

robust spincs.

Entactinosphaera (?) sp. I

(Figs 2H, 3F)

Description

Shell spherical with four three-bladed spines

lying in one plane. Distal parts of spines some-

timcs display small sinistral torsion. Shell with

subspherical pores rhat arc variable in size and

cnclosed in rectangular pore frames with promi-

nenc nodes at vertices. Shell surface sometimes

with small thin secondary spines.

Remarks

Akhough the external morphology is well preser-

ved, the inner structure is uncertain. These forms

are assigned tentatively to genus Entactino¬

sphaera.

Entactinosphaera (?) sp. 2

(Fig. 3A)

Remarks

Uncomplete specimen with visible inner shell

illustrated. Nevertheless, che internai spiculé can-

not be observed due to the préservation (replace¬

ment by pyrite).

Family SepSAGONIDAE

Kozur & Mostler, 1981

Genus Sepsagon

Dumitrica, Kozur & Mostler, 1980

Type SPECIES. — Triactoma longispinosum Kozur &

Mostler, 1979.

Sepsagon sp.

(Fig. 3E)

Description

Shell subspherical with rough nodose surface,

with small pores in rectangular pore frames.

Three main spines long, curved, with Y-shaped

cross-section and moderately developed dextral

torsion.

Remarks

Only one specimen was observed.

Genus Pseudostylosphaera

Kozur & Mostler, 1981

Type SPECIES. — Pseudostylosphaera gracilis Kozur &

Mock, 1981.

Pseudostylosphaera (?) sp.

(Fig. 71)

Remarks

This form is characterized by short thin apo¬

physes at the médian parts of the main spines. It

did not represent a typical double layered shell of

Pseudostylosphaera and may belong to another

genus.

Family HexapyiüMELLIDAE

Kozur & Mostler, 1979

Genus Praenanina Kozur, 1994

Type species. — Praenanina veghae Kozur, 1994.

Praenanina veghae Kozur, 1994

(Fig. 2B, C, E)

Praenanina veghae Kozur, 1994 in Kozur àc Mostler,

1994: 247, pl. 2A, fig. 2; pl. 4A, figs 1, 3.

Occurrence. — Middle (?) to upper Carnian of

Hungary, lower Norian of Cyprus.

Family Pentactinocarpidae

Dumitrica, 1978

Genus Pentactinocarpus Dumitrica, 1978

Type species. — Pentactinocarpus fusiformis

Dumitrica, 1978.

GEODIVERSITAS • 1999 • 21 (4)

543

Bragin N. Yu. & Krylov K. A.

Fig. 2. — A-D. Carinaheliosoma carinata Kozur & Mostler; D. detail; B. C, E, Praenanina veghae Kozur; E, detail; F,

Archaeocenosphaera sp.; G, Heliosoma (?) sp.; H, Entactinosphaera (?) sp. 1. Scale bar: A, B, C, F, 100 pm; D. E, 20 pm; G, H,

200 pm.

Pentactinocarpus sp.

aff. P, tetracanthus Dumitrica, 1978

(Fig. 7D)

Remarks

This form ditFers from Pentactimcarpm tetr'acari-

thus (Dumitrica, 1978: 44, pl 2, fig, 1) by larger

and widcr test. It difFers from P. sevaücm (Kozur

& Mosder. 1981: 21, pl. 52, %. 3, pl. 53, figs 2,

5, pl. 55, fig. I) by more delicaie meshwork of

cortical shell with smaller pores in hexagonal to

pentagonal pore frames with small nodes at ver-

tices. P magnus (Kozur & Mostler, 1979: 55,

pl. 10, fig. 1) bas larger pores enclosed in the

variable polygonal pore frames without nodes at

vet tices.

Pentactinocarpus sp.

(Fig. 7E)

Remarks

This form possesses a délicate small test with

544

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

very thin and long apicaK antapical and basal

spines. The position of basal spines is similar to

chose of Pentactinocnrfiis tetracanthus Dumitrica

but specimen from Cyprus differs by small sue

of test and by thin necwork-like meshwork of a

cortical shell.

Superfamily AcTINOMMACEA Haeckel, 1862

Family XlPHüS'l'YLlDAE Haeckel, 1881

Genus Archaeocenosphaera

Pessagno & Yang, 1989

Type SPECIES. — Archaeocenosphaera ruesti Pessagno

& Yang, 1989.

Archaeocenosphaera sp.

(Fig. 2F)

Remarks

This form is similar to Archaeocenosphaera sp. aff

A. laseekensis Pessagno & Yang (Carter 1993: 67,

pl. 1, figs 14, 19, 20). It difters by smaller test

with pores chat are more unitorm in size.

Family ActinommidAE Haeckel, 1862

Genus Carinahelmoma

Kozur & Mostler, 1981

Type SPECIFS. — Carmaheliosoma densiporata Kozur

&Mock, 1981.

Carinaheliosoma carinata

(Kozur Mostler, 1979)

(Fig. 2A, D)

Heliosoma carinata Kozur 6c Mostler, 1979: 52, pl. 9,

fig. 1-3.

Carinaheliosoma carinata (Kozur & Mostler, 1979) -

Lahm 1984: 65, pl. 11, fig. 8.

Occurrence. — Upper Triassic, Carnian to lower

Norian of the European Tethys.

Genus Heliosoma Haeckel, 1882

entend. Kozur &: Mostler, 1979

Type SPECIES. — Heliosoma radians Haeckel, 1887.

Heliosoma (?) riedeli

Kozur 6c Mo.siler, 1981

(Fig. 3B, D)

Heliosoma (?) riedeli Kozur 6i Mostler, 1981: 65,

pl. 1, fig. 4. — Lahm 1984: 63. pl. Il, figs 2, 3.

Occurrence. — Middle Triassic, Ladinian, Upper

Triassic, Carnian (?) to lower Norian of the European

Tethys.

Heliosoma (?) sp.

(Fig. 2G)

Description

Small roughly subspherical to rectangular test

with cen long thin thrce-bladed spines. Cortical

shell with small roughly subcircular pores.

Proximal parts of spines with deep grooves that

becomc narrow at the middle parcs and disappcar

at the distal parcs.

Remarks

This form differs from Heliosoma (?) riedeli

Kozur 6c Mostler by small size of cortical shell

and its roughly spherical to rectangular shape.

Genus Kahlerosphaera

Kozur 6c Mostler, 1979

Type SPECIES. — Kahlerosphaera parvispinosa Kozur &

Mostler, 1979.

Kahlerosphaera aspinosa

Kozur & Mock, 1981

(Fig. 7A)

Kahlerosphaera ? aspinosa Kozur 6c Mock, 1981 in

Kozur 6c Mostler, 198L 36, pl. 47, fig. 3.

Occurrence. — Upper Triassic, lower Norian of the

European Tethys.

Kahlerosphaera norica

Kozur 6c Mock, 1979

(Fig. 6G. H)

Kahlerosphaera norica Kozur 6c Mock, 1981 in Kozur

& Mostler, 1981: 36, pl. 15, fig. 4.

Occurrence. — Upper ’Friassic, Carnian to lower

Norian of the European Tethys.

GÉODIVERSITAS • 1999 • 21 (4)

545

Bragin N. Yu. &C Krylov K. A.

Fig. 3. — A, Entactinosphaera (?) sp. 1 ; B. D. Heliosoma (?) riedeli Kozur & Mostler; C. Entactinosphaera sp. aff. E. simoni Kozur &

Mostler; E. Sepsagon sp.: F. Entactinosphaera (?) sp. 1. Scale bar: A, 50 pm; B-F, 100 pm.

Genus Vinassaspongus

Kozur & Mostler, 1979

Type species. — Vinassaspongus subsphaericus Kozur

& Mostler, 1979.

Vinassaspongus transitus

Kozur & Mock, 1981

(Fig. 6D, F)

Vinassaspongus transitus Kozur & Mock, 1981 in

Kozur & Mostler, 1981: 69, pl. 64, figs 1, 2.

Occurrence. — Upper Triassic, lower Norian of the

European Tethys.

Genus Zhamojdasphaera

Kozur & Mostler, 1979

T\te species. — Zhamojdasphaera latispinosa Kozur

& Mostler, 1979.

546

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 4. — A, Capnuchosphaera deweveri Kozur & Mostler; B, Capnuchosphaera sp. cf. C. deweveri Kozur & Mostler; C, Sarla (?)

sp.: D. E, Capnuchosphaera thelvides minor Bragin n. ssp.; E. holotype; F. H. I. Capnuchosphaera sp. et. C. iheloides De Wever; G,

Capnuchosphaera sp. atl. C. carpathica Kozur & Mock. Scale bar: A-C, F-l. 100 pm: D, E, 80 pm.

Zhamojdasphaera proceruspinosa

Lahm, 1984

(Fig. 8E)

Zhamojdasphaera proceruspinosa Lahm, 1984: 75,

pl. 13, fig. 6.

Occurrence. — Upper Triassic, Carnian-lower

Norian of the Tethys.

Family CAPNUCUUSIHtAERIDAE

' De Wever, 1979

Genus Capnuchosphaera De Wever, 1979

Type SPECIES. — Capnuchosphaera triassica De Wever,

1979.

Capnuchosphaera deweveri

Kozur & Mostler, 1979

(Fig. 4A)

GEODIVERSITAS • 1999 • 21 (4)

547

Bragin N. Yu. & Krylov K. A.

Capnuchosphaera tj'iassica var. a De Wever, 1979: 84.

pl. 4, figs 3-5.

Capnuchosphaera dewevert Kozur Ôc Mostlct,1979: 77,

pl. 10, figi 2, 4-8i pl. 12, fig. 1. — De Wever 1982:

152, pl. üp 10, 11; pl. 4. figs l, 2.-Blome 1983:

16, pl. l, figs 3, 8, 9, 16, 18; pl, 11, fîgs 1, 2, 16, —

Lahm 1984: 81, pl. 14, fig. 7. - Yeh 1990: 8. pl. 2,

fig. 5; pl. 10,flg. 8.

Occurrence. — Upper Carnian to lower Norian of

European Tethys and Pacific coastal areas.

Capnuchosphaera sp.

cf. C deweveri Kozur & Mostler, 1979

(Fig. 4B)

aff. Capnuchosphaera deweoeri Kozur & Mostler,

1979; 75, pl. 10. figs 4-7; pi- 12, fig. 1.

Remarks

This form has shorter and thicker tumidaspinae

than C deweveri Kozur & Mostler. The new

taxon cannoc be described because of poor pré¬

servation.

Capnuchosphaera theloides minor

Bragin n. ssp.

(Fig. 4D, E)

Capnuchosphaera theloides yjiï. a De Wever, 1979:

p, 84, pl. 4, fig. U - Nakaseko & Nishimura 1979:

p. 75, pl. 7, fig. 7. - De Wever 1982: 158, pl. 6,

fig. 8.

Capnuchosphaera theloides 1982: pl. 1, fig. 23. -

Yoshida 1986: pl. 12, fig. 4. — Bragin 1991a: p. 77,

pl. 5, figs 14. 15.

Holotype. — Fig. 4E. GIN-4858-42. Cyprus, Agia

Varvara Village, Maraonia Complex, Upper Triassic,

lower Norian.

Etymology.— Minor {Latin)-younger.

Dimensions (based on fivc spccimens). — Diameter

of cortical shell 130-135 pm. total length of spincs

220-260 pm, length of distal rod-likc parts of spines

145-160 pm, maximal width ol spines 80-90 pm.

Occurrence. — Upper Tria.ssic, upper Carnian to

lower Norian of European Tethys, Japan and eastern

Russia.

Descripi'ion

Cortical shell spherical with three tumidaspinae

.situated in rhe same plane. Proximal parts of

tumidaspinae smooth, moderacely ihick, central

parts three-bladed, tetrahedrical, without torsion,

distal parts verj* long and chin wtihoui dcar dif¬

férentiation from central parts. Cortical shell per-

forated by small circular pores in the irregular

rhorny pore frames.

Remarks

The.sc forms differ from Capnuchosphaera the-

laides theloides (De Wever, 1979; 83, pl. 3,

figs 10-13) by the characier of tumidaspinae

with thinner proximal parts and longer distal

parts vhar are not well differenriated from the

central tetrahedrical parts.

Capnuchosphaera sp.

cf. C theloides De Wever, 1979

(Fig. 4F, H, I)

et. Capnuchosphaera theloides De Wever, 1979: 83, 84,

pl. 3, figs 10-13: pl. 4, fig. 1.

Remarks

This form ha.s poorly preserved central and distal

parts of tumidaspinae. Due to this préservation it

is difficult to give a précisé détermination.

Capnuchosphaera sp.

aff. C. carpathica Kozur & Mock, 1981

(Fig. 4G)

aff. Capnuchosphaera carpathica Kozur & Mock,

1981:74, pl. 48, fig. 5.

Occurrence. — Upper Triassic, lower Norian of

Cyprus.

Description

Cortical shell subspherical with three tumida¬

spinae in the sanie plane and thin rod-likc addi-

tional spine petpendicular to the tumidaspinae.

Tumidaspinae with moderately thick proximal

parts, central parts subtetrahedrical, concave,

without torsion, distal parts long and thin.

Cortical shell with small subcircular pores in irre¬

gular pore frames.

548

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Remarks

This form differs from C carpathica Kozur &

Mock by more concave charactcr of tumidaspi-

nae and by the presence of additional spine.

Genus SarU Pcssagno, 1979

Type species. — Sarla prietoensts Pessagno, 1979.

Sarla (?) sp.

(Fig. 4C)

Description

Cortical shell subspherical, slightly flattened to

subdiscoidal, with thrce spines in the same plane.

Spines thrce-bladcd» without torsion, with slight¬

ly inflated middlc parts. Distal parts of spines

with tetragonal-like structures, poorly preserved.

Pores of shell small, subcircular, encloscd in irre-

gular pore frames.

Remarks

Only one specimen was found. It is similar to

Eptinghim sp. A (De Wever 1982: 277, pl. 35,

figs 3, 4; Grapes et al. 1990, fig. 9h) but pos-

sesses more inflated shell. Due to poor préserva¬

tion, it is difficult to conclude that it is the same

spccies as illustrated by De Wever. The generic

assignment is utider question. The terminations

of spines resemble similar structures of

Kablerosphaera.

Genus Sulovella Kozur àc Mock, 1981

Type species. — Sulovella constricta Kozur & Mock,

1981.

Sulovella constricta

Kozur &: Mock, 1981

(Fig. 5A, B)

Sulovella constricta Kozur & Mock, 1981 in Kozur &

Mostler, 1981: 77, pl. 64, fig. 2.

Capnuchosphaera cf. comtricta - Halamic ôc Gorican

1995;pL 2, fie. H.

? Capntichosphaera crassa Yeh, 1990: 8, pl. 1, figs 8,

11-13, 18. 19. — Halamic Ôr Gorican 1995: pl. 2,

fig. 12.

Occurrence. — Upper Triassic, lower Norian of

Carpachians, Croatia, Philippines (?) and Cyprus.

Genus Icrioma De Wever, 1979

Type species. — Icrioma tetrancistrum De Wever,

1979.

Icrioma tetrancistrum De Wever, 1979

(Fig. 5G)

Icrioma tetrancistrum De Wever, 1979: 86, pl. 4,

figs 13-15; 1982; 262, pl. 22, figs 1-6.

Occurrence. — Upper Triassic, upper Carnian to

lower Norian, European Tethys.

Icrioma sp. aff. L tetrancistrum

De Wever, 1979

(Fig. 51)

Remarks

This form differs from Icrioma tetrancistrum De

Wever by tetrahedrical rather then subspherical

form of shell with arms less well differentiated

from the central part of shell.

Genus Kinyrosphaera Bragin n. gen.

Type species. — Kinyrosphaera trispinosa n. sp.

Sl’ECIKS INCLUDEO. — Kinyrosphaera trispinosa Bragin

n. sp., K. helicata Bragin n. sp.

EtymOLüCV. — Kinyras (Greek), legendary king of

Cyprus, founder of pre-Greek Cypriot dynasty.

Occurrence. — Upper Triassic, lower Norian of

Cyprus.

Description

Capnuchosphaeridae with three spine.s parrly

covered hy porous extensions ol cortical .shell.

Cortical shell spherical or subspherical, with wall

typical for the fâmily. Ceniial parts of .spines

with three large pores, distal parts thin, some-

rimes rod-like.

Remarks

Kmyrosphaera Bragin n. gen. differs from Icrioma

De Wever by présence of three spines, from

Capnuchosphaera De Wever by porous extensions

of cortical shell to the proximal parts of spines.

GEOOIVERSITAS • 1999 * 21 (4)

549

Bragin N. Yu. & Krylov K. A.

Fig. 5. — A. B. Sulovella constricta Kozur & Mock; C-E, Kinyrosphaera trispinosa Bragin n. gen., n. sp.; C, holotype; D, detail of

spine; F, H. Kinyrosphaera helicata Bragin n. gen., n. sp., F. holotype; G, Ichoma tetrancistrum De Wever; I, /chôma sp. aff. I. tetran-

cistrum De Wever. Scale bar: A-C, G. I. 100 pm; D, F, H, 80 pm; E, 35 pm.

Kinyrosphaera trispinosa Bragin n. sp.

(Fig. 5C-E)

HolotyI’E. — Fig. 5C, GIN-4858-49, Cyprus, Agia

Varvara Village, Mamonia Complex, Upper Triassic,

lower Norian.

Ettmolocîy. — Trispinosa (Latin), wirh thrcc spincs.

Occurrence. — Upper 'Lriassic, lower Norian of

Cyprus.

Dimensions (based on cight spedmens). — Diameter

of cortical shell 155-180 pm, length of spines without

terminal parts 140-155 pm.

DESCRIPI'ION

Cortical shcll spherical with nodose surface, with

small subcircular to subrectangular porcs in

weakly devcloped rectangular pore franies. Spines

xnoderacely long, lie in rhe same plane. Proximal

parts of spines short, cylindrical, with small sub-

550

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

circular pores arranged in longitudinal rows

somerimes displaying small dexrral twisting.

Central parts of spines Y^shaped in cross-section,

with threc large pores. Distal parts of spines are

dividcd into three rod-likc terminations slightly

curved distally with small smooth node at their

joints.

Rf.marks

Kinyrosphaera trispinosa Bragin n. gen., n. sp. dif-

fers from K. helicata Bragin n. gen., n. sp. by

non-twistcd central parts of spines and by trifur¬

cation of distal parts of spines.

Kinyrosphaera helicata Bragin n. sp.

(Figs 5F, H. 6A)

? Capnuchosphaera (?) sp. — Halamic & Gorican 1995:

pl. 2, fig, 10.

HolüTYPE. — Fig. 5F, GlN-4858-51> Cyprus, Agia

Varvara Village, Mamonia Complex, Upper Triassic,

lower Norian.

EtymologY. — Hélix (Greek), spiral shell.

OcCURRENCn. — Upper Triassic, lower Norian of

Cyprus, upper Carnian of Croatia.

Dimensions. — Diamcter of cortical shell 160-

200 um, total length of spines 220-270 pm, maximal

widrn of spines 60-80 fim,

Descri P rioN

Cortical shell spherical with nodo.se surface, with

small subcircular to subrectangular pores in

weakiy developed rectangular porc framcs. Spines

long, lie in the same plane. Proximal parts of

spines cylindrica), with small subcircular pores

arranged in longitudinal rows and with longitu¬

dinal ridges berween rows of pores. Central pans

of spines srrongly twisted sinisirally, Y-shapcd in

cross-section, with three large porcs. Distal pans

of spines long, thin, rod-like.

Remarks

Kinyrosphaera helicata Bragin n. gen., n. sp. dif-

fers from K. trispinosa Bragin n. gen., n. sp. by

the twisting of central parts of spines and by the

long rod-like distal parts of spines.

Kinyrosphaera (?) sp.

(Fig. 6B)

Remarks

This form bas three porous extensions of the cor¬

tical shell at three main spines, but does not dis¬

play typical Y-shaped in cross-section médian

parts of spines. Only one spécimen was observed.

Capnuchosphaeridae gen. et sp. indet.

(Fig. 6E)

Remarks

This form bas four tetrahedrically arranged solid

twisted spines. It differs from the représentatives

of gen us Sarla Pessagno by the number of spines.

Family Pantanelliidae Pessagno, 1977

Subfamily CapnodüCINAE Pessagno, 1979

Genus Capnodoce De Wever, 1979

Tyi*E SPECIES. — Capnodoce anapeies De Wever, 1979.

Capnodoce ruesti Ko/ur & Mock, 1981

(Fig. 7B, C)

Capnodoce mesti Kozur & Mock, 1981, in Kozur &

Mosder, 1981: 74, fig. 65, fig. 2.

Occurrence. — Upper Triassic, lower Norian of

Carpathians and Cyprus.

Genus Pessagno, 1979

Tyve SPECIES. — Loffa mulleri Pessagno, 1979.

Loffa (?) sp.

(Fig. 60

Description

Shell subtctrahedrical, spongy» with four tubular

.spines (typical for Subfamily Capnodocinae).

Spines tetrahedrically placed, smooth, cach with

three internai channels which end by threc pores

at terminarions.

Remarks

This form belongs to genus Loffa Pessagno due

to che presence of four smooth tubular spines

GEODIVERSITAS • 1999 • 21 (4)

551

Bragin N. Yu. & Krylov K. A.

Fig. 6. — A. Kinyrosphaera helicata Bragin n. gen., n. sp.; B, Kinyrosphaera (?) sp.; C, Loffa (?) sp.; D, F, Vinassaspongus transitus

Kozur & Mock; E. Capnuchosphaeridae gen. ef sp. indet.; G, H, Kahlerosphaera norica Kozur & Mock. Scale bar: B. C, F, H,

100 pm; A, D. G. 80 pm. E. 50 pm.

without pomus cxteasions of a cortical shell. It is

characterizcd hy irregularly spongy meshwork of

shcll and by ihickcr spincs than other représenta¬

tives of gen us Loffii.

Superfamily Spongodiscacea

H aeckel, 1862

Family SPONGURlDAt: Haeckel, 1862

Genus Spongostylus Vizeckei, 1882

Type species. — Spongostylus hastatus Haeckel, 1882.

Spongostyhis camicm

Kozur & Mostlcr, 1979

(Fig. 7F)

Spongostyius carnicus Kozur & Mostlcr. 1979; S8,

pl. 9, figs 5, 6, 8. 9; 1981, pl. 38, fie. 3. - I.alim

1984: 69) pl. 12. fig. 4. — Carter et al, 1989: pl. 1,

fig. 5. - Ych 1989: 67) pl- 13, fig. 8. - Grapes et al.

1990: fig. 80. — Halamic & Gorican 1995: pl. 2,

figs 18, 19. — Knipper ^i/. 1997: pl. 2, fig. 1.

552

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 7. — A, Kahlerosphaera pan/ispinosa Kozur & Mostler; B. C. Capnodoce ruesti Kozur & Mock; D. Pentactinocarpus sp. aff.

P. tetracanthus Dumitrica; E, Pentactinocarpus sp., F, Spongostylus camicus Kozur & Mostler; G, Kamospongella bispinosa Kozur &

Mostler; H. Pentaspongodiscussp. 1; I. Pseudostylosphaera sp. Scale bar: A-C. E, G-1,100 pm; D, F, 50 pm.

Occurrence. — Uppcr Triassic, Curnian to lower

Norian, worlclwiclt? in thc low paleolaritudcs.

Spongostybis tortilis

Ko/ur & Mostler, 1979

(Fig. 8A)

Spongostylus tortilis Kozur & Mosrlcr, 1979: 58, pi. 4,

fig. 2; pl. 11. fig. 6; pl. 18, fig. 2; 1981: pl. 40, fig. 2;

pi. 56, fig. 3. — Lahm 1984: 68, pl. 12, fig. 3.

Spongostylus — Knipper et al. 1997: pl. 1, figs 5, 6.

Occurrence. — Upper Triassic, Carnian to lower

Norian, worldwide in thc low palcolatirudes.

Genus Kamospongella

Kozur & Mostler, 1981

Type SPECIES. — Kamospongella bispinosa Kozur &

Mostler, 1981.

GEODIVERStTAS • 1999 * 21 (4)

553

Bragin N. Yu. & Krylov K. A.

KamospongelLi bispinosa

Kozur & Mostlcr, 1981

(Fig. 7G)

Spumellaria gcn. et sp. indet. - Kozur & Mostler

1979: pLil.fig. 2.

Kamoipüngeiiû bhpinosa Kozur & Mostler, 1981: 42,

pl. 50, fies 1,2.

Gombemlus bhpinosus (Kozur ôc Mostler) - Gorican

et Baser 1990. 146, pl. 1, Pig. 10. - Halamic et

Gorican 1995.' pl. 1. fig- 6.

Kamospongellii B-Yeh 1989: pl. 14, rig. 16.

Bemoullîtis (?) capricorrms — Bragin 1991b: 83, pl. 1,

figs 1-5.

OCCURRP.NCE. — Middle to Upper Triassic, Ladinian

to lower Norian, Tethys.

Remarks

This finding represents rhe highest present-day

known occurrence of Karnospongella bispinosa

Kozur & Mostler.

Family Ferresiidae Carter, 1993

Cçnua Ferrestum Blome, 1984

Type SPECIES. — Ferresium laseekense Blome, 1984.

Ferresium sp. aff. F. conclusum

Carter, 1993

(Fig. 8B)

aff. Ferresmm conclusum Carter, 1993: 68, pl. 9,

figs 1-5.

RE MARKS

This form differs from F conclusum Carter by

more strong torsion of main spines.

Family Patulibracchiidae

Pessagno, 1971

Genus Paronaella Pessagno, 1971

Type SPF.CIES. — Paronaella solanoensis Pessagno,

1971a.

Paronaella norica Kozur & Mock, 1981

(Fig. 8G, H)

Paronaella norica Kozur & Mock, 1981 in Kozur &

Mostler, 1981: 63, pl. 46, fig. 2.

Occurrence. — Upper Triassic, Norian, worldwide

in low paleolatitudcs.

Paronaella sp.

(Fig 81)

Description

Thrce-rayed spongy shell with short rays that

have bulboLis distal parts.

Remarks

Due to poor préservation this form is difFicult to

compare with other représentatives of genus

Paronaella.

Genus TriassocrucellaYsmxx, 1984

Type SPECIES. — Hagiastrum triassicum Kozur &

Mostler, 1978.

TriassocrucelUi triassica

(Kozur Mostler, 1978)

(Fig 8J)

Hagiastrum triassiam Kozur & Mostler, 1978: 144,

pl. 1, f'g- 4; pl. 2, fig. I I.

Crucella ninsstca (Kozur & Mostler) - l^hm 1984:

91, pl. 16. fig. 9.

Truissocrutrlla triassicum (Kozur & Mostler) - Kozur

1984: D.

Oc:cURRENCE. —Upper Trias.sic, Carnian to Norian,

European Tethys.

Superfamily Pyloniacka Haeckel, 1881

Family Orbiculiformioae Pessagno, 1973

Genus I^aeorbiculiformella

Kozur & Mostler, 1978

T\TE SPECIES. — Praeorbiculijhrmella plana Kozur &

Mostler, 1978,

Praeorbiculiformella goestlingetuis

Kozur & Mostler, 1978

(Fig. 8D)

Praeorbiculiformella goestlingensis Kozur &: Mostler,

1978: 164, pl. 1, figs 10, 13; pl. 4, fig. 3. - Lahm

1984: 93, pl. 17, fig. 2.

554

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 8. — A. Spongostylus tortilis Kozur & Mostler; B. Ferresium sp. aff. F. conclusum Carter; C, Pentaspongodiscus sp. 2;

D, Praeorbiculiformella goestUngensis Kozur & Mostler; E. Zhamojdasphaera proceruspinosa Lahn; F, Veghicyclia sp. cf. V. robusta

Kozur & Mostler; G, H. Paronaella norica Kozur & Mock; I, Paronaella sp.; J, Triassocrucella triassica (Kozur & Mostler). Scale bar:

A-H, J, 100 pm; I. 80 pm.

Occurrence. — Uppcr Triassic, Camian to lowcr

Norian, Europcan Teihys.

Supcrfamily Saturnalucea

D etlandre, 1953

Family SArURNAl lDAF Deflandre, 1953

Subfamüy Far.\SATURNAUNA£

Kozur &c Mosder, 1972

Genus Palaeosaturnalis Donofrio & Mosder, 1978

Type SPECIES. — Spongosaturnalis triassicus Kozur &

Mostler, 1972.

Palaeosaturnalis triassicus

(Kozur & Mostler, 1972)

(Fig. 9A, B, E)

Spongosaturnalis triassicus Kozur & Mostler, 1972: 40,

pl. 1, fig. 10; pl. 4, figs 1, 2. - De Wever et al. 1979:

81, pl. 2, fig. 2.

GEODIVERSITAS • 1999 • 21 (4)

555

Bragin N. Yu. & Krylov K. A.

Acanthocircus friassicus (Kozur & Mostler) - De

Wever 1982: 207, pL 13, fig. 10.

Palaeosatiirmlis triassicm (Kozur & Mostler) - Lahm

1984: 97, pl. 17,%. II.

Occurrence. — Upper Triassic, Carnian to lower

Norian, Tethys.

Palaeosaturnalis mocki

Kozur & Mostler, 1983

(Fig. 9G, H)

Palaeosaturnalis mocki Kozur & Mostler, 1983: 21,

pl. 5, %. 2.

Occurrence. — Upper Triassic, lower Norian,

Carpathians, Cyprus.

Palaeosaturnalis latiannulatus

Kozur & Mostler, 1983

(Fig. 9D)

Palaeosaturnalis latiannulatus Kozur & Mostler, 1983:

20, pl. 5, %. 1.

Occurrence. — Upper Triassic, lower Norian,

Carpathians, Cyprus.

Genus Liassosaturnalis

Kozur & Mostler, 1990

Type SPECIES. — Liassosaturnalis parvus Kozur &

Mostler, 1990.

Liassosaturnalis parvtis

Kozur & Mostler, 1990

(Fig. 9C)

Liassosaturnalis parvus Kozur & Mostler, 1990: 203,

pl. 4, figs 3,7, 12, pl. 6, fig. 6.

Occurrence. — Upper 3'rias.sic (Norian) to Lower

Jurassic (Hettangian) of the European l'ethys.

Genus Praemesosaturnalis

Kozur & Mostler, 1981

Type SPECIES. — Spongosaturnalis bifidus Kozur &

Mostler, 1972.

Praemesosaturnalis sp.

cf. P, multidentatus

(Kozur 6c Mostler, 1972)

(Fig. 9F)

cl. Spongosaturnalis multidentatus Kozur & Mostler,

1972:38. pl. 1. fig. 20.

Description

Ring with two pcripolar short main spines, with

numerous vcry small auxiliary spines, and with

eleven short outer rays. Main spines asynimetri-

cally arrangcd.

Re\urks

This form difFers from rypical P. multidentatus

(Kozur & Mostler) by the asymmetrical arrange¬

ment of main spines and by .shorrer outer rays.

Genus Veghuydia

Kozur & Mostler, 1972

Type SPECIES. — Veghicyclia pulchra Kozur &

Mostler, 1972.

Veghicyclia sp. cf. V, robusta

Kozur & Mostler, 1972

(Fig. 8F)

cf. Veghicyclia robusta Kozur & Mostler, 1972: 15,

pl. 3, %s I, 4, 7.

Rhmarks

This form has poorly preserved central part. It

possesses longer and thinner rays than typical

V. robusta.

SpumellARIINA incertae famÜiae

Genus Pentaspongodiscus

Kozur & Mostler, 1979

Type SPECIES. — Pentaspongodiscus tortilis Kozur &

Mostler, 1979.

Pentaspongodiscus sïi. 1

(Fig. 7H)

556

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 9. — A, B. E. Palaeosatumalis triassicus (Kozur & Mostler); C, Liassosaturnalis parvus Kozur & Mostler; D. Palaeosaturnalis

latiannulatus Kozur & Mostler; F. Praemesosaturnalis sp. cf. P. multidentatus (Kozur & Mostler); G, H, Palaeosatumalis mocki Kozur

& Mostler. Scale bar: 100 pm.

DeSCRIP'I'ION

Shell small, flartened, discoidal, with five main

spines. Spines short, thick, spindle-shaped, with

Y-shaped cross-section and strong dextral tor¬

sion.

Reniarks

This form differs from other représentatives of

genus Pentaspongodiscus Kozur & Mostler by the

spindle-shaped thick spines with strong torsion.

Pentaspongodiscîis sp. 2

(Fig. 8C)

Remarks

The illustrated specimen is uncomplete. It has

probably six very thin spines.

GEODIVERSITAS • 1999 • 21 (4)

557

Bragin N. Yu. &: Krylov K. A.

Order NASSELLARJA Ehrenberg, 1875

Family PoULPIDAE De Wever, 1981

Genus Potdpus De Wever, 1979

Type SPECIES. — Potdpuspiahyx De Wever, 1979.

Poulpus piabyx De Wever, 1979

(Fig. lOA-C)

Poulpus piabyx Wever, 1979: 98. pl. 7, figs 12, 13.

- Kozur & Mostler 1979; 89, pl. 4, fig. 3. - De

Wever 1982: 328, pl. 48, Ftg.s. 5, 6. — Yeh 1990: pl. 8,

figs 3, 7> 9. - Sugb'ama 1997: fig. 49 (15).

OcCURKfNCF.. — Triassic, upper Carnian to

lower Norian, worldwide H\ the |ow-paîçolaritudes.

Genus Neopylentonema Kozur, 1984

Type SPECIES. —• Neopylentonema mesotriassica Kozur,

1984.

Neopylentonema sp.

aff. N procera Sugiyama, 1997

(Fig. lOE)

? Poulpus (?) sp. C—Yeh 1989; 74, pl. 6, figs 5, 10.

aff. Neopylentonema procera Sugiyama, 1997: 161,

figs 46-3a, b.

Rkmarks

This forni has longer and thinner apical spine

and three feet chan typical N. procera. Il is more

similar ro Poulpus sp. C (Yeh 1989). Only a few

specimens were obtained, mosdy poorly preser-

ved.

Family ForemanELUDAE Dumitrica, 1982

Genus Foremanellina Dumitrica, 1982

Type species. — Foremanellina helenae Dumitrica,

1982.

Foremanellina (?) sp.

(Fig. lOJ)

Description

Small form with three-bladed apical horn and

three latéral horns, slightiy inclined downwards.

Remarks

This form has poor préservation and cannot be

determined on the species level.

Family PSEUOOSATURNIFORMIDAE

Kozur ôz Mosilcr, 1979

Genus l^seudosaturniforma

Kozur ÔZ Mostler, 1979

Type species. — Pseudosaiurniforma latimarginata

Kozur & Mostler, 1979.

Psetidosnturnifonna camica

Kozur & Mostler, 1979

(Fig. 101, K, L)

Pseudosaturniforma carnicu Kozur Mostler, 1979:

94, pl. 17, fig. 3; 1981: pl. 22, fig. 3.

Occurrence. — Upper Triassic, Carnian to lower

Norian of European l'ethys.

Family Ultranaporidae Pessagno, 1977

Genus TrialatusYA^ 1990

Type species. — TrialalusnwgacomutusYeh, 1990.

Trialatus robnstus

(Nakaseko & Nishimura, 1979)

(Fig. HA, B)

Napora robuita Nakaseko Nishimura, 1979: 78,

pl. 8, figs 4-6. - Yoshida 1986: pl. 7, figs 1, 6, 8. -

Bragin 1991a: 97, pl. 6, figs 2, 3.

Trialatus robtatus (Nakaseko & Nishimura) -

Sugiyama 1997': fig. 27 (16).

Occurrence. — Upper Triassic, upper Carnian to

lowxr Norian, Japan, eastern Russia and Cyprus.

Remarks

Specimens obraincd from Cyprus differ from

rypical by the présence of an addiüonal posrrho-

racic segment. This segment (abdomen?) has

sLibtrapezoidal outlinc and very thin laiiiced

Wall. Commun .specimens from Japan and cast-

ern Russia were obtained from cberts and did

not represent this element, probably due to the

préservation.

558

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 10. — A-C, Pouipus piabyx De Wever; D, H. Triassobipedis (?) sp.; E. Neopylentonema sp. aff. N. procera Sugiyama;

F. Napora (?) sp. 1; G. Napora (?) sp. 2; I, K. L. Pseudosaturniforma carnica Kozur & Mostler; J, Foremanellina (?) sp. Scale bar:

A. D-H, J, K, 100 pm: B, 35 pm: C, 80 pm; I. 50 pm; L, 20 pm.

Gémis Napora Pessâgno, 1977

Type SPECIES. — Napora bukryi Pessagno, 1977.

Napora (?) sp. 1

(Fig. 10F)

Description

Small subconical test with short thin three-bla-

ded apical horn and three long, straight three-

bladed feet. Very short and thin inclined vertical

horn can be seen at apical part.

Remarks

Only one specimen was obtained and illustrated.

Napora (?) sp. 2

(Fig. lOG)

Description

Small test with apical horn and three feet.

GEODIVERSITAS • 1999 • 21 (4)

559

Bragin N. Yu. & Krylov K. A.

Cephalis dome-shaped witli moderately long

slighdy inclined apical horn and small inclined

vertical horn. Thorax hcmisphericaU inflated,

with numerous small pores. Feet moderately

long, strongly flattened.

Remarks

Only one specimen of imperfect préservation

was found.

Family BueBOCVUI IDAK

Kozur &. Mostler, 1981

Genus Bulhocyrtium Kozur & Mostler, 1981

Type SPECIES. — Bulhocyrtium reticulatum Kozur &

Mostler, 1981.

Bulhocyrtium latum Braein n. sp.

(Fig. 111, J)

Bulhocyrtium alF reticulatum Kozur & Mostler -

Carter 1989: pl. 1, fig. 1.

Holotyph. — Fig. IIJ, GlN-4S58-23^ Cyprus, Agia

Varvara Village, Mamouia Complex, Upper Triassic,

lower Norian.

Etyiviology. — Latus (Latin), broad.

Occurrence. — Upper Triassic, lower Norian,

Cyprus.

Dimensions (based on tbree specimens). — Length

of test wiihout apical horn 260-320 pm, width of

cephali.s 165-175 pm, nuiximal width of test 280-

340 pm, length of apical horn 80 pm.

Description

Test with four chambers- Cephalis large, spheri-

cal with thin rhree-bladed apical horn. Cephalis

surface with network*like System of small nodes

connected by thm ridgcs ihat form polygonal

framework. Tores of cephalis small. subcircular,

irregularly arranged. ITorax subc^’lindrical, more

than twice shorter than cephalis. Abdomen sub-

cylindrical to subtxapezoidal. Tostabdominal seg¬

ment with expanded termination and wide open

aperture. 1 leight of ail postcephalic segments Icss

than of cephalis. Small strictures are developed

between cephalis, thorax and abdomen. Pores of

postcephalic segments small, subcircular, irregu-

larly arranged.

Remarks

Bulhocyrtium latum Bragin n. sp., differs from

B. reticulatum (Kozur & Mostler 1981: 106,

pl, 11, fig. 1) by larger cephalis with fincr net-

work-like surface and by wider last segment.

Family DEFI^ANDRECYKI IIDAE

Kozur Mostler, 1979

Genus Caphtorocyrtium Bragin n. gen.

Type SPECIES. — Caphtorocyrtium tenemm n. sp.

SpECIES INCEUDED. — Caphtorocyrtium tenerurn

Bragin n. sp.

HtymüLOGY. — Caphtorim-Biblic name; ancestor of

Cypriots.

Occurrence. — Upper Triassic, lower Norian,

Cyprus.

Description

Dicyrtid (or tricyrtid) form with small cephalis,

large, conical postcephalic part, with an apical

horn and three latéral horns.

RFJvURKS

Caphtoroiyrtiuvj n. gen. differs from Deflandrc'

cyrtium (Kozur &: Mostler, 1979: 98) by the pré¬

sence ül latéral horns. Genus Plauhpinoryrtis

(Kozur & Mostler, 1981: lll) has muhicyrtoid

test. Il is very diffieuh ro conclude how many

segments chls genus has (rwo or three). Due to

replacement by pyrite, rhe inner siructurc of api¬

cal part cannot be observed. Nevertheless, coni-

cai distal part of test has open aperture and

represents one segment (thorax or abdomen).

Caphtorocyrtium tenet'um Bragin n. sp.

(Fig. 1 IC'H)

lloLOlYPE. — Fig. IIP, CIN-4858-71, Chorus, Agia

Varvara Village. Manionia Complex, Upper Triassic,

lower Norian.

Etymology. — Tener (Latin), tender.

560

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 11. — A. B, Trialatus robustus (Nakaseko & Nishimura): C-H, Caphtorocyrtium tenerum Bragin n. gen.. n. sp.; F, holotype; I, J,

Bulbocyrtium latum Bragin n. sp.: J, holotype; K, Sethocapsa (?) sp. Scale bar: A, D-H, J, 100 pm; B. I, 80 pm; C, K, 35 pm.

Occurrence. — Upper Triassic, lower Norian,

Cyprus.

Dimensions (bascd on eleven specimens). — Length

of test including apical horn 290-335 pm» maximal

width of test 233-290 pm.

Description

Dicyrtid or tricyrtid form. Cephalis small, pore-

less, conical with long thin rod-like apical horn

and threc latcral horn.s a.s prolongations of D and

L (?). Latéral horns thin» Jong, rod-like, slightly

inclined distally. Postcephalic parc large, conical

to concavc-conical with 5-6 transversal rows of

subcircular to subrectangular pores, variable In

size. Widih ol postcephalic part rapîdly increa-

sing distally, aperture wide, open.

GËODIVERSITAS • 1999 • 21 (4)

561

Bragin N. Yu. & Krylov K. A.

Family NEOSCIADIOCAPSIDAE

Pessagno, 1969

Genus Haeckelicyrtium

Kozur & Mostler, 1979

Type SPECIES. — Haeckelicyrtium ausîriacum Kozur &

Mostler, 1979.

Remarks

Following Sugiy'3ma (1997) the tsvp-chambered

hat-like Triassk na^sellarians, which belong to

neither Deflandreiytttum Kozur ôz Mostler» 1979

nor Dreyericyrtium Kozur dc Mostler» 1979 and

bave no basal feet, are assigned to genus

Haeckelicyrtium Kozur & Mostler.

Haeckelicyrtium cartera^ Bragin n. sp.

‘(Fig. 12A-C, £. F)

Holotype. — Fig. 12A, GIN-4858-79, Cyprus, Agia

Varvara Village. Mairionia Complex, Upper Triassic,

lower Norian.

EtymOLüGY. — New species is named after Dr.

Elisabeth Carter in honour of her contributions to

Mesozoic Radiolaria.

Occurrence. — Upper Triassic, lower Norian,

Cyprus.

Dimensions (based on seven specimens). — Length

of test without apkai horn 190-235 pm, maximal

length of apical horn 400 pm (Fig. 12E), maximal

wicith of test 265-490 pm.

Description

Cephalis Mnall subconical with long thin rod-like

apical horn. Thorax large with hemispherical

inflated proximal part and with strongly expanded

distal part with a broad thoracic skiri. Ccphali.s

and thorax singlc-laycrcd with circular pores enlar-

ging distally and arranged into hexagonal (rarae-

work. Pores of thoracic sldrc large, subspherical.

Vélum not devcloped, aperture large, open.

Remarks

Haeckelicyrtium carterae Bragin n. sp. differs

from H. îeren Sugiyama, 1997 by inflated proxi¬

mal part of thorax, well-developed stricture bet-

ween thorax and thoracic skirt and by very long

and thin apical horn.

Genus Nabolella Petrushevskaya, 1981

Type species. — SquinaboUlla bngispinosa Kozur &

Mostler, 1979.

Re.marks

According to the original définition (Petru-

shevskaya 1981: 76) only rwo-chambered hat-

like forms with basal feet are assigned to this

genus.

Nabolella trispinosa Bragin n. sp.

(Fig. 12D, G-I)

Holoitpe. — Fig. 12G, H, GIN-4858-82, Cyprus,

Agia Varvara Village, Mamonia Complex, Upper

Triassic, lower Norian.

EIYMOLOGY. — By the presence of three basal feet.

Occurrence. — Upper Triassic, lower Norian,

Cyprus.

Dimensions (based on three specimens). — Length

of test without apical horn and basal feet 180-

200 pm, maximal width of test 290-300 pm, length

ol apical horn 100 pm.

DESC’RJPTION

Cephalis dome-like with long thin rod-like

slightly inclined apical horn and small indistinct

pores. Distinctive stricture i.s developed berween

cephalis and thorax. Thorax hat-like with infla¬

ted proximal part and wide skJrt-like distal part.

Wall of thorax .single, lauiced with subcircular

pores increasing distally. Médian part of thorax

with deep stricture. Three long rod-like spines

begin from cephalis and are partly incorporared

into thoracic wall. Their distal parts forra three

basal feet. Spines can be supposed as prolonga¬

tions of D and L. Vélum not developed.

Remarks

This species differs from Nabolella longispinosa

(Kozur Mostler, 1979) having only three basal

feet.

562

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 12. — A'C, E. F. Haeckelicyrtium carterae Bragin n. sp.: A, holotype; D, G-l, Nabotella trispinosa Bragin n. sp.; G, H, holotype.

Scale bar: 100 pm.

Family Syringocapsidae Foreman» 1973

Genus Syrmgocapsa Ncviani, 1900

Type SPECIHS. — Theosyringiurn rohusturn Vinassa,

1901.

Syringocapsa batodes De Wever, 1979

(Fig. 13L, M)

Syringocapsa hatodes De Wever, 1979: 91, pl. 6,

figs 10, 12. — Nakaseko &c Nishimura 1979: 81, pl, 8,

figs 9, 10. - De Wever 1982: 292, pl. 4l, figs 13, 14;

pl.42, fig. 0.

Syringocapsa ci', batodes De Wever — Yoshida 1986:

pl. 6, fig. 9, 10.

? unnamcd Podobursa-Yi^ic nassellarian - Pessagno et

ai 1979: pl. 4. fig.7-

OccUKRfiNCE. — Upper Triassic, uppcr Carnian to

lower Norian, worldwide in rhe low-palaeolatitude

régions.

GEODIVERSITAS • 1&99 • 21 (4)

563

Bragin N. Yu. & Krylov K. A.

Fig. 13. — A-C, I, Xiphotheca rugosa Bragin; D, Xiphoiheca sp.; E, G. Xiphotheca longa Kozur & Mock; F. Nassellaria gen. et sp.

indet.; H. Xiphotheca (?) sp.; J. K. Xiphotheca (?) spinellifera Bragin n. sp.; J. holotype; L. M, Syringocapsa batodes De Wever.

Scale bar; A, B, D-M, 100 pm; C, 35 pm.

Syringocapsa sp.

(Fig. 141)

Description

Test smalK with subconical apical part, subsphe-

rical, inflated rniddlc parc and distal part rhar

tends to bc tubular (incomplecely preservcd).

Apical part poreless, wiih tiny, vcry short apical

horn. Middle pan with numerous circular pores

in rectangular porc frames with sharp nodes at

vertices, with occasional short spines.

Remarks

This form cannot be compared or described as

new taxon due to uncomplete préservation.

Family PSEUDODICTYOMITRIDAE

Pessagno, 1977b

Genus Whalenella Kozur, 1984

Type SPECIES. — Dictyomitra arrecta Hinde, 1908.

564

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Fig. 14. — A, B, Whalenella robusta Bragin n. sp.; A, holotype; C, Annulotriassocampe sp. cf. A. sulovensis (Kozur & Mock);

D, Multimonilis pulcher'Yeh; E, G, Triassocampidae gen. et sp. indet.; F, J, Laxtorum (?) sp.; H, Whalenella sp. aff. W- perfecta

Blome; I, Syringocapsa sp. Scale bar: A-C, H-J, 35 pm; D-G, 100 pm.

Wljalenella sp.

aff. W. perfecta (Blome, 1984)

(Fig. 14H)

aff. Corum pefectum Blome, 1984: pl. 13, Figs 2, 7,

16; pl. 17, hg. 11.

Remarks

This form cliflFers from Whalenella perfecta (Blome)

by larger number of chambers (twelve vs seven).

Other external morphological features are very

similar. There arc discontinuous costae and single

row of small pores ar each postabdominal chamber.

Whalenella robusta Bragin n. sp.

(Fig. 14A, B)

Holotype. — Fig. 14A, GIN*4858'12, Cyprus, Agia

Varvara Village, Mamonia Complex, Upper Triassic,

lower Norian.

GEODIVERSITAS • 1999 • 21 (4)

565

Bragin N. Yu. & Krylov K. A.

EtymOLOGY. — RobustUvS (Latin), strong, stout.

Occurrence. — Uppcr Triassic, lower Norian,

Cyprus.

Dimensions (based on five specimens). — Length of

test 180-205 pm, maximal widrh of test 85-90 pm.

Description

Test multicyrtoid with 8-9 chambers. Cephalis

poreless, dome-shaped, without apical horn.

Thorax subrrapczoidal, smooth. Abdomen and

postabdominal chambers with we|l-developed

smooth discontinuons costae. Chambers of the

middle part of the test hâve 16-18 costae (8-

9 visible). Each chamber has single row of large,

deep, circulât to slighily elliptical pores. Height

of chambers incrcases very slowly. Width of

chambers increases to the fourth postabdomina)

chamber, rhen becomes constant or slighrly

decreasing.

Remarks

This species differs trom Whalenella speciosa

(Blome, 1984) by less inflated, smooth costae

that did not merge at final chambers, and by lar-

ger pores.

Genus MullimonilisYch. 1989

Type species. — Midtimonilispulcher Yoh, 1989.

Multimonilispulcher Ych, 1989

(Fig. 14D)

MultimonilispukherYçh.., 1989; 72, pi. 9, figs 9, 19.

Occurrence. — Uppet Triassic, upper Carnian-

lower to middle Norian of Oregon and Cyprus.

Family TriaSSOCAMPIDAE

Kozur & Mostler, 1981

Gcmxs Annulotriassocampe Kozur, 1994

Type species. — Annulotriassocampe baldii Kozur,

1994.

Annulotriassocampe sp.

cf. A. sulovensis (Kozur & Mock, 1981)

(Fig. 14C)

cf. Triassocampe sulovensis Kozur & Mock, in Kozur

& Mostler, 1981: 99, pl. 13, fig. 3. - Yeh 1989; 76,

pl. 2, fig. 13.

ReMAKK-S

Only a few poorly preserved specimens were

found.

Triassocampidae gen. ersp. indet.

(Fig. 14E, G)

Description

Test multicyrtoid, small. Cephalis dome-shaped,

with indistinct pores, with thîn apical horn. Test

has 5-6 segments, rhe lasc ones with transversal

rows of srnall pores. A fiai, leaf-like extension

begins from the proximal part of the apical horn

and surrounds test as widc ellipsoidal ring. Two

sides of ring form an angle (120°).

Remarks

Only a few imperfect specimens were found.

Family Sethocapsidae Haeckel, 1881

Genus Sethocapsa Hacckcl, 1881

Type species. — Sethocapsa cometa (Pantanelli, 1885).

Sethocapsa (?) sp.

(Fig. 11 K)

Descri RnoN

Test small. Cephali.s poreles.s, dome-shaped, tho¬

rax subtrapczoidal with few pores between seve-

ral longitudinal smooth ridges. Postabdominal

part of test inflated with spongy wall and five to

six (?) short basal feet. Aperture indistinct, might

be closed.

Rkmarks

This species is ver)’^ rare in studied material.

Nassellaria incertae familiae

Gtmxs Xiphotheca DcSf/cYtu 1979

Type species. — Xiphotheca karpenissionensis De

Wever, 1979.

566

GEODIVERSITAS • 1999 • 21 (4)

Early Norian Radiolaria from Cyprus

Xiphotheca rugosa Bragin, 1991

(Fig. 13A-C, I)

Xiphotheca rugosa Bragin, 1991a: 107, pl. 5. fig. 11,

13.

Occurrence. — Upper Triassic, upper Carnian to

iower Norian of eastern Russia and Cyprus.

Xiphotheca longa Kozur & Mock, 1981

(Fig. 13E, G)

Xiphotheca longa Kozur & Mock, in Kozur & Mostler,

1981: 113, pl.41,fig. 2.

Occurrence. — Upper Triassic, Iower Norian of

European Tethys.

Xiphotheca (?) spinellifera

Bragin n. sp.

(Fig. 13J, K)

Holotype. — Fig. 13J, GIN'4858-3, Cyprus, Agia

Varvara Village, Mamonia Complex, Upper Triassic,

Iower Norian.

Etymology. — Spinellifera (Latin), wearing small

spines.

Occurrence. — Upper Triassic, Iower Norian,

Cyprus.

Dimensions (based on three specimens). — Length

of test 700 pm, maximal width of abdomen 150-

180 pm, maximal width of the second postabdominal

chamber without équatorial spines 165-225 pm.

Description

Test large, very long, multicyrtoid. Cephalis

small, dome-like. Thorax small, hemispherical.

Cephalis and thorax without distinct pores.

Abdomen large, inllated, with equatorially arran-

ged thin .short spines. First postabdoniinal seg¬

ment iwice smallcr than abdomen, without

spines. Second postabdominal chamber larger

than abdomen, ïnflared, with equatorially arran-

ged spines thaï ,are longer and ihicker than spines

of abdomen. Three last postabdominal chambers

smaller than abdomen, nioderately inflated,

without équatorial spines, Last segment with

small spines around open, small, subcircular

aperture. AH postthoracic segments with small

subcircular pores in polygonal irregular pore

frames.

Remarks

Xiphotheca (?) spinellifera Bragin n. sp. differs

from other descrihed species oï Xiphotheca De

Wever bv the presence of équatorial spines and

by srrong inflation of the second postabdominal

segment, This form differs from représentatives

of Syringociipsa Neviani by weU-dcvclopcd seg¬

mentation of postabdominal part. The taxono¬

mie positions oï Xiphotheca (?) spinellifera Bragin

n. sp. is still unclear.

Xiphotheca sp.

(Fig. 13D)

Remarks

This form has strongly inflated first postabdomi¬

nal chamber. The tubular part of test begins

from the third postabdominal chamber.

Xiphotheca (?) sp.

(Fig. 13H)

Remarks

Only long fragments of tube without apical part

were found. Tube without segmentation, with

very small pores and thîn longitudinal curved

and bifurcated ridges is very characteristic and

unknown among other représentatives of

Xiphotheca De Wever.

Genus/.Æx/orww Blome, 1984

Type species. — Laxtomm hindei Blome, 1984.

Laxtorum (?) sp.

(Fig. 14F, J)

Description

Test multicyrtoid, spindle-shaped. Cephalis

small, dorne-shaped, poreless, .sinooth. Thorax

subtrapezoidal, poreles.s, smooth. Postthoracic

segments short, inflated, divided cach from other

by wcll-devcloped deep and narrow stricturcs.

Width of segments slowly increasing up to the

tenth segment and become decreasing at the dis¬

tal part of test. Each postthoracic segment has

GEODIVERSITAS • 1999 * 21 (4)

567

Bragin N. Yu. & Krylov K. A.

numerous small circulât pores. They form single

transversal row at strictures between segments.

Remarks

This form differs from other représentatives of

genus Laxtorum by absence of apical horn and

weak development of pores.

Genus Triassobipedis Koziir, 1984

Type SPECIES. — Triassobipedis halatonica Kozur,

1984.

Triassobipedis (?) sp.

(Fig. 10D,H)

Re,marks

These small forms hâve two basal fcet like repré¬

sentatives of généra Triassobipedis Kozur and

Bipedis De Wever. They hâve characteristic tubu-

lar distal part of test thar is sometimes longer

than basal fect. Both illustrated specimens hâve

imperfeci préservation. Characier of cephalic

structure and segmentation ol test are unclear.

Nassellaria gcn.. et sp. indet.

(Fig. Î3F)

Descripi’ION

Test multicyrtoid. Céphalothorax subconical,

smooth, without stricture between cephalis and

thorax, wirh apical horn and three latéral horns.

Ail horns short and .smooth. Abdomen inflatcd,

subspherical, divided from rhorax by deep stric¬

ture. Postabdominal part suhcylindrical. Abdo¬

men and postabdominal part wirh numerous

subcircular pores enclosed in hexagonal to penta¬

gonal pore frames.

Remarks

Only lew specimens were found. They did not

show affinity with any Triassic lorm described

before.

Acknowledgements

We are gratefui to Prof P. De Wever for valuable

advice at the beginning of this study. We thank

Dr. S. Gorican for many important comments

and improvement of manuscript. This work was

SLipported by Russian Science Foundation, grant

97-05-64646.

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Submitted for publication on 24 Febmary 1998;

accepted on 1 December 1998.

GEODIVERSiTAS • 1999 • 21 (4)

569

Cuboctostylus n. gen., a new Late Cretaceous

spicule-bearing spumellarian Radiolaria from

Southern Sakhalin (Russia)

Lubov G. BRAGINA

Geological Institute of Russian Academy of Sciences,

Pyzhevsky 7, Moscow, 109017 (Russia)

bragin@ginran.msk.su

Bragina L. G. 1999. — Cuboctostylus n, gen., a new Late Cretaceous spicule-bearing spu¬

mellarian Radiolaria from Southern Sakhalin (Russia), in De Wever P. & Caulet J.-P. (eds),

InterRad VIII, Paris/Bierville 8-13 septembre 1997, Geodiversitas 2^ (4) : 571-580.

KEYWORDS

Radiolaria,

Entactinaria,

systematics,

new raxa,

Upper Cretaceous,

Sakhalin,

spiculé.

ABSTRACT

A new spicule-bearing gcnus of Spumellaria (Radiolaria) Cuboctostylus, and

three new species — Cuboctostylus kasinzovae, C. sakhalinensis, and C trifurca-

tus, are described from the Late Cretaceous deposits of Sakhalin (Russia).

This genus bas many characters in common wich the Lower-Middle

Cretaceous genus Pyloctostylus Dumitrica, from which it differs essentially in

having no pylome and the spiculé centrally placed. The genus has aiso some

characters in common with the Paleozoîc family Polyentactiniidae and the

Cenozoic family Orosphaeridae.

MOTS CLÉS

Radiolaria,

Entactinaria,

systématique,

nouveaux taxons,

Crétacé supérieur,

.Sakhaline,

spiculé.

RÉSUMÉ

Cuboctostylus n. gen., genre nouveau de spumellaires à spiculé mitial du

Crétacé supérieur, Sakhaline du Sud (Russie).

Le nouveau genre de spumellaires (radiolaires) Cuboctostylus et trois nou¬

velles espèces — C kasinzovae, C. sakhalinensis, C. trifiircatus sont décrit dans

les sédiments du Crétacé supérieur, Sakhaline du Sud, Russie. Ce taxon nou¬

veau est très proche du genre Pyloctostylus Dumitrica du Crétacé inférieur-

moyen, mais il en diffère principalement par l’absence du pylome et par la

localisation du spiculé dans la zone centrale. Le genre rappelle aussi les repré¬

sentants de la famille paléozoïque Polyentactiniidae et de la famille céno-

zoïque Orosphaeridae.

GEODIVERSITAS • 1999 • 21 (4)

571

Bragina L. G.

INTRODUCTION

The spicule-bearing Spumellaria are common in

the Palcozoic (Forcman 1963; Nazarov 1975,

1988; Isakova & Nazarov 1986) and Triassic

(Dumitrica 1978; Duminica et al. 1980; Kozur

& Moscler 1981, 1982, 1994). They are well-

known among che Cenozoic and Recenr faunas

(Hollande &: Enjumct I960; Friend &: Riedel

1967). On rhe conrrary, only few 5uch taxa werc

illustraied and described Irom the Jura-s.sic and

Cretaceous (Dumiirica 1994; Yeh 1995). During

rhe posi'Triassic cime some spicule-bearing

Spumellaria survived wich a low frequency. These

large-sized Radiolaria can be recognized only in

the case of good préservation of initial structures.

Frequent spicule-bearing forms were found in

the Upper Creraceous radiolarian assemblages of

the Southern SakhalLn. These forms hâve mor-

phological affinities wiili the Early-Middlc

Cretaceous genus Pylovtosiylus Dumitrica, 1994

and may be descendants of this taxon. The géné¬

ra Pyloctostyhis Dumitrica and (Ziiboctostylus

n. gen. hâve large eight-rayed spiculé with long

primary spincs showing morphological atfinity

with the Palcozoic Encactînaria. Many Triassic

spumellarians havc small spiculé without connec¬

tions with primary spincs (likc généra

Pseîidostylosphaera Kozur ôc Moscler, 1981,

Sepsagan Dumitrica, Kozur & Mostler, 1980)

and cannot be ancestors of the Cretaceous taxa

described herein.

GEOLOGICAL SETTING

The Upper Cretaceous key-section of the South¬

ern Sakhalin is located in the middle flow of

Naiba River (Matsumoto 1938, 1954;

Verecshagin et al. 1987) (Fig. 1). This section is

represented by thin- and coarse-grained clastics

with carbonate (calcilutite) concrétions contai-

ning abundant amnionites, inoceramids and

foraminifer.s. Several stratigraphie levels in the

intervaJ from die y\lbian to Campanian are cha-

racterized by bearing radiolarians (Kasinzova

1979, 1981; Verecshagin et al. 1987; Zonova et

ai 1993).

The Cenomanian, Turonian and Coniacian

doposits of the Naiba Section wcrc scudied and

sampled by rhe author in 1992. Several radiola¬

rian a-ssemblages with spicule-bearing radiola¬

rians wcrc found, This parc of section can be

seen in outerops at Shadrinka River and

Naidcnov Creek (wesr rributaries of Naiba River)

(Fig. 1). The upper part of Cenomanian deposits

is represented by the Naibinskaya Formation

(Unies 3, 4, 5) and Bykovskaya Formation

(Units 1, 2). The Turonian is represented by che

Bykovskaya Formation (Units 3, 4, 5 and the

lower part of Unit 6), and the Coniacian is repre¬

sented by the Bykovskaya Formation (upper part

of Unit 6 and Unit 7).

Naiba Sbci ion (Fig. l)

Naibviskaya Formation (upper part)

Unît 3. Greenish'gre}^ massive medium-grained

sandstones with inrercalarions of grey silrstones.

The ihickness of this unit is 250-300 m.

Unit 4. (Inoceramiis tychljnwajamemis zone,

lower Cenomanian-lüwer part ol middle

Cenomanian). Dark-grey massive mudstones and

siltstones wjth small carbonate concrétions with

Inocerarnus lychljawajamemfs Vcreschagin, 1967,

/. concentricus nipponims Nagao & Matsumoto,

1939, Anagatidryccrus buddha (Forbes, 1846).

The thickness of this unit is 300-450 m.

Unit 5. {bioceramus pennatulia-L gradtlis zone,

middle Cenomanian). Grey fine- to medium-

grained sandstones and grey siltstones with rare

carbonate ctmcretions and beds ot gravelires.

This iticmhcf is characterized by tnaeetamin pen-

mttulu> Pergameju, 1966, I. gradilh IVrgament,

1966, / pressul-u^ Zonova, 1980. Radiolarians are

rcprc-senccd by Cromyomma (.^) nodosa IVs-sagno,

1976, llex'dpyrurtih puntanellii Squiiubol, 1903b,

Orhiiuliformd maxima Pessagno, 1976,

Amphipyndax stvcki (Campbell & Clark, 1944),

A. ellipticus Nakaseko & Nishimura, 1981,

Diityomitra multicostata Zictel, 1876,

Ciihoctostylus sakhalinensis n. sp., C. kasinzovae

n. sp. rhe thickness of this unit is 100*150 m.

Bykotfskaya Formation (lower and middle parts)

Unit 1. (Upper Cenomanian). Alternation of

lighr-grcy fine-grained sandstones, dark-grey

siltstones and black mudstones wich abundant

shell détritus of inoceramids and numerous car-

572

GEODIVERSITAS • 1999 • 21 (4)

Cuboctostylus n. gen., a new spumellarian Radiolaria from Southern Sakhalin (Russia)

Fig. 1 . — The Upper Cretaceous section at Naiba River (Southern Sakhalin). A. stratigraphie column; B, géographie position; C. geo-

logical map of the middie flow of Naiba River; K 2 cm, Cenomanian; Kjt. Turonian; KjCn. Conîaeian; nb. Naibinskaya Formation; nb3,

third unit; nb4. fourth unit; nbS, fifth unit; bk. Bykovskaya Formation: bk1. first unit; bk2, second unit; bk3. third unit; bk4, tourth unit;

bkS. fifth unit; bk6. sixth unit; bk7, seventh unit.

bonate concrétions with ïnoccramus nippanicm

Nagao & Matsumoto, 1939, L sp. aff. /. tennis

Mantell, 1822, Gaudryceras varagnrense Kossmat,

1895 and radiolarians; Cromyomma (?) nodosa

Pessagno, 1976, CycUtstrurn satoi (Tumanda,

1989)» Dnmitricam maxweHemis Vessa^no, 1976,

Qiiadriga.strum instilsum O'Doghercv, 1994,

Savaryella ^ttadra (Foreman, 1978a),

Phaseliforvta .sp. ex gr. P. taxa Pessagno, 1972,

P suhearinata Pessagno, 1972, Cornu tel la sp.,

Paronâella sp., Stylvdruppa sp., Amphipyndax

Nalcaseko & Nishimura, 1981, À stocki

(Campbell & Clark, 1944), Archaeodictyomitra

squinaboli Pessagno. 1976, Cassideus yoloetisis

Pessagno, 1969, Neosciadiocapsa jenkinsi

Pessagno, 1975, Saturniforma abastrum Pessagno,

1970. Cuboctostylus kasinzovae w. sp., C. sakhali-

nensis n. sp., C. trifarcatus n. sp. The thickness of

this unit is 140-190 m.

Unit 2. (Upper Cenomanian). Dark-grey and

grey siltsione.s with large carbonate concrétions

with Inoceramus sp. atf /. tenuls Mantell and a

radiolarian assemblage siniilar to that in

Member 1 The thickness of this unit is 70-

150 m.

Unit 3, (Lower Turonian). Alternarion ot greeni-

sh-grey medium-grained .sandstonc.s and dark-

grey silcsrones with Inoceramus sp. aff. l. ternds

Mantell. The thickness of this unit is 60 m.

Unît 4. (Turonian). Dark-grey and black silr-

scones and mudstones with large carbonate

concrétions with Mytiloides sp. aff. M. labiatus

GEODiVERSiTAS • 1999 • 21 (4)

573

Bragina L. G.

(Schlotheim, 1813). The thickiiess of this unit is

450 m.

Unit 5. {Inoceramm hobetseiisis zone, middie part

ofTuronian). Grey siltstones with large carbona¬

te concrétions with Nippojiites mirabilis

Matsunioto, 1954, Inoceramus bobetsensis Nagao

èc Matsumoto, 1939. The thickness of this unit

is 180-200 m.

Unit 6. (hwceranms teshioensis zone, upper part

of upper Turonian-lowcr Coniaciaii). Dark-grey

siltsrones and mudstones with carbonate concré¬

tions coniaining inoc(^ramus ttshioensis Nagao &

Matsumoiov 1939» Gaudryceras dcnseplicatum

(Jimbo,. 1894) and radiolarians: Archaeospongo-

prunum cortinaensis Pcssagno, 1971b, Crucella

sp. ex gr. C plana Pessagno. 1971a, Histiasîntm

sp. ex gr. H. aster Lipnian, 1952, H. latum

Lipman, 1952» Orhiculiforrna monticelloensis

Pessagno» 1971b, PatelluUt minusculn

O’Doghercy» 1994, Patulibracchium sp. aff

P. arbucklemis Pessagno, 1971a, Phaseltfortna sp.

ex gr. P. carinata Pessagno, 1972, Spongotripus

ctfwwww/x Squinaboh 1903b, Vitoffits brustolrnsis

(Squinabol, 1903b), A'fultastrum sp.* Afens

liriodes RiedeJ bc Sanfilippo, 1974, Dictyodedalus

sp. aff D. acutii'epbalus (Squinabol. 19Û4),9L/Vwr

sp. ex gr. X. anielopensis Pessagno, 1977c, X. spi-

cularim (Aliev, 1965). Cuhoctostylus kasinzovae

n. sp., C sakbalinensis n. sp. The thickness of

this unit Ls 500-600 m.

Unit 7. Dark-grey siltstone.s and niudstones. The

thickness of this unit is 100-150 m.

SYSTEMATICS

Class RADIOLARIA Muller, 1858

Order POLYCYSTINA Ehrenberg, 1838

Suborder ENTACTINARIA

Koztir & Mostler, 1982

? Family POLYENTACriNIIDAF Nazarov, 1975

Genus Cuhoctostylus n. gen.

Type species. — Cuhoctostylus kasinzovae n. sp.

Species INCLUDED. — Cuhoctostylus kasinzovae n. sp.,

C. sakbalinensis n. sp., C. trifiircatus n. sp.

Fig. 2. — Cuboctostyius kasinzovae n. sp., suggested recons¬

truction. Scale bar: 200 pm.

EiymolOGY. — From the Greek cubo — ciibic, octo ~

cight, stylos — .spike, style.

OCCLIRFNCE, — Cenomanian to Campanian so far as

icnown.

Description

Skcleton large, with initial spiculc in the center,

and two or three conceniric Systems ot cubic

anrhe.s, the outermost wiih a subspherical latticed

shell which may be mi.ssing. Spiculé with a very

short médian bar and four spines at each end.

Spincs not dilferentiated into apical or basal.

Thcy rcsult Irom successive bifurcation in hori¬

zontal and vertical planes. Spires cylindrical in

the portion between MB and che innerrno.st Sys¬

tem of arches. Thcy rapidly increase in width

and become three-bladed outside cortical shell.

Spines with two or three verricils ol straight bars

that unité rhe spines ut two or three levels for-

ming weakly developed cube-like shclls. Spines

aJigued with the diagonal ot the cubc-likc shells.

Remarks

Cuhoctostylus n. gcn. differs from the Early to

Middie Cretaccous genus Pyloctostylus Dumitrica

hy the central position of spiculc and absence of

pylome.

The gênera Pyloctostylus Dumitrica and Cubocto-

Stylus n. gen. undoubtedly belong to the same

574

GEODIVERSITAS • 1999 • 21 (4)

Cuboctostylus n. gen., a new spumellarian Radiolaria from Southern Sakhaiin (Russia)

Fig. 3. — Cuboctostylus sakhalinensis n. sp., suggested recons¬

truction. Scale bar: 200 pm.

phylogenetic lineagc, Since Cuboctostylus n. gcn.

lias no pylome it is morphologically doser to the

Paleozoic genus Po/yentacunia Foreman

(Foreman 1963). Finding of this new genus

shows thac the spicule-bearing SpumelUria arc

much more frequent in rhe Creraceoits than was

previously supposed. Dumitrica (1994) mentio-

ned that there are many other spicule-bearing

forms in the Cretaceous which are to be descri-

bed.

Two Cretaceous spumellarian species — Falso-

cromyodrymus ? frtigosus O’Dogherty, 1994 and

F. ? nehulostis O’Doghcrty, 1994 hâve some affi-

nity with Cuboctostylus n. gen. (O Dogherty

1994). Unfortunatcly, there is no évidence of

their initial spiculc and these taxa cannoc be assi-

gned now co the new genus.

Cuboctostylus kasinzovae n. sp.

(Figs 2, 5A-G, 6D, 7D-F, H)

Hoi.OTYPE. — GIN 4845-1. Fig. 5B, .Southern

Sakhaiin, Naiba River, N.iibinskaya Formation, midd-

le Cenomanian.

EtytvIOI.OGY. — rhe species is dedicated in honour of

l.udmila I. Kasinzova, who discovered the Cretaceous

Radiolaria of the Naiba sequence (south-western

Sakhaiin) and publishcd their rirst descriptions.

Fig. 4. — Cuboctostylus trifurcatus n. sp., suggested reconstruc¬

tion. Scale bar; 200 pm.

Occurrence. — Middle Cenomanian to Conîaeian

.a.s bit as known.

Dimensions. — Length of the outer cube-like shell

side 480-500 pm, length of the inner cube-like shell

side 200-250 pm, total length of spine 900-1000 pm.

Drscripi'ion

Shell âs with genus. Very short median bar with

eight spines is pJaced in rhe central part of the

shell. Robust outer shell and a single inner shell

form two conccntric cubc.s. Lcngdt of bars of the

inner shell approxiniatdy hall than of the outer

shell. Spines cylindrical in the portion beween

MB and tuner shdl, beyond ît tlirec-bladed and

increasing in thickness up to the outer shell.

Each bar of the inner cube-like shell bas one

crestenr-like apophyse at the corner. These apo¬

physes form weakly developed .seeondary .s[)heri-

cal level over inner shell. Each bar of the outer

cube-like shell bas two opposite apophyses in the

middle and few short secondary spines.

Remarks

This species differs from the species C. trifurcatus

n. sp. by the absence of trifurcations of the distal

GEODIVERSITAS • 1999 • 21 (4)

575

Bragina L. G.

Fig. 5. — A-G, Cuboctostylus kasinzovae n. sp.; B, holotype, GIN 4845-1; C, D, two foreshorîening on internai part of Shell;

E, F, fragments of Shell; G, part of B. Scale bar: A-D, 130 pm; E, F, 200 pm; C, 300 pm.

576

GEODIVERSITAS • 1999 • 21 (4)

Cuboctostylus n. gen., a new spumellarian Radiolaria from Southern Sakhalin (Russia)

Fig. 6. — A, C. Cuboctostylus trifurcaîus n. sp., spines; B. E. Cuboctostylus trifurcatus n. sp., holotype, GIN 4845-3; B, external view

of Shell; E. internai view of Shell; both two fragments belong to one specimen; D, Cuboctostylus kasinzovae n. sp., main spine;

F. G. Cuboctostylus trifurcatus n. sp., uncomplete shell; H, Cuboctostylus trifurcatus n. sp. Scale bar: A-E, 130 pm; F-H, 200 pm.

GEODIVERSITAS • 1999 • 21 (4)

577

Bragina L. G.

Fig. 7. — A, Cuboctostylus sakhalinensis n. sp., holotype. GIN 4845-2; B. C, Cuboctostylus sakhalinensis n. sp., uncomplele Shell;

D, E. Cuboctostylus kasinzovae n. sp., two fragments of one Shell; F. Cuboctostylus kasinzovae n. sp., internai cube-like Shell with

developed apophyses; G, Cuboctostylus sakhalinensis n. sp.; H, Cuboctostylus kasinzovae n. sp., fragment of shell. Scale bar:

A-C, G, 200 pm; D-F, H. 130 pm.

578

GEODIVERSITAS • 1999 • 21 (4)

Cuboctostylus n. gen.. a new spumellarian Radiolaria from Southern Sakhalin (Russia)

part of its main spines and from the species

C. sakhalinensis n. sp. by the presence of apo¬

physes at the outer and inner shells.

Cuboctostylus sakhalinensis n. sp.

(Figs 3, 7A-C. G)

HolotypE. — GIN 4S45-2. Fig. 7A, Southern

Sakhalin, Naiba River, Bykovskaya Formation, upper

Cenomanian.

EtymoloGY. — From Sakhalin, eastern Russia.

Occurrence. — Cenomanian to Campanian as far

as known.

Dimensions. — Length of the outer cube-like shcll

side 300-330 pm, lengrh of the inner cube-like shell

side 90-100 pm, total It'rigth of spine.s 600-800 pm.

Description

Large shell as wiih genus. Spines vcry long,

simple. The outer and inner .shells consist of the

horizontal and vertical bars forming the edges of

cube. Bars of the outer cube-like shell twice as

long as those of chc inner shell. Secondary spines

or apophyses on thèse bars absent.

Remarks

d’his specics differs from C kasinzovae n. sp. by

having more délicate shells without secondary

spines or apophyses. C sakhalinensis n. sp. is cha-

racterized by a more exact gcometrîcal form than

the other représentatives of Cuboctostylus n. gen.

Cuboctostylus trifiircatus n. sp.

(Figs 4, 6A-C, E-H)

Holotype. — GIN 4845-3, Fig. 6B, E, Southern

Sakhalin, Naiba River, Bykovskaya Formation, upper

Cenomanian.

EtymüLOCîY. — From the Latin tri — Û\xcty furcatus —

flircate.

Occurrence. — Middle to upper Cenomanian so

far as known.

Dimensions. — Length of sidc*s ofthe outer cube-like

shell 300-350 pm, length of sides of the inner cube-

like shell 80-100 pm, total length of spines 800-

900 pm.

Dem:ription

Shell -sub.sphericaJ with eight ver)^ long trifurcate

spines. Spiculé wdth very short médian bar is

siruaied in the central part of the shell. Spines

cylindrical in the position between MB and

inner cube-like shelL They become three-bladed

in the portion between inner and outer cube-like

shells and rapidiy increa.se in widih. Oulside the

outer tube-like shell spines hâve a constant

width, They hâve deep and narrow grooves and

thick rounded ridges. Each spine divides into

three rerminations with same trcloil-likc cross-

section. Outer cube-like shell bars hâve nume-

rou.s apophyses forming base of a latticed

subspherical shell.

Re.marks

This species differs from C. sakhalinensis n. sp.

and C kasinzovae n. sp. by the trifurcation of

spines, trefoil-like cross-section of chc distal por¬

tions of main spines and by the presence of a lat¬

ticed outer subspherical shcll.

Acknowledgements

I woiild like to thank P. De Wever who gave

valuable recommendations in the early beginning

of this work. The manuscripi has been conside-

rably improved by the critical reading of

P. Dumirrica, E. Urquhart, and A. Ohler. This

work M'as suppocted by the Russian Science

Foundation (Grant 97-05-64646).

REFERENCES

Dumitrica P. 1978. — Family Eptingiidae n. fam.

extinct Nassdlaria (Radiolaria) with sagital ring.

Dari lie Seama alv ^e/iintehr, Institutul de Géologie si

Geafizica-Paleontologie 54 (3): 27-38.

— 1994. — Pyloitostylus n. gen., a Crctaceous

Spumellarian RaJiolarian genus with initial spiculé.

Revue de murofyaleomology 57 (4) : 235-244.

Dumitrica P., Kozur H. &c Mosrler H. 1980. —

C-tmtribution to the radiolarian taiina of rhe Middle

l'riassic of the Southern Alps; Geologisbe-

Pakionwlogishe Afirteiltmgen,\nx\shï\xcV 10(1): 1-46.

Foreman H. 1963- — Upper Devonian Radiolaria

from the Fluron Member of the Ohio shale-.

Mlcropakonioloyy 9 (3): 267-304.

Friend J. K. & Riedel W. R. 1967. — Cenozoic oro-

sphaerid radiolarians from tropical Pacific sédi¬

ments. Micropaleontology 13 (2): 217-232.

GEODIVERSITAS • 1999 • 21 (4)

579

Bragina L. G.

Hollande A. & Enjumec M. 1960. — Cytologie, évo¬

lution et systématique des Sphaeroides (Radio¬

laires). Archives du Muséum national d'Histoire

naturelle, Paris, série 7, 7 : 1-134.

Isakova T. N. & Nazarov B. B. 1986. — Late

Carboniferous-Early Permian stratigraphy and

microfauna oF Southern Urals. Transactions of

Geological Institute, Academy of Sciences SSSR,

Moscow, 402, 184 p.

Kasinzova L. I. 1979. — Campanian Radiolaria of the

Western Sakhalin mountains: 93-100 [in Russian],

in Zharaojda A. I. (ed.), Fossil and recent Radio¬

laria, Zoological Institute, Academy of Sciences

SSSR, Leningrad.

— 1981. — Cenomanian Radiolaria of the Western-

Sakhalin mountains: 88-91 [in Russian], in

Zhamojda A. I. (ed.), Systematicsy évolution and

stratigraphie importance of Radiolaria. Nauka,

Moscow.

Kozur H. & Mostler H. 1981. — Beitrage zur

Erforschung der mcsozoischcn Radiolarien. Teil.

IV: Thalassosphaeracca Hacckel, 1862, Hexa-

stylacea Haeckel, 1882, cmend. Petrushevskaya,

1979, Sponguracca Hacckel, 1862 emend. und

weiterc triassischc Lithocycliacea, Trematodiscacea,

Actinommacea und Nassellaria; Geologishe-

Palàontologishe Mitteilungen, Innsbruck, Sonder-

band 1: 208.

— 1982. — Entactinaria subordo nov., a new radiola-

rian suborder. Geologishe-Paliiontologishe Mittei¬

lungen, Insbruck 11/12: 399-414.

— 1994. — Anisian to middlc Carnian radiolarian

zonation and description of some stratigraphically

important radiolarians, Geologishe-Palaofîtologishe

Mitteilungen, Insbruck, Sonderpand 3: 39-255.

Matsumoto T. 1938. — Zelandites, a genus of

Cretaceous ammonites. Japanese Jourtial of Geology

and Geography 15 (3-4): 137-148.

— 1954. — Selected Cretaceous leading Ammonites

in Hokkaido and Saghalien: 243-324, in The

Cretaceous System in the Japanese Islands. Japan

Society Prom. Sciences, Tokyo.

Nazarov B. B. 1975. — Lower and Middle Paleozoic

radiolarians of Kazakhstan (research methods, sys-

tematics, stratigraphie importance). Transactions of

Geological Institute, Academy of Scietîces SSSR,

Moscow, 275, 204 p. [in Russianj.

— 1988. —Paleozoic Radiolaria, in Practical tnanual

of microfauna of the USSR. Volume 2. Nedra,

Leningrad, 232 p. [in Russian],

O’Dogherty L. 1994. — Biochronology and

Palconiology of Mid-Cretaceous Radiolarians from

Northern Âpennines [Italy and Betic Cordillera

(Spain)]. Mémoires de Géologie, Lausanne 21 :

1-415.

Vereeshagin V. N., Budrin V. S., Zonova T. D. et al.

1987. — The Cretaceous key-section of Sakhalin,

(Naiba section), Poyarkova Z. N. (ed.). Nauka,

Leningrad, 194 p. [in Rassian).

Yeh K. Y. 1995. — Feriestrula n. gen., Lower Jurassic

internai spicule-bearing spherical radiolarians from

Easr-Ccntral Oregon. Bulletin of the national

Muséum of natural Science, Taiwan 6; 91-105.

Zonova T. D, Kasinzova L. I. ôz Yazykova E. A.

1993. — Atlas of the Cretaceous key-fossils of

Sakhalin. Nedra, Sankt-Peterburg, 326 p.

Submitted for publication on 24 Fehruary 1998;

accepted on Î8 September 1998.

580

GEODIVERSITAS • 1999 • 21 (4)

A Middie Devonian radiolarian fauna from the

Chotec Limestone (Eifelian) of the Prague Basin

(Barrandian, Czech Republic)

Andréas BRAUN

Institute of Paleontology, University of Bonn,

Nussallee 8, 53115 Bonn (Germany)

pal-inst@ uni-bonn.de

Petr BUDIL

Cesky geologicky ustav,

Klarov 3, 118 21 Praha 1 (Czech Republic)

budil@cgu.cz

Braun A. & Budil P. 1999. — A Middie Devonian radiolarian fauna from the Chotec

Limestone (Eifelian) of the Prague Basin (Barrandian, Czech Republic), in De Wever P. &

Caulet J.-P. (eds), InterRad Vlll, Paris/Bierville 8-13 septembre 1997, Geodiversitas 2^ (4) :

581-592.

KEYWORDS

Radiolarians,

Middie Devonian,

upper Eifelian,

Barrandian,

Chotec Limestone,

Kacak evenr.

ABSTRACT

The occurrence of radiolarian faunas in the upper part of the Chotec

Limestone is discussed in terms of fâunal composition, systemarics and geo-

logical implications. The most common entaednid species arc treated syste-

marically. The occurrence of radiolarians in large numbers in the rock

succession began approximatcly 2 meters below chc onser of rhe black shale

sédimentation (Kacak Member). The abrupt sedimentological change, corn-

monly viewed as an event therefore does not coincide with the faunal turno¬

ver, leading to a radiolarian dominance well before the onset of black shale

déposition.

MOTS CLÉS

Radiolaires,

Dévonien moyen,

Eifelien supérieur,

Barrandien,

Calcaire de Chotec,

Kacak Formation.

RÉSUMÉ

Une faune de radiolaires du Calcaire De Chotec (Devonien moyen, Eifelien

supérieur) du bassin de Pra^e (Barrandien, République tchèque).

La présence de faunes de radiolaires dans la partie supérieure du Calcaire de

Chotec est discutée en tenant compte de la composition faunique, de la sys¬

tématique et des implicadons géologiques. Les espèces d’entaednés les plus

communes sont traitées systématiquement. Les radiolaires sont présents en

grand nombre dans la .succe.ssion sédimentaire environ 2 mètres au-de.ssous

des premiers schistes noirs (Kacak Formation). Le brusque changement de

sédimentation ne correspond donc pas comme habituellement à un change¬

ment faunique, comme l’indique cette dominance des radiolaires bien avant

le début de Faccumuladon des schistes noirs.

GEODIVERSITAS • 1999 • 21 (4)

581

Braun A. & Budil P.

INTRODUCTION

The Paleozoic area around Prague is a famous

and classical région for many investigations in

paleoiitology and biostratigraphy. The occurren¬

ce of radiolatians in certain rocks cspecially of

Silurian âge has been commonly mentioned

(Rodic 1925; Prantl 1949) and some very detai-

lcd pétrographie studies hâve been carried out

(Rodic 1931). Although typical radiolarian rocks

(radiülarian chens, Jydites) are not very common

especially in ihc Devonian sequence it has been

known for some décades, ihar some lirhologies

may bear radiolarian skeletons in significant

amounts (Fabian 1933). The fiict,. rhar some of

the sedimeiuary rocks in the Baudndian area

bear well preserved radiolatians, is not well

known. although in cases whcre préservation is

good such occurrences might be of spécial

importance for our knowledge of stratigraphy

and development of radiolarian faunas during

the Silurian and Devonian. The fauna that is

figured and partly described in this paper has

been considered in rwo earlier papers (Cejehan

1987; Budil 1995). The présent paper intends to

supply some addional information, observations

and a sy.stematic treatment of the common

entactinid species in these faunas. The spécial

lithologie framework in which these faunas occur

may be woith noting in the context of the “bioe-

vent character” of the Kacak .sequence (and the

“otomari-event", cf.Walliser 1984), immediately

overlying the source rocks of our faunas.

CZECH REPUBLIC

Fig. 1. — Distribution of the Kacak Member (in black) In the

Barrandian area and géographie situation of the discussed loca-

Hties.

dings of radiolarian faunas corne from rocks 4 m

below the Kacak sequence (Budil 1995)^

2. Knezi hora liill near Karlstejn. This localtty,

although offering a good sequence through the

uppermost Chotec Limestone and the base of the

Kacak Member in its typical development, liad

noi been studied in detail unril quire recently

(Budil 1995: 4-8). Radiolatians are even better

preserved here ihan those from the Hlupocepy

railway eut, Our sainpie cornes from two limes¬

tone beds approx. 2 m resp. 1 m below the

Kacak base (beds -10/-12 and -20).

LOCALITIES (cf. Figs 1,2)

Radiolarian bearing rock samples corne from two

localities situaied near Prague:

1. Railway eut in Praha 5-Hlupocepy. This expo-

sure has been figured and described several times

(e.g., in Budil 1995: 2-4; Chlupac 1960, 1993).

It exposes a sucession Irom the highec part of the

Chotec Limestone until ihe Roblin beds, over¬

lying the Kacak Member. The Radiolatians hâve

been extracted from a 15 cm thick bed of Chotec

Limestone 50 cm below the base of the predomi-

nantly black siliceous Kacak sequence. Rare fin-

LITHOLOGY

The radiolarians corne from the uppermost part

of the Chotec Limestone (biomicritic limcstones

with intercaladon.s of pelbiodctritic limestones)

underlying the predominantly siliceous black

sequence. the latccr representing the so called

Kacak event (Chlupac 1989). The limestone

oceufs in beds oi thicknesscs between 5 and

30 cm. It is dai'k grcy in colour and bituminous.

The cherts of the Kacak sequence, restricted to

the area around Prague, hâve long been known

to contain radiolarians (Fabian 1933; see

582

GEODIVERSITAS • 1999 • 21 (4)

Czech Middle Devonian radiolarians

Praha-Hlubocepy Karlstejn-Knezi

raiiway eut hora Hil(

12 3 4

Fjg. 2. — Lithotogic succession ot lhe sequences exposed at

Praha-Hlubocepv raiIway eut and Karistejn-Knezi hora hlll. Note

the different Hihologic composition of lhe Kacak Member at the

two localities. 1. massive biomicriihc limeslones: 2. thin bedded

biomichtic limeslones; 3. fine bioOetrital limeslones; 4. coarse

biodeirital limestones; 5, Hlhociàstic breccia (not piesent In the

sequence shown): 6. dark calcareous claystones and clay ümes-

tones; 7. thin bedded cherts; 8. calcareous siltstones and biode-

tritic limestones with silt.

Chlupac 1960; ] 76) for changes in terminology

of the sequences). Radiolarian préservation seems

to be more favorable in the limestone beds com-

pared to the Kacak chéris.

AGE C.ONTROL

According to fàunal data, the Kacak succession

2 m above the upper Chotec Limestone was ini-

tially considered to be basal Givetian (Chlupac

1960: I^7)r and larer regarded uppcrtno.st

Eifelian ( Chlupac Ôc KukaI 1986, 1988;

Chlupac 1993). Kalvoda (1992) discusscd the

strarigraphic implications of conodonts in beds

near the hase of the Kacak sequencc which in

terms of the conodont chronology indicate an

upper Tnrtodus kackelianus zone age (near the

base of the Polygnnthm ensensis zone). In terms of

modem conodont chronologies (Sandberg &

Zieglcr 1996; Weddige 1996) ihîs zone is well

belüw the acrual Ltfelian/Givetian boundaxy. As

our samplc horizon is lücated a maximum uf 2 m

below the Kacak base our radiolarian faiina pre-

sumably also bcloiigs to the upper Tortodus km-

keliantti zone. Biidil (1995) discusses the

considered interval (Chotec-Kacak boundary

interval) in terms of the uppermost Eileliaii.

Because of the scattiry oi well preserved cono¬

donts and other faunas, the question of where

the actual Eifelian/Givetian boundary i-s siiuaicd

withiii lhe sequence has not been resolvcd. It is

clear however, thaï on the basis of rccent cono-

doni zonation schemes (Sandberg & Zicgier

1996) the radiolarian faunas discussed hcrein

stratigraphically belong to the upper Eifelian.

TECHNIQUES OF STUDY

The limestone samples were acid treated as in

any processing for conodonts, in this case with

acctic acid. Isolated radiolarians ftom the residue

hâve been eirher picked and mounied on SEM

stubs or embedded in Gaedaxfor light microsco-

py. The laiter technique serves well in the inves¬

tigation of internai structures, which are of

importance in generic and suprageneric taxono-

my of spherical radiolarians.

GEODIVERSITAS • 1999 • 21 (4)

583

Braun A. & Budil P.

SYSTEMA'riC PALEONTOLOGY

The radiolarian fauna in general is dominated by

Entactiniidae in rerms of absolute numbers and

species diversity. Ceraroikiscids and Palaeo-

sceniids arc ran:r. Ail radiolarians are exceprional-

ly well-preserved; in many of the cncactinids thc

internai siruciurcs arc présent. Whcrcas in the

CeratoikLscids several clearly different morpho-

types are distinguîshable^ the genus Pnlaeo-

scenidhm is présent only with one spccies. As thc

ceratoikiscids and palaeoscenids hâve bcen systc-

matically rteated in the paper of Cejehan (1987)

no detailed raxononiic discussions of these will

be made here. A more detailed taxonomie rreat-

ment is given (or the most common species of

eniactinids.

Matcrial figured and mentioned in ihç text (SEM

stubs, lighi microscope slides) are housed at the

collection ol the Institute of Paleontology,

University of Bonn. Coordinates given for spéci¬

mens on numbered slide.s refer to the cross stage of

a “Biolam microscope belonging to A. Braun.

Order ALBAILLELLARIA Dcflandre, 1953

Family CuiWOïKlsdDAE Floldsworth, 1969

Genus Ceratoikiscum Deflandre, 1953

emend. Holdswortb, 1969

(Fig. 3G. H)

Species of Ceratoikiscim arc pre.sent in a remar-

kably good State of présentation. At least seven

different species arc présent, but presently no

further important additions can bc made to thc

descriptions and figures iii Cejachan (1987). As

in other Systems (Siluiian, Power Carboniierous)

Ceratoikiscids are potentially uscfiil for biostrati-

graphic zonations in the Lo\ver and Middie

Devonian. The Ceratoikiscids in chis fauna show

strong similarities to the species de.scribed in

Foreman (1963) from thc North American

Famennian.

Order ? SPUMELLARIDA Ehrenberg, 1875

mon faunal consiitucnts in the investigated fau-

nas.

Genus Stigmosphaerostylus Rüst, 1892

For synonymy with Entactinia l'oreman, 1963 and

remarks sec Aitchison & Stratford 1997-

Type species — Stigmosphaerostylus notabilis Rüst,

1982.

Stigynospbaerostylus herculetis (Foreman, 1963)

(Fig. 4B)

Description

Spherical skcleton bearing six three-bladed

spines, the length of whicli is approximacely

cqiial to ihe diameter of rhe skelecal sphere.

Spines mviy be disposed ai 90“ angles to one ano-

ther or placcd slightly asymmetrical. No sccon-

dary spines bave been observed, only small

rhornlikc élévations are présent at the corners of

rbe lattice. About len faily large^ subcircular

porcs are présent per half circumferencc. The

specimen in -slide K.h. -20 AC/3, r; 22v h: 13,5

shows a bar centered internai spiculé, the spicular

rays display a rrifureation before rhey reach the

base of the spines. The specimen in slide K.h. -

20/1, r: 22, h: 19 shows an excentric double spi¬

culé.

Re MARKS

'Fhe specimens from our .samples closely corres¬

pond in mor|)holog)'^ to the paratype of S. bercu-

lea (Foreman, 1963) in Foreman (1963; pl. 1,

figs 3C, D). Gcneric détermination is based on

characterisiics of the internai structures of the

skeleton.

Stigrnosphaerostylus sp.

aff. 5. herculeaus (Foreman, 1963)

(Fig. 4C, E. H)

aff Entactinia herculea Foreman, 1963; pl. 1, fig. 3A-

D (specimen in pl. 1, fig. 3B)

Family Entactiniidae Riedel, 1967

Members of the Entactiniidae are the most com-

Description

Spherical skeleton wirh small, subangular pores

(15 to 20 per half circumferencc) and six three-

584

GEODIVERSITAS • 1999 • 21 (4)

Czech Middle Devonian radiolarians

Fig. 3. — SEM micrographs of radiolarians from the Upper part of the Chotec Limestone (upper Eifelian). Knezi hora hill near

Karlstejn. Palaeosceniidae and Ceratoikiscidae. A-F, Palaeoscenidium cladophorum Deflandre, 1953. Specimens displaying diffe¬

rent sizes and numbers of basal spinules. G. H, Ceraîoikiscum sp. Scale bars: 100 pm.

GEODIVERSITAS • 1999 • 21 (4) 585

Braun A. & Budil P.

bladed spines dlsposed approximately ar right

angles to one anorher. The length of rhe spines

varies from one co one time and a half rhe dia-

meter of the skcleral sphere. Small tliorn-like by-

spines are présent on rhe edges of the skelcraJ

framew^ork.

Remarks

This taxon summarizes the entactinid morpho¬

types characterized by a spine morphology simi-

lar to S. herculeus (Foreman, 1963) but uni-

formly having smaJler and more niimerous pores.

The character of pore size and number was

observed hcrc to be not higWy variable and tran-

sitional between morphotypes, whereas length

and widtli of spines wAh found to be much more

variable. We therefore do not include the spccies

with small pores into S. htrculea ,as bas been

donc by Foreman (1963)» but place it in a diffe¬

rent, presumably closely related species.

Stigmosphaerostyliis sp.

aff. proceraspinus (AitchLson, 1993)

(Fig- 41)

Description

Sphericai skelccon possessing a larrice-shell and

six rhree-bladed spines, one of which is conside-

rably longer rhan the ochers. The longer spine is

slightly rw'isted along its axis. Lattice with roun-

ded pores of irregular size (about 10 per hall cir-

cumferencc). Tire speeimen in slidc Kh -20/1,

r: 20.5, h: 26.5 displays a wcll preserved internai

double spiculé, the center of which is placed

excentrically towards the large spine.

COMPARISON and remarks

Generic assignment is based on characterisiics of

the internai skelcTon. There are several externally

very similar species characterized by an internai

sphere and thcrcforc referred to Trilnnche Hinde,

1899 (ex Entactinosphami Foreman, 1963) in the

lirerature. In pore size and general shapc our

material is similar to some specimens of 5. proce¬

raspinus (Aitchison 1993: 113, pl. 6, fîg. 1).

Other spécimens refeired to the sa me taxon in

Aitchison (1993. pl. 7, fig. l) hâve much longer

and more equally sized spines and arc prcsumably

not conspecific with our material. Considering

the smalier pores in the lattice sphere of the type

of E. pYoceraspina Aitchison, 1993, wc leave the

spécifie désignation open, but place our material

in clo.se connection to S. proceraspinus.

Stigfnosphaerostylusl sp.

aff. S, hysti'icuosus {Asic\nsony 1993)

(Fig- 4F, G)

Description

Small sphericai skeleton possessing six long

chree-bladed spines. The length of the spines is

more ihan chree cimes the diameter ot the skele-

tal sphere.

Each spine bears a set of tlirec spinules at one

half of their length, each spinule being placed on

one of che spine blades. A few specimens in light

microscope slides possess reninants of more spi¬

nules (slide K.h. -20/2, r: 23-5, h: 26) which are

not ahvays disposed at the same levcl of the

spines (slide K.h. -20 AC/3> r: 20.5, h: 17). The

spécimen in slide K.h. -20 AC/1, r: 26, h:

22 show.s a distal hifurcation in some of the spi¬

nules. rhe skeletal lattice possesses fairly large,

polygonal pores of irregular size (four to six per

half drcumlerencc).

COMPARISON AND REMARKS

Aitchison (1993) dcscribed several entactinid

species possessing main spines with spinules from

the Frasnian of Western Australia. Only in

S. hysrriaiosus (Aitchison, 1993) however the size

relations of the central shcll and spines aie com¬

parable with our Bohcmian material. In contrast

to the type material of hystrituosus, only a few

of our Specimens possess more than a single lier

of spinules on tlieir main spines wheras 5’, hyslri-

cuosus is regularly characterized by several tiers of

spinules. Concerning the externally similar mate¬

rial described as Entactinui additiva ? Foreman,

1963 by Nazarov et âl, (1982), we refer to the

remarks in Aitchison (1993; ! 13).

Genus 7r/Zo«r/?c Hinde, 1899 emend. Foreman,

1963; Aitchison &: Stratford, 1997

For synonymy with Entactinosphaera Foreman 1963

and further taxonomie discussions see Aitchison &

Stratford (1997: 373).

586

GEODIVERSITAS • 1999 • 21 (4)

Czech Middie Devonian radiolarians

Fig. 4. — SEM micrographs of radiolarians from the Upper part of the Chotec Limestone (upper Eifeüan). Knezi hora hill near

Karlstejn. A, Trilonche ? echinata (Hinde, 1899) sensu Foreman, 1963; B, Stigmosphaerostylus herculeus (Foreman, 1963): C, E, H,

Stigmosphaerosiylus sp. aff. S. herculeus (Foreman, 1963); D, Trilonche sp. aff. T. riedeli (Foreman. 1963); F, G,

Stigmosphaerostylus ? sp. aff. S. hystricuosus (Aitchison, 1993); I, Stigmosphaerostylus sp. aff. S. proceraspinus (Aitchison, 1993).

Scale bars: 100 pm.

GEODIVERSITAS • 1999 - 21 (4)

587

Braun A. & Budil P.

Type species. — Trilonche vetusta Hinde, 1899.

Trilonche sp.

affi TT (Foreman, 1963)

(Fig. 4D)

Description

Fairly large sphcrical skeleton possessing eight

narrow three-bladed main spines and numerous

small pores. The spines are narrow and only

indistinctiy three-bladed. Small acute rhorn likc

by-spines are arlsing from the edges of the latrice

sometinies giving ri,se to a délicate meshwork

pardy covering the pore bearing skelecal latrice.

Light microscope slides (K. h..-20/l| r; 24,

h: 21) show an internai sphere.

Remakks

The spécifie désignation has been done on the

basis of the characteristic spine morphology as

well as on the basis of the overall morphology of

the sphcrical skeleton. Pore size however in the

type material in Foreman (1963, pl. 5, fig. 4 A-

C) is larger and the number ot spines in

Foreman'.s material is smallcr (only six compared

ro eight in our material), The specimen from the

Frasnian oi Western Australia figured as

}Spongefitavtinella sp. 1 GSWA F44073 in

Aitchison (1993, pl. 7, fig. 5) is exccrnally very

similar to our material.

Trilonche ^ echinata (Flinde, 1899)

sensu Foreman 1963

(Fig. 4A)

Description

Medium sized sphcrical larrîced skeleton posses¬

sing six three-bladed main spines bc-sides long

rod-likc by-spines. The length of the main spines

is exccedmg the diâmeter of the central skeleton,

the length of the by-spines approximately cquals

the skeletal diameter. Latiice shell with smaJl.

regularly sized, angular pores (about 20 per half

circLimference).

Rkmarks

The species désignation is based on the morpho¬

logy of che spines in the sense used by Foreman

(1963). Generic assignment remains questio-

nable as no internai structures could bc found.

The spine morphology in this taxon has in our

material been found to bc a constant character

wiihout grear variabilicy and transitions to other

species. Similar material has been figurcd and

described as Entactinosphaera echinata (Hinde)

(now T. cchinàta by synonymy) by Aitchison

(1993: 113, pl. 3, figs 6, 11, 14, pl. 7, fig. 3)

from the Frasnian uf Western Australia.

Order Incerrae Sedis

Family PamEOSCENIIDAH Riedel, 1967

entend. Goodbody, 1986

Genus Palaeoscenidium Deflandre, 1953

Palaeosceniditim cladophorum Deflandre,

1953

(Fig. 3A-F)

Remarks

The figures show the skeleton of R cladophorum

in various orientations. Four distinct apical

spines are présent The development of spinules

on the basal spines is variable both in sîze and

density. R cladophorum is aiso common in

Frasnian (Aitchison 1993)» Famennian (Foreman

1963; Schmidr-Effing 1988; Kiessling &

Tragelehn 1994) and Lower Carboniferous

(Braun 1990) radiolarian faunas (up to che

Albitillella dejlandrei zone of the radiolarian zona¬

tion in Braun & Schmidc-Effing ( 1993)

RELEVANCE OF THE FAUNA IN THE

EVOLUTIONARY CONTEXT

Radiolarians from the Upper Silurian and the

Upper Devonian are difterent in various aspects.

One of the main dilfcrence.s is the suprageneric

composition ot the spherical radiolarians, which

bclong to the Entaciiniidae in rhe Upper

Devonian (and are prédominant at leasc in che

Upper Palcozoic) and to other distinctiy different

groups in the Silurian (Inaniguttidae Nazarov &

Ormiston, 1984, Rota.sphaeracea Noble^ 1994

and other groups not yet taxonomically separa-

ted). Looking at spherica] radiolarians only, the

impression arises, that there was a kind of “major

turnover’ somewherc during the Early or Middle

588

GEODIVERSITAS • 1999 - 21 (4)

Czech Middle Devonian radîolarians

Devonian, Icadiiig co ihe disappearance of the

Silurian Sphacicllaria and ihe prédominance of

thc Entactinids. Bascd on these obser\'ations pos¬

tulations of a sharp faunal change during Early

or Middle Devonian hâve been made (Nazarov

6C OrmisTon 1986). Recenc findings of well-

preserved radiolarian faunas from this interval

indicate however chat this trend was more gra¬

duai than originally assumed (Furutani 1983;

Kiessling 5C Tragclchn 1994). Descriptions of

well-preserved faunas are of ga*at importance for

any further considciation ot tins time interval in

radiolarian évolution. In ternis of this question,

the spherical radiolarians of thc upper Eifelian

fauna prescntly treated are “complerely’ modem

with respect to Upper Devonian and Carbo-

niferoLis to Permian faunas. Thcre are no rem-

nants of groups of higher raxonomic level charac-

terLstic for the Silurian as far às our investigations

hâve proceeded. I hiis, the major Silurian groups

must hâve disappeared before the Late Eifelian

and by that time the Entacrinids must liavc gai-

ned their numéral prédominance and modernity

of their morphologie characters. This évolution

probably rook place durîng ihe Early Devonian,

still devoid of any radiolarian fauna well enough

preserved to makc subsranciaied statements on

the taxonomie constitution. Probably, future

investigations will be successfui in lînding wcll

preserved faunas in uppermo.se Silurian and

Lower Devonian strata in thc Barrandian area.

The présence of uppermost Silurian (Pridolian)

radiolarians in limeslone.s of ihis area lias been

proven [Literature data and marerial donared by

Dr. H, Jaeger, Berlin (!)]> but other well preser¬

ved material nceds lo be found (or lurtlier work

and other llthologies in the Lower Devonian

need to be investigated.

h is worth noting, that the seemingly sharp diffé¬

rence between Upper Silurian and Upper

Devonian radiolarians exisrs only in the spherical

radiolarians, According to thc material coUected

up to now, Ceratoikiscids develop at a fairly

constant rate from their first known occurrence in

the Wenlockian. and the spicular Palaeosceniidae

are seemingly only going througli a décline becau-

se this group is présent in Upper Silurian faunas

with considerably greater taxonomie variety

(Goodbody 1986; Àmon et ai 1994).

Lithology Radiolarians

Fig. 5. — Schematic représentation of the observed différences

between lithologie and faunal change near the Chotec

ümestone-Kacak Member boundary.

GEOLOGIC SIGNIFICANCE (A. Braun)

Conspiciious change in sedimentary composition

between the Chotec I.imesrone and thc Kacak

seqiiencc is a feature .similar to thaï of niany sedi¬

mentary units assinged lo this time interval in

other areas (Weddige 1986: 281) and may indi-

cate somc form ol transgressive changes (sec

Housc 1984; Haas J994; Walliser 1994, 1995).

Observations of the colours and composition of

sedimenrs attributed to this stratigraphie intcrval

indicate that a transgre.ssive deepening evenr i.s

the most likely explanation for thc observed geo-

logicaJ plienomcna (Walliser 1995, fig. 3).

Transgression may have lead ro réduction in sédi¬

ment supply b}' drowning source areas ot clastic

sédiments. Planctonic organisms pcnecontenipo-

raneou.sly began to dominate the communities

because of the changes in water depth (and pro-

hably drculaiioii). This may finally have rcsulted

in the formation of “biosiliceous" deposits

within condensed sédiments, such as the cherrs

of the Kacak Member which devcloped in the

area around Prague.

Furthermore the above mentioned change in

sedimentary composition is interpreted in terms

of a short termed, abrupt event (“Kacak event”;

GEODIVERSITAS • 1999 • 21 (4)

589

Braun A. & Budil P.

Chlupac 1989: 483). The abrupt change in sedi-

nientolügical composition Irom the Chotcc

Limestone to the Kacak chert sequence scems ro

imply a similaiiy abrupt change in environmen-

tal factors and it is general opinion, thac most

“bio-events‘* coincidc with lithological changes

(“most of the global bio-events arc coiinectcd

with a litho-event, i. c. a strong lacies change";

Walliser 1995: 4). Looking at the prédominant

iithology it may scem to bc obvious in our

example ro assume a sudden bloom of radiola-

rians following a “norinar* Chotcc Limestone

organism assemblage (trilobites, renraculites,

conodonts etc.) which led to a similarly sharp

lithological boundaty beeween limestone and

radiolarian-dominatcd cherts in sections near

Prague (Hlupocepy railway eut, Barrandov), and

to some extent in uther sections as well.

The Barrandian localitics rreated in this paper

may, becausc ol iheir particular .sedîmentary

faciès concribucc to dtis discussion because the

sédiments présent here (limesrones) allow for a

good préservation of the organisms under consi¬

dération (calcarcous hard parts as well as radiola-

rian skeletons)-

The following observations can be made:

The abrupt change in sédiment type is, in terms

of paleoecology, not paralleled by an abrupt

change in Ibssil content. Prédominance and pré¬

servation of Radiolaria began ai least as early as

déposition of the uppermost 2 m unir of the

Chotec Limestones in the uppermost part of the

Chotec Limestone, typical “Chotec-Limestone"-

organisms become rater and less welLpreserved

as mentioncd by several authors. Some last

remains of the typical ‘‘Chotec Limestone fàuna"

however hâve been described from the last few

décimètres of the Chotec limestone formation

(Budil 1995). Only after such a general shift in

organism population did the abrupt change in

sedimentological realm occur.

There were biological changes wirhin the consi-

dered interval of uppermost Chotec limesrones

and lower Kacak Mcmber. In biological terms

however, gracfual ‘extinctions" and entrances in

organism ecology occur well before the clearly

visible changes in sédiment faciès and can be

observed over at least 2 m of sédiment thickness.

Disregarding the highly hypothetical question as

to how much tlrne may be reprc.sentcd by these

2 meters, it is obvious in non-turbiditic sédi¬

ments ot sedimentary basins like the Barrandian,

that the time interval neccessary for cheir déposi¬

tion cannot be called an abrupt evenr in ternis of

day.s, months or even a few years

Highcr up in the sequence (ai the Kacak base)

such ccological shifts were paralleled by changes

in the prédominant composition of the sedi-

mciifs, and it Ls quiic probable, rhat snch compo-

sitinnal changes were in our case also later

diagcnctically enhaneed lo give the sharp

contrast as scen in todays outerops.

Thu.s, the Kacak evenr. being prcsumably due to

changes tn water depth and sédiment supply lea-

ving traces în maiiy other areas, can be .shown to

hâve occurred ecologicaJly more graduaJly than

implLcd when only considering the scdimcntolo-

gical boiindarics. Thèse observations exclude

catastrophic pictures arising when tcading the

terminology sometimes used in event discus¬

sions, and contribute to the picture of many of

such events as '^müd'’ unes in the terminology of

Walliser (1995).

It is not oui* aim to cast doubi on the general

existence of telatively short-termed processes

known to be présent during the Phanerozoic

(Walliser 19951, thac changed sedimentological

characters as \sxll as the livîng conditions of orga¬

nisms and causing ccological stresses as a possible

rcason for larger scale exüncuons, organism dis¬

placements etc. And in view of ihc published

considérations on possible causes and natures of

“events" (Walliser 1995), it would surely be not

jusiificd to restrict our view of events to astetoid

impacts and lo discuss any proposed eveiu (sedi-

mentologically or organism-bascd) in the lighc of

such excraterresirial causes% which arc the excep¬

tion rather than the ruie (Walliser 1995). Thus,

we do not reject the exi.stence of ihe Kacak

“events" as long a-s the use of rhe terrn evenr does

not impiy a short terni cacastrophical happening.

Many such processes as far as we know today

seem to be closely connecccd ro changes in sea

level (Johnson étal. 1985; Ross & Ross 1985;

Walliser 1995), whatever rheir causes might hâve

been, and il is dear, that such changes could well

hâve lasted even a few million years. At least in

some cases however such changes do not coinci-

590

GEODIVERSITAS • 1999 • 21 (4)

Czech Middle Devonian radiolarians

de with lithological bouiidatics. l'his, based on

the présent observations, can be shown to be true

in the case of the Kacak event, The latrer as far as

il is represented by the typlcai (cherty) sédiments

was only the culmination of a transgressive deep-

ening, leaving its faunal traces well before the

actual Kacak scqucnce.

Acknowledgements

The authors wish to thank J. Aitchison (Hong

Kong) and R Noble (Reno) for critical remarks

and hclpful comments on an early version ot the

paper.

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Submitted for publication on 29 January 1998;

accepted on 17 Mar ch 1999.

592

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian

diatomites of Falconara (Sicily, Italy)

Giuseppe CORTESE

Department of Earth Sciences, University of Florence

Via La Pira, 4, 50121 Florence (Italy)

Alfred Wegener Institut for Polar and Marine Research

Columbusstrasse, P.O. Box 120161,27515 Bremerhaven (Germany)

gcortese@awi-bremerhaven.de

Kjell R. BJ0RKLUND

Paleontological Muséum, University of Oslo

Sars’gate, 1,0562 Oslo 5 (Norway)

k.r.bjorklund@toyen.uio.no

Cortese G. & Bjorkiund K. R. 1999. — Radiolarians from the cyclic Messinian diatomites of

Falconara (Sicily. Italy), in De Wever P. & Caulet J.-P. (eds), InterRad VIII, Paris/Blerville 8-

13 septembre 1997, Geodiversitas2^{4) : 593-624 .

KEYWORDS

Radiolariuv

Miocene»

Italy»

ciclicity.

ABSTRACT

The diatomitic sédiments in Falconara (6*93 to 6.08 Ma) hâve a total thick-

ness of c. 27 m, and rhe sequence is composed of 41 diatomite/claystone

couplets. The déposition of these biosiÜceous sédiments, seemingly modula-

ted by the astronomical prcccs.sion cycle (21,000 ycar.s period), ha.s bcen sug-

gested to hâve taken place in a shallow basin with diatomaceous and

ciaystone sédiments being deposited during iow and high sea level stands,

respectively. Polycystine radiolarians show major changes in the assemblage

compositions and the total abundances benveen rhe different cycles, from

being barren in Cycle 2 till > 142,000 radiolarians/g in Cycle 26.

Radiolarians arc usually not présent in the ciaystone samples» this is also the

case with diatoms. However, one ciaystone (Sll) had a significant high

number, > 43,000 radiolarians/g sédiment, while nine otliers had a Iow

content of radiolarians. We hâve in our counts recognised 68 morphot)'pes.

Q-Mode Factor anidysis has been used on the raw counting data. By using

fivc factors, wc werc ablc to explain 83.65% of the cumulative variance,

while using nine factors allowed us to explain 96.52% of rhe variance. These

nine factors displayed well-defined peaks that can be used to navigate within

the profile and to correlate between sections. Another high resolution srrati-

graphical tool could be represented by the peculiar faunal composition of

each of the diatomites. In our pilot study we selected three diatomites and

GEODIVERSITAS • 1999 • 21 (4)

593

Cortese G. & Bjorkiund K. R.

comparée! their assemblage composition and radiolarian abundances.

Cycle 11 is dominated by Stichocotys delmontensh and Lithomitra lineata-,

c. 50 and 36% maximum values rcspcctively. In Cycle 21, S. delmontensh

and Bouyostrobus auritiislaustralh are most common, with 40 and 30% as

maximum values respecrively. In both these cycles nassellarians arc tlie domi¬

nant group. In Cycle 26 Larcoidea sp-, Porodiscus sp., and Spongotrochus gla-

cialis arc the dominant taxa.

MOTS C^S

Radiolaires,

Miocène.

Italie,

périodicité.

RÉSUMÉ

Radiolaires des sédiments messiniens à diatomées de Falconara (Sicile, Italie).

Les sédiments à diatomées de Falconara (âgés de 6,93 à 6,08 milHon.s

d’annéf.s) ont une épaisseur totale d’environ 27 m. La séquence est composée

de 4l paires diatomice/argile. Le dépôt de ces sédijiients biosiliccux est appa¬

remment modulé par le cycle de précçssion astronomique (avec une période

de 21000 ans) et semble avoir eu lieu dans un bassin peu profond; le,s sédi¬

ments à diatomées et argileux correspondent respectivement à des périodes

de bas et haut niveau marin. La composition des assemblages à radiolaires

polycystines et l’abondance de ceux-ci varient beaucoup d’un cycle à l’autre,

d’absent dans le cycle 2 jusqu’à plus de 142000 radiolaires/g dans le cycle 26.

Les radiolaires, ainsi que les diatomées, sont généralement absents des échan¬

tillons argileux. Cependant, une argile (SU) a une concentration élevée

(> 43000 radiolaires/g) et neuf autres ont une faible concentration. Nous

avons compté 68 morphoiypes. Les données brutes om été soumises à une

analyse faaoricllc en mode Q. Avec cinq facteurs, nous pouvons expliquer

83,65 % de la variance cumulée, tandis que neuf facteurs sont nécessaires

pour rendre compte de 96,52 % de cette variance. Ce.s neufs facteurs mon¬

trent des maximums bien définis qui peuvent être utilisés pour naviguer le

long du profil et pour corréler les differentes coupes. Lhie autre méthode per¬

mettant une bonne résolution stratigraphique pourrait être fondée sur la

faune particulière à chacune de ces diatomitc.s. Dan.s une étude pilote, nous

avons choisi trois diatomites et nous avons comparé la composition de leurs

assemblages et leur abondance en radiolaires. Le cycle 11 c.st dominé par

Stichocorys delmonterisis et Lithomitra lineata, avec des maximum à environ

50 % et 36 % respectivement. Dans le q'cIc 21, 5. delmontensh et Botryo-

strobus uurhus/australh som les plus communs, avec des maximum à environ

40 % et 30 % rc.spcctivement. Pour ces deux cycles, les nassellaires forment

le groupe dominant. Dans le cycle 26, Larcoidea sp., Porodiscus sp., et

Spongotrochus glacialh sowi les taxons dominants.

INTRODUCTION

The biogenic siliceous sédiments of Sicily hâve

been knovvn for almost 125 years. Ehrenberg

(1854) and Mottura (1871) reported on radiola-

rians from the Sicilian Neogene, while Sauvage

(1873) described, in fairly good detail, foliated,

radiolarian bearing shale outerops near Licata

(Fig. 1). He assigned a Messinian-Zanclean âge

to them. Stohr (1876, 1878) and Schwager

(1878) studied Tortonian and Zanclean diato¬

mites and tuffs containing rich radiolarian

assemblages. Nicotra (1882) examined Tortonian

diatomites containing radiolarians near Messina.

594

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites ofSicily

13“ 14° 15° 16°E

FtG. 1 . — LcKîation map, showing the geographical posrtion of the Falcona/a Section. The shaded area représente the Cattanissetla

Basin, while the solid line depicts (he paleo-shore line. Modified from Gautier {1994).

Cocco (1905) did the same with different litho-

logies (maris, euffs, diatomites) outeropping ar

several Sidlian localitics.

Several cruises of the Deep Sea DriIJing Project

(DSDP) and of the Océan Drilling Program

(ODP) hâve raken place in rhe Medirerranean

Sca: DSDP Legs 13, 42, ODP Legs 107. 160

and 161, and biogenic opal bearing localitics

from the former Tethys Sca area hâve been repor-

tcd on by several authors as: Sanfilippo (1971,

1974)> Sanfilippo et al. (1973), Rio et al. (1989).

Ail these authors failcd to apply rhe .standard

radiolarian biostratigraphic scheme for uopical

latitudes, or to establish a local one.

Biogenic opal is generally nor well preserved in

rhe Ncogcnc sédiments of ihe Medirerranean Sea

(Dumitrica 1973; Ricdel et al. 1985). The lutter

authors report on only cight deep-sea localities in

the Mediterranean Sea where siliceous remains

are présent in isolated levels. Morcover, ai several

of these localities the radiolarians are scarce or

présent in only a few of the samples- Further-

morc, the species that are used in the standard

low latitude stratigraphical radiolarian scheme

are found in low numbers and are often morpho-

logically different from the truc oceanic ones.

Messinian sÜiceous diatomiric oozes outerop at

many localitics in chc Caltanissctta Basin, Sicily.

These sédiments yield abundant and diversifîcd

radiolarian làunas, thus having a potcncial tor the

compilation of a new local radiolarian strarigra*

phy bascd on acme zones and peak occurrences,

through calibrations wiih other microfossjl

groiips. As wc coLild not apply the standard low

latitude bioscratigraphicaJ radiolarian scheme to

the Falconara .Section, we used Q-rnode factor

analysis to facilitate faunal comparisons hetween

samples as an alternative tool for corrélation.

This allows us ro recognise, through time. diffe¬

rent associations being indicative of spécifie cco-

logical seteings (i.e. peak occurrences), evenrs

that later may be used as a corrélation tool both

wichin rhe Falconaia Section and hetween other

sections in the Calranissetta Basin.

Hilgcn & Ivrijg-sman (1999) stress the uncertain-

ty and concroversy about horh the âge of the

Tripoli Formation and the origin of rhe cyclic

bedding (Gautier et al. 1993; Butler et ai 1995;

McClelland et al. 1996; Sprovieri et al. 1996; Vai

1997). They also summarise the following scena-

GEODIVERSITAS • 1999 • 21 <4)

595

Cortese G. & Bjerklund K. R.

Fig. 2. — Corrélation between Sprovieri et al. (1996) field*log for the Falconara Section, the polarity time*scale and the variations of

the Cp/Rp (the two nannofossil species Coccolithus pelagicus and Reticulofenestra pseudoumbilicus) ratio at OOP Site 552.

Selected bio-markers are also shown. Modified from Sprovieri étal. (1996).

rios to explain the qrclic diatomite formation as a

resuit of: (l) the intensification of Atlantic

inflow due to glacio-eustatic sea-Icvcl changes

(Van derZwaan dc Gudjonsson 1986); (2) pcrio-

dic upwcllings (Gersondc 1980); (3) surface

water warming (Broquet eml. 1981); (4) increa-

sed continental run-oft (Meulenkamp et al.

1979); (5) global sea-leve| rise in combination

with enhanced upwelling (McKenzie et al.

1979); (6) pulsating lectonics (Pedley & Grasso

1993).

With the imcertainty of the âge of the Tripoli

Formation and the exact origin of rhe cyclic bed-

ding, Hilgen Krijgsman (in prep,) conclude

that the substitution of sapropel c>'cles by Tripoli

diatomite cycles point to an orbital control on

the sedimentary cyclicity, since sapropels are

astronomically controlled (Hilgen étal. 1995;

Sprovieri er/z/. 1996).

The palaeoclimatic interprétation ot the diatomite-

claystone couplets however, differs strongly from

author to author. Sprovieri et ai (1996) suggest,

based on planktonic foraminifers, that the dépo¬

sition of claystones (or sapropels by some

authors) took place during cold periods. while a

warmcr planktonic foraminifers assemblage is

présent in the diatomites. Müller (1985)

concludes> based on nannofossil warm water spe¬

cies, thaï the claystones were depositcd during

warm periods, whüc diatomites rcllcct the

inlluence of cold periods and upwelling. Hilgen

ÜC Krijgsman (1999) conclude that the diato¬

mites (laminites) correspond to the precession

minima and sommer insolation maxima, and

that the homogenous maris correspond to pre¬

cession maximaand insolation minima.

The main goal of ihis paper is to examine the

polycystine radiolarian faima in the biosiliceoas

deposits in the Tripoli Formation as it outerops

at Falconara, Sicily (propo.scd by CoLilongo et al.

1979) as a pocential référencé section for the

Tortonian/Messinian boundary). The radiolarian

596

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites of Sicily

fauna is rich and well-preserved in most diato¬

mites in the section and the radiolarian response

to the cyclic changes are promising for a high-

résolution biostraiigraphic and corrélation tooh

as chc radiolarian assemblages show major and

significant changes berween and within scicctcd

cycles (bulk radiolarian abondance, radiolarian

tlux, relative abundance of selected species, factor

loadings, Spumellaria/Nassellaria ratio, etc.).

Tbese severe assemblage Lhanges, in the radiola¬

rian fauna in rhe biosiliceous sédiments at

Falconara may provide information to improve

and beteer understand the oceanographical and

ecological évolution of ihe area.

STRATIGRAPHIC FRAMEWORK

In recent years Hilgen (1991), Langereis &

Dekkcr (1992), Gautier et al (1994), Suc et ni

(1995), and Sprovieri ei al (1996) hâve been

working on sédiments of Messinian age in Sicily,

whilc Flodcll et al. (1994) wotked up an age

équivalent section in Morocco.

Hodcll étal (1994) convincingly démonsrrated a

high-resolutioii isotope, carbonate, magnetostra-

tigraphic, and biostratigniphic record of a part of

the Bou Regreg Section in north-western

Morocco. The investigated drill cote covered rhe

rime spait from paleomagnetic Chron C4n par-

tim to C3r (earliest Gilbert). This represents ihe

rime leading to and including the isolation and

desiccation of the Mediterranean, i.e. the

Messinian sahnity crisis. They demunstrated that

during Chvons C3An and C3Ar (6.935 to

5.894 Ma) rhe isotope and carbt)nate signais dis-

played a quasi-periodic variation vvitli estimated

periods of 40 and 100 kyr respeciively. The

L\ 40 kyr period 3**^0 signal was inierpreied to

rcilect changes in dic global ice volume causcd

by obliqiiit}"'induced changes (4l kyr period) in

solar insolation in polar régions, They aiso

concluded that the 100 kyr period carbonate

variations were probably related to a long rcrm

modulation of the amplitude of the precessional

cycle (c. 21 k}T period) which was not resolved

due to their low sampling frequency.

The Falconara Section was First published by

Catalano & Sprovieri (1971). D’Onofrio et al

(1975), Colalongo et al. (1979), van der Zwaan

(1982), and Theodorites (1984) published on

the calcareous plankton biostratigraphy in this

section, Gersonde (1980) and Gersondc

Schrader (1984) teported on the diarom biosrra-

tigraphy, whüe stable oxygen and carbon isotope

data were provided by van der Zwaan (1982),

and van der Zwaan & Gudjonsson (1986).

Langereis et al. (1984), Hsü (1985), and

Langereis Dekker (1992) did not succeed in

establishing a paleomagnetic stratigraphie frame-

work for che section, while Gautier et al (1994)

clairned to hâve ohrained paleomagnetic results

from the Tripoli Formation

Sprovieri et al (1996) rejcctcd the paleomagnetic

results from Falconara proposed by Gautier et al

(1994). Instead they corrclatcd the palcomagnc-

tic record of ODP Site 552 (North Atlantic)

with ODP Site 654 (Thyrrenian Sea), after

having relnterpreied rhe magneiosuaiigraphic

boundaries and their âges according to the

magnctic polarity reversais record proposed hy

Cande & Kciu (1992, 1995). ’J'he abondance

fluctuations in chc Glohigerinoides population

at Site 654 were then corrclatcd to the record ol

the samc fluctuations in the Falconara Section.

ODL Site 552 from the North Adantic was used

by Sprovieri et al (1996) to obtain the paleoma-

grieric boundary âges of Chton 3An by using the

nannofüssil abundance fluctuations published by

Beauforr & Aubry (1990). Site 552 provides a

complété sequence of abundance fluctuations

(Fig. 2). forced by the asrronomical prccession

cycles from the middic latc Tortonian to che base

of Zanclean. Sprovieri et ai (1996) were able to

accuraiely corrdafe sedimenrary and biostratigra-

phic events recorded in the Mediterr.inean ba.sin

with similar events in rhe North Atlantic

(Site 552), and demonsrrated chat the âges could

be estimated by comparison widi ihe sequence of

abundance fluccuaclons linked to dic prccession

cycle. By this technique Sprovieri et al (1996)

estimated the base and top of the Tripoli

Formation at Falconara to be 6.93 Ma and

6.08 Ma rcspecTivcly (Fig. 2), which Is the age

modcl adopted in our présent paper.

This deviates signiFicancly from the age model

provided by Hilgen & Krijgsman (in prep.).

GEODIVERSITAS • 1999 • 21 (4)

597

Cortese G. & Bjorklund K. R.

Metric

Scale

0 '

Fig. 3.

Diatomite

code

D35

D30

D20

D 15

D 10

Basal Limestone

dm Diatomite

^■iCIaystone

E^mCovered

— The 1995 field-log for the Falconara Section.

l'hcy used the position ot the first and last occur¬

rence of the planktonic foraminifer Globorotalia

nicoLie as the starting point for their tuning expe-

riment. These events hâve been astronomically

datcd at 6.829 and 6.72 Ma in sections on Crete

and Northern Italy (Hilgen et al. 1995;

Krijgsman et al, 1997) and are located in the

Tripoli cycle T9 and Tl4, respectively. Wirh

thèse âges as the starting point, ail diatomite

cycles hâve been mned to the La90^, precession

and summer insolation rime sériés (Hilgen &

Krijgsman 1999). They provide absolute âges for

ail sedimentary cycles bascd oit their astronomi-

cal calibration^ rcsulting in 7.008 and 5.99 Ma

for thé base and the top of the Tripoli

Formation. According lo ihis new âge model the

Falconara Section starts with Tripoli cycle T8

(6.847 Ma) and contains 4l cycles* (Hilgen &

Krijgsman 1999), suggesiing that Sprovieri et ai

(1996) are missing seven Tripoli cycles. In future

Work, we will u.se the new âge model of Hilgen

& Krijgsman (1999). In labié 8 we bave tabula-

ted the sample age.s according to Sprovieri et ai

(1996) and indicated ihc corrélation to the

Tripoli cycles and absolute âges according to

Hilgen & Krijgsman (1999).

MATERIAL AND METHODS

The study area covers the valley and hilly région

delimited by the Sicani, Madonie and Erei

Mountain Ranges (SW Sicily, Southern Italy),

roughiy coinciding to the Agrigento and

Caltanissetta provincial territory (Fig. 1).

Hitheno rhe best known Tcniary marine opal

bearing sédiments on Sîcily are included in the

Tripoli Formation, the so called diatomites or

laminites, which are nicely exposcd in the

Falconara Section.

ÜLir sampling program (May-June 1995 and

Augusf 1997) concentrated on the Messinian

portion of the 27 m thick Falconara Section

(Fig. 3). In 1995 we sampled a total of 30 out of

41 diatomites and 18 out of 41 ciay.stones,

(Table 2) and the remaining litbologies were

sampled in 1997. The diatomites in Cycles 7, 21

and 28 were continuousiy sampled and are inclu-

598

GEODIVERSITAS • 1999 • 21 (4)

Radioiarians from the q^clic Messinian diatomites of Sicily

ded in rhis work. The sampling of the Falconara

Section resultcd in two dififerenr sample sets:

(1) one central sample per lithological unit for

the 49 sampled Üthologies; (2) one consisting in

a conrinuous sampling of ail the diatomites

observed in the field. The maximum number ot

samples for a single diatomite wa.s 4S, resulcing

in a time-resolurion of a few hundred yeais only.

In the Tripoli formation Sprovieri et al. (1996)

referred to rhe lithological levcls and labelled the

diatomites from 1 1 to T4l and rhe inrercalated

claystones from Ml to M42, wirh every négative

or positive fluctuation in the nannoplankton flora

representing a hall-cycle. The claystones are arbi-

trarily ossutned lo represent the base of the cycles.

We hâve processed a total of 162 samples

(Tables 2-5) from rhe Falconara Secrion and

made slides for quantitative and qualitative ana¬

lyses following ihe method proposed by Goll &

Bjorklund (1974).

We selected ihc sample from tlie central part of

each sampled lithological unit for botli che diaco-

mites and the claystones, assuraing it to be repré¬

sentative for rhat lichology. Ail samples were

analyscd for their content of total organic carbon

(TOC) and calcium carbonate by ihe use of an

infrared gas analyser (LECO). This instrument

measures, by infrared absorption, the anioum of

CO, rcleased from che samples during combus¬

tion. The CaCO^ conienc was cakulated by the

dififercnce of C„„,| and multiplied by

rhe factor of 8.3 (aromic weight ratio of CaCO,

to carbon).

Samples from wirhin a single cycle hâve been

coded, when ploited (Figs 7-12), as XX.[XX

indicates rhe référencé number for the cycle

(Tables .3-5) and YY indicates the position of the

sample wirhin rhe cycle, given as a percentage of

the time elapsed from the bottom of rhe cycle].

This lias been donc in order to simplify compari-

sons between different cycles, based on the

assumption thaï tlie déposition of each cycle was

influeneed by the precesslon cycle, and therefore

took place over an average time span of

21000 years (as demonstrated, for che Falconara

Section, by T lilgen et al 1995; Sprovieri et al

1996). As a working hypothesis we had to assu¬

me that the sédimentation rate was constant

throughout the cycle, in order to calculate

TOC

Fig. 4. — TOC {Total Organic Carbon) measurements through

the section.

sample âges. Flux estimâtes are therefore based

on the assLimption that the déposition of each

cycle took place over 21,000 years. These calcu¬

lations were carried out on sédiment cubes 2 X

2x2 cm.

The Factor Analysis Method (Imbrie & Kipp

1971) and the Fortran program CABFAC

(KIovan &C îmbrie 1971) were used for rhe statis-

tical trearmetu of the data set, The Cabfac Q-

Mode factor analysis program wavS used for

grouping rhe samples in the Falconara Secrion

into varimax a.ssembldges based on the similariry

between samples. This is donc by transforming

rhe raw data into variables (the factor compo-

nents), each of which bas a set of values (the vari¬

max factor scores) giving an indication of which

species are most important in each factor.

The species rhat were treated staristically had to

occur as more fhan 2% of the total launa in at

least one sample, as rccommcnded by Imbrie &

Kipp (1971). Tbis teduced the original 68 mor¬

photypes (Table 1) counted during this study to

4l morphütypes used in the first factor analysis

run. A sélection of the morphotypes included in

our factor runs are shown in Figs 20-22.

RESULTS

The organic carbon values from the central part

GEODIVERSITAS • 1999 • 21 {4)

599

Cortese G. & Bjorklund K. R.

% CaCOa

Fig. 5. — Percent of CaC 03 through the section.

of the 49 lithologies (Table 2, Fig. 4) from

Falconara are low, 0.06 < TOC < 0.18%, throu-

ghouc the section. These low values are in good

agreemenc with Brosse & Hcrbin (1990) who

also reporced on values much lowcr than 1%

TOC in the upper Messinian of ODF

Sites 654A and 652A in the Thyrrenian Sea. The

CaCO, values (Table 2, Fig. 5) show fluctuations

between 7.92 and 50.09%.

The abundance of radiolarian specimens in the

49 studicd lithologies ranges from zéro in

Cycle 2 till more than 169000 radiolarians/g

bulk sédiment in Cycle 26 (Fig. 6), therelore

indicating ihar the diflerenr cycles display mar-

ked variations in the total abundance of radiola¬

rian specimens and in the spccies composition as

demonstrared by the changes in factor loadings,

as we will show later (Figs 15-19, Tables 6-8).

Our data show that radiolarians are usually not

présent in ihe claystones fFablc 2, Fig. 6), as also

documenled lor rhe dialoms (Gersonde 1980;

Gersoiidc &C Schrader 1984). Ol our 19 clays¬

tones, ninc were barren for polycystine radiola-

rians, while eight had low numbers, les.s than

3,000 radiolarians/g carbonate free sedimeni.

However, two claystones had .sîgnificant liigh

numbers, more than 43,000 (Sll) and about

21,500 (S18) radiolarians/g bulk sédiment.

The abundance of radiolarian skeletons is sho-

wing great changes between the different diato-

Fig. 6. — Number of radiolarians per gram bulk sédiment in the

diatomites through the section. Dashed line refers to claystones.

mites (Fig. 6). To test how the radiolarian abun¬

dance changed within a cycle and berw'een cycles,

we arbirrarily selecred rhree conrinuously sam-

pled diatomites, the lowest at r. 5 m, the middie

at c. 12 m and che uppermost at r. 18m irno the

section, respectively:

Cycle 7. (Figs 7, 10; Table 3); diatomite D7, in

rhe lowcr part of the section, Is 46,9 cm ihick

and the cbysione/diatomite boundar)' is 46.6%

into the cycle, 'l’his pcrccntagc notation has been

adopted in order lo hâve a way to directiy com¬

pare the data obtalned front different cycles, with

the assumption that the scdimentological évolu¬

tion of cach cycle is che .samc.

Cycle 21 . (Figs 8. 11; Table 4): diatomite D21,

in the middie of the .section, is 64 cm thick and

the claystone/diatomite boimdary is about 11%

into the cycle.

Cycle 28 . (Ftgs 9, 12; ‘Fable 5): diatomite D28,

in the uppei pari of the section, is 49.7 cm thick

and che claystonc/diacomirc boimdary is about

49.2% into the cycle.

In dre three cercles chosen in this experiment, the

abundance of radiolarians varie.s between

c. 3,200 in Cycle 28 and c. 117,000 radiola¬

rians/g bulk sédiment in Cycle 7. Wc hâve no

calcium carbonate data for the continuous sam-

pled diatomites but che variation patterns of the

radiolarian abundance number within the three

cycles are however distinct (Figs 7-9).

600

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites of Sicily

Fig. 7. — Number of radiolarians per gram bulk sédiment

through Cycle 7. The dashed horizontal line marks the transition

between claystone and diatomite.

In the following wc will discuss only the diaro-

niitcs from chc chrec selected cycles.

Cycle 7. Radiolarians are présent wirh highesr

abundances (Fig. 7) in the lower 10% of the

diatomite (t*. 117,000 radiolarians/g bulk sédi¬

ment), while the number gradually dccreases

towards the top of the diatomite (c. 27,200), As

can be seen from ihe .Spumellaria/Nassellaria

(S/N) ratio, spumellarians arc dominating over

nasscllariajis in the botcom five samples (with

one exception), while in the rest of the diatomite

the S/N ratio fluctuâtes around a value of 0.7,

indicating a dominance of nassellarians (Fig. 10).

Cycle 21. Radiolarians are présent with highest

abundances in the lower 10% of the diatomite

(r. 1 14,000 radiolarian.s/g bulk sédiment). This

number rapidly dccreases to f. 40,000 c, 20%

into die diatomite, thercafrer it fluctuate.s from

between c. 24,000 and 49,000 towards rhe top

(Fig, 8). In rhe lower 15% of the diatomite (with

the exception of the oldest sample), die S/N ratio

is higher than oiic. while for the remaining part

of the diatomite nassellarians are the dominant

group (Fig. 11).

Cycle 28. Radiolarians are présent with highest

abundances in the lower 10% of the diatomite

{c. 55,000 radiolarians/g bulk .sédiment). 'l'his

number rapidly dccreases to less than 10,000

c. 15% into the diatomite, thereafter it remains

Fig. 8. — Number of radiolarians per gram bulk sédiment

through Cycle 21. The dashed horizontal line marks the transi¬

tion between claystone and diatomite.

almost constant (Fig. 9). In this diatomite the

spumellarians are dominant throughout, in

contrast to the previous cwo cycles, where nassel¬

larians are rhe dominant group. In the topmost

20% of the diatomire the S/N ratio flucruates

benveen 10 and 65 (Fig. 12).

In order to take ihe dilution effect of carbonate

into considération we plottcd the number of

radiolarians/g carbonate free sédiment of the

central sample from ail lithologies (Fig. 13). We

hâve sampied 19 out of 4l claystoncs and only

two hâve a significant radiolarian content, bet¬

ween 30,000 and 50,000 radiolarians/g carbon¬

ate free sédiment, wliilc two diatomites bave

values rcachiug more than 250,000 radiola¬

rians/g carbonate free sédiment.

The di.stürting clfect of the (most likely chan-

ging) sédimentation rate through the section was

then considered, and we calculated a radiolarian

flux curve for the .section (Fig. 14), accepting the

diatomites and claystoncs to bc prcccssion

controlled, with an average duration of

21.000 years. This curve depicts the changes of

the number of radiolarian.s per time- and per sur-

facc-unic (e.g., number of radiolarians/

kyear/cm'), thus being an image of the changes

in radiolarian productivity through rime, which

is independent both from the composition and

GEODIVERSITAS • 1999 • 21 (4)

601

Cortese G. & Bjorkiund K. R.

Fig. 9. — Number of radiolanans per gram bulk sédiment

through Cycle 28. The dashed horizontal line marks the transi*

tion between claystone and diatomite.

from thc accumulation rate of the sédiment hos-

ting thc microfossils. h is apparent that only onc

diatomiie (D26) represenrs one major high pro¬

duction puise wiih an outsianding radiolarian

flux (304,000 radiolarian skeletons/kyear/cm^)

when compared to thc rest of the diatomiies

(Fig. 14;; Table 2). This abundance peak is a

potential evenr to be used as a key-Ievel in local

and régional corrélation.

The application of Q-mode facror analysis to a

total of 4l morphorypei rcsultcd in 10 factors

(polycystine radiolarian associations), cxplaining a

cumulative variance of 95.89?4> (data hom chis

run are nor presented herein). The 13 morpho¬

types having a varimax factor component value

higher than 2.000 (i.e. the most "iniporranr" spe-

cies for each factor) in rhis run were then used

once again in a second factor analysis run. The

results between the ttvo runs are not significantly

different, thereforc enabling us to work with only

13 radier than the 68 morphotypes that we staned

out with. This réduction in species will speed up

the couriting time, and rhis rechnit|ue can, there-

fore be a poicncially usefui tool for corrélation.

The screening (the first iactor run) and reducrion

to only thc 13 most important morphotypes wÜI

make it casier to compare and use data from orher

authors. Of the factor component peaks resuldng

from this run we tabulated In Fable 8, 46 factor

component values higher than 0.400 (Table 6).

Fig. 10. — S/N ratio Ihrough Cycle 7. The dashed horizontal line

marks the transition between claystone and diatomite.

Factor 1 (doininated by the S. delmontensis

group, Table 7) reaches high values in different

poruons of the section, but i.s more significant in

sédiments oldcr than 6.50 Ma (Fig. 15).

Facror 2 (dominated by Larcoidca sp.. Table 7) is

common throughout thc section bccoming more

important în sédiments vounger than 6.54 Ma

(Fig. 16).

Factor 3 (dominated by l.ithornitrn lineata^

Fable 7) Ls the only factor that gives a good oppor-

tuniry lo split the Falconara Section in a higher

and lower portion, a.s high v;ilues for this Iactor

are only found in thc lower portion of thc sect ion,

in sedimems older than 6.60 Ma (Fig. 17).

bacior 4 (dominated by Didymocyrtis Fig. 18;

i'able 7) is one facror assigned to thc claystones,

peaking in Si3 and SI6. On the quantitative

slidc of sample SI6 no radioiarians were found

(Table 2), however, on the cnriched fauna slides

an almosr monospecific Didynmyrtis sp. assem¬

blage occiirred.

Factor 7 (dominated \yY Anthocynidium ehrenbet’

gu Fig. 19; Table 7) is the second factor a.ssigned

CO the claystones with one peak in S21.

DISCUSSION

The Falconara Section is peculiar in its radiola¬

rian assemblage and species morphology. These

602

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cycÜc Messinian diatomites of Sicily

Fig. 11. — S/N ratio through Cycle 21. The dashed horizontal

line marks the transition between claystone and diatomite.

deposits are immediately prc-dating the isolation

and desiccation of the Mediterranean Sea, cau-

sing “stressed** ecological conditions for the

plankton. The following scénarios hâve been

used to explain the cyclic diaromiie formation,

eA'ents thar can aiso cause ihese strcssed ecologi-

cal condition.s: (l) the intensification of Atlantic

infiow due lo glacio-eustatic sea-lcvel changes

(Van der Zwan èc Gudjonsson ( I986); (2) pcrio-

tiic upwellings (Gersoiide 1980); (3) surface

water warming (Broquet et al. 1981); (4) increa-

sed continental run-otf (Meuleiikamp et al.

1979); (5) global sea level risc in combination

with enkanccd upwelling (McKenzie et al.

1979); (6) pLilsating tcctonics (Pedlcy & Grasso

1993). Hilgcn Krijgsoian (1999) point out

that the Miocene sapropcls had the same origin

as the Plioccnc-Plcistocene ones, namely domi-

nantly precession controlled ‘‘dry-wet’^ oscilla¬

tions in the circum-Medicerranean cUmare.

These alternations certainly cau.sed différences

in the living conditions for the marine micro-

plankton.

The âge of the Tripoli Formation exposed in the

Falconara Section was determined by Hilgen &

Krijgsman (1999) to range from 6.847 to

5.980 Ma, siâning with Tripoli Cycle T8, com¬

pare Sprovicri et al. (1996) giving the range of

6.93 to 6.08 Ma, corresponding to the nannofos-

sil C. leptoporus zone. The standard radiolarian

Fig. 12. — S/N ratio through Cycle 28. The dashed horizontal

line marks the transition between claystone and diatomite.

zonation cannot directiy be applied to the

Mediterranean Sea, nor to the Messinian sili-

ceous deposits on Sicily.

l'he base oi the radiolarian Stichocorys peregrinu

zone is defined as the transition from S. delmon^

ternis lo S. porgmut. dated to occur ac c. 6.2-

6.3 Ma (Theycr & Hammond 1974). l^icdel et.

al. (1974) reported on one radiolarian-rich

sampic in rhe Trubi maris of the Capo Rossello,

assigned to the Zanclean stage, lower Pliocène,

stating: “...the “Trubr assemblage is to be placed

between the rime of evolutionar)'' transition Iroin

S. delmontemis to 5. peregrtnay and that from

Spongaster berminghami to S. peaias, and thus

evideiuly bclongs to the Stiihocorys peregnna

zone.” From the same profile Riedel ÔC

Sanfilippo (1978) also report on conimon typical

üceanic specintens uf S. peregriaa with truncated-

conical tliird segment.

In the Falconara Section, assigned to the older

Tripoli Formation, wc hâve not been able to

observe this transition. We include in the S. del-

?«/?//re/WW groiip several morphologies, somc with

a rhkk silicified test, oihers with a very thin test,

and scvcral forms having irregularly shaped seg¬

ments with tilted strïctures between segments.

No real specimens of the oceamc form of S. pe-

regrina have been observed in our material. We

cherefore assign the section to predate the

Stichocorys peregrina zone.

GEODIVERSITAS • 1999 • 21 (4)

603

Corcese G. & Bjorklund K. R.

Fig. 13. — Number of radiolarians per gram CaCOg-free in the

diatomites through the section. Dashed line refers to claystones.

Foraminiferal assemblages arc generally présent

in the diatomites with a rich and divcrsified

fauna, whtlc the diver.siry is generally lower in the

claystones. Insome ebystone units the foramini¬

feral as.sembJages are mlssing, e.g., M3Ü, M4l,

and M42 (Sprovîeri er al. 1996). They sugge.si

that the clay.siones are deposited during cold per-

iods while the diatomites are deposited during

warm periods, as they generally hâve a warmer

planktonic foraminifer assemblage.

Muller (1985) on the other haiid concludes the

opposite- The claystones hâve a higher amount

of nannoplankton and a more diversifîed assem¬

blage with input of warm water species (i.e.

Sphenolitlms abies) and sonie discoasters. She the-

refore concluded thaï the claystones were deposi-

red during warm periods, while the diatomites

were formed during cold periods and rimes with

upwelling related lo changes in the prevailing

wind direction.

The Sîicochorys delmontemn group îs présent

throughout the section and varies greatly in

abundance as well as morphology, as also obser-

ved in the Gibliscemi Section (Caulet pers.

comm. 1997). The variation in rhe skeletal nior-

pholog)’ jn chc S. delmonf^ensis group is a poten-

tial tool in interprecing the paleoclimate if wc

can décode the meaning of thèse variations.

The S. delmontensis association (Factor 1, Fig. 15)

and Lithomitra lineata association (Factor 3,

Fig. 14. — Radiolarian flux (number of radiolarians/kyear/cm^)

through the section. Dashed line refers to claystones.

Fig. 17) show aimost the sanie pattern of major

and rapid variations in rhe lower part of the sec¬

tion. oldcr rhan 6.5 Ma, inrerpreted a.s rapid eco-

logical changes over very short time intervals.

In Factor 2 Larcoidea sp., Porodiscus sp., and

SpongotroL'ht4:i glacialis arc the dominant taxa,

after 6.5 Ma and modem équivalents of rliese

categories arc often found in deeper and coder

water, excepi for Stylochlamldtum venusium

(forms that we included in the Porodiscus sp.)

showing a .shallow and warm waicr affinity in the

Pacific (Mullineaux & Westbcrg-Smith 1986).

As the modem équivalents of chese groups do

refer to open océan conditions, it Ls not easy to

inrerprei the Falconara vScciion in a scénario

where die shallow Caluiiisscaa basin has a res-

rricted comniunicaiion with the océan.

Diatoras are generally absent or badly preserved

in the claystones (Gersonde 1980; Gersondc &

Schrader 1984). Siniilarly for the radiidarians,

but two claystones bave significant aniounts of

radiolarians, SIS (21^500 radiolariaas/g hulk

sédiment) and Sll (43,000 ladiolarians/g bulk

sédiment). In addition rhree claystones arc clia-

racccnstic by their fauna associations, Si3 and

Si6 (by Factor 4, dominaicd by Didynwcyrtis sp.)

and S21 (by Factor 7, dominaced by

Anihocynid'mm ehmibergii). These fivc levels are

potential good local or régional markers within

the Caltanissetta basin.

604

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cydic Messinian diatomites of Sicily

Factor 1

Fig. 15. — Factor components through the section (Factor 1 ).

The Didymocyrtis sp. is almost monospecific and

as the section is predating the Stkhocnyys peregri-

na zone, the Didymocyrtis periultima zone would

seem natural, but wc cannoi assign our assembla¬

ge to this zone vvith certainty. l'his form ol

Didymocyrtis sp. might bc tlie occanic counter-

part oi Didymocyrtis penultima, howcA^er, it dd-

fers so much that it probably i.s a new species.

We do not think thaï rhis morphology is simply

a resulr of different ecolog)^ and corresponding

ontogenesis.

The diatomites show great variation in the num-

ber of radiolarians/g sédiment, both berween rhe

diflercnl diatomites and within them (Figs 6-9).

‘Ib test the hypochesis if thcrc is a fhythmic deve¬

lopment tliroagh lime between the different

diatomites, we assigned each sample tu its lime

équivalent position widiin each cycle, assuming a

claystonc and a diaiomite couplet to represent

21,000 years. Each claystonc and diacomice has

its own polycy^siine radiolarian ‘Tingerprint"

(assemblage or event) as deiermincd by the per¬

cent distance inre the cycle, l'his will provide an

excellent stratigraphie tool wiih a high and préci¬

sé time résolution (Table 8).

Another “fingerprint” that can help to recognise

the different diatomites is the Spumellaria/

Nassellaria (S/N) ratio. D7 and D21 show a very

similar and systcmatic évolution in this ratio,

where spumellarians dominate the lower part of

Factor 2

Fig. 16. — Factor components through the section (Factor 2).

the cycle, while the nassellarians take over in the

upper part of these cycles (Figs 10-11). D28

shows a dirterent trend in ihe Spumellaria/

Nassellaria ratio .since ihc spumellarians are

aiways dominant and rhey bccome much more

so in rhe upper part of the cycle (Fig. 12).

The différences in rhe polycystinc radiolarian

“fingerpfint” berNveen cycles can not be explained

at présent, but only speculated upon. The mlcro-

fauna of the l'iipoU Formation, both at

Capodarso (Suc et al. 1995) and at Falcon.ira

(Sprovicri et al. 1996) is rich in planktonic fbra-

minifcr,-î, a typical oceanic imprint. The sédi¬

mentation histojy of the Calt.inissett.a basin has

chaiigcd rhrough the Messinian. as documented

by the alternation of diatomites and claysrones

due to processes causing tlie isolation, changes ni

production and préservation of organic material,

changes in ptimary and sccondary production,

and desieçation of the basin, compare the scéna¬

rios outlinod elsewhere. Suc et al. (1995) point

ouc that the diatomitc-claysrone couplets are a

rcsult of sea-level fluctuations. Sprovieri et al.

(1996) on the other hand concluded that the

rhythmites are asironomically forced due to che

21,000 yrs periodicity based on the occurrence

of planktonic foraminifers, as also siipported by

Flilgen et al. (1995) and Hilgen & Krijgsman

(1999).

Whatever causes the rhythmites, the presence or

GEODIVERSITAS • 1999 • 21 (4)

605

Cortese G. & Bjorkiund K. R.

Factor 3

Fig. 17. — Factor components through the section (Factor 3).

absence of polycystine radiolarians is a resuit of

changes in the ecological, as well as in the preser-

vational conditions within the Caltanissetta

Basin. Suc et al. (1995) concluded that the

Contrada Gaspa Scaion, constiaited by 108 m

oi sédiments ranging front diatoniitcs to claycy

diatomites, was a rcsult of déposition in a sinall

basin intermittently isolatcd Irom the

Caltanissetta Basin. The Falconara Section, near

to the rim of the Caltanissetta Basin, has a diffe¬

rent lithological structure than the Capodarso

Section, therefote muking corrélations diftlcult.

This makes the Caltanissetta basin an analogue

to modem Nonvegian fjords. Polycystine radiola¬

rians hâve heen shown (Swanberg Bjorklund

1986, 1987) to live and thrive in very landlocked

environments such as l7ords and poils, wherc

they occur in the plankion in concentrations of

c. 10000 radiolarians/m^ scawàtcr. In one poil

the assemblage is almost rnonospccific (Aniphi-

melissa setosa) shuwing a different skeletal nior-

phology than the occanic counterpart period

Bjorklund & Swanberg (1987) suggested tliat in

the warm end of its température range, m the

fjords, the availability of nutrition gave a much

higher grtnvch rate that resulred in smaller and

reticulated forms. while ihe oceanic fornis, in the

cold end of its température range, grew slower

and over a longer rime period, resulting in a lar-

ger and more siHcified skeleton with rounded

Factor 4

Fig. 18. — Factor components through the section (Factor 4).

pores. An analogue is the S. delmontensis in the

Caltanissetta Basin which shows a big variation

in its morpholog)', where we Identified and coun-

ted tour different morphotypes. It is apparent

that in certain parts of the .section, and even in

certain parts within the single diatomites, the

different morphologies of 5. dehnofitensis must be

a response to ecological changes. The ‘'dry-weC

oscillations in the Mediterranean climate and the

enhaneed coniinental run-off (Meulenkanip et

al. 1979) must certainly be kepi in mind.

The high iieritic plankton values are in conflict

with the general undetstanding that radiolarians

are noi abundant in the ncriiic environments. In

the fjord sédiments 1,000 polycystine radiola-

rians/g is a normal value, as the terrigenous input

due to river discharge is high and the microfossil

remains arc very nluch diluted.

The Caltanissetta Basin, if compared with a fjord

situation, must bc of a different magnitude and

structure. Icrrigenous sédiments must bc trap-

ped m near Und “sub-basins" with the possibility

to producc, accumulate and préservé biogenic

sédiments rich in both carbonate and opal

microfossil remains, probably the Caltanissetta

ba-sin was more open than the analogue fiords,

High levels of organic maierial and opal micro-

fossils arc, howcvci, deposited in present day

anoxie basins such as in the Tyro Basin in the

eastern Mediterranean (Bjorklund & de Ruiter

606

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites of Sicily

Factor 7

Fig. 19. — Factor components through the section (Factor 7).

1987) in contrasr to the oxygenated sédiments in

the Mediterranean proper (Caulet 1974) which

are poor in opal microlossils.

The Spurnellaria/Nassellaria ratio lias becn used

as a poceniial lool to discriminace bctwccn

assemblages in ncritic environments (Palmer

1986) whcre spumellarians predominare rhe

plankton, tfs opcn oceanic environments where

nassellarians tend to be rhe dominant group

(McMillan 1979, 1981). Swanbcrg &c Bjorklund

(1987) clearly dcmonsirared chat rhe radiolarian

fauna of Sogndalsfiorden was dominated by early

developmencal stages oï Amphinielissa sp. whtch

compriscd 11%, 39% and 60% of rhe plankton

fauna proceeding from ihc outer to the inner

fjord basin. In nvo orher landlocked basins the

same species made up 91 and 99% of rhe fauna,

This clearly demonstraie.s rbe occuramte of tias-

sellarians with more than 99% in the ncritic

plankton, in opposition to vhe conclusions by

Palmer (1986) and McMillan (1979, 1981), and

does not signal open océan conditions.

If our detailed investigation of ihc S/N ratio in

rhe three different cycles (J'igs 10-12) should bc

interpreted as dcpiciing ncritic and oceanic

conditions, boih D7 and D21 woiild then show

a graduai évolution from nericic to oceanic

conditions as ihey are dominated by spumella-

rians close to the base ol the diatomites, whüe

nassellarians arc increasing towards the top. The

S/N ratio in D28 suggests on the contrary that

this cycle was exclusively depostted in a neritic

environment. We cannot see any direct connec¬

tion beeween the S/N ratio and the neritic vs

oceanic environments (distance from shore), as

interpreted by Palmer (1986), The change in the

S/N ratio is more subject to local ccological

changes within the basin, and noi so much a

resuh of the sites position in relation to the coast

or the open oceanic. Boltovskoy (pers, comm.

1997) also observed that che S/N ratio behaves

incoiisistently on different sédiment types.

Our conclusion i.s therefore that che .S/N ratio in

the .scdiment cannot bc used to discriminatc bet-

ween neritic nt oceanic conditions, mostly as this

ratio is very sensitive to di.ssohition, a common

problem in the hemipelagic province. Locally,

however, (hc S/N ratio can bc a iisefui stratigra¬

phie tool to rccognisc polycystine distribution

patterns, both within and bciwccti cycles in a

section, as wcll as between sections. This bccause

the S/N ratio in thi.s .scénario probably dcpicts

changes and différences in the ccology and in the

production, as well as in the accumulation and

préservation conditions of microlossils.

The diatomites are generally very rich in radiola¬

rians and we tend to condude thaï nuiricnt avai-

lahiliry in lhe basin du ring their formation is

good, probably as a resuit of continental run olf

(Meulenkamp et tfl. 1979). The almosi total lack

of pLmktonic lîfe in the claystone lithologies tn

rhe Capodarso Section (Suc n/il. 1995) indicates

that the absence of siliccous niicrofossils is not

only a resiilr of silica dissolution. Also planktonic

foraminifers are absent or rare, while the benthic

foraminifer fauna is restricted (Suc e/ ai 1995),

indicaiing that an envi ion mental stress is affec-

ting lhe basin. The micro lamination do indicate

periodic anoxie conditions.

Panicularly high values of the factor component

peaks for che final nine factors (higher than

0.400» framed in Table 6) werc used to trace the

most impartant “radiolarian factor peaks'’ throu-

ghout lhe section. The pcalcs (Table 8) are coded

as X.Y, where X represenrs the factor number

and Y represencs a reference nunrber for the “fac¬

tor peaks”> arranged in an ascending order from

base to top of the section.

Some factors (Table 8, e.g., Factor 1) display “16

GEODIVERSITAS • 1999 • 21 (4)

607

Cortese G. & Bjorklund K. R.

factor peaks" (framed values in Fable 6) in diffe¬

rent portions of the section (e.g., from diato-

mites D4 to D34), which bave to be interpreted

as the récurrence of équivalent ecological or

hydrograpliical conditions at dilferent times.

The peak pattern ns presented in Table 8, is our

First atrempt to makc a radiolarian stratigraphie

synthesis of chc FaJconara Section bascd on “fac¬

tor peaks’\ and rhe peak order obviously repre-

sent an évolution ot the radiolarian assemblage as

a response ro changiug eavi'ronments. To use the

peaks as a corrélation tool betvveen our référencé

section (Falconara) and anolher section we hâve

to pick a sequence ot factor peaks from the sec¬

tion we wanr to correlate and look for the samc

peak partern in the référence section. We see chis

technique to be especially useful when corrcla-

ting profiles in the same section where visual cor¬

rélation is difFicult due to tectonism.

CONCLUSIONS

1. In diatomites the number of radiolarians/g bulk

sédiment fluctuâtes between 1,200 (D35) and

169.500 (D26). One diatomite (02) is barren.

2. On a CaCO^ free basas, D26 has a flux of

303.500 radiolarian skclctons/kyear/cm^. A pos¬

sible régional marker for corrélation.

3. In D7 and D2i spiimellarians are dominant

in the lower 10-15% of the diatomites, while

nassellarians dominate the upper parc.

4. In D28 spumellarians dominate the whole

diaromice.

5. The S/N ratio rcflects local ecological changes

(as shown in D28).

6. In claysrones rhe number of radiolaria/g bulk

sedimenr is generally barren or low. Two clay-

stones, Si 8 and Sll, hâve high numbers of

21.500 and 43,000, respectively, and may serve

as a corrélation rool.

7- Sl3 and Sl6 hâve factor component peaks of

0.997 and 0.997 respectively, two claystones thaï

may serve as a régional marker, dominated by an

almost inonospecitic Didynwiyrils sp. (not

Didymoçyrùs peuuliima) itssemblage.

8. S21 bas a factor cOmponent peak of 0.993,

Anthocyrtidium ehrenbergii is the important spe-

cies, and may be a stratigraphical marker.

Acknowledgements

We arc thankful to Dr. J. P. Caulet who reviewed

and made comments that greatly improved the

manuscript.

Dr. G. Cortese would like to thank the following

institutions for the économie support during the

rcaii-sacion of chc manuscript: the PaJcontological

Muséum (University of Oslo), the Norwegian

Research Council (KAS fcilow.ship) and the

Norwegian Acadeiny oi Sciences ihrough the

program "'Nansenfondei og de Dcrmed foibund-

ne fond^\

Prof. K. R. Bjorkiund would acknowlcdge the

support and inspiration provîded by Dr. M.

Marcucci, Dipartimento Scienze délia Terra,

Florence, Iraly. Wc are thankful ro Dr. H. A.

Nakrem for the support and facilitics provided

by the Paleontological Muséum, and for his ins-

pirarion and practical help during tins work.

Tins is the Coiurihuiion number 415 from the

Paleontological Muséum, University of Oslo.

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Submitted for publication on 27 April 1998;

accepted on îî June 1999.

GEODIVERSITAS • 1999 • 21 (4)

611

Radiolarians from the cyclic Messinian diatomites of Sicily

APPENDIX

Table 1 . — The taxa which hâve been identified and counted for the statistical exercise in this study. Literature references are given

to illustrations of the most important taxa.

Taxa References for illustrations

1 Botryopyie sp.

2 Acrobotrys sp. cf. A. disolenia

3 Actinomma sp. cf. A. medianum

4 Actinonma sp.

5 Acf/nomma sp. 1

6 Ampb/rrhopalum sp.

7 Anoms/oaanr/ia dontafa

8 Anfhacyrf/dii/m ohrenbergi

9 Aracbnocoraftim^P-

10 Hymtrfidstrum ap.

11 Boiryosirobus auritus/australis

12 Carpocananum papillosum

13 Carpocanisifum sp.

14 Cenosphaera cristata?

15 Ceftùsphdûra ap. 2

16 Camtncyrfi$ sp.

17 Comiit&Iia proiunda

18 Cyriocapsolhi cyltndroides

1 9 Didymocyrtis sp

20 Euchitonia taicaîa

21 Etjcyrtidium denkowskü

22 Eucyrîidfum bexagonatum

23 Eucyrtidium sp. cl. E. holospira

24 Eucyriidtum puncfatum

25 HekoOiscus astenscus

26 HeUodlscuâ echintscus

27 He.xaœntium drachnoidale

28 Hexacontium pachydermum (big)

29 Htixacaniiüm pachydermum (small)

30 Haxaconttum sp.

31 Hexapyle sp.

32 Hymeniastrum sp.

33 Larcoidsp. 1 (spiral)

34 /.arcorc/sp. 2 (small)

35 Larcoidea sp

36 Larcopyie buetschlii

37 Larcopyh sp.

38 Larcospira quadrangula

39 Lipmaneita sp.

40 Litharachniuni sp.

41 Uthomdfsria Rp. cf. L setosa

42 Uthomitm arachnea

43 Uthûrnitru ap. Cf. L lineata

44 Lophnphaona huntschlii

45 Lophophaena ap.

46 Tetrapyle octacantha

47 PhormosUchoartus corbula

48 Phartiaium pulyciadum

49 Porndiscussp

50 Ptôfocaniumsp.

51 Spcngaster bcrminghami

52 Spongotrochus glacialis

Fig. 20A-E

Petrushevskaya (1981; fig. 495)

Nigrini & Moore (1979; pl. 3, fig. 5)

Nigrini & Moore (1979; pl. 4. fig. 4)

Fig. 21F, J; Nigrini & Lombari (1984; pl. 27, figs 1-2)

Riedel étal. (1985; pL 3, figs 13a-c)

Riedel étal. (1985; pl. 2. fig. 2a)

Fig. 21 K. N; Riedd et ai (1985; pl. 5. fig. 7)

Nigrini & Moore (1979; pl. 21, fig. 3)

Fig. 210, S; Riedel eiat. (1985: pl. 5, figs 2-3)

Nigrini & Moore (1979; pl. 4, figs 2a'b)

Fig. 20B. E. Nigrini & Moore (1979; pl. 4, fig. 3b)

Riedel efa/. (1985: pl 3. fig. 14b)

Fig. 21Q. l; Nignni & Lombari (1984, pi. 22, fig. 1)

Nigrini & Lumbari (1984; pl. 23, fig. 2)

Fig. 2tG, J; Nigrini ^ Moore (1979; pl- 4, fig. 3b)

Nigrini & Lombari (1984. pl. 8. fig. 1)

Nigrini & Lombari (1964; pl, 23, fig. 6)

Nigrini S Lombari (1984; pi. 23, fig. 8)

Petrushevskaya (1981 ; fig. 295)

Fig. 22n. W; Riedel et al. (1974. pl. 62. Fig. 6)

Nigrini & Lombari (1984; pl, 5. Fig. 4)

Riedel étal. (1974. pl. 56, Fig. 5)

Fig. 20D; Hollande & Enjumet (1960, pl. LUI, Fig. 1)

Fig. 20F: Riedel et ai (1985; pl. 1, Fig. 6a)

Fig. 20C; Riedel étal. (1985; pl. 1, Fig. 6c)

Fig. 201; Riedel étal. (1985; pl. 2. Fig. 2b)

Fig. 20K. L

Nigrini & Moore (1979; pl. 17, figs 1a-b)

Riedel étal. (1985; pl. 2. figs 11a-b)

Nigrini A Lnmbnri (1984; pl. 13, Fig. 3)

Riedel étal (1985; pt. 4.,Fig.9)

Fig. 22M. Riedel êt al. (1965, pl, 4, fig.11)

Fig. 22F L; Riedel et ai (1985; pl. 3, fig, 15c)

Riedel étal (1985: pt-5, Fig. 8b)

Fig. 21H. L, M; Riedel étal. (1985; pl. 5, Fig. 8a)

Pelru.shevsknyn (197l, Fig. 58 l-X)

Fig. 210, S

Nigrini & Lombari (1984; pf. 12, Fig. 3)

Nigrini 8 Lomban (1984; pl. 31, Fig. 4)

Nigrini & Lombari (1984; pl. 12, Fig. 1)

Riedel étal. (1985; pl. 2, figs 3-4)

Riedel étal. (1974, pl 60. figs4-6)

Nigrini & Lombari (1984; pl. 9,. Fig. 1)

Nigrini & Lombari (1984; pl. 11, Fig. 2)

GEODIVERSITAS • 1999 • 21 (4)

613

Cortese G. & Bjorkiund K. R.

Taxa References for illustrations

Gig. 20A; Nigrini & Lombari (1984; pl. 11, Fig. 1)

53 Spongotrochus resurgens osculosa

54 Hexalonche sp.

55 Stichocorys delmontensis

56 Stichocorys delmontensis (dwarf)

57 Stichocorys delmontensis (thick)

58 Stichocorys delmontensis (thin)

59 Stichocorys peregrina?

60 Stylochlamydium venustum

61 Stylodictya aculeata

62 Stylodictya îenuispina

63 Stylodictya validispina

64 Stylosphaera angelina

65 Thecosphaera grecoi

66 Theocapsa? cretica

67 Trissocyclidae sp.

68 Zygocircus productus

Fig. 21A-E; Nigrini & Lombari (1984; pl. 25, Fig. 4)

Nigrini & Lombari (1984; pl. 25, Fig. 6)

Fig. 20M; Nigrini & Lombari (1984; pl. 11, Fig. 3)

Jorgensen (1905, pl X, Fig. 41)

Bjorkiund (1976, pl. 4, Fig. 5)

Bjorkiund (1976, pl. 4, fig. 4)

Riedel étal. (1974, pl. 56, fig. 2)

Fig. 20H; Riedel étal. (1974, pl. 56, fig. 3)

Fig. 22T-V Riedel étal. (1985; pl. 4, fig. 15)

Fig. 21T-Y

Nigrini & Lombari (1984; pl. 15, figs 1-2)

614

GEODIVERSITAS • 1999 • 21 (4)

Correse G. & Bjorklund K. R.

Fig. 21. — A-E, Stichocorys delmontensis {D17.1); F, J, Anthocyrtidium ehrenbergi (D20.2): G, I, Cornutella profunda (D17.1);

H, L, M, Lithomitra lineaîa (D4.9); K, N, Botryostrobus auritus/australis (D21.22); O, S, Carpocanistrum sp. (D26.11);

P-R, Lophophaena sp. (D26.11): T-Y, Trissocyclidae sp. (D17.1). Scale bar; 100 pm.

GEODIVERSITAS

W , ï^^-'4^ ’M

[ ■

1 • rnms. - - ,prt" J

i jWüiv ^

kj3»MI.^J£.

Cortese G. & Bjorkiund K. R.

Table 2. — Estimated âge above section base, radiolarian flux, number of radlolarians per gram CaCOg-free sédiment, number of

nassellarians. spumellarians and radioiarians per gram bulk sédiment, Spumellaria/Nassetiaria ratio, CaC 03 and TOC content for

each of the samples collecied during the 1995 fieid-trip (one sample for each lithology)

Sample

Code

Years above

Section base

Flux

in ky/cm*

Rads

gct

Number of

Spum/g

Number of

Nass/g

Number of

Rads/g

S/N

ratio

Percent

CaCO^

Percent

TOC

D36

757000

23698

62123

28553

12437

40990

2.30

50.09

0.100

D35

736000

1351

1447

173

1038

1211

0.17

16.29

0.095

D34

715000

8397

6595

810

5263

6073

0.15

7.92

0.000

D33

694000

108560

269415

107042

33627

140669

3.18

47.79

0.116

D32

673000

27978

37831

14613

5874

20487

2-49

45.85

0,139

D31

652000

48261

55561

23518

20356

43874

1.16

21.04

0.096

D30

631000

3261

4787

1786

2273

4058

0,79

15.22

0,144

D29

610000

8967

8240

2141

4587

6728

0.47

18.35

0 158

D28

589000

61163

73836

19427

14417

33845

1.35

54.16

0.131

D27

567000

24777

41790

7242

5850

13092

1.24

68-67

0 070

D26

546000

303644

256157

95126

74368

169495

1.28

34.34

0.129

D21

525000

57511

71345

14480

20916

35396

0.69

50.39

0.174

S 21

504000

3217

2121

437

1310

1747

0.33

17.64

0.133

D20

399000

46565

45089

12654

10328

22982

1.23

49.03

0.117

S 20

399000

139

155

36.62

0.106

D 19

378000

101764

65397

16756

28966

45722

0.58

30.09

0.120

S 19

378000

17.76

0.069

D 18

357000

31793

64398

20134

32215

52349

0.63

1871

0-115

S 18

357000

15897

34789

9099

12408

21507

0.73

38.18

0.139

D 17

336000

63761

54258

14449

29106

43555

0.50

19.73

0.113

S 17

336000

33.52

0.118

D 16

315000

40402

118495

20516

39013

59529

0.53

49.76

0.129

S 16

315000

23.73

0.063

D 15

294000

110185

109436

22199

46934

69133

0.47

36.83

0.091

S 15

294000

505

500

312

37.68

0.139

S 14

273000

40.49

0.121

D 13

273000

62848

76710

21456

24369

45825

0.88

40.26

0-149

S 13

252000

1598

2033

1463

28.02

0.148

D 12

231000

39217

48788

17328

13017

30345

1.33

37-80

0.144

S 12

231000

24.38

0.115

D 11

210000

54022

43391

7658

24324

31982

0.31

26.29

0.165

S 11

210000

77799

55215

26947

16105

43053

1.67

22.03

0.167

D 10

189000

41511

35230

14907

12836

27743

1.16

21.25

0.150

S 10

189000

16.07

0.112

168000

117065

53363

21005

19977

40982

1.05

23.20

0.166

168000

25.59

0.110

147000

52728

33096

15088

12665

27753

1.19

16.14

0.173

147000

13.67

0.150

126000

124783

50841

15618

27358

42977

0.57

15.47

0.144

126000

609

284

115

230

1.00

18.82

0.172

105000

109467

44065

18243

17761

36004

1.03

18.29

0.105

105000

293

173

122

29.35

0.178

84000

89435

66214

17864

18447

36311

0.97

45.16

0.111

84000

478

306

117

234

1.00

23.64

0.154

63000

45446

34871

13299

10000

23299

1 33

33.19

0.118

63000

30.59

0.070

42000

34.48

0.083

21000

28.94

0.058

21000

190

169

120

29.20

0.166

618

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites of Sicily

Table 3. — Number of nassellarians, spumellarians and radiolarians per gram bulk sédiment and S/N ratio for each of the samples of

diatomite D7. Cycle 7 is 84.9 cm thick, with the diatomite and claystone lîthologies making up 46.9 and 38 cm, respeclively.

Sample

Number

Distance from base

(cm) (%)

Years from base

cycle section

Spum/g

Number of

Nass/g

Rads/g

Spum/Nass

ratio

F97- Dia 7.28

84.9

1.000

21000

147000

13686

21773

35459

0.63

F97- Dia 7.27

82.6

0.973

20431

146431

12306

21632

33938

0.57

F97- Dia 7.26

81.2

0.956

20085

146085

11261

15878

27140

0.71

F97- Dia 7.25

79.7

0.939

19714

145714

13445

20483

33929

0.66

F97- Dia 7.24

78.2

0.921

19343

145343

17670

24537

42207

0.72

F97- Dia 7.23

76.0

0.895

18799

144799

19434

29434

48868

0.66

F97- Dia 7.22

75.1

0.885

18576

144576

14175

18986

33162

0.75

F97- Dia 7.21

73.0

0.860

18057

144057

14725

29126

43851

0.51

F97- Dia 7.20

72.1

0.849

17834

143834

15123

30435

45558

0.50

F97- Dia 7.19

70.3

0.828

17389

143389

15570

26023

41594

0.60

F97- Dia 7.18

68.0

0.801

16820

142820

18945

34892

53837

0.54

F97- Dia 7.17

66.5

0.783

16449

142449

17131

27888

45020

0.61

F97- Dia 7.16

64.8

0.763

16028

142028

27557

33239

60795

0.83

F97- Dia 7.15

63.1

0.743

15608

141608

25047

36622

61670

0.68

F97- Dia 7.14

61.4

0.723

15187

141187

16997

23597

40594

0.72

F97- Dia 7.13

60.4

0.711

14940

140940

24356

33262

57618

0.73

F97- Dia 7.12

59.0

0.695

14594

140594

29529

37059

66588

0.80

F97- Dia 7.11

57.5

0.677

14223

140223

29266

41253

70518

0.71

F97- Dia 7.10

56.0

0.660

13852

139852

21444

34914

56358

0.61

F97- Dia 7.9

54.4

0.641

13456

139456

14881

25794

40675

0.58

F97- Dia 7.8

52.7

0.621

13035

139035

18472

35694

54167

0.52

F97- Dia 7.7

50.2

0.591

12417

138417

17090

39594

56684

0.43

F97- Dia 7.6

48.3

0.569

11947

137947

25338

52196

77534

0.49

F97- Dia 7.5

46.5

0.548

11502

137502

30425

33884

64308

0.90

F97- Dia 7.4

44.8

0.528

11081

137081

28993

24029

53022

1.21

F97- Dia 7.3

43.0

0.506

10636

136636

72072

45195

117267

1.59

F97- Dia 7.2

41.3

0.486

10216

136216

38832

60745

99577

0.64

F97- Dia 7.1

39.6

0.466

9795

135795

49799

36419

86217

1.37

GEODIVERSITAS • 1999 • 21 (4)

619

Cortese G. & Bjorklund K. R.

Table 4. — Number of nassellarians. spumellarians and radiolarians per gram bulk sédiment and S/N ratio for each of the samples of

diatomite D21. Cycle 21 is 74 cm thick, with the diatomite and claystone lithologies making up 64 and 10 cm, respectively.

Sample

Number

Distance from base

(cm) (%)

Years from base

cycle section

Spum/g

Number of

Nass/g

Rads/g

Spum/Nass

ratio

F95- Dia21.0

74.0

1.000

21000

420000

16311

26866

43177

0.61

F95- Dia21.1

73.0

0.986

20716

419716

15772

24497

40268

0.64

F95- Dia21.2

72.0

0.973

20432

419432

15846

24311

40167

0.65

F95- Dia21.3

71.0

0.959

20149

419149

21343

27655

48998

0.77

F95- Dja21.4

70.0

0.946

19865

418865

22346

17318

39665

1.29

F95- Dia21.5

69.0

0.932

19581

418581

15962

21009

36972

0.76

F95* Dia21.6

68.0

0.919

19297

418297

13426

23495

36921

0.57

F95- Dia 21.7

67.0

0.905

19014

418014

16762

19810

36571

0.85

F95- Dia 21.8

66.0

0.892

18730

417730

11816

24378

36194

0.48

F95- Dia 21.9

65.0

0.878

18446

417446

18607

16895

35502

1.10

F95- Dia 21.10

64.0

0.865

18162

417162

15256

22692

37949

0.67

F95- Dia 21.11

63.0

0.851

17878

416878

16951

19723

36674

0.86

FOS* Dia 21.12

62.0

0.838

17595

416595

10808

17795

28603

0.61

F95- Dia 21.13

61.0

0.824

17311

416311

17584

21292

38876

0.83

F95- Dia 21.14

59.5

0.804

16885

415885

10758

23182

33939

0.46

F95- Dia 21.15

58.0

0.784

16459

415459

11364

23529

34893

0.48

F95- Dia 21-16

56.5

0.764

16034

415034

16412

23282

39695

0.70

F95- Dia 21.17

55.0

0.743

15608

414608

11944

25833

37778

0.46

F95- Dia 21.18

53.5

0.723

15182

414182

10976

23018

33994

0.48

F95- Dia 21.19

52.0

0.703

14757

413757

8411

19938

28349

0.42

F95- Dia 21.20

50.5

0.682

14331

413331

12791

33866

46657

0.38

F95- Dia 21.21

49.0

0.662

13905

412905

12431

27901

40331

0.45

F95- Dia 21.22

47.5

0.642

13480

412480

14480

20916

35396

0.69

F95- Dia 21.23

46.0

0.622

13054

412054

10853

21318

32171

0.51

F95- Dia 21 24

44.5

0.601

12628

411628

11887

22304

34191

0.53

F95- Dia 21.25

43.0

0.581

12203

411203

15833

27024

42857

0.59

F95- Dia 21.26

41.5

0.561

11777

410777

13523

13295

26818

1.02

F95- Dia 21.27

40.0

0.541

11351

410351

12529

14988

27518

0.84

F95- Dia 21.28

38.5

0.520

10926

409926

10684

13355

24038

0.80

F95- Dia 21 29

37.0

0.500

10500

409500

10462

14402

24864

0.73

F95- Dia 21,30

35.5

0.480

10074

409074

14321

18272

32593

0.78

F95- Dia 21 31

34.0

0.459

9649

408649

13921

16241

30162

0.86

F95- Dia 21,32

32.5

0.439

9223

408223

13079

16898

29977

0.77

F95- Dia 21 33

31.0

0.419

8797

407797

13270

14692

27962

0.90

F95- Dia 21.34

29.5

0.399

8372

407372

16085

22569

38653

0.71

F95- Dia 21 35

28.0

0.378

7946

406946

15179

13616

28795

1.11

F95- Dia 21.36

26.5

0.358

7520

406520

19036

21687

40723

0.88

F95- Dia 21-37

25.0

0.338

7095

406095

15556

14198

29753

1.10

F95- Dia 21.38

23.5

0.318

6669

405669

18750

17428

36178

1.08

F95- Dia 21.39

22.0

0.297

6243

405243

18810

19881

38690

0.95

F95- Dia 21.40

20.5

0.277

5818

404818

35455

21932

57386

1.62

F95- Dia 21.41

19.0

0.257

5392

404392

30383

26077

56459

1.17

F95- Dia 21 42

17.5

0.236

4966

403966

34852

23517

58369

1.48

F95- Dia 21 43

16.0

0.216

4541

403541

34709

14071

48780

2.47

F95- Dia 21 44

14.5

0.196

4115

403115

46758

29371

76130

1.59

F95- Dia 21.45

13.0

0.176

3689

402689

44615

41868

86484

1.07

F95- Dia 21.46

11.5

0.155

3264

402264

48364

42545

90909

1.14

F95- Dia 21.47

10.0

0.135

2838

401838

41189

72687

113877

0.57

620

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites of Siciiy

Table 5. — Number of nassellarians, spumellarians and radiolarians per gram bulk sédiment and S/N ratio for each of the samples of

diatomite D28. Cycle 28 is 95.7 cm thick, with the diatomite and claystone lithologles maklng up 49.7 and 46 cm, respectively.

Sample

Number

Distance from base

(cm) (%)

Years from base

cycle section

Spum/g

Number of

Nass/g

Rads/g

Spum/Nass

ratio

F97- Dia 28.36

95.7

1.000

21000

588000

6911

256

7167

27.00

F97- Dia 28.35

94.2

0.984

20671

587671

5876

100

5976

59.00

F97- Dia 28.34

92.5

0.967

20298

587298

5753

105

5858

55.00

F97- Dia 28.33

91.1

0.952

19991

586991

3035

160

3195

19.00

F97- Dia 28.32

89.9

0.939

19727

586727

4006

148

4154

27.00

F97- Dia 28.31

88.8

0.928

19486

586486

3482

418

3900

8.33

F97- Dia 28.30

87.6

0.915

19223

586223

5307

5390

64.00

F97- Dia 28.29

85.5

0.893

18762

585762

3765

235

4000

16.00

F97- Dia 28.28

84.0

0.878

18433

585433

3282

290

3571

11.33

F97- Dia 28.27

82.3

0.860

18060

585060

4340

362

4702

12.00

F97- Dia 28.26

80.6

0.842

17687

584687

3623

580

4203

6.25

F97- Dia 28.25

79.4

0.830

17423

584423

4364

285

4649

15.33

F97- Dia 28.24

77.7

0.812

17050

584050

3583

489

4072

7.33

F97- Dia 28.23

76.7

0.801

16831

583831

2490

1452

3942

1.71

F97- Dia 28.22

75.7

0.791

16611

583611

5724

818

6542

7.00

F97- Dia 28.21

74.3

0.776

16304

583304

5889

1501

7390

3.92

F97- Dia 28.20

73.0

0.763

16019

583019

8918

2778

11696

3.21

F97- Dia 28.19B

72.0

0.752

15799

582799

3101

1163

4264

2.67

F97- Dia 28.19A

70.8

0.740

15536

582536

6393

2295

8689

2.79

F97- Dia 28.18

69.8

0.729

15317

582317

5938

3438

9375

1.73

F97- Dia 28.17

68.7

0.718

15075

582075

7943

3010

10953

2.64

F97- Dia 28.16

67.4

0.704

14790

581790

7177

3589

10766

2.00

F97- Dia 28.15

66.3

0.693

14549

581549

6377

3050

9427

2.09

F97- Dia 28.14

64.9

0.678

14241

581241

8701

3016

11717

2.88

F97- Dia 28.13

63.7

0.666

13978

580978

12808

4803

17611

2.67

F97- Dia 28.12

62.5

0.653

13715

580715

19118

5042

24160

3.79

F97- Dia 28.11

61.5

0.643

13495

580495

21261

6944

28205

3.06

F97- Dia 28.10

60.4

0.631

13254

580254

18448

4580

23028

4.03

F97- Dia 28.9

58.5

0.611

12837

579837

17108

11153

28261

1.53

F97- Dia 28.8

57.2

0.598

12552

579552

18689

8611

27299

2.17

F97- Dia 28.7

55.9

0.584

12266

579266

33293

15865

49159

2.10

F97- Dia 28.6

54.7

0.572

12003

579003

36830

18192

55022

2.02

F97- Dia 28.5

53.3

0.557

11696

578696

27660

13032

40691

2.12

F97- Dia 28.4

52.2

0.545

11455

578455

41333

10917

52250

3.79

F97- Dia 28.3

50.5

0.528

11082

578082

42285

12725

55010

3.32

F97- Dia 28.2

49.1

0.513

10774

577774

35327

8323

43650

4.24

F97- Dia 28.1

47.1

0.492

10335

577335

41444

10444

51889

3.97

GEODIVERSITAS • 1999 • 21 (4)

621

Cortese G. & Bjorklund K. R.

Table 6. — Varimax Faclor Components Matrix {Samples vs Factors).

Samples

Factor 1

Factor 2

Factor 3

Factor 4

Factor 5

Factor 6

Factor 7

Factor 8

Factor 9

D36

0.082

0.724

0.078

-0.016

0-418

0-398

0.049

0.059

0.074

D35

0.007

0.149

0.009

-0.011

-0 003

0.904

-0.003

-0.011

-0.004

D34

0.858

0.175

0.092

-0.011

-0.079

-0.Ô34

-0.001

0 425

-0 036

D33

0.043

0.423

0.048

-0.013

0.883

-0,021

0.092

-0.035

-0.003

D32

0.089

0.842

0.092

-0.029

0.489

0.044

0.091

0.042

0.093

D31

0.505

1 0.785_,

0.134

-0.025

0.223

0.048

0.021

-0.155

0.157

D30

0.111

0.894 i

0.108

0.247

-0.140

0.109

0.001

0.131

0.033

D29

0.115

0.863

0.043

-0.052

-0 113

-0.113

0.005

0.403

•0.010

D28

0.207

0.672

0.032

-0.062

0.024

-0.229

0.026

-0.281

-0 233

D27

0 122

0901

0.124

0.003

-0.086

0.247

0.043

-0.094

Û.Û31

D26

0.158

0.793

0.063

0.274

0.271

0.050

0.053

0.427

-o.on

D21

0-623

0.265

0,066

-o.on

-0.043

0.018

0.083

-0.003

0.708

S21

0.008

0.074

0.010

-0.001

0.086

0.005

0-993

0-003

0.034

D20

0.133

0.832

0.121

-0.026

0.263

0.052

0.048

-0.419

0.035

D19

0.976

1 0.141

0.120

-0.007

-0.013

0.000

0.010

-0.084

-0.073

D18

1 0.981

0.036

0.124

0.005

-0.036

0.045

0.009

-0.072

-0.003

S18

0.964

0.099

0.133

0.004

0.024

0043

0.046

-0.109

-0.016

D17

0.958

0.197

0.138

-0.007

0.040

-0,001

0.027

-0.115

-0.035

D16

0.226

0.097

0.965

0.005

0.049

0.012

0.003

-0.070

0.009

S16

0.039

0.045

0.004

0.997

0.004

-0.017

0.000

-0.006

D15

0,695

-0.105

0.698

0.005

0.068

0.000

0.006

0 083

0-022

D13

0.978

0.059

0.108

0.011

0.118

0.037

0.016

0 070

0.079

S13

0.002

0.Q50

-0.005

0.997

0.004

•0013

0.007

0.009

-0.006

D12

0,022

0.508

0.807

-0.005

-0.146

0.001

0.002

-0.087

0.139

D11

' 0.633

-0.109

0.755

0.004

0.024

•0.011

0.005

0.079

-0.026

0.960

0.030

0.101

0.074

0.182

0.072

0.013

0.098

-0.002

D10

>0.069

0,115

0.982

0.000

0.109

•0.011

0.001

-0.021

0.018

0.870

0.259

0.110

-0.010

0.010

0.013

0.011

-0.045

0.398

0.121

0.800

0.065

-0.041

0.171

-0 112

0-019

-0.008

0 499

0.984

0112

0.122

-0.005

0.053

0.008

0.014

0.012

0.014

0.934

0.226

0.116

-0.012

-0.043

-0.023

0.011

-0.115

0.200

0.448

0.113

0.876

0.001

0052

0021

0.017

0.116

0.038

0_,876

, 0.206

0.321

-0.004

0.111

0.082

0.042

0.176

0.079

Var.

35,414

22,699

14,255

6,486

4.792

3,507

3,110

2.951

3,304

Cum. Var.

35,414

58,113

72,368

78,854

83,646

87,153

90.263

93,215

96,519

Table 7. — Scaled Varimax Factor Scores Matrix (Species vs Factor Scores). Absolute values of factor scores higher than one hâve

been outlined.

Factor 1

Factor 2

Factor 3

Factor 4

Factor 5

Faclor 6

Faclor 7

Factor 8

Factor 9

Anthocyrtidium ehrenbergi

-0.037

-0.048

0.000

0.011

-0.262

-0.014

3.111

0.018

0.065

Botryostrobus auritus/australis

0.183

0.264

-0.088

-0.058

-0.209

-0.488

-0.030

-0.300

3.360

Carpocanistrum sp.

0.000

0.060

0.005

-0.002

0.309

0.012

1.819

0.036

•0.073

Cenosphaera sp. 2

-0.005

-0.024

-0.012

-0.016

-0.164

1.939

-0.014

-0 197

-0,016

Didymocyrtis sp.

0.006

0.147

-0.031

1 3.595

0.013

-0.065

-0.010

0.020

-0.026

Lâfcoidea sp.

0.169

2.160

0.198

0.002

-0.220

1 116

0.046

0.705

0.465

Utbomeiissa L se/osa

0.266

1.239

-0.136

-0.224

-0.599

-1.082

0.003

-0.767

1.197

Lithomitra sp. et. L Uneaîa

-0.376

-0.307

3.547

0.022

-0.010

-0.093

•0-009

0 176

0.034

Porodiscus sp.

0.068

1.282

0.151

-0.077

3.249

-0.164

0.059

-0.349

•0.027

Spongotraebus gtadalis/osculosa

0.066

1.472

0051

•0.102

-0.724

-0.602

-0.068

2.540

-0.168

Stichocorys delmontensis

3.635_j

-0.509

0.316

0.018

0.161

0,099

0 032

0.298

-0.087

Theocapsa 7 cretica

-0.050

0.095

-0.014

-0.033

•0.046

2484

•0.021

0,029

■0.095

TrissocycOdae sp.

0.459 1

1.591

0.473

0.018

-1.118

-0.002

-0.009

-2.256

-0.089

622

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from the cyclic Messinian diatomites of Sicily

Table 8. — Factor component peaks (values higher (han 0.400) used to establish the most important “radiolarian factor peaks" throu-

ghout the section. The peaks are coded as X.Y, where X represents the factor number and Y represents a reference number for the

“factor peaks”. arranged in an ascending order from base to top of the section.

Samples

Factor

Peaks

Factor

Component

Sapropel

Age (Ma)

Diatomite

Age (Ma)

Astro.

âges

Tripoli

Cycles

D36

2.12

0.724

6.183

S36

6.194

6.132

T43

D35

6.1

0.904

6.204

S35

6.215

6.145

T42

D34

1.16

0.858

6.225

8.4

0.425

S34

6.236

6.164

T41

D33

2.11

0.423

6.246

5.2

0.883

S33

6.257

6.184

T40

D32

2.10

0.842

6.267

5.1

0.489

S32

6.278

6.205

T39

D31

1.15

0.505

6.288

2.9

0.785

S31

6.299

6.226

T38

D30

2.8

0.894

6.309

S30

6.320

6.257

T37

D29

2.7

0.863

6.331

8.3

0.403

S29

6.342

6.278

T36

D28

2.6

0.672

6.352

S28

6.363

6.299

T35

D27

2.5

0.901

6.373

S27

6.384

6.320

T34

D26

2.4

0.793

6.394

8.2

0.427

S26

6.405

6.342

T33

D26

S25

T32

D24

S24

6.373

T31

D23

S23

6.393

T30

D22

S22

6.413

T29

D21

1.14

0.623

6.499

9.2

0.708

S21

7.1

0.993

6.510

6.432

T28

D20

2.3

0.832

6.520

8.1

-0.419

S20

6.531

6.452

T27

D19

1.13

0.976

6.541

S19

6.552

6.470

T26

D18

1.12

0.981

6.562

S18

1.11

0.964

6.572

6.490

T25

D17

1.10

0.958

6.583

S17

6.594

6.509

T24

D16

3.6

0.965

6.604

S16

4.2

0.997

6.614

6.524

T23

GEODIVERSITAS • 1999 • 21 (4)

623

Cortese G. & Bjorklund K. R.

Samples

Factor

Peaks

Factor

Component

Sapropel

Age (Ma)

Diatomite

Age (Ma)

Astro.

âges

Tripoli

Cycles

D15

1.9

0.695

6.625

3.5

0.698

S15

6.636

6.544

T22

D14

S14

6.563

T21

D13

1.8

0.978

6.667

S13

4.1

0.997

6.678

6.585

T20

D12

2.2

0.508

6.688

3.4

0.807

S12

6.699

6.606

T19

D11

1.7

0.633

6.709

3.3

0.755

S11

1.6

0.960

6.719

6.635

T18

D10

3.2

0.982

6.730

S10

6.741

6.657

T17

1.5

0.870

6.751

6.762

6.678

T16

2.1

0.800

6.772

9.1

0.499

6.783

6.699

T15

1.4

0.984

6.793

6.804

6.721

Tl 4

1.3

0.934

6.814

6.825

6.752

Tl 3

1.2

0.448

6.835

3.1

0.876

6.846

6.771

T12

1.1

0.876

6.856

6.867

6.792

T11

6.877

6.888

6.810

T10

6.898

6.909

6.829

6.919

6.930

6.847

624

GEODIVERSITAS • 1999 • 21 (4)

Taxonomie study of Ordovician (Llanvirn-

Caradoc) Radiolaria from the Southern Uplands

(Scotland, U.K.)

Taniel DANELIAN

Department of Geology and Geophysics.

The University of Edinburgh, West Mains Road, Edinburgh EH9 3JW (U.K.)

Laboratoire de Micropaléontologie,

Université Pierre et Marie Curie, CNRS-ESA 7073,

C. 104, T. 15-25, 4 place Jussieu, F-75252 Paris cedex 05 (France)

danelian@ccr.jussieur.fr

KEYWORDS

Radiolaria,

Ordoviciaa,

Llanvirn,

Caradoc,

Southern Uplands,

Scotland,

United Kingdoni,

laperas Océan,

Caledonides,

radiolarian chert.

Danelian T. 1999. — Taxonomie study of Ordovician (Llanvirn-Caradoc) Radiolaria from the

Southern Uplands (Scotland. U.K.), in De Wever P. & Caulet J.-P. (eds), InterRad VIII.

Paris/Blerville 8-13 septembre 1997. Geodiversitas 21 (4) :625 ‘635.

ABSTRACT

Over 100 years ago, Hinde (1890a, b) described Radiolaria in thin sections

from Ordovician chert.s of the Southern Uplands of Scotland and established

for the First time the presence of the group in the Early Palaeozoic.

Radiolarians from the Southern Uplands hâve now been successfully cxtrac-

tcd by hydrofluoric acid ieaching and the systematic palaeontolog)^ ot some

of the yieldcd morphorypes is discusscd herein. The studied fauna corne

from two outerops of radiolarites: one at upper Hawkwood Burn and the

orher north-west of the village of Crawford. Amongst the radiolarians cxtrac-

red from the latter ourcrop, the généra Imnihlguttii and Prdtoccratoikiscum

are common. The presence of the spccies hianihiguttti diffusa (Hinde),

Inanibigiitîa (?) minuta Wang and înanihigutta sp. cf. verrucultt (Nazarov)

allows the corrélation of the Crawford fauna with ihc Haplcntactinm juncta-

Jnanigîitta unica assemblage in Nazarov s (1988) biozonation, of upper

Llanvirn (Llandeilian)-Caradoc âge, and with the assemblage documenred by

Wang (1993) in China, of earliest Caradoc âge.

GEODIVERSITAS • 1999 • 21 (4)

625

Danelian T.

MOTS CLÉS

Radiolairfs,

Ordovicien,

Llanvirnicn,

CamdoaVn,

l.cojwe.

Royaume Uni,

radîolarites,

Océan lapetus,

Calédonides.

RÉSUMÉ

Etude taxonomique des radiolaires ordoinciens (Llanvirnien’Caradocien) de

Southern IJplands (Écàsse^ R. U.).

Des radiolaires ordoviciens ont été extraits à l’acide fluorhydrique des radio-

larites de Tunicé structurale des Southern Uplands en Écosse. Étudiés en

lame-mince il y a plus d’un siècle (Hinde b) ceux-ci oui servi comme

témoin de la présence certaine de ce groupe dans Je Paléo/oiquc inferieur. La

faune ici étudiée vient de deux affleurements: riin des radiol.iikcs rouges

brunâire.s à Hawkvvood Burn, l'autre des radiolaritcs grises qui affleurent au

nord-ouest du village de Crawfdrd. La paléontologie sysrémariqiie de cer¬

taines formes intéressantes est ici discutée. Les genres Inanihtgutra et

Protoceratoîkiscum sont communs parmi les radiolaires extraits des radiol.i-

rites de Crawford. La présence des espèces Inanibigutta dijfusa (Hinde)»

fnanihigutta (?) minuta Wang et Inanibigutta sp. cf. verrucula (Na^arov)

permet la corrélation de la faune de Crawfoid avec l’association

Haplenracîintd junaa-Inaniguna unica de la biozonation de Nazarov (1988),

d’âge Llanvirnien supérieur (Llandeilien)-Caradocien, ainsi qu’avec l’associa¬

tion décrite par Wang (1993) en Chine, d’âge Caradocien basal.

INTRODUCTION

Despite significant improvements in our under-

standing of Palaeoxoic Radiolaria over the last

35 years, Early Palaeo/oic assemblages are still

poorly documented (Noble Sc Aîtehison 1995).

As a rcsiilr, our knowledge of the early stages of

évolution of ihi.s significant planktonic group

remains limitcd, 1 he oJdest radiolarian fossils

corne from late Cambrian shallow-water lime-

stones ol China» front which one species bas

been reccntly described (Dong et al. 1997).

Diversification markedly increased during the

Ordovician and from the limited work that has

been donc so far, it is clear thaï radiolarian cvolu-

tionary change during ihis time was more rapid

than prcvioLisly bclieved (Renz 1990). The group

has thereforc rhe potential co bccomc a valuable

biostratigraphic tool for chc yct poorly explorcd

Early Palaeozoic interval, with an increasing

number of easily identifiable, diagnostic taxa

(Aitchison ôé Noble 1997; Aitchison 1998;

Aitchison et ai 1998).

There are relanveiy few localities in the world

where well-preserved Ordovician assemblages are

known and most of them represent carbonate

platform/slope environments (Fortey ôé

Holdsworrh 1971; Nazarov Popov 1980:

Webby èic Blom 1986; Renz 1990; Wang 1993).

Radiolaria of oceanic affinitv are common, but

less wcll picservcd, in rocks of deep water origin

such as radiolarites (ribbon radiolarian cherts

with shaly intcrvals) which are ofren associated

with remnants ot oceanic crust in accretionary

prisms of ancient subduction zones. Thcy reflect

rhe significant biogeocheinical rôle that

Radiolaria staried to play in the océans (i.e. the

silica q^cle) from the Early Palaeozoic.

rhe occurrence of r.tdiolarians in cherts of the

Southern Uplands terrane (Fig. I ) has been

known for over a ccncury. It was on material

from this région that Hinde (1890a, b) first esta-

blishcd the definite presence of Radiolaria in the

Early Palaeozoic. Outerops of radiolarian cherts

were extensivdy discussed by Peach & Home

(1899), wlio were responsible for a major map-

ping compilation of tho goology of Southern

Scotland. Radiolaria from the Southern LIplands

hâve also been reported by Nicholson (1889)

and Smith (1900). The techniques available at

626

GEODIVERSITAS • 1999 • 21 (4)

Taxonomy of Ordovician Radiolaria from the S. Uplands

Fjg. 1. — Geological outline of the Southern Uplands. Based on McAdam étal. (1993).

that time only allowed for study of Radiolaria in

thin section, which provided very lirnited infor¬

mation on iheir morpliology. Tliis wa.s naturally

the case for the single previous taxonomie work

of Radiolaria trom the Southern Uplands (Hinde

1890b) in which 23 new spccics wcrc described.

Recügnising rhe potential of ladiolarian studics

in the Southern Uplands, a number of radiolar-

ian chcrc outerops hâve alteady been examined

and the results briefly reported (Danelian &

Clarkson 1998). This paper foenses on the syste-

marie study of sonie of the yicldcd morphotypes

based on modem radiolarian taxonojny (e.g.,

Nazarov & Popov 1980; Nazatov 1988). It

attempis to link matrix-free forms to the species

described originally by Itinde and to gradually

build a detailed and integrated picture of the

radiolarian assemblages occuring in these historic-

ally important Scottish localities.

graptolite

zones

conodont

zones

greywacke

LEADHILLS

SUPEHGROUP

Bur.

" MOFFAT

Aur.

gracilts

SHALE

GBOUF»

ansennus

Llandeil.

Aber.

Fenn.

? ^

Whit.

radiolarite

0 V a e

■ ^

Mor.

lava

Fig. 2. — Simplified stratigraphy for the Lower-Middle

Ordovician of the Southern Uplands. focusing on the Crawford

Group. Lithostratigraphic terminology according to Floyd (1996).

Chronostratigraphy and biostratigraphy from Fortey et al.

(1995).

GEODIVÊRSITAS • 1999 • 21 (4)

627

Danelian T.

Fig. 3. — Geological map of the studied localities. A, north-west of the village of Crawford ^after Leggett & Casey 1980); B, at

Hawkwood Burn (after Clarkson étal. 1993).

STRATIGRAPHICAL FRAMEWORK

The Southern Uplands consist largely of

Ordoviciiin and Silurian sedimenrary rocks of

deep-w:Uer origin. The oldest rocks at ihe base of

the succession are composed mainly of basaltic

lavas, radiolarian chcjts and siliceous mudstoties.

A formai lithostratigraphy for the Ordovidan has

recently been defined by Floyd (1996). The lavas

and radiolarites are part ol the Crawford Group

of Arenig-Llanvirn âge (stfuu Fortey étal. 1995),

although based on recent conodont evidence the

Group probably extends into ihc Caradoc

(Armstrong al. 1990, 1996). The overlying

graptoliiic shalcs of the Moffat Shale Group

(Caradoc-LUndovery) are in turn succeeded by

the greywackc successions of the Leadhills

Supergroup (Fig. 2).

üntil rccendyv che varions outerops of radiolarian

cherts in the Southern Uplands were considered

as being part of a single concinuous stratigraphi-

cal sequence, spanning the Arenig and Llanvirn,

and ovcrlain by the early Caradoc [Nemagiaptus

gradlis graptoliie biozone) Moffat Shale Group

(Leggett 1978, 1987), However Armstrong rr rfA

(1996), after an extensive révision, suggested thar

radiolarian cherts could reprc.sent rwo distinct

sedimenrary events: one during ihc mid Arenig

{Oepikodus evae conodont biozonc), and onc of

latest Llanvirn to earliest Caradoc âge {Pygodus

anserinus conodont biozone).

BIOSTRATIGRAPHICAL DISCUSSION

The fauna discussed herein were extracred from

two chert samples, onc from an outerop along

the lowcr part of a trackside cutting, north-west

of the village of Crawford (National Grid

Référencé NS 941 215; Figs 1, 3A) and che other

from radiolarites cropping oui at upper

Hawkwood Burn (NS 972 248), a cributary of

the Wandei Burn (Figs 1, 3B). Samples were pro-

cesscd with the laboratory technique of hydro-

fluoric acid (Dumitrica 1970; Pessagno &

Nowport 1972).

At Hawkwood Burn, the r;tdiolarian cherts are of

red-brownish colour and were recently descrihed

by Clarkson et al. (1993). From the base of thèse

cherts a conodont launulc of lare Llanvirn

(Llandeilian)-earliest Caradoc âge was reponed

(Armstrong 1990, 1996). Alrhoiigh nidiola-

rian préservation here does not allow any confi¬

dent identification of established species, the

fauna seem to be comparable lo rhe Haplentac-

thiia juncta'InanigHtta unicn assemblage of

Nazarovs biozonation (Llandeilian-Caradoc;

Nazarov 1988; Nazarov & Ormiston 1993),

which i.s consistent with the age given on the

basis oi conodonts..

In the second locality, ncar the village of

Crawford, the radiolarites are mainly greeni.sh-

grey in culour. No biostratigraphic data other

than that provided by the radiolarians exist for

628

GEODIVERSITAS • 1999 • 21 (4)

Taxonomy of Ordovician Radiolaria from the S. Uplands

the âge of this oiitcrop. The presence of the

genus Protoceratoikiscum is important because it

suggests a Llanvirn-Caradoc iiiterval {sensu

Fortey et ai 1995) as a First approximation for

the âge of these chcrts (Daiiclian & Clakson

1998). lhe présence of ihe specLes Inanibigutta

diffiisay established hercin (Fig. 4A-D), now

allows the corrélation of tlic Crawford tauna

vvith lhe Haplentiictinia junvta-lnanigutta unica

assemblage of Nazarov’s biozonation of late

Llanvirn (Llandeilian)-Caradoc agc. Morcover,

the identification of Inünlhigutîa (?) minuta

(Fig. 4F-G) and inanibigutta sp. cf. /. vetrucula

(Fig. 4H) allows tfie corrélation of the Crawford

assemblage with the one docuinented by Wang

(1993) from the Pingliang Formation, dated as

of carliest Caradoc âge (commun interval be-

tween the N. gracilis and P. anserinus biozones).

SYSTEMATIC PALAEONTOLOGY

Subclass RADIOLARIA Muller, 1858

Superorder POLYCYSTINA Ehrenberg, 1838

entend. Ricdel, 1967

Order SPUMELLAHIA Ehrenberg, 1857

Family InaniguTTIDAE

Nazarov & Ormiston, 1984

Genus Inanibigutta Nazarov, 1988

Inanibigutta Nazarov, 1988: 56. — Nazarov &

Ormiston 1993: 35.

Typf SPECIRS. — Entactinosphaera aksakensis Nazarov,

1975.

Inanibigutta diffusa (Fïinde, 1890b)

(Fig. 4A-D)

Suutroplegtna diffiLKum Hindt, 1890b: 50, pl. 4, fig. 4.

Entactinosphaera ? diffusa (Hinde) - Nazarov Popov

1980: 37, 38, rexi-hg. 16, pL 2, fig. 4, pl. 13, fig. 8.

Inanibigutta dijftisa (blinde) - Nazarov 1988, fig. 31.

OcCL’RKENCF.. — Middic Ordovician (l.landcilan lo

Lower Caradoc) Bestomakskaya Suite, Eastern

Kazakhstan, southwestern foothills of the Chingiz

Range, Chagaii River (Nazarov & Popov 1980);

Broughron Hcights, Peehlcshire, Southern Uplands

(Hinde 1890b); grey radiolarites of the Crawford

track, Southern Uplands, this study.

MEASURëMENT.S (one specimen). — Diameter of che

flattened part of the outer shell, 133-136 pm: dianic-

cer ol rhe elongated part of the outer .shell, 152-

154 pm; length of main spines, 40-50 pm; diameter

of inner shell, 63-66 pm.

Description

A nearly spherical outer shell bearing six radia-

ting main spines positioned with hexagonal sym-

metry. The outer shell is perforated by circulât to

oval pores of varions dimensions. The main

spines are robust. rod-like, and gently tapering

distally. They are almost half che length of the

diameter of che outer shell. A nuniber of needle-

like sccondary spines cover ihc surface of rhe

outer shell. The inner shell is relarively small,

perforated and linked to the outer .shell through

radial beams that continue as main spines out-

side the outer shell. Its position is eccentric in rela¬

tion to the center of the outer shell (Fig. 4C-D).

Remarks

The eccentric position of the inner shell was

pointed out by Nazarov (/// Nazarov & Popov

1980) and can be observed on the holotype illus-

traced by Hinde (1890b), which is obviously a

section through an équatorial plan encompassing

four s'pines. Only one specimen in our sample

was identifiable with certamty. NeverchelesSj

several orher naturally broken but incomplète

specimens may bclong to this species (Fig. 4E).

The dimensions of our specimen correspond pre-

cisely co the ones ineasured by Hinde (1890b).

However, Nazarov (in Nazarov & Popov 1980)

accepted a largcr variabÜicy of sîze for this spe¬

cies, especially as far as the length of spines ïs

concerned. The latrer author also mencioned that

a spongiform texture was observed on the outer

shell of somc of his specimens from Kazakhstan.

Inanibigutta (?) minuta Wang, 1993

(Fig. 4F-G)

Inanibigutta minuta Wang, 1993: lÜO, pl. 6, figs 9-

12 .

Occurrence. — Middle part of the Pingliang

Formation, Gansii Province, China (Wang 1993);

grey radiolarites of the Crawford track, Southern

Uplands, this study.

GEODIVERSITAS • 1999 • 21 (4)

629

Danelian T.

Fig. 4. — Scanning électron micrographs of radiolaria extracted from cherts of the Southern Uplands. A-D, Inanibigutta diffusa

(Hinde), different views of the same specimen; C-D, view of Internai structure after the Shell was broken with a razor:

E, ? Inanibigutta diffusa (Hinde); F-G, Inanibigutta (?) minuta Wang; H, Inanibigutta sp. cf. /. verrucula (Nazarov): I. Inanibigutta sp.

cf. I. aksakensis (Nazarov); J, Inanibigutta (?) sp. A. Scale bar: A, 82 pm; B, 89,5 pm; C, 106 pm; D, 70 pm; E, 76 pm; F. G, 94 pm;

H, 124 pm; I. 83 pm; J, 129 pm.

630

GEODIVERSITAS • 1999 • 21 (4)

Taxonomy of Ordovician Radiolaria from the S. Uplands

Remarks

The observed morphotypes are identical to

Inanibigiitta minuta as described and illustrated

by Wang C1993). They possess nearly spherical

outer shellswith nunierous sccondary spines, dis-

tally tapcring main spines with apophyses in

their proximal pan and both the outer shell and

main spines hâve appropriate dimensions. Never-

theless, the attribution of this species to Inanibi'

gutta is questionable because in neither the

type-series (holotype and paratypes), nor in our

material has the exact number of main spines

cvcr bccn observed.

Inanibigiitta sp. cf. L VeiTucula

(Nazarov in Nazarov &L Popov, 1976)

(Fig. 4H)

Entactinosphacra verrucula Nazarov in Nazarov &

Popov, 1976: 408-409, fig. id. — Nazarov & Popov

1980: 38-39, texr-fig. 17, pl. 3. fîg. 6, pl. 11, fig. 6.

Inanthigutta verrucula (Na/.arov) — Nazarov 1988,

fig. 31. — Wang 1993: 100, pl. 6, figs 2-3, 5-8.

OcrURRHNCH. — Middle part of the Pingliang

Formation, Gansu Province, China (Wanç, 1993);

grey radiokrites of ihe Crawford track, Southern

Uplajids, thb .siudy.

Remarks

The illustrated specimen is comparable to /. ver-

rucula as described originally by Nazarov (1976).

The spherical outer shell (diamcter: 185 pm) is

perforated by angular to subanguLir pores and

bears short conoidal sccondar)'^ spines, as wcll as

main spines (length of intact spine: 174 pm).

Mowever, it ddfers as main spines are capering

rather than cylindrical and apophyse.s tend to be

clustercd ncar the proximal part of the spines.

My material rescmbtes Wang s (1993) spccimens

in ail respects, d'his species can bc distinguished

from L (?) minuta Wang by the larger size of its

outer shell, of diameter usually grcatcr than

180 pm, and by the longer main spines

(> 150 pm).

Inanibigutta sp.

cf L aksakensis (Nazarov, 1975)

(Fig. 41)

Entactinosphaera aksakensis 1975: 68, pl. 16,

figs 4-8, pl. 21, fig. 1 (noc 2). - Nazarov & Popov

1980: 35, 36, text*fig. 15a-b, pl. 3, figs 8, 9, pl. 8,

fig. 6, pl. 1 K figs 8, 9.

Inanibigutta aksakensis (Nazarov) — Nazarov 1988,

tcxt-lig. 17, pl. 10. fig. 7-8. — Nazarov & Ormiston

1993: 36, pl. 3, fig. 1.

Ot.]CURRENCE. — Grey radiolarites of the Crawford

track, Southern Uplands, this study.

Remarks

This morphotype has distally tapcring main

spines, small secondary spines on rhe perforated

outer shell and an inner spherical shell (diameter:

70 pm approxinvately) comparable lo /. aksaken¬

sis. Howcver, the sizc of the omet shell (diameter

less than 150 pm) is nearly hall the size ol the

larter species. The holotype of L aksakensis in

Nazarov’s (1975) work is the specimen illustrated

on pl. 21, fig. 1 (see pl. 3, fig. 8 in Nazarov àc

Popov 1980).

Inanibigutta (?) sp. A

(Fig. 4J)

Occurrence. — Red-brown radiolarites at

Hawk\vood Biirn, Southern Uplands, this study.

Description

The outer shell is a nearly perfect sphere perfora¬

ted by relarively large circular pores. It also bears

small secondary spines, Two thin rod-like main

spines, positioned along an axis and almost half

the length of rhe diameter of the outer shell, dis¬

play a few thorn-shaped apophyses,

Remarks

The nature of the thin rod-like main spines dis-

tinguishes this morphotype from ail other

Tnanigurridae. The exact number of spines and

internai srructurc of the shell are unknown.

Genus Inanigutta Nazarov & Ormiston, 1984

Inanigutta Nazarov & Ormiston, 1984: 72, 86. —

Nazarov 1988: 56.

Type species. — Entactinia unica Nazarov, 1975.

GEODIVERSITAS • 1999 • 21 (4)

631

Danelian T.

hmnigiitta (?) sp. K

(Fig. 5A)

OccURKtNCF.. — Grev radiolaritcs of the Crawford

track, Southern Uplands, this study.

Description

Small inaniguttid with six robiist main spines,

four of chem situated on an équatorial plane and

the other two along an axis perpendicular to it.

The four équatorial spincs are themselves posi-

tioned along two axes, perpendicular to each

other. Ail spines are rod-like, gently tapering dis-

tally. Thcir bases are large, perforared and joined

to the outer perforated shell in such a way as to

give a bîpyramidal outlinc. No secondary spines

are visible on the surface of the outer shell.

Remarks

Uncertainty regarding generic assignement is due

to die unknown internai structure ol this morpho-

type.

Genus Oriundogutta\^^T. 2 xov^ 1988

Oriundogutta Nazarov, 1988; 57- - Nazarov &

Ormiston 1993: 36, text-fig. 7h.

Type SPECIES. — Astroentactinia ramificans Nazarov,

1975.

iOriundopitta riisti

(Ruedeniann & Wilson, 1936)

(Fig. 5B)

? Heliosphaera riisti Ruedemann & Wilson, 1936:

1572, pi, 5. figs 13-^15, 31, pl. 7> % 8.

? Astroentitetinia ? riisti (Ruedcmanit & Wilson) —

Nazarov ÔC Popov 1980: 46, text-fig. 24, pl. 12,

figs 10-11,

Occurrence. — Red-brown radiolaritcs at Hawk-

wood Burn, Southern Uplands, this snidy.

Remarks

The size of the outer shell (diamerer 150 pm

approximately) and the presence of stout and

thinner spines are comparable to O. rüsti.

Doubts regarding taxonomie assignement remain

owing to uncertainty about the internai structure.

^Oriundogutta 1993

(Fig. 50

? Oriundogîitta bella Wang, 1993: 101, pl. 9, figs 1-

13.

Occurrence. — Grey radiolaritcs of the Crawford

track, Southern Uplands, this study.

Re.marks

Alchough only six spines are visible, their distri¬

bution and angle on the spherical shell suggests

that thcir total number is possibly cight.

Inaniguttid (?) gen. et sp. indet.

(Fig. 5D-E)

Occurrence. — Grey radiolaritcs of the Crawford

track, Southern Uplands, chis study.

Description

.Star-shaped shell, Icnricular in cros.s*secrion, bea-

ring five n»bust conical spines. I be shell is perfo-

raied by numerous pores ol varions sîzcs and

shapes (subangular, oval), Pores near the base of

the spines are disiinctly larger and elongated,

encompassing part ol the spine. The internai

structure is unknown.

Order ALBAILLELLARIA Deflandre, 1953

emend. Holdsvvorth, 1969

Family Ceratoikiscidae Holdsworth, 1969

Genus P}‘otoceratoikîscum

Goto, Umeda & Ishiga, 1992

Protoceratoikîscum Goto-, Umeda àc Ishiga, 1992: 165.

Type SPECIES. — Protoceratoikiscum chinocrystallus

Goto, Umeda & Ishiga, 1992.

Protoceratoikisctim sp.

aff. P, similistellatum Li, 1995

(Fig. 5F-G)

aff. Protoceratoikisctmi similistellatum Li, 1995: 337,

pl. 2, figs 2, 4.

Occurrence. — Grey radiolaritcs of the Crawford

track, Southern Uplands, this study.

632

GEODIVERSITAS • 1999 • 21 (4)

Taxonomy of Ordovician Radiolaria from the S. Uplands

Fig. 5. — Scanning électron nnicrographs of radiolaria extracted from cherts of the Southern Uplands. A. Inanigutîa (?) sp. K;

B. ? Oriundogutta rüsti (Ruedemann & Wilson); C, ? Oriundogutta bella Wang: D E, Inaniguttid (?) gen. et sp. indet.;

F'G, Protoceratoikiscum sp. aff. P. similistellatum. Scale bar: A. 51 pfT»; B. 79 pm; C, 73 pm; D. 65 pm; E, 72 pm; F. 63 pm; G.

66.5 pm.

Description

Three to four spincs distributcd radially along a

semi-circle forrned by rwo to threc rows of arches

joining the spincs. Spincs taper gently distally,

but aiso towards the centre very rapidly.

RE MARKS

From the presence of arches between spines this

morphotype is comparable to the species descri-

bed by Li (1995). However, it differs in its smal-

1er size and the smallcr angle between adjacent

spincs. Only incomplète .specimens were encount-

ered in the yiclded matcrial.

Acknowledgements

Financial support from the Royal Society of

GEODIVERSITAS • 1999 • 21 (4)

633

Danelian T.

Edinburgh (B. P. Granr) is gratefully acknowled-

ged. The author is inosr indebted to E. K. N.

Clarksoii for having iatroduced him to the stu-

died outcrops and J. Floyd for discussion on the

geolog)' of the scudied areas. Many rhanks also ro

J. C. Aicchison and fi J. Noble for hcipfui coiti-

ments on the manuscript, S. Zatsepin for hclp

with translation of Russian liierature and M. Lee

for helpfui advice and assistance with SEM

images. This is a contribution to IGCP No. 410

“The Great Ordovician Biodiversification

Event”.

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Submitted for publication on 29 January 1998;

accepted on 21 September Î998.

GEODIVERSITAS • 1999 • 21 (4)

635

Radioiarians as tracers for provenance of

gravels in Lower Cretaceous molasse

(Outer Zone of SW Japan)

Keisuke ISHIDA

Laboratory of Geology, Faculty of Integrated Arts and Sciences, University of Tokushima

1-1 Minamijosanjima, Tokushima 770-8502 (Japan)

ishidak@ias.tokushima-u.ac.jp

Ishida K. 1999. — Radioiarians as tracers for provenance of gravels in Lower Cretaceous

molasse (Outer Zone of SW Japan), in De Wever P. & Caulet J.-P. (eds), InterRad VIII,

Paris/Bierville 8-13 septembre 1997, Geodiversitas 2^ (4) : 637«656.

KEYWORDS

Provenance,

conglomerarc,

molasse,

radiolarian dacing,

Jurassic accretionary complcx,

Cretaceous,

SW Japan.

ABSTRACT

This paper discusscs the results and the recent .status of the study by radiolar-

ians as tracers for erosional events, especially for those of Jurassic and pre-

Jurassic accretionary complexes in the Outer Zone of SW Japan. As a test

case ro darifÿ the provenance of radiolarian-bearing gravels in conglomérâtes,

the author reviewed the work previously donc to trace the source rocks

within oceanic-plate stratigraphy successions from monomictic chert-pebble

conglomérâtes of the Lower Cretaceous Ryoseki-Monobegawa group. The

group is a molasse rypical of paralic sedimenrary faciès in the Outer Zone of

SW Japan.

MOTS CLÉS

Provenance,

conglomérat,

molasse,

datation par radiolaires,

complexes

d’accrétion jurassiques,

Crétacé.

SW Japon.

RÉSUMÉ

De Vutilisation des radiolaires comme indicateurs de provenance des graviers

dans les molasses crétacées inférieures (zones externes du SWJapon).

Le présent article discute des implications qu'a l utilisation récente des radio¬

laires comme indicateurs d'événements érosifs, en paniculier de ceux de com¬

plexes d’accrérion jurassiques et anté-juras.siqucs au SW Japon. Comme

étude de cas pour éclairer la provenance de graviers à radiolaires des ct)ng!o-

merats, l’aurcur cffcccuc une revue des séries stratigraphiques synrhériques à

partir des conglomérats monogéniques à galets de clierts du groupe Ryoseki-

Monobegawa du Crétacé inférieur. Ce groupe molassique est de faciès .sédi-

mentaire paralique typique des zones externes du SW Japon.

GEODIVERSITAS • 1999 • 21 (4)

637

Ishida K.

INTRODUCTION

In the last two décades, radiolarian researchers in

Japan made an effort ro clarify the Permian,

Triassic and Jurassic biostratigraphy, and estab-

lished many radiolarian biostratigraphic zones

(e.g., Lsliiga D)H6. 1^)90; Matsuoka Yao 19S6;

Yao 1990; Matsuoka 1995 eic.) wiihin accre-

tionary complexes (AC; ’laira et tiL 1981). Thcy

analyzed bed by bed the faunas froni blocks o(

pclagic sédiments in mélangés and oli.stosrromes.

It contributed to reconstrucr the oceanic plate

stratigraphy {OP5) from thcse lectonically dis-

rupted -sedimentary rocks (e.g., Marsuoka 1984;

Ishida 1987; Hada & Kurinioto 1990; Ksozaki

1997a), as well a.s to di.stingiiish géologie uniis

and to clarify tlieir spatial distribution (Mizutani

1995).

Radiolarians arc important indexes lor the

Paleozoic and rhe Mesozoic. Thcir size averages

10'^ mm. They are therefore .small enough to be

reworked as an inclusion into clasts of various

size and even in sand grains. This property is

effective to analyse erosional events. Radiolarians

are available lor identifying source rocks ol clas-

tics.

The “clastic appruach’^ of radiolarian daring

appears particularly appropriate ior cheri-bearing

rerrane analysis of the Canadian Cordillera

(Cordey 1992). In case of California Cousi

Ranges, analysis of radiolarian chcrt-pcbbics is

more effective than sandstonc component not

only for the provcnancial scudy but also for clari-

fying the tectonic movement along the transform

fault (Seidcrs & Blome 1984» 1988).

This paper dcals with erosional events following

the setting ofaccretionary complexes. This is one

test case in the reconstruction of OPS from the

gravels and clasts in the monomktic conglomé¬

râtes. In this case, radiolarians in gravels are used

as tracen; for erosional events. This type of test

will become a greac help to scudy the orogenic

and/or erosional events in the marginal area of

the Late Mesozoic East Asian continent.

GEOLOGY OF SW JAPAN

With respect of the continuity of the pre-

Neogene orogenic unies and ACs> ac Icast the

Southwest side of the Tanakura Tectonic Line is

regarded as SW Japan. The post-Neogene geolog-

ical province of SW Japan is subdivided into the

Inncr Zone on the continental sidc and the

Outer Zone on the trench side by the Médian

Tectonic Line (MTL). Based on a palcobiogeo-

graphical study, ihe left-latcral slip movement

along the M EL is legardcd to rcach about

1 500 km after the Early Cretaceous tlme

(Tazawa 1993). Concerning ihe pre-Neogene

geology, nappes and klippes of ihe Permo-

Triassic orogenic unies and Jurassic ACs are dis-

tributed in the Iriner and ihe C)urer zones of SW

japan (l'ig, 1). The Inner Zone of SW Japan is

composed of the Hida, Marginal Hida, Akiyoshî,

Sangun, Mai/.uru, UIrra-’lamba. and the Mino-

Eainba bclts (rom the north lo the south.

The Hida Bcit is mainly composed of gneisses

with intrasion of Permian-Jurassie granités. The

d’etori gruup of the Middic Juras.sic-Lûwer

Cretaceous shallow-murine and non-marine for¬

mations unconformably overlics tliese gneisses'

and granités. The Hida Bêlt is siruatccl in the

mosT condncnial side of SW Japan, and is sup-

posed to thrust on the Akiyoshi, Sangun,

Maizuru and ihe Ultra-Tamba beks.

The Marginal Hida Bell is situatod between the

Hida and the Mino- lamba bclis. It is supposcd

to thru-st upon ihe Mino-'J'airiba Belts together

with the Hida Belt. 'Ehc Marginal Hida Belt is

composed of Paleozoic compicx with Triassic for¬

mation chat are unconformably overlain by rhe

Lower-Middlc Jurassic Kuruma group. The

Paleozoic complexes appear to be serpentinite

mélangés chat include blocks of glaucophane

schist.s, amphihnitrcs, F.arly-Late Paleozoic clastic

sédiments with limestones.

The Akiyoshi Belt is composed of rhe Middlc-

Late Paleozoic ACs and the Mesozoic cover for¬

mations, The Late Paleozoic ACs connain large

blocks of CarboniferoLis and Permian limestones

with basales as well as blocks of Permian cherts,

mudstoncs and sandstones. The Mesozoic shal-

low-inarinc and brackish cover formarions are

the Triassic Natiwa group and the Jurassic

Yamaoku formations.

rhe Sangun Bell is mainly composed of 180-

230 Ma glaucophane schists and slates that are

638

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Cretaceous molasse (Outer Zone of SW Japan)

Fig. 1. — Zonal distribution of pre-Neogene orogenic units and accretionary complexes in SW Japan. A, Hida, B, Marginal HIda; C,

Akiyoshi; D, Sangun; E. Malzuru; F, Ultra-Tamba; G. Mino-Tamba belts of the Inner Zone; H, Sambagawa-Mikabu; l. North Chichibii;

J. Kurosegawa; K, Soulti Chichibu belts; U, Sbirnanto Superbelts of the Outer Zone. MTL. Médian Tectonic Une; TTL, Tanakura

Tectonic Une,

originated from mudstoncs, sandscoiies, and d’he Mino-'Jamba Belt is composed mainly of

basakîi with chcrcs of the Latc Permian ACs. the Early Jurassic-earliest Cretaceous ÂCs rhat

*rhc Maizuru Belt is oomposed of Paleozoic basic are intruded by the Late Cretaceous Ryoke grau-

rocks (Yaküno ophiolite) and Middie-Late ucs. ’l’hey are unconformably overlain by rhe

Permian slope basin deposits (Maizuru group) Latc Cretaceous volcano-clastic formations

thar are unconformably overlain by the Lower- (Nohi rhyolites) and ihe Paleogene non-marine

Middie Triassic Yakiino group. conglomérâtes. The Larly Jurassic-earliest

The Ultra-Tamba Belt is subdivided inco chree Cretaceous ACs are subdividcd into sevcral tec-

nappes. The highest nappe of the UT3 ûs com- tonie unirs. They are composed of Permian^

poscd of Upper Permian mudstoncs and green- Middie-Upper Triassic and Lower-Middle

srones with cherts and Upper Carbonilcrous Jurassic cherts with Early Triassic siliceous clay-

limestones. Intermédiare nappe ol rhe UT2 is stonc.s, Jurassic-earliest Cretaceous mudstonçs

composed of Upper Permian siliccous mudstone.s and turbidites. These ACs also contain blocks of

with Lowcr-Middle Permian bedded cherts. The Upper Paleozoic limestones and basalric green-

lowcst nappe ot the UTl is composed of Middle- stories.

Late Permian mudstoncs and grceni.sh sand- The Durer Zone of SW Japan is composed of

stoncs. l'he Permian formations of the UTl are the Sambagawa-Mikabu, Norrh Chichibu,

unconformably overlain by the non-marîne Kurosegawa, South Cluchibu belts and the

Lower Cretaceous Sasayama group. Shimanto Superbelt from the north to the south.

GEODIVERSITAS • 1999 • 21 (4)

Ishida K.

The Sambdgawa-Mikabu Bclc is composcd of the

Sambagawa cryscallinc schists and thc Mikabu

greensconcs. fhis belt is supposed to consisc of

the Early jurassic-Early Crctaceoiis ACs.

Multiple nappe structure is churucteristic in this

bcit. The Sambagawa crystalline schists arc com-

posed of basic and pcliiic schists wiih quartz and

psammitic schists. Somc of the inrercalaccd calcar-

eous schists in thc basic schists arc oiiginaced

from thc Upper Triassic limestones (Suyari et al

1980a). The Mikabu greenstones are composcd

of low-metamorphosed gabbros, dolerites, pillow

basalts and ba-saltic hyaloclastites witb Upper

Jurassic cherts (Faure et al 1991), mudvsrones

and Upper Triassic limestones, They experieneed

H-P/L-T metamorphfsm during thc Cretaccous.

Metamorphic grade is higher in the northern

nappes.

The geometP}' of rhe Kurosegawa Belt with res¬

pect to the Jurassic AC is not yet settled siiffi-

cicntly However, alter the Early C]rctaceous

time, the non-rnetamorpliosed jurassic AC and

the pre-jurassk AC ot rhe Outer Zone of SW

japan arc distrlbuted in a tcrranc that is called

the Chichibu Supertei rane. The Chichibu

Supcrtcrranc is subdivided into rhe pre-jutassic

AC of thc Kurosegawa Beir, and the jurassic AC

of the Norrh Chichibu and the South Chichibu

bclts.

The Kurosegawa Belt is situated in thc central

part of thc Chichibu Superterrane, and is com-

posed ot rhe Paleozoic AC that is unLoniormably

overlain by thc Mesozoie cover formations. This

belt is subdivided into rhe iioith and the soiith

units. In the south unit, pre-jurassic AC is com-

posed of Pefinian and Middle Paleozoic forma¬

tions that are unconformably overlain by shaJIow

marine and paralic formations of the Middle-

Upper d'riassic Daonella-Monnth beds, Middle-

Upper jurassic Torinosu group and the Lower

Cretaccous Takegatani group. The Permian for¬

mations arc mélangés and slope basin faciès. The

Middle Paleozoic fromations appears witli ser-

pentinites as lenticular bodies ihar are composed

of gneisses. gmnite.s and ihe Silurian limestones.

The nonh unit is composed of the Permian AC

that is unconformably overlain by thc Lower

Crecaceous paralic formations of the Ryoseki-

Monobegawa group. The north unit lacks the

Middle Paleozoic formations and thc Triassic-

Juiussic cover formation.s.

l’he North Chichibu Belt (NCR) is distributed

in ihc north sidc of thc Chichibu Superterrane.

rhe NCB is composed ot laiesi Triassic-Middle

Jurassic ACs that con.sist of Permian, Middlc-

Upper Triassic and Lower Jurassic cherts with the

Early driassic siliccous claystones, Lower-Middie

Jurassic mudstones and turbiditcs. I hcsc ACs

also contain blocks of the Upper Paleozoic lime-

stones and basaltic greenstones.

The South Chichibu Belt (SCB) is composed of

Middle Jura.ssic-earliest Crefaceous ACs

(Nakagawa group) and the Late Jurassic-Early

Cretaceous slope basin formations of the

Torinosu group. The Middle Jurassic-earJiest

Cretaceous ACs arc subdivided into severai tec-

ronic unies that hâve the acenetion polarity reju-

venating from the norrh to the south- They arc

composed of Permian, Middie-Upper Triassic

and l.ower-Middle jurassic cherts with ihe Early

rriassit siliccou.s ckiy.stone.s, Middle Jura.ssic-car-

licst Cretaceous mudstones and turbidltc sand-

stoncs. Tlicse ACs also contain Upper Paleozoic

limestones and basaltic greenstones.

The Shimanro Superbelt is subdivided into thc

North Shimanto Belt (NSB) and the South

Shinianto Belt (SSB). The NSB is composed of

latc Early-Late Cretaceous ACs and slope basin

formations. Tliesc ACs contain thc Lower-Upper

Cretaceous cherts, and rhe Iziihara and Hayama

slope basin formations contain olistolichs ot the

Triassic limestones from the SCB. The SSB is

composed of the Palcogene-Miocene ACs and

ihe slope-ba.sin formations.

GEOLOGICAL SETTING

A nappe model of the SW Japan was proposed

when the reeem radiolarian Works in Japan has

sianed (Faure 1983a, b). At first, the Kurosegawa

Rcir was proposed lo be a lower unit as a rem¬

uant üf the subducted microcontineni (Faure

1985; Caridroit &: Charvet 1986). In compari-

son wjth the gcology of the Innci Zone of SW

Japan, the Kurosegawa Belt Wiis proposed to be a

klippe above the Chichibu Klippc (Isozaki et al

1992). According to Suzuki & Itaya (1994), the

640

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as traccrs for provenance of gravels in Lower Cretaceous molasse (Oucer Zone of SW Japan)

34''N

Fig. 2. — Geologicâl outline map of the Chichibu Superterrane. 1^ Sotoizumi group (Upper Cretaceous slope basin sédiments);

2, Ryoseki-Monobegawa group (Lower Cretaceous paralic sédiments): 3, Takegatani group (Lower Cretaceous shallow marine sédi¬

ments); 4, north Unit of the Kurosegawa Belt (Permian accretionary complex); 5. south unit of the Kurosegawa Bell (Permian accre-

tionary complex with Middie Paieozolc blocks and Triassic-Jurassic cover formations): 6. North Chichibu Belt (Lower-Middle Jurassic

accretionary complex); 7. South Chichibu Bell (Middie Jurassic-Early Cretaceous accretionary complex).

K-Ar age.s of ihe pre-Jurassic AC in tlic

Kurosegawa Dclt arc Laie Triassic to Early

Jurassic (194-225 Ma). TKe K-Ar âges of the

jurassic AC in the North Chichibu Belt are

Mitldle jurassic ro earliest Cretaceous.

The Ryoseki-Monobegawa group in the Ou ter

Zone of SW japan is characterisiit o( paralic

tacies of the Early Cretaceous âge (Tishiro 1986;

Tashiro &c Kozai 1991; Koziiî 1996; Ishida et a/.

1992, 1996). The group unconlorniably overlies

pre-jurassic (Permian) mélangés of the nortlr unit

of the Kurosegawa Bell (Ishîda et///. 1992). The

Kurosegawa Bell i.s subdivJded into ihc north

and the south umts. They are sicuaccd berween

the jurassic AC of chc North and the South

Chichibu belts (Fig. 2). In the south unir, pre-

jurassic AC wirh blocks of gneisses, granités and

Silurian Ümescones is unconformably overlain by

the Triassic shallow-marine formations (Sakashu

unconfoimicy: Icliikawa et///. 1953). Thus, rhin

shallow-nuuine TriuSsic and jura.ssic tormatioas

overlie the Paleozoic complexes in the South

Kurosegawa unit, whercas ihey never dlsiributc

in the north unit. The Ryoseki-Monobegawa

group and the équivalent Takegatani group

unconformably averlii: boih uniis of the

Kurosegawa Belt. The group is composed of

brackish conglomérâtes and shallow-marine sédi¬

ments. rhey yield auiochthonous Barrcmian

imdlusks (Mai.sukawa & Eio 1987).

The Lower Cretaceous formations of ihc

Ryoseki-Monobegawa group are composed

mainly of conglomerates> sandstones and mud-

srones with seams of ciiffs, limestones and coals

(Fig. 3). In F.asr Slukokii, the group is .subdi-

vided into lhe Tatsukawa, Lower and Upper

Manoura, Moji and Fujikawa formations (Ishida

et///. 1992, 1996). These formations yield

GEODIVERSITAS • 1999 • 21 {4)

641

LOWER FORMATIONS OF THE RYOSEKI-MONOBEGAWA GROUP

Ishida K.

reddtsh cgi.

Kfl chert-pebbte cgi.

pebbly sandstone

□ massive sanstone

parallel-bedded sdst.

ait. sdstVmudst.

pelitic beds

calcareous beds

lîSSÎI coal seam

luff seam

pre-Cretaceous basement

O radiolarians (autochthonous)

9 radiolarians (reworked)

O foraminifers

@1 ammonites

A trigoniids

C? marine bivalves

Ochiai

[=□

Hanoura

V brackfsh bivalves

if echinoids

4» iand plants

Il trace fossils

CO wave ripples

A-F sampling horizons

100m

Fig. 3. — Stratigraphie columns of the lower formations of the Ryoseki-Monobegawa group in East Shikoku.

642

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Cretaceous molasse (Outer Zone of SW Japan)

Fujikawa Fm

Hoji Fm

Base Hoji Fm

Upper Hanoura Fm

Base Up Hanoura Fm

Lower Hanoura Fm

Base L Hanoura Fm

Tatsukawa Fm

Base Tatsukawa Fm

Q quartz vein

e granité

a quartz porphyry

■ serpentinite

a greenslone

■ limestone

D sandslone

s mudstone

□ acidic tuffite

(D chert

Fig. 4. — Composition and vertical change of gravels in the Rvoseki-Monobegawa group, East Shikoku.

autochthonoiis jmnioniies, bivalves, echinoids,

foraminifers and radiolarians wilh alloclichonoiis

plants, non-marine bivalves and dinosaur teeth.

They indicate Baircmian to Albian âges. The

radiolarian zonation of the Ryoseki-Monobegawa

group is Mibdivided irito the At^hdeodictyomitm

pseudoicdlaris (Barremian), Stichomitra ionnnunis

(upper Aptian) and Pseuchdutyo>nitm pentaco-

laensis (middle Albianj assemblage zones in

ascending order (Ishida àc Hashinioto 199Ta).

'These zones arc calibrated by co-occurring

ammonites. These formations form sedimeniary

cycles chat are characterized hy üpward thinning

and fming sequences under the cffcct of trans¬

gressive events. CTowth of the dcitaic fan is syn-

chronoLis with the eusraric change. The

conglomérâtes are more than 100 m thick, and

are frequcntly intercalated in rnany horizons

(Fig. 3).

Characteristics of the conglomérâtes, especially

dic size, roundness, lithology and soning of the

gravels differ in horizons. Basal conglomerate of

the group is characterized by basaltic greenstonc

gravels and serpentinire blocks that arc interpre-

ted as the resuit of débris flows. Round gravels of

quartz-porphyry and fine granité inctcase in the

upper horizons, especially above the Upper

Hanoura formations. In the upper part of the

Tatsukawa formation and the Lower Hanoura

formation, there are many chert-pcbblc conglom¬

erate beds of monomictic origin (Fig. 4). The

chert-pcbble conglomérâtes are composed of

round chert pebbles of a few cm in diamerer that

occupy more than 90% of the gravels (Fig. 4).

They are well sorted. and clast-supporced. For

this study, ihc author studied these monomictic

chert-pebble conglomérâtes with spécial respect

to recoiisiruct the provcnancial OPS, and exrrac-

ted radiolarians from chert pebbles and mud¬

stone clasts.

PREPARATION AND PROCESSING OF

.SAMPLES

This study needs some information about OPS

of sedimentary basements and/or terranes of ori¬

gin (rom radiolarian-bearing gravels in mono¬

mictic conglomérâtes. For this purpose, it is

nccessary to clatify the relarionship betweeii the

lithology ol gravels and thdr radiolarian âges.

Paxticularly, reconstrutting the ÜPS of terranes

from gravels in monomictic conglomérâtes

requires to be able lo disringui.sh riic lithology of

graveU, wlicther they are of pelagic or continen¬

tal origin, as well as to déterminé their radio-

GEODIVERSITAS • 1999 • 21 (4)

643

Ishida K.

Fig. 5. — Mlddle-Laîc Tiiaiîsic and nartlGSl Jurasse radiolnrian» from the nhert pebbles of the Ryoseki-Monobegawa groüp »n East

Shikoku. A. Tfisa^iX'^fnpê lont^icppimlis Ko/iir Ô Mosilof; B, Atinulotriassocampe camp,tnifis Knrur A Mostic/-; C. O, Trt.isaocfimp9

aff. scalaris DiirTvitnca, Kojrur & Mûutitîf; E. C5(£7/ tucUs De WeveT; F, Pamhâuum simplom Yan; G. Corurn ,spPùiO)i{irn Rlooie;

H, Pararucsttcyrtium medlotassanlcum Kû 2 ih R Mnstlor I. HinfledOn:.nst Ntipftwtnihi Suijiyania; J. Tpeoctjty'^ 6p. A ol Nakaecko &

Nishimura. K. Harmadla reticulatà Oumîti-ca, Ko^uf & MosUef; t. Tibofpfte cochle&ta (Naka&eKo 5 Nichimura); M. Bvturmlfa robusta

Dumitrica. Ky^ui A MosUer N, BpUngium rrKintrefd} rcbusfum Kozur & Mostler O. BptfngfUfn nahasffkol Koîiir & Mo&tler;

P. Eptingiumd. man/rec* Uumiirica; Q. Pseudoslytosphaera spinuloRum (N.ikaseko & NÆliimura), R PsaydoHtyhtsfthatttta wp, C of

Ko)fnia & Minutant, 1^87, S, Psoudosiylosphaot'n japonicft (NaKaseko /V Nishifiui^a): 7, Of^pnodoco sarisa De Wevor; U, Jnlonche

japonica Nakaseko & Nishimura; V, Sarla (?) exîerna Blome; W, Acanthocircus vigrassi Blome. Scale bars: 100 pm; a, W; b, H, L-P,

R-V;c. A-G,J. K. Q; d, I.

644

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Creraceous molasse (Outer Zone of SW Japan)

larian âge. In the marginal area of Easi Asia and

Japanese Islands, Jurassic and prc-Jurassic ACs

originale from OPS that arc mainly composed of

cherc-clastic séquences. Iri these cherr-clastic

scquences> sédiments sçart irom pielagit bedded

cherts, and they gradually change upwards

towards ahernating beds of curbidire sandstones

and mud5tonc.s (irench-fill turbidite) by way of

hemipelagic slliccous raudstonc beds.

Rcgardiiig the conglomerares in the Lower

Cretaccous Ryoseki-Monobegawa group, the foL

lowing mechod of processing is used. If gravels

are larger than 20 mm in diameter, and it is easy

to isolate them from the matrix, gravels of cherts

and mudstones are chemiediy processed separate-

ly. Tf gravels are roo .small (Icss than 20 mm in

diameter) and difficult tu isolate sepaaately from

the hard matrix, sJabs ot conglomérâtes about

5 mm thick arc made. Thcn, gravels arc eut oft

using pliers. Altcr that. che fragments of pebbles

are classifed lid>ologicaily into cherts or inud-

stones. In rhe Rvoscki-Monobcgawa group, the

matrices of conglomérâtes arc asually composed

of sandstones. They contain not only cherc clasts

but also mud-stonc grains that arc Icss rhan 2 mm

in diameter. Jn the sttidy, the matrices of con¬

glomérâtes are separated from the gravels beiore

Processing. Tbis method shows that rhe matrices

yield quite diflerent kind of radiolarians ahun-

dantly compared with those Irom che thert grav¬

els. The samples were processed by 3-7% diluted

H F for about 12 hours. The process was repeaied

several times.

RADIOLARJAN AGE OF GRAVELS AND

CLASTS

The chert gravels of chert-pebble conglomérâtes

of the Ryoseki-Monobegawa group yield Middle-

Late Triassic, and earlicst Jurassie radiolarians

(Fig. 5). Among rhem, Hindedorcm hnldsworthu

EpUngium nakasekou E. cf. maiijirdi, Triasso-

campe aff. icalaris, Armuhiriassocampe campanilis,

Trilonche japonicUy Pseudostylosphaera japnnkay

Beturiella robusta, Pscudostylosphaem apinulomm^

P. sp C of Kojima Mizutani (1987),

Triassocampe longtcephalis, Pararuesticyrtium

mediofassan 'îcumy Hozumadia reticulatay Tiborella

cochlema are characteristic of the Middie Triassic.

Hindedorcus holdsworthi was reported from the

chert beds of the Kinkazan, Mino-Tamba Belc

(Sugiyama 1992). Thi.s species is chatactcristic in

Hozmadin gifuemis assemblage of the caily

Anisian âge. Epùngium ?iiikasekni was reported

from the Pameeratîtes ty-inodouis zone (lllyrian) in

che Balaton Hills, Hungary fKozur &r Mostler

1994). Epîtngiam cf. mayjfirdi i.s clo.sely adated

with the same speeies. that wa.s reptïrtcd fmm rhe

bedded chert sequences in the Inuyama area of

the Mino-Tamba Relt. The species occiir.s with

Triassocampe dewtveri and Ladiniati conodoncs

(Ya.o 1982). Truissocampe Âi. co-occurs

with Ani.sian conodonts from the chcrc beds of

the South Chichibu Bclt (Ishida 1984).

Annulotriasuicanipe campanilh was reported from

the Fassan beds of the Balaton Hills, Hungary

(Kozur & Mosrlcj 1994). Trilonche japonicû co-

occurred with Triassocampe deweveri in the chert

of the South Chichibu Bclt (Nakaseko &

Nishimura 1979). Pseudostylo-sphaera japoriica

was dcsciibcd from the chc/t beds of the South

Chichibu Beir (Nakaseko Ssc Nishimura 1979).

This spccies cu-occurs with Neogondolella httsla-

chensis in rhe lare Anisian-early I^adinian chert

beds of the Sikhote-Alin and Sakhalin (Brag'm

1991). Anoiher reports on occurrences are from

bedded chens in the Mino-Tamba Be-li (Yao

1982) and the Nad;uihada, NE China (Kojima

ik Mizurani 1987). Bctunella robnsta was report¬

ed from rhe ‘'"Nodosus bed" about ihe Anisian/

Ladinian boundary in the .Southern Dolomiten

Alps (Dumitrica étal. 1980). Pseudosiylosphaera

spiriulasum was reported from chert beds of the

South Chichibu Belc (Nakaseko & Nishimura

1979), and from the upper Anisian-lower

Ladinian chert beds in rhe norrhernmost

Sakhalin with Pseudostylosphavra japonica (Rragin

1991) Pseudostyloshaera sp. C of Kojima

Mizutani (1987) has slightiy rwisted polar spines.

This spccies was reported from the latc Anisian

to Ladinian bedded chert in the Nadanhada

Range. Triassocampe longtcephalis îs described in

tlie early Ladinian (middie Fassanian) beds of the

Vincentinian Alps, Italy (Kozur ÔC Mostler

1994). Pararuesticyrtium mediofassnnicum is

known in the Ladinocampe multiperforata zone of

the middie Fassanian beds in the Vincentinian

GEODIVERSITAS • 1999 • 21 (4)

645

Ishida K.

Fig. 6. — Photomicrographs showing clasts (sand sizes) oî mudstones (dark) and cherts (light) in the matrix part of the chert-pebble

conglomérâtes. These mudstone clasts contain many radiolarian tests (small round circles). A-D. Psammitic matrices of the chert-

pebble conglomérâtes in the Ryoseki-Monobegawa group. East Shikûku Scate bars: 1 mm.

Alps, Italy (Kozur 6c Mostler 1904). Hoztimadia

reticulata is reporccd from chc lowcr Ladinian

beds in the Southern Alps (Diimitrica et aL

1980). The species is characreristic in Spofigo-

silîcarmigcr tUtlicus zone oF the lowcr Fassanian

(Kozur Si Mostler 1994). Tihorell-a cochleatn i.s

reported with Truimcampe dewiiueri From chert

in Inuyama, Mino-lamba Bck (Nakaseko &

Nishimura 1979).

The Upper Triassic radiolarians such as

Capnodoce sarisa, Theocoiys sp. A, Snrla (?) exter^

na, AcanthocircHS vigrassi and Corum specwsum

are extractcd from chcri pcbblcs. Capnodoce sari-

sa is described frorn the Uppet Triassic forma¬

tions in Turkey and S'icily (De Wever et al.

1979). This spccies occurs with Theocorys sp. A

and Carnian conodonts From the gray cherc in

Shimo-aso ol rhe Mino-Taniba Belr (Nakaseko

& Nishimura 1979). Sarla (?) externa is reported

From the upper Carnian (?)-middlc Norian beds

fn Mid-Easi Oregon (Blome 1983). Avatitho-

circtis vigrassi was reported from the Triassic

(upper Carnian (?)-middle Norian) Obin mud¬

stone in East Oregon (Blome 1984). Corum spe-

ciasum is described from the Rail Cabin

mudstone (lower-midJle Norian) in Oregon

(Blome 1984). Paleosaturnalis sp. are extracted

with Sarla (?) exteruit from a chert pcbbic in che

conglonierate.

ParahsHum sirnplum and Gigi Jusris of the earliest

Jurassic materiai.s are ai.so found in the other

chert gravcls. Paralmmm nmplmn is the index

specics of the P. sirnphon zone (Hori 1990). This

specics is widely reported From the bedded chert

in Mino-Tamba, Ashio, Notth CFiichibu and

South Chichibu bcits (Yao 1982; Suyari et al.

1982; Ishida 1983; Sashida 1988). fiislts is

reported from the calcareous chert in the lower

646

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Crctaceous molasse (Outer Zone of SW Japan)

Fig. 7. — Early. Middie and Late Jurassic radiolarians (rorti ihe small clasts and pebbles of mudslones in the chart-pebble conglom¬

érâtes of the Ryoseki-Monobegawa group in East Shikoku A. Parahsuum ovale Hori & Yao: B, Parahsuum (?) grande Mon & Yao;

C, Dictyomitralla kamoensts Muutani & KIdo; D, Ristola dhimenaensis (Baumgartner); E. F, Archaeodlctyomitra suzukif Alta;

G. Tricolocapsa fusiformis Yao; H. Tricolocapsa atf fusiformis Yao; I K, Tricolocapsa plicarum Yao; L» Tricolocapsa cf. ruesft Tan;

M, Stichocapsa japontca Yao; N, Tricolocapsa ci. parvtpora Tan of Yao, O, Theocapsomma cordis Kocher, P, Q. Stylocapsa oblon-

gula Kocher; R, Eucyrtidiellum unumaensis (Yao); S, Eucyrtidiellum nodosum Wakita. Scale bars: 100 pm; a. A. D; b, B. C, E-G, l-L;

c, H, M-S.

GEODIVERSITAS • 1999 • 21 (4)

647

Ishida K.

Fi6. 8. — MicWle-Late Jurassic and earliest Cretaceous radiolarians from the small clasls and pebbles of mudstones in the chert-

pebble conglomérâtes of the Ryoseki-Monobegawa group in East Shikoku A, B. Pseudodlctyomitra primiüva Yao; C, Sethocapsa

pseudouterculus Ai\a\ D, EucyiHdiellum pyramis (Aita); E, Sethocapsa horokanaiensis Kawabata; F, Hsuum maxwelli Pessagno; G,

H, Stichocapsa naradaniensis Matsuoka; I. Proîunuma japonicus Matsuoka & Yao;- J. Cingulotums carpatica Dumitrica, K, L,

Tricolocapsa conexa Matsuoka; M, Stylocapsa lacrimaris Matsuoka; N. Stylocapsa (?) spiralis Matsuoka; O, Gongylothorax favosus

Dumitrica: P. Stichocapsa robsta Matsuoka. Scale bars: 100 pm; a. A-J, L, M. P: b, K, N, O.

648

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Cretaceous molasse (Outer Zone of SW Japan)

Liassic (Sinemurian'?Plicnsbachian) Bndva zone

in tlie Dinarides, Monténégro (GorLcan 1994).

The related species co-occur witli P. simplum

from cherr in thc Kdtsuy.ïmj Section of ilie

MinO'Tamba Bell (Hori 1990).

Matrices of the chen-pebbic conglomcr.ites

contain many small clasts of mudstoncs as wcll as

small clasts of chcrts. l'hcir dianictcrs arc Icss

than 2 mm. Among these mudstonc clasts, somc

arc conipo.scd ot micaccous black mudstoncs.

The othcis arc siliccoiis mudstoncs and tuffa-

ceoiis oncs that arc usually dark gray or black

colored. Thcy commonly contain many radiolar¬

ians (Fig. 6). These small clasts of mudstoncs

and some mudstonc pcbbles in the chert-pebblc

conglomérâtes yield thc Early Jurassic, Middle-

early Late Jurassic, Latc Jurassic, atid tfie earliesi

Cretaceous radiolarians (Figs. 7^ 8). Among

them. the Eatly Jurassic materials are Parahsuum

ovale and Parahsuum (?) geaiuie, Parahuum ovale

hus irs range in ihe Pnratmium ^ioiplum zone.

This species is nearly the same age as P. simplum.

but appeaoi later in the bedded chert séquences

of thc Mino-J’amba Bclc (Hori 1990). This spe¬

cies is also reported from che black mudstonc of

the North Chichibu Belt in Kytishu, SW japar»

(Hori 1990; Miyamoto &c Kuwazuru 1993).

Parahsuum (?) g^aude is the index species of the

zone that belongs to chc Upper Lower Jurassic

(Hori 1990). The Middle-early Lace Jurassic

materials arc Tricolocapsa pliiarunu T fi4siformis,

T, atf. fusiformisy X conexa^ T parvipora, T. cf.

nmii, Gongylofhorax favosusy EucyrtidicllufN uuu-

macusisy H. nodosunu Theocapsomma cordi-s,

Diayomiîrella kamoensis, Archacodictyomiira cf.

sHzukiiy SPfchocapsa japoutcay S. robustfU

Stylocapsa oblongnla^ Hsuufn maxwclli^ Ristola

dhimenaeusis. Tiicy are reported from the

Tricolocapsa pücantm zone and Tricolocapsa conexa

zone or Stylocapsa (?) spiralis zone of Matsuoka

(1995), and/or Tricolocapsa tetraga)7a intcrval

zone (IZ; Callovian)-7v?reWi;j/e/A2 bipposidericiu

zone (Oxfordian) of Aita (1987). For example,

Tricolocapsa conexa ranges from thc Tricolocapsa

tetragona VA to thc Porananella bipposidericus

zone ol Aita (1987). Il also ranges from the

Tricolocapsa conexa zone (upper Bathonian) to

the Stylocapsa (?) spiralis zone (.Oxfordian) of

Matsuoka (1995). This species is regarded to

indicate thc UA zones 6-15 of Gorican (1994)

and thc U A zones 4-7 of IncerRad J-C WG

(1995). These zones arc correlated with the late

Bajocian to Bathonian or Callovian. Tricolocapsa

parvipord has irs range In thc Tricolocapsa fetrago^

na VL-Amphipyndax isunoensis VL of Aita (1987).

This species is regarded vo indicate the UA zones

3-5 of Bauniganncr (1984), and the UA zones

6-7 (IntcrRad J-C WG 1995) that arc correlated

with the latc Middle-early I..'iic Jurassic (middie

Bathonian to Callovian or early Clxhïrdiarl).

dyiguloturris carpatica^ Stylocapsa lacrimariSy

Stybfcapsa (?) sphnlisy Siichocapsa naradaniefisiSy

Proîunuma japonicus arc charactcriscic of thc

Stylocapsa (?) spiralis lonc-Cinguloiurris carpalka

zone (l.üwer-iniddle Upper Jurassic) oi Matsuoka

Yao (1985), and the Styloutpsa (?) spiralis zonc-

Hsuum maxiifelli zone (upperniost Callovian-

Kimmcridgian) uf Matsuoka (1995). T'hc latcst

Jurassic and earliest Cretaceous materials arc

Pseudodiciyonîitra primitivay Sethocapsa horoka-

naiemisy Serhocapsa pscudotnerculus, Eucyr-tidtel-

lum pyramis, Among them, Pseudodictyo-mitra

primttiva is thc zone index species (Matsuoka

1995). Set ho capsn pseud o u tenu ! us and

Eiicyrtidiellum pyrnm 'is are charactet;istic of the

lowesi Cretaceoti.s Ditrabs saffsalvadorensis zone

(Aita 1986). According to Kawabata (1988),

Sethocapsa horokanaiensis ranges from the

Tricolocapsa yaoi assemblage zone (AZ) ro the

Pseudodlctyomiira prtmhiva KL of Matsuoka

Yao (1985). This species occurred part [y wuli

P primitiva or E. pyramis in the cherr-siliceous

mudstonc séquences of the Sorachi group.

Other assemblages include Early and Late

Petmian radiolarians such as P^eudnalhdillella

scalprata morphotype postscalprata, FoUicucultus

porrcctus, F. scholasticttSy F. charved, Albaillelta

asynutieirica^ A. triangularis, A. excelsUy A. aff

levis and Nazarovella sp. (Fig. 9). According to

Lshiga (1990), PseudoalbailleÜa scalprata morpho-

type postscalprata has its range in thc upper

Lower Pcrmian. Alhaillella asymmetrica ranges

irom thc upper Lower co lower Middlc Pcrmian.

T he otlicr spccics have ranges în the Upper

Pcrmian F. scholasticus zone to thc NeoalhatllelLt

omithoformis zone oi die K. optima zone (lshiga

1990, 1991). Among them, Folltcuctdlus scholas-

ticusy F. porrectus and A. triangularis are cxtracted

GEODIVERSITAS • 1999 • 21 (4)

649

Ishida K.

Fig. 9. — Permian radlolarians Irom the inudslone clasls (A*H) and chen pebbles (1-T) m lhe chert-pebble conglomérâtes of the

Ryoseki-Monobegawa group in East Shikoku. A-D, Follicuculius charveti Caridroit & De Wevor, every ventral spine below sinus is

broken oft; E. Follicuculius scholasticus Ormiston & Babcock.; F G, Follicuculius porrectus Rudenko; H-J, Alballlella tnanguiaris

Ishiga, Kito & Imoto: I. Ventral wing-side view. Ventral wing is broken off; K, Albaillella aff. levis Ishiga Kito & Imoto of Kuwabara,

1997; L, Alballlella ekcelsa Ishiga. Kito & Imolo^ M, Follicuculius scholasticus Ormiston & Babcock; N. O, Follicuculius porrectus

Rudenko; P, Nazarovella sp.; Q. Alballlella asymmethca Ishiga & Imoto; R-T, Pseudoalbaillella scalprata morphotype postscalprata

Ishiga. Scale bars: 100 pm; a, D. F-H. N, P, Q; b. A-C. E, l-M, O, R-T.

650

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Cretaceous molasse (Outer Zone of SW Japan)

trom chéri pcbbles and mudstone clasrs.

FoIUcucuUns charveti is only excracted from ihe

mudstone clasrs. whereas PsendoalhaiUella seul-

prata moiphotype postscnlprata^ Albaillelta tisyrn-

metricUy A. exceba^ A, afh lnn> and Nazarovella

sp. are excracted from the cherc pebbles.

RECONSTRUCTION AND CORRELATION

OF OCEANIC PLATE STRATIGRAPHY

Age déterminations on cherr and mudstone grav-

els and fine clasts of mudstones allows a recon¬

struction of “continuous" stratigraphy ranging

from Middie Iriassic lo ihc lowest Cretaceous

(Fig. 10). Fhe succession rcveals a cliert-clasdc

sequencc that is usually foimd In place in the

Jurassic AC, with clear lithologie boundaty be-

tween chert and mudstone jiist m the Parahsuum

simplurn zone ol the Lower Jurassic (Flori 1990;

Matsuoka 1995).

In rhe Chichibu Superterrane, Jurassic AC is dis-

iributed both in the Sourh and North Chichibu

bclts (Fig. 2). Thcy are very close to the studied

lormations, and have OPSs ol chert-ciastic

séquences. Comparing the OPS ot the North

Chichibu Belt with the OPS uf the Sourh

Chichibu Belt, the complex of rhe North

Chichibu Belt was accreted carliêr (Fig. 11). Ihe

chéri faciès of the Norili Chichibu Belt ends in

the uppermost Triassic Camption îtiassicum zone

or the lowest Jurassic Parahsuum simplurn zone

(Suyari, et ai 1982; Tshida 1985). On the otlicr

side. chert faciès ol rhe South Chichibu Belt

continues inro the Middie Jurassic Laxtorum (?)

jitrassîcum z.one-lower Lfpper Juras.sic Stylocapsa

(?) spiralh zone (Matsuoka 1984, 1996; Ishida

1985. 1987a; Hoshina et al. 1995; Isozaki

1997b). The OPS of origin inferred from the

gravels is corrélative with the OPS of the North

Chichibu Belt rather than with the OPS of the

South Chichibu Belt (Fig. 11).

Concerning the Permian, iwo types of geological

columns are rcconstrucced. The first one is corn-

posed of chen ranging from the Lower to the

Llpper Permian. The second one is composed of

the Llpper Permian mudstone faciès character-

ized by the occurrence of Follicucullus charveti.

The distribution of F. charveti is strictly restricted

among the Late Permian faunas. The fauna that

includes F charveti is di-stributed in the Upper-

Permian peliric faciès of the Maizuru, Ukra-

Tamba and the Kurosegawa bclts (Caridroit &

De Wever 1986; Ishiga 1990; Isozaki 1997a).

Llpper Permian nnidstone-clasis are probably

derived from these beirs. On rhe conrrary, Llpper

Permian cherts are commonly includcd in rhe

Jurassic AC of the North and South Chichibu

belts in rhe Qiiier Zone of SW Japan (Fig. 11).

In the Inner Zone, they are common in the

Jurassic AC of the Mino-Tamba Belt (e.g., Ishiga

& Imoto 1980; Kuwahara 1997).

PROVENANCE OF CHERT AND

MUDSTONE GRAVELS IN RYOSEKI-

MONOBEGAWA GROUP

Among thèse radiolarian-bcaring gravels and

clasts. Triassic to Early Jurassic chert pebbles and

Early to carly Middie Jurassic mudstone clasts are

probably derived from the AC of the North

Chichibu BcJt. On the contrary, chc late Middie-

Late Jurassic and earliest Cretaceous mudstone

chîst.s are consideied to be derived from the équi¬

valents ol the Torinosu group (Isliida 1994). The

same species of lace Middie-Latc Jurassic and the

carlicsc Cretaceous radiolarians are common in

the Torinosu gioup, The Torinosu group is

upper Middle-Uppcr jurassic and lowest

Cretaceous open-sca and shallow marine sédi¬

ments composed of mudstone fades with srnall

amouiu of sandstones. muddy limestones and

conglomérâtes. The thickness Is thinner than

250 m. 'Fhe Torinosu group is now distnbuicd

in the South Chichibu Belt and the somh unit of

the Kurosegawa Belt whcre the group unconform-

ably ovcrlies the pre-Jurassic ACs and the Triassic

shallow^marine formations (Fig. 11). Ün one

hand, rhe shallow-marine Triassic formation is

never distributed in the norçh unit of the

Kuro.scgawa Belt nor North Chichibu Belt where

the Ryoseki-Monobegawa group unconformably

overlies the Permian AC directly. Thene are large

stratigraphie and faciès gaps between the

Permian AC and rbe Lower Cretaceous paralic

formations in rhe north unit of the Kurosegawa

Belt, whereas the Lower Cretaceous Takegatani

GEODIVERSITAS • 1999 • 21 (4)

651

Ishida K.

Age Lithology Assemblage or index species

Archaeodictyomitra pseudoscalaris

Reworked into Ryoseki-Monobegawa

group by érosion

Sethocapsa pseudouterculus

Eucyrtidiellum pyramis

Pseudodictyomitra primitiva

Sethocapsa horokanaiensis

Cinguloturhs carpatica

Stylocapsa {7) spiralis

Tricofocapsa conexa

Eucyrtidiellum unumaensis

Thcolocapsa fusiforwis

Tricolocapsa plicarum

Parahsuum (?) grande

Parahsuum ovale

Gigi fustis

Parahsuum simplum

Corum speciosum

Sarla (?) extenta

Capnodoce sansa

' Triassocampe long _ _

Pararues ticyrîium mediofassanicum

Hozmadia reticulata

^ Annulotriassocampe campanilis

^\PseüdostvlosDhaera iaponica

\Pseudosty/osphaer3 japonica

[ Eptingium nakasekoi

\ Triassocampe aff. scalaris

\Hindedorcus holdsworthi

Albaillella aff. levis

Albaillella triangularis

Albaillella exceTsa

Follicucullus porrectus

Follicucullus scholasticus'

'Follicucullus charveti

Albailella triangularis

Follicucullus porrectus

Follicucullus scholasticus

E M

^Albaillella asymmetrica

Pseudoalbaillella scalprata

\m. postscalprata

chert

dethtal fine clastics

black mudstone & siliceous mudstone

conglomeratic formations of

Ryoseki-Monobegawa group

Fig. 10. — Schematic columns showing the oceanic plate stratigraphy of the provenancia! terranes. They are inferred from the radio-

larian-bearing chert-pebbles and mudstone-clasts in the chert-pebble conglomérâtes of the Ryoseki-Monobegawa group.

652

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians as tracers for provenance of gravels in Lower Cretaceous molasse (Outer Zone of SW Japan)

Cret.

Jura.

L 1

Trias.

Perm.

[

M [

Fig. 11. — Stratigraphy of lhe upper Paleozoic and Mesozoic formations in the North Chichibu, South Chichibu and Kurosegawa

belts in the Chichibu Superterrane. East Shikoku.

group and the Masakidani formation that are

équivalent of the Ryoseki-Monobegawa group

overlic the dbrinosu group in the south unit of

the Kurosegawa Belt and the South Chichibu

Belt. Therc are not important stratigraphie gaps

nor facial différences among the Ibrinosii group,

Ryoseki'Monobegawa group tind its équivalents

(Fig. II).

As a resuit, the auchor considers that chese cherr

pcbbles probably originated from the cherr-clas-

lic séquences and/or complexes of the North

Chichibu Belt. It also indicates that the Lower to

lower Middie Jiiras.sic ACs of the North

Chichibu Belt probably croppcd ont at the conti¬

nental side of the Ryoseki-Monobcgavva group,

and were already croded tn the Harly Cretaceous.

On onc hand, pcbbles and sniall fragments of

mudstones conr.aining the Laie Middie ro Late

Jurassic and tlie earliest Cretaceous radiolarians

probably originated froin the late Middie

Jurassic-carlicst Cretaceous cover formations that

arc the équivalent of the Torinosu group. The

équivalents of the Torinosu group were spread

widely above rhe North Chichibu Bell and they

were eroded together at the samc orogenic event.

PROVENANCE OF ACCOMPANIED

FUSULINACEAN-LIMESTONE PEBBLES

In addition ro chert pcbbles, the conglomerate of

the Lower Hanoura formation also conrains

small gravels of micritic limestones. Limesrone

gravels usually do not dérivé from long distances,

as river warets usually hâve acidic chemical

conditions, *I*hey contain Permian and Carhoni-

ferous (usLilinids specics nf FîL<iilinellt7^ Neo-

schwageririti and Yfiheiun. Among ihem,

N. cratictilifera i.s characteri.siic of rhcsc micritic

limcstonc gravels. Large blocks of white micrircs

that contain species of Ffeoschwagerina, Yabeina

and Fusulinelld arc characteristk in rhe Jurassic

ACs of the North and South Chichibu belts,

whereas rhe Cvlnniii-Lcpidolnta bearing niuddy

limesione.s are charactcri.stic in ihc Kurosegawa

Belt (Ishii 1990). Ir suggests thaï the North

Chichibu and rhe Kurosegawa belts belong to

two distinct units. It is also remarkable thaï the

fusulinid'bearing whiie micriie pebblcs are in-

cluded in rhe cherr-pebble conglomérâtes.

Thcretorc, iliese rniciite pebbles aie piobably

derived from the limesrone blocks of the North

GEODIVERSITAS • 1999 • 21 (4)

653

Ishida K.

Chichibu Belt. They are rransported together

with the radioUrian-bcaring chert pcbbles and

mudscone clasrs. Based on paleocurrcnc évi¬

dences (Marsukawa bc Tsuncoka 1993) and

faciès analysis (Ishida et ai 1992, 1996), sédi¬

ments of the Ryoseki'Monobcgawa group were

transported from the norchwesr to the southeast.

The direction of transport is relevant ro a poten-

tial provenance from the Norrh Chichibu Bcit.

Acknowledgements

The author would like to thank Prof. P. De

Wever, Prof. M. Faure and Dr. F. Cordey for

rheir critical readiug of the manuscript. I also

thank Dr. A. Matsuoka and Dr. K Hirsch sugges¬

tion about iny plan for the presenrarion. Sinccre

thanks arc also due co Dr. S. Kojima and Dr.

N. Bragin w'ho gave me valuable comments and

suggestions on the distribution and confinuiry of

the Jurassic accrcrionar)^ complex in East A.sia.

Dr. Y. Ispzaki is sinccrely chanked lor giving

frank comments about the Mikabu-Sambagawa

metamorphism. I also would like to thank

E. Lambert and A. Shinomiya who helped me

for the préparation of the manuscript.

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Islands. in Chatig K.-H. (cd.), Environmcntal and

tectonic history of East and South A.sia with

emphasis on Cretaceous corrélation (IGCP 350),

Procccdinei of }5th Internotittnal Symposium oj

Kyungpook National [JmveniTy^ Taegu: 11-41.

Miyamoto 1- & Kuwazuru J. 1993. — Findings of

Early Jura.ssic radiolarians from the liashirimizu

formation ar thc Mîkawa valley, Kumamoto prcfcc-

ture, Kyushu and its geological significancc. in Yao

A. (ed.), Proceedin^ ofdth Radiolarian Symposimn^

News of Osaka Mkropaleontolo^sts^ Spécial Volume,

Osaka 9: 165-175.

Nakaseko K.. & Nishimura A. 1979. — Upper

Triassic rudiolaria Iront Southwest Japan. Science

Report of CoUeg^t of General Education Osaka

Univeriity^ 0.s.tka 28: 61-109.

Sashida K 1988. — Lower Jurassic multisegmented

Nassellaria front the Itsukaichi are;i. western part of

Tokyo l'refetturc, Central Japan. Science Report of

Institme of Geosciences. LTnivcrsity of T.sukuba,

Section B. l'sukuba 9; 1-2"’.

Seiders V. M. be: Blomc C. D. 1984. — Clasi compo-

nenc of Upper Me.sozoic congloniçrates of thc

California Coast Ranges and their tectonic signifi-

cance, in Blake M. C. Jr. (ed.), Franciscan Geology

of Northern California, Society of Economie

Palcontologists and Mineralogists, Pacific SectioHy

Bakfsficld 43: 135-148.

— 1988. — Implications of upper Mesozoic con-

glomerate for suspect terrane in western California

and adjacent arca.s. Geological Society of America,

Bullerin, Boulder 100: 374 -391.

Sugiyama K. 1992. — Lower and Middie ‘Lriassic

radiolarians from Mt. Kinkazan, Gifu préfecture,

central j-jp.an. l'ranutctions and Proceedings of

Paleontological Society of fapan, New Sériés, 'Eokvo

167:1180-1223.

Suyari K., Kuwano Y. & Ishida K 1980. —

l^iscovery of lare Tiiassic conodonts from the

Sambagawa metamorphic belr proper in Western

Shikoku. journal oj Geologita! Society oj Japan,

Tokyo 86: 827, 828 [in Japanese with Hnglish ab¬

stract].

— 1982. — Scratigrapbv and geological structure of

rhc Mikabu grcenrock terrain and its cnvtron-

mcncs. IL Soinc information abour thc Mc.sozoic

stratigraphy of thc North subbcit of the C'hkhibu

Belt. Journal of Science, üniversity of Tokushima,

Tokushima 15: 51-71 [in Japanese with English

abstract].

Suzuki H- bc [tyya T. 1994. — Acerctionarv com¬

plexes of the Kurosegawa» northern Chichitu and

Sanbagawa beit.s in the Kamikatsu town area

(Shikoku), Southwest Japan. of Geological

Society oj Japan. lOkyo 100 (8): 585-599 [in

Japanese with English abstract].

Taira A.. Saito Y. bc Hashimoro M. 1981. —

Fundamernal process in lurrnation of thc Japanese

Islands. Oblitine subduction of plates and strike-

slip movemenr. Kagaku, l'okyo 51: 508-515 [in

Japanese].

Ta.shiro M. 1986. — Palcobiogcograpby and palcoe-

cology of thc Creiaccous System of Southwest

Japan. Fwi/Zf, Tokyo 4î : 1-16 (in Japanese].

Tashiro M. Zk Ko/.ai T. 1991. — Bivalve fossils from

lhe type Monobcgavva gtoup (Pan V). Research

Report of Kochi UniverdtVi Kotbi 40: 189-204.

Tazawa J. 1993. — Pre-Neogene tecronlcs of the

japanese Islands lrc»m the viewpoint of paleobio-

Joutnal oj the Gealoyjxal Society of Japan,

Tokyo 99 (7): 525-543 |in Japanese wirh English

abstract].

Yao A. 1982. — Middie l'riassic to early Jurassic

radiolarians from the Inuyama area, Central japan.

humai of Geoscience of Osaka City Vnivcrsity,

Osaka 25; 53-70.

— 1990. — Triassic and Jurassic radiolarians, in

Ichikawa K. et ai (eds), Pre-Crctaccous Terranes of

Japan, Publication of IGCP Project: Prc-Jurassic

Evolution ofEasiem Asia, Osaka 224: 329-345.

Suhmitted for publication on 29 january 1998;

accepted on 3 November 1998.

656

GEODIVERSITAS • 1999 • 21 (4)

Lower Triassic (Spathian) radiolarians from the

Kuzu area (Tochigi Préfecture, central Japan)

Yoshihito KAMATA

Department of Earth Sciences, Faculty of Science, Yamaguchi University

Yamaguchi 753-8512 (Japan)

kamakama@po.cc.yamaguchi-u.ac.jp

Kamata Y. 1999. — Lower Triassic (Spathian) radiolarians from the Kuzu area (Tochigi

Préfecture, central Japan). in De Wever P. & Caulet J.-P. (eds), InterRad VIII,

Paris/Bien/ilte 8-13 septembre 1997, Geodiversitas 21 (4) : 657-673.

KEYWORDS

Ashio Terrane,

conodonts,

Entaciiniidac,

Palaeoscenidiidae,

Radiolaria,

5paihUn.

Lower Triassic.

ABSTRACT

A well-preserved Lower Triassic radiolarian fauna was found in a siliceous

claystone and cherr séquence in the Kuzu area of the Ashio Terrane, central

Japan. This fauna includes “Paleozoic type” radiolarians represented by spi-

cular type Palaeoscenidiidae and Entactiniidae with some common species of

the Latc Early Lriussic Purentactinin rtakatsugawaemis (Pn) Assemblage.

Spathian conodonts Ncospathodus trianguLiris (Bcnder) and Neohindfoddla

benderi (Kozur & Mosricr) co-occur with these radiolarians. Bascd on the

faunal analy.sis and chronological dating by conodonts, ihis radiolarian buna

probably represents an older part of the Pn Assemblage, w'here “Paleozoic

t)'pe’' Enractiniidac are still a dominant componenr in Early Triassic time.

MOTS CLÉS

1 errane d’Ashio.

conodontes,

Emactiniidac,

Palaeoscenidiidae,

Radiolaria.

Spathien,

Trias inferieur.

RÉSUMÉ

Ritdiolaires triassiques inférieurs (Spathien) de la région de Kuzu (Préfecture de

Tochigi, Japon central).

Une faune bien conservée de radiolaires du Trias inférieur a été trouvée dans

une série de pciites siliceuses et de jaspes dans la région de Kuzu, Ashio

Terrane, Japon central, (’ette faune inclut des radiolaires de « type paléo¬

zoïque » représentés par des spiculés de type Palaeoscenidiidae et Entacti¬

niidae avec quelques espèces communes de l’Assemblage à Parentactinia

nakatsugatoaensts (Pn) de la fin du Trias inférieur. Des conodontes spathiens

Neospathodus triangularis (Bendcr) et Neohindcodrlla benderi (Kozur ôf

Mostler) co-existent avec ces radiolaires. Sur la base des faunes analysées et de

la datation par les conodontes, cette faune de radiolaires représente probable¬

ment une partie ancienne de l'assemblage à P. nakatsugawaensis, dans lequel

les Entactiniidae de « type Paléozoique » sont encore dominants au Trias

inferieur.

GEODIVERSITAS • 1999 • 21 (4)

657

Kamata Y.

INTRODUCTION

Since radiolarian extraction by the HF method

was established, the biostratigraphy and taxono-

my of Triassic radiolarians has developed rapidiy

mainly in the European Terhys (e.g., Ko7Air 6c

Mostler 1972; Duniitrica 1978a, b; De Wever ei

ai 1979), western North America (e.g-, Pessagno

et al. 1979; Blome 1984), and western Pacific

régions (e.g., Naltaseko & Nishimura 1979; Yao

1982). Due to rhe scarcir>' of radiolarian-bearing

Lower Triassic vsequences around the world,

Power Triassic radiolarian biostratigraphy lags

well behind thaï of the Middit Triassic to

Jurassic (e.g., Matsuoka Yao 1986: Hori 19S8,

1990: Matsuoka 1995a. b; Sugiyaina 1997).

Lithological and geochemical investigations hâve

recently been undertaken in Upper Permian and

Power Triassic sequences involving the Permian-

Triassic (P-T) boundary in varions areas in Japan

(Yamakita 1987; Ishida et ai 1992; Kuwahara et

ai 1991; Sugiyama 1992; Kamata & Kajiwara

1996). Only limited information is available on

the biostratigraphy of Diwer Triassic radiolarians

(Sashida 1983, 1991: Sashida & Tgo 1992;

Sugiyama 1992, 1997; Blome Reed 1992;

Nagai & Mizutani 1993: Kozui et al. 1996).

Biostraiigraphic and taxonomie investigations arc

important to establish the transition betM'cen the

Paleozoic and Mesozoic radiolarian faunas.

Accordingly, rhis paper présents results of a detai-

led investigation of Power Triassic radiolarians in

the Kuzai area of the Ashio Terrane, Tochigi

Préfecture. In a preliminary report, Kamata

(1995) described Power Triassic radiolarian bios¬

tratigraphy from a section belonging to die Kuzu

Complex. In rhis paper, the systematics ol Power

Triassic radiolarians from two samples in the

same section are presented.

GEOPOGIC SETTING

Power Triassic radiolarians were obtained from a

Maebashi

139 15

36”20'H

Ashio sedimentary complex | ; Granitic rocks

[ ~ I Tertiary and Quaternary volcanic rocks | | Alluvial deposits

Utsunomiya

SEA OF JAPAN

Fig. 1 . — Index map showing A, the distribution of Inner Zone of Southwest Japan; B. the outline of geology of the Ashio Mountains;

M.T.L.. Médian Tectonic Line; l.-S.T.L., Itoigawa-Shizuoka Tectonic Line; T.T.L,, Tanakura Tectonic Line.

658

GEODIVERSITAS • 1999 • 21 (4)

Spathian radiolarians

siliceous claystone and bedded chcrc sequence of

the Kuzu Complex (Kamata 1996) in the Ashio

Terrane (Fig. 1). The Kuzu Complex consists

mainly ot stacked slices of a cherr-clasric séquen¬

ce with huge rhrusi sheeis of greenstone and

limestone. The chert-claitic sequence is formed

of Lower Trlas.sic black carbonaceous or siliceous

claystone, Middie Triassic to Lower Middle

Jurassic chert, and Middle co Lower Lfpper

Jurassic clasric rocks (Kamata 1996, 1997). The

investigated section, bclonging to die lower part

of rhis complex, is located at the southeastern

part of Tanuma Town, Aso-Gun, Tochigi

Préfecture (Fig. 2). Ir is exposcd along a coad-cut

of the Natund Laboratory of Tofq'o Universiry of

Agriculture and Technology. The section is com-

posed of altcrnating black .siliceous claystone and

dark gray cherr with pale green siliceous clay-

scone interbeds. The occurrence of représentative

species of the Parentactina nukatsugawaemis (Pn)

Assemblage uf Sugiyama (1992) were reported

from rhis section prcviously (Kamata 1995). The

tentative stratigraphy of this section is established

in ascending order as follows (Figs 3, 4):

Unît A. Srrongly sheared sandstonc, approxima-

tely 2 m rhick.

Unit B. Gray, medium-grained sandstone inclu-

ding blocks of bedded cherr yielding Upper

Triassic radiolarians, about 8 m thick.

Fig. 3. — Route map along the road*cut of the Natural Laboratory of Tokyo Institute of Agriculture and Technology showing the

occurrence of siliceous rocks and radiolarian localities. a, gray bedded chert; b, greenish gray siliceous claystone intercalated with

black siliceous claystone and black chert; c, sandstone; d, sheared zone; e, strike and dip of bedding plane; f, strike and dip of fault

plane.

GEODIVERSITAS • 1999 * 21 (4)

659

Kamata Y.

TNK-R-09

TNK-R-08

TNK-38

TNK-37

TNK-36

TNK-35

TNK-34

10 m

Fig. 4. — Columnar section of the study section, a. bedded

chert; b. siliceous claystone with layer of chert; c, sandstone;

d, sheared zone: e, fault.

Units C, D. Both unies composed of pale green,

fissile, siliceous clRysrone; wcll-developed .scaly

cleavages developed siibparallel to bedding plane.

Unît E. Unit composed mainly of pale green

claystone wîili inrercalation.s ol black siliceous

and/or gray ro black chert layers a few centime-

ters thick. The black siliceous claystone is rather

muddy cornpared with the chert, and more sili¬

ceous than the pale green siliceous claystone. The

black siliceous claystone is similar lo the muddy

chert of Sugiyama (1992). Thickness and

amount ot the black siliceous claystone and chert

layers increases upwards in the unit; siliceous

claystone and chert layers alternate in the upper

part. Minor folding is présent. Ahcrnacing black

siliceous claystone (TNK-R-08) and black chert

(TNK-R-()9) front the upper part of Unit E

contain Spathian radiolarians and conodonts.

Radiolarian fauna from samplcs ’l’NK-34 to

38 described by Kamata (1995) is also of

Spathian âge.

Unit R Well-hedded gray to black chert contai-

ning Mîddiç Triassic radiohirians of the

Triasîocanxpe deweiKi'l Assemblage of Yao (1982).

GEOLOGIC AGE AND RADIOLARIAN

FAUNA

Sample TNK-R-OO contains a radiolarian fauna

comparable to the Parentactima nakatsugawaensis

Assemblage of Sugiyama (1992) and also a rich

conodont fauna composed of Neospathodm tri-

U7iguLirh (Bcndei 19*^0), N. clinatm Orchacd &

Sweet, 1995, Cornudina igoi Koike, 1996,

Neohmdeodella baideri (Ko/ur & Mostler, 1970),

and manv unidentified ramiform éléments

(Fig. 5). No agc-diagnostic conodonts are présent

in sample TNK-R-08 whicli contains very well-

preserved radiolarians.

Neospathodus triangularis (Bender, 1970) and

Neohindeodella henderi (Kozur Ôc Mostler,- 1970)

are well-known l/ate Early Triassic conodont spe-

cies (Fig. 6). The occurrence ol Ne<npathodus tri-

angularis (Bender, 1970) has bcen reported from

the Spatitian of ihe Tcthyan région in Kitshmir,

the vSalt Range, Spin, and Japan (e.g., Sweet et ai

1971: Gocl 1977; Koike 1981; Matsuda 1985).

Matsuda (1985) and Sweet (1988) summarized

the conodont zonations and indicated ranges of

Lowei Triassic conodonts based on these biostra-

tigraphic investigations. In thcsc régions, N. tri-

angiilaris îs onc of the main componenrs of the

Spathian conodont fauna. The base of the N. tri-

iinguLiris-N. hormeri zone (Matsuda 1985) and

N. triangulatis zone (Sweet 1988). both indicati¬

ve of the lower Spathian, are defmed by the first

occurrence of rhis species. In Japan, N. triarigu-

laris is a characierisiic specie.s of the A^.

triangularP-N. ? collinsoni zone of the lower

Spathian (Koike 1981). Furthermore, Koike

(1996) described Cornudina igoi from the Taho

Formation distributed in Ehime Préfecture south-

660

GEODIVERSITAS • 1999 • 21 (4)

Spachian radiolarians

Fig. 5. — Spathian conodonts from the TNK-R-09. A, Neospathodus triangularis (Bender); B, C, Cornudina igoi Koike; D, H,

Neohindeodella benderi ^Kozur & Mostler); E, F, Neospathodus sp.; G, ? Neospathodus clinatus Orchard & Sweet. Scale bars:

100 pm.

wcst Japan, and indicated that this species occurs

in the basal part of the N. trunigubris-N, horme-

ri zone of û\c lowex Spàihian (Fig. 6).

The radiolarian fauna in this paper consists

mainly of Palaeoscenidiidae and Encactinudae

with some common specics of the Pn Assemblage

of Sugiyama (1992) and TRI zone of Sugiyama

(1997). The fauna is rcpresented by species of

Archaeoseniautis, Parentactinia, Entactiriia (?),

Enlactinoiphaera (?), Ctypiostephanidiunh and

Pantancllium (?) (F'ig. 7). Tripod or mono-seg-

mentcd Nasse!larians, such as Hozmadia and

mulci-scgmcnr Nasscllaria such as Triassocampe

rarcly occur.

SERIES

LOWER TRIASSIC : MT.

Stage

Smithian : Spathian Ani.

conodont zones (Koike 1981)

N. dieneri- « N.triangularis- ^

N. conservatius ' N.7 collisoni

Neospathodus triangularis

(Bender)

Cornudina igoi Koike

Neohindeodella benderi

(Kozur & Mostler)

Fig. 6. — Known ranges of detected conodont species plotted on the conodont zones proposed by Koike (1981).

GEODIVERSITAS • 1999 • 21 (4)

661

Kamaca Y.

number

TNK-34

TNK-35

TNK-36

TNK-37

TNK-38

TNK-R-08

TNK-R-09

species Lithology

s.c. ch. s.c. ch. ch. s.c. ch.

-Arc/iaeosemanf/s brevispinosa Kamata

Archaeosemantis crisiianensis Dumitrica

Archaeosemantis sp.

Archaeothamnulus sp.

Parenîacîjnia karasawavamaensis Kamata

1 + + + 1

1 + + 1 1

1 1 1 1 1

1 1 1 1 i

+ + + + +

1 1 + + 1

\Parentactin(a nakatsugawaensis Sashida

Parentactinia sp. A

iParentactinfa okuchichibuensis (Sashida)

Parentactinia sp.

\Protopsium sp.

+ - + + + + +

+ + + -- + +

+ + + - + - +

Plafkenuwsp.

Pantaneihum (?) virgeum Sashida

Pantanelliurrt (?) sp. A

Pantanellîum (?) sp.

\Tiborelfa agrfa Suqiyama

1 + 1 + i

i + 1 1 1

+ +II +

1 + i 1 1

1 + + + 1

1 + 1 1 1

Hozmadia et. ozawai Sugiyama

Hozmaciia sp.

Cryptostephanidium longispinosum (Sashida)

\Cryptostephanfdium sp.

'Oer//;sponaus sp.

1 + 1 1 1

+ + + + +

1 1 1 1 1

1 + + + 1

+ + +I +

1 1 1 1 1

Triassobipedts (?) sp.

Zeviusi?) sp.

Ëntactinia (?) îanumaensis Kamata

Bniactima nikorni Sashida and Igo

Potventactinia (?) crux SuQiyama

1 1 1 1 1

1 + + 1 +

1 1 1 1 1

+ 1111

+ 11 + 1

+ + 1 1 1

1 1 1 1 1

Polyentactinia furutanii Sugiyama

Poiyûntacbnis sp.

Entactinosphaera (?) sashidai Kamata

Entactinosphaera chiakensis Sashida and Igo

Entactinosphaera sp

1 1 1 1 1

+ 1111

1 1 1 1 1

+ + + + +

+ 1111

Thaisphaera (?) Igoi Kamata

^Entactiniidae gen. et sp. indet

1 1

+ +

1 1

1 +

Fig. 7. — List of Early Triassic radiolarians from the study section, s.c., siliceous claystone: ch,, chert.

Sugiyama (1992) considered the âge of Pn

Assemblage as late Spathian based on co-occur-

ring conodonts belonging to the Neospathodus

hormeri Assemblage but suted that the lower

limit of this assemblage is unknown. Rccently,

Sugiyama (1997) comparcd TRO and TRI with

the lowcr part and the upper part of the Pn

Assemblage of Sugiyama (1992), respectively. In

this study, N. triangiilaris (Bender, 1970) and

Cornudina igoi Koike, 1996 arc associated with

some commun radiolarian spccies of the Pn

Assemblage. Kusunoki & Imoto (1996) also

reported a radiolarian fauna attributed to the Pn

Assemblage associated with the lower Spathian

conodonts N. triangulam and Gondolella jubata

(Sweet, 1970). They emphasized that the Pn

As.scmblage ranges down to the lower Spathian.

This présent evadence suggests that the range of

some species of the Pn Assemblage may extend

down to the lower Spathian.

As hriefly stated above, the radiolarian fauna dis-

cussed herc has both Palcozoic and Lower Triassic

affinities. The family Entactiniidae is panicularly

abondant exceeding more than 50% of the cotai

number of the idcntified radiolarian species within

this fauna. Considering the range of the cono¬

donts, the radiolarian fauna represents an older

part of the Pn Assemblage (Sugiyama 1992) and

662

GEOOIVERSITAS • 1999 • 21 (4)

Spachian radiolarians

TRO (Sugiyama 1997), and “Paleozoic type”

Entactiniidae are still a dominant component in

Early Triassic assemblages. Futher analysis of

Spathian radiolarian faunas is necessary because

FollicuculuSy a représentative species of TRO, bas

not been found in the studied section.

METHODS AND TECHNIQUES

Radiolarian specimens were separated from sili-

ceous rock .samples in the following manner:

(1) rock samples were crushcd inio small frag¬

ments of several centimeters; (2) crusiied samples

were placed in five percent hydri>fluoric acid for

24 hours; samples were wa.shcd and sieved

using a mesh ot 50 pm opening, tlic residue was

dried in an oven. Well-prescn^d radiolarian .spé¬

cimens were mounted on an SEM plug and gold

coared in a vacuum evaporator. The surface tea-

tures and inner .structures were observed with the

Scanning Electron Microscope.

SYSTEMATIC PALEONTOLOGY

Ail figured specimens are deposited in collcctionvS

of the Department of Earth Sciences, University

of Yamaguchi (DEUY).

Subclas-s RADIOLARIA Müller, 1858

Order POLYCYSTINA Ehrenberg, 1838

emcfid. Riçdel, 1967

Suborder SPUMELLARIA Ehrenberg, 1875

Family PalaEOSCI-NIDIIDAE Riedel, 1967

emend Holdsworth, 1977

dmws Archaeosemantis Dumitrica, 1978b

Archaeosentantis brevispinosa n. sp.

(Fig. 8A-C)

Types. — Holor^’pc, Figure 8A, TNK-R-08, DEUY-

YK3617; pararvpes, Figure 8B, TNK-R-08, DEUY-

YK3627, Figure 8C, DEUY-YK3618.

Etymology. — Brevispinosa means having short

spines.

Occurrence. — Sample TNK-R-08, Kuzu area,

central Japan.

Dimensions (pm). — Based on eight specimens:

Icngth of apical spines 5.0 to 21.8 (average 15.9);

length of basal spines 72.8 to 126.0 (average 85.3).

Description

Species composed usuaJIy of eight spines consis-

ting of four apical spines and four basai spines,

arising from a short médian bar (MB). The four

basal spines are conical, short, rod-like, and rug-

ged. Two, conimonly straight basal spines diver¬

ge from one end of MB. Three or four apical

spines; spines conical, very short, and obliquely

divergent upward from end of MB at a smaller

angle.

Remarks

(3ompared with other ArchaeosemantiSy the basal

and apical .spines of this species are shorter.

Archaeosemantis cristianensis is similar to this spe-

cies, but difiers by possessing long and down-

wardly curved basai spines.

Archaeosemantis cristianensis

Dumitrica, 1982

(Fig 8D, H)

Archaeosemantis pterostephanus Dumitrica (part)

I978h: 52. pl. 5, figs 7, 8 (non pl. 5.Tigs 9-12).

ArchaeosCfTianfis erhtianensts Dumitrica, 1982; 423,

pl, 1, lig. lli pl. 3, ftg. lE pl 4, figs 5, 7, 11, pl 6,

fig. 2, pl. 7. figs 3. 12, 13. - .Ando er ai 1991, pl. 9,

fig. 12. -Nagai & Mi/utani 199.3:7, pl. 1, fig. 9.

Archaeosernanrii ventata Sashida, 1983: 171, pl. 36,

figs 1-9; 1991; 686. fig. 5-4. 5, 6, 7, 8. - Nagai &

Mizuuni 1993; 7. pis 1. U.

Archaeosemantis sp. aff. A. venusta .Sashida, 1991: 686,

figs 5-9. - Kamata 1995: fig. 6-1,2.

Archaeosemantis .sp. - Sashîda 1991: 686, fig. 5-1, 2,

Archaeosemantis cristianensis Dumitrica, 1982 mor¬

photype A Sugiyama, 1992; 1209, fig. 14-3.

Archaeosemantis cristianensis Dumitrica, 1982 mor¬

photype B Sugiyama, 1992: 1209. fig. l4-6.

Occurrence. — Common in TNK-R-08, 09, Kuzu

area, Tochîgi Préfecture. Mc. Kinkazan and

Minokamo City, Gifu Prélecture. Kanto Mountains,

Saitama Préfecture, central Japan. Vicentinian AIp.s,

Italy.

Remarks

Dumitrica (1982) described specimens ofA. cris¬

tianensis having broad variation in the disposi-

GEODIVERSITAS • 1999 • 21 (4)

663

Kamata Y.

tion and lengch of spines. Sugiyama (1992) pro¬

posée! rw'o morphorypes A and B for rhis species,

and staced chat phenotypic variation is cau.sed by

the rotation of half of morphotypt? A around the

axis of the médian bar (MB).

Genus Parentactinia Dumirrica, 1978b

Parentactinia karasawayamaensis n. sp.

(Fig. 9G^M)

Tyi’es. — Huloiypc, Figure 9H, TNK-R-OS, DEUY-

YK3493: Pararypes, Figure 9G. TNK-R-08. DEUY-

YK3654; Figure 91, TNK-R-OH, DElJY^YK3h53;

Figure 9J, FNK-R^OS, DEUY-YK3650; Figure 9 K,

TNK-R-08, DHIJY-YK363S; Figure 91., l’NK-R-08,

DFUY-YK3657; Figure 9M. TNK-R-08, DEUY-

YK3533.

Etymology. — Species name karasawayamaensis

cornes irom Karasawayama Shrine close to rhe studied

section.

OccUR-RENCn. — Abundant in TNK-R-OS, Kuzu

area, central Japan.

DimeN-SION.S (pni). — Ba.scd on ten .speciinens: .shell

diameter, 160 to 190 (average 178); length of apical

or basal spines 100 to 220 (average 175); ail spines

broken, see Fig. 9L; wall thickness less than 10.

Description

Species with spherical latticed shell and a spiculé

consisring of seven or cighr rod-likc spines ari-

sing from à short eccentric MB. Rod-like spines

straiglit and penetrating the wall ol shell.

Cortical shell, ttiin, and relaiively smooih surfa-

ccd, enclosing an ecceniric spiculé widi seven or

eight radial spines ând a very short MB. Cortical

shell nearly .spherical and supported by ail radial

spines. Pore pattern of .shell composed of inter¬

sections of bars forming numerous quadrangular

or triangular pore frames. Main radial spines

long, rod-like, and occasionally ciirved tipward

outside of shelh Internai spines arise Irum MB

and penetrate the shell wall, Main spines slightiy

thicker outside shell wall than in the internai

portion. Four apical spines situated in the iipper

hémisphère diverge upwardly at about 45° above

the horizontal plane. Commonly three or four

basal spines. MB is eccentrical.

RJ'MARKS

This new species is similar to Polyentactinia (?)

phauhahingensis^ reported by Sashida & Igo

(1992), but the latter lias an uneven shell wall

lorincd ot intcrsccting bars.

Parentactinia nakatsugawaensis

Sashida, 1983

(Figs 8E-G, I-N, 9A)

llnuamcd Spumellaria — Matsudn üt Isozaki 1982:

pl. 3. fig.s 33-35.

Varcntaeiinia nakatsugawaensis Sashida, 1983:

172-173. pl. 37, fig.s 1^9; 1991: 687. Fig. 5-15, 16,

lies 6-1, 3-6. — Sugiyama 1992: 1212, fig. 14-7-10, ~

Bloine A' Rffd 1992: 376, Fig. 14-3, 4. — N.ïgai &

Mizurani 1993: pl. I, Hgs 1-6. * Kamata 1995: hg. 6-

4. not 8. - Kusunoki & Imoio 1996: 91, Fig. 1, -

Sugiyama 1997-* 184. llg. 27-2.3.

Parentactinia Sa.shida, 1991: 689, Fig. 7.

OCCUKRENCE. — Abundant in TNK-R-08, 09, Kuzu

area, Tochîgi Préfecture. Mt. Kinkazan and

Minokamo City, (.îifli Prélecture. Southern Kameoka

City. Kyoto ITefecture. Kanto Mountains, Saîtama

PrcFccUire, central Japan Oregon, USA.

Dimensions Ipm). — Based on forty-ihrec spéci¬

mens: length of apical spines 21 lo 65 (average 42);

length of basal .spines 65 ro 234 (average 106); diame¬

ter of incomplète .shclls 120 ro 230 (average 136).

Remarks

This species consists of four apical and four basal

spines with a loosc latticed shell. The basal spines

of .sonie spccimcnvS bave stout, slightiy curved,

long branches. Four or fivc branches diverge

medially lo distally along the basal spines. Two

shorter brandies are conical and diverge upward.

Two additional long stout, rod-like branches

diverge inw'ard. Diameter of branches slightiy

sniallcr less diai of basal spines. Each long brandi

beats two to four directional vspinules distally.

The spinales anastomose with each oiher for¬

ming a loosely reticulare shell. Some spccimen.s

posscs.s an almo.st complote single shdl. Surface

of the shell riigged due to minuic spinulcs; porcs

irregular in shape. Shdl is supported by ihc basal

spines and is incomplète apically MB eccentric-

ally situated or tangent lo the shell.

Pareniacnnia nakatsugawaensis was First described

by Sashida (1983) from black chert of the Kanto

664

GEODIVERSITAS • 1999 • 21 (4)

Spathian radiolarians

Fig. 8. — A-C, Archaeosemantis brevispinosa Kamata n. sp., A, holotype, DEUY'YK3617: B, paratype, DEUY-YK3627; C, paratype,

DEUY-YK3618: D, H. A. cristianensls Dumitrica; D, DEUY-YK3629. H. DEUY-YK3481; E-G. I-N, Parentactinia nakatsugawaensis

Sashida; E. DEUY-YK3538; F. DEUY-YK3479; G, DEUY-YK3545; I. DEUY-YK3509: J. DEUY-YK3603: K. DEUY-YK3486; L.

DEUY-YK3506; M, DEUY-YK3588; N, DEUY-YK3422. Scale bars: 100 pm.

GEODIVERSITAS • 1999 • 21 (4)

665

Kamata Y.

Mountains; later Sugiyama (1992) described this

species in greater detail and con.sidered it dia¬

gnostic of the Pn Assemblage of the upper Lower

Triassic. The shell ol this specics is well preserved

and shows variations in development in my

mater i al.

Parentactinia sp. A

(Fig. 9 B)

Figured SPECIMEN. — Figure 9B, TNK-R-08,

DEUY-YK3609.

Occurrence. — Rare in TNK-R-OS, Kuzu area,

central Japan.

Dimensions (pm). — Bascd on two Spccimens: Icngth

of long apical spines 100 to 160 (avetage 129): length

of short apical spines Icss rliaji 20; diarnerer of incom¬

plète shelis 140 10 175 (average 157); width of basal

nemisphere approximately 350.

Remarks

This species is composed of four apical and four

basal spines with an incomplète lauiced shcll.

Basal spines very long, ihick, rod-like, slightly

curved upward, and genily tapered distally. Loose

hemispheric shcll is supported by the four basal

spines.

Parentactinia sp. A is easily distinguished from

P. nakatsugawaemis by possessing very thick basal

and apical spines.

Parentactinia oktichichibtiensis

(Sashida, 1991)

(Fig. 90

Archaeothamnulus okuchichibuensis Sashida, 1991:

687,%. 5-10^ 14.

Parentactinia okuchichibuensis (Sashida) — Sugi)'ama

1992: 1213» fig- l6-2a, 2b. — Nagai & Mizutani

1993: pl. 1, %s 7. 8. - Kusunoki & Imoto 1996: 91,

%. 2 .

Occurrence. —Common in l*NK-R-08, 09, Kuzu

area, Tochîgi Préfecture. Mt. Kinkazan and

Minokamo City, Gifu Préfecture. Southern Kameoka

City, Kyoto Prcfcctiire. Kanto Mountains, Saitama

Préfecture, central Japan.

Remarks

Sugiyama (1992) transferred this species from

Archaeothamnulus to Parentactinia because it pos-

sesses two apical spines. In my material, this spe¬

cies also has two apical spines.

Family Entactiniidae Riedel, 1967

Genus Entactinia Foreman, 1963

Entactinia (?) tanumaensis n. sp.

(Fig. 9D-F)

Types. — Holotypc, Figure 9D. TNK-R-08, DEUY-

YK3500; paratvpc.s, Figure 9F.. TNK-R-OH, DEUY-

YK3522; Figuré 9F, TNK-R-08, DEUY-YK3643.

Etymology. — Tanumaensis is derived from Tanuma

’Fcnvn. Suidied section is located at the southeastern

part of Tanuma Town.

Occurrence. — Common in TNK-R-08, Kuzu

area, central Japan.

Dimensions (pm). — Based on five specimens: length

of main spines 50 to 110 (average 78.7); diameter of

sheli 80 to 100 (average 90).

DESaUPlION

Species with a well-developed latriccd shell with

five to six rod-like main spines and numerous bi-

spines. Latticed shell spherical with five to six

needle-like primary spines. Primary spines pos-

sess shallow groove.s proximally and strongly

taper distally. Spine length ncarlv cqual to dia-

mcccr of shcll. Shcll wall rachcr thick, pcnctratcd

by variably-sized rounded pores. Numerous

radial and very short bi-.spLnes arise Irom the

shell wall. Internai construction unknown.

Remarks

This species is similar to Entactinia nikorni

Sashida Igo (1992), but differs from the later

by possessing strongly tapered nccdlc-like prima¬

ry spines. This species is questionably assigned to

Entactinia because of the absence of three-bladed

spines.

Genus Entactinosphaera Foreman, 1963

Entactinosphaera (?) sashidai n. sp.

(Fig. lOA-D)

Types. — Holotypc, Figure lOA, TNK-R-08, DEUY-

YK3483; paratypes. Figure lÜB, TNK-R-08, DEUY-

\TC3490; Figure lOC. TNK-R-08, DEUY-YK3508,

Figure lOE, TNK-R-08, DEUY-YK3434.

666

GEODIVERSITAS • 1999 • 21 (4)

Spathian radiolarians

Rq. 9. — A. Parentactinia nakatsugawaensis Sashiüa, DEUY-YK3Ô93; B, Parentactinia sp. A, DEUY-YK3609; C. Parentactinia oku-

chichibuensis (Sashida). DEUY-YK3616:,D-F, Enlactinia (?) îanumaensis Kamata n. sp.. D, holotype, DEUY-YK3500; E. paratype.

DEUY-YK3522; F, paratype. DEUY-YK3643; G-M. Parentactinia karasawayamaensis Kamata n. sp.. G. paratype. DEUY-YK3654;

H. holotype. DEUY-YK3495: I, paratype. DEUY-YK3653: J, over View, paratype, DEUY-YK3650; K, paratype, DEUY-YK3653:

L, long apical and basal spines are preserved, paratype, DEUY-YK3657; M, over view, paratype, DEUY-YK3533. Scale bars:

100 pm.

GEODiVERSITAS • 1999 • 21 (4)

667

Kamata Y.

Ei YMOlonv, — Specics name, sashidai is nanied for

Associate Professor Kacsuo Sashida oF Tsukuba

Universiry in honor of his contriburion to the srudy of

Lower Tnassic radiolarians.

OccURRJiNCK. — Commun in TNK-R-08, Kuzu

area, central Japan.

Dimensions (pm). — Ba-sed on fivc specimens : shell

diameter, lüO tu 150 (average 128); length of main

spines, 120 to 210 (average 145).

DESCRJiniON

Test small, spherical, spongy wiih four to six

needle-like main spines. Shell wall of some speci¬

mens des'elops minute circular pores and humps.

Main spines taper to a point. Spines one to rwo

times diameter of shell. Internai structure un-

known.

Remarks

Entactinosphaera (?) sashidai n. sp. is similar to

E. chiakensis but diffcrs by possessing a spongy

shell.

Entactinosphaera chiakensis

Sashida àc Igo, 1992

(Fig. 101, J, L-N)

Entactinosphaera chiakensis Sashida & igo, 1992:

1302, fig. 14-1-7, 9. 10. 15.

Occurrence. — Common in TNK-R-08, Kuzu

area, central Japan. Phatthalung, Southern Peninsular

Thailand.

Remarks

This species consists of outer and inner shells

with four to six needle-like spines. Two shells are

connected by secondary spines.

Family Aci inommume Haeckel, 1862

entend. RJedel, 1967

Gcnus Sashida & Igo, 1992

Thaispbaem (?) igoi n. sp.

(Fig. lOE-H, K)

Types. — Hok.typc> Figure lOF, TNK-R-08, DEÜY-

YK3647; paratypes, Figure lOF., TNK-R-08, DEUY-

YK3637; Figure lOG, TNK-R-08, DEUY-YK3655;

Figure lOH, TNK-R-08, DEUY-YK3622; Figure

lOK, TNK-R-08, DEUY-YK3591.

EtvmOLOGY. — The species is named in honor of

Prof. Emeritus Hisayosht Igo who introduccd me to

the study of the Ashio Terrane.

Occurrence. — Common in. TNK-R-08, Kuzu

area, central Japan.

Dimensions (pra). — Bascd on nine specimens: cor¬

tical shell diameter, 14() to 180 (nverage 160); medul-

lary shell diameter, 50 to 60, length of main spines

100 to 180 (average 110); wall rhicl^ess 13-20 (avera¬

ge 15);. porc diameter less than 20.

DKSCRiniüN

Test consisting of a cortical shell with five to six

priinary spines and an inner medullary shell;

both shells are spherical. Cortical shell rhin-

wallcd, composed of circular lu subcirculaj* pores

with smail nodes at vertices. Inner shell mucb

smaller than outer .shell; diameter approxîmately

one ihird of ihe outer shell. Ckirricjl and mediil-

lary shells connected by six tbin, rod-like beams.

Four to fivc primary spines are ihick, thrcc bla-

ded, and taper distally; primary spines aligned

with internai beams. Length of primary spines

commonly cqual to diameter of cortical shell.

Remarks

Thuisphaera (?) igoi n. sp, resembles Entactino-

sphaem chiakensis Sashida & Igo, but differs from

il by possessing thrce-bladod and shorter main

spines. Thaïsphdera (?) igoi is also vety similar to

T. minuta Sasfiida Igo, but differs by huving

longer and thicker primary spines.

Family Pan rANELl.lUME Pessagno, 1977

Pantanellium (?) tnrgeum Sashida, 1991

(Fig. ljD,G^),L)

Paritanellîum (?) inrgetwi Sashida, 1991: 691, fig. 7-

9-14. — Nagai & Mizutani 1993: pL 3, fig. 4-6. -

Kamata 1995: fig. 6-6, 7,

OccURHENCt. — Rare in TNK-R-08, 09, Kuzu area,

Tochigi Prefocrurc, Mt. Kinkazan and Minokamo

City, Gifu Préfecture. Kanto Mountains, Saitama

Préfecture, central Japan.

RHMy\RKS

Test composed of an ellipsoidal to subspherical

cortical shell, a spherical medullary shell and two

rod-like bipolar spines. Well-prcscrved matcrial

668

GEODIVERSITAS • 1999 • 21 (4)

Spathian radiolarians

Fig. 10. — A-D, Bniactinosphaera (?) sashidai Kamata n. sp.. A, holotype, DEUY-YK3483, B. paratype, DEUY-YK3490; C, paratype,

DEUY-YK3508; D, paratype. DEUY'YK3434; E-H, K, Thaisphaera (?) /go/Kamata n. sp.; E. paratype, DEUY-YK3G37; F, holotype,

DEUY'YK3647, G, paratype, DEUY-YK3655; H. showing internai structure, paratype, DËUY-YK3622: K, paratype, DEUY-YK3591:

I, J. L-N, Entactinosphaera chiakensis SasU\6a & Igo; 1, DEUY-YK3492: J, DEUY-YK3520; L, DEUY-YK3421: M, DEUY-YK3433;

N. showing inner Shell, DEUY-YK3485. Scale bars: 100 pm.

GEODIVERSITAS • 1999 • 21 (4)

669

Kamata Y.

Fig. 11. — A*C, K, Crypfostephanidium longispinosum (Sashida). A, DEUY-YK3625; B, DEUY-YK3634; C. showing arch-like skele-

ton of aj, DEUY-YK3641; K. showing internai structure of A. L. D. and V spinules. DEUY-YK3633; 0. G-J, L. Pantanellium (?) vir-

geum Sashida; D. 0EUY-YK3474; G, DEUY-YK3614; H. DEUY-YK3649; I. DÊUY-YK3438; J, DEUY-YK3498: L. entarqement of D

showing cortical shell and beams, DEUY-YK3475; E, F, Pantanellium (?) sp. A; E, DEUY-YK3466; F, DEUY-YK3430. Scaie bars:

100 pm.

670

GEODIVERSITAS • 1999 • 21 (4)

Spathian radiolarians

shows the medullary shell connectée! to the corti¬

cal shell by numerou-s radia! beams (Fig. l ID, L).

Pantanellium (?) sp. A

(Fig. IIE, F)

Figured SPECIMENS. — Figure IIE, TNK-R-08,

DEUY.YK3466î Figure 11F, TNK-R-OS. DEUY-

YK3430.

Occurrence. — Rare in TNK-R-08r 09, Kuzu area,

central Japan.

Remarks

Test consists of a subspherical to spherical shell

with bipolar spines. Shell wall has very small,

irregular elliptical to circulât pores with well-

developed nodes. Bipolar spines very thin and

possessing slight grooves proximally.

Vantanellium (?) sp. A is distinguished from P. (?)

vïrgeum Sashida by having thin spines and a

spherical to subspherical shell with many pores.

Suborder NASSELLARIA Ehrenberg, 1875

Family Eptingiidae Dumitrica, 1978a

Genus Cryptostephanidium Dumitrica, 1978a

Cryptostephanidium longispinosum

(Sashida, 1991)

(Fig. 11A-C,K)

Spon^rtntepimmdium lon^pimmm Sashida, 1991: 694,

hg. 7-1-8.

? Tripocycliû japonka Nakaseko ^ Ni.shiiTiura, 1979 —

Blome €titl 1986, pl. 8.3, hg. 18.

Cryptostephanidium lungispinosum (Sashida) —

Sugiyama 1997: IKIS, hg. 13-1, 2. - Nagai &

Mhurani 1993- pl. 2, fig. l'3. - Kamata 1995: 28,

Hgs 6-16.

Occurrence. —Abundant in TNK-R-()8. 09, Kuzu

area, Tochigi Préfecture. Mt. Kinkazan and

Minokamo City, Gifu Prcfccuirc. Kanto Mountains,

Sairaina Préfecture, central Japan. Oregon USA.

Remarks

Studied specimens are quite similar to those

above listed for Cryptostephanidium longispino-

sum. Internai shell structure i.s well observed in

broken specimens (e.g., Fîg. 11-C, K) which

clearly show a MB, long apical and primary laté¬

ral spines, and the vertical and dorsal spines as

well as the sagittal ring.

Acknowledgements

I wûuld like to thank Professor Emeritus H. Igo

(Institutc of the Geoscience, University of

Tsukuba) for his valuable suggestions throughout

the course of tins study. 1 heartily thank Prof.

T. Koikc (In.stitLitc of Geology, Yokohama

National University of Yokohama) tor conodonr

identifications and important suggestions:

Associatc Prof. K. Sashida (Institutc of Geo-

science, University of Tsukuba) for his sugges¬

tions and critical readiiig of the manuscript; and

P. Dumitrica. S. Gorican. and A. Ohler for theic

rigorous review and variable comments and sug¬

gestions. Finally, spécial thanks to E. S. Carter

for her révision of English text of the manus¬

cript.

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Triassic lEultoUria frnm Siniihwcsi j.apan. Science

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Nak.îzawa K., Ishibashl 7’., Kîniura P., Koike T.,

Shimizu D. bi Yao. A. 1994. — Triassic hiosrrati-

graphy of Japan bosed on varîous taxa, tn Guex j.

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Pessagno E. A. jr. 1977. — Upper jurassic Radiolaria

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Sashida K. 1983. — Lower Triassic Radiolaria from

the Kanto mountains central Japan. Part 1:

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— 1991. — Early Triassic Radiolarians from the

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Submitted for publication on 3 June 1998;

accepted on 6April 1999.

GEODIVERSITAS • 1999 • 21 (4)

673

Radiolarian biostratigraphy of the Jurassic-Early

Cretaceous chert-clastic sequence in the Taukha

Terrane (South Sikhote-Alin, Russia)

Igor V. KEMKIN

Far East Geological Institute, Far Eastern Branch, Russian Academy of Sciences

Prospect 100-letiya Vladivostoka, 159, Vladivostok, 690022 (Russia)

fegi ©online, marine,su

Raisa A. KEMKINA

Far East State Technical University

Poushkinskaya Street, 10. Vladivostok, 690090 (Russia)

Kemkin I. V. & Kemkina R. A. 1999. — Radiolarian biostratigraphy of the Jurassic-Early

Cretaceous chert-clastic sequence in the Taukha Terrane (South Sikhote-Alin. Russia), in

De Wever P. & Caulel J.-P. (eds). InterRad VIII, Paris/Blerville 8-13 septembre 1997,

Geodiversitas21 (4) ; 675-685

ABSTRACT

This paper présents rhe results of biostradgraphic investigations of cherrv' and

cerrigenous cleposits from the Taukha Terrane. Twelve successive radiolarian

assemblages which correspond lo the upptr Pliensbachian-lowcr Toarcian,

lowcr-middlc Toarcian. upper Toarcian-middie Aalenian, upper Aalcniaiv

lower Bajocian, middic Bajocian, upper Bajocian-lowcr Bathonian, middle

Bathonian-lowcr Callovian, middic Oxfordian-Iowcr Kimmcridgian. middle-

upper Kimmeridgian, lower-middle Tithonian, upper Fiihonian, and lower

Valanginian-luwer Barrcmian deposiu ot ihe continuons section hâve becti

distinguished. Characteristics of the radiolarian assemblages are shortiy given.

RÉSUMÉ

Biostratigraphie à radioLiire d'une séquence siliciclastique d'àge jurassique-créta¬

cé inférieur dans la ïaukha Terrane (stul de Sikhote-Alin, Russie).

Cet article priJscntc les réstilrats d'une recherche biosirarlgrapliiquc réali,sc^c

sur des dépôts siliceux et dccritiqucs de la Taukha Terrane. Une douzaine

d’assemblages consécutifs de radiolaires a pu être reconnue dans les sédiments

d'une série continue ou Ton peut reconnaitre le Pliensbachien .supérieui-

Toarcien inférieur, le Toarcieii moyen inferieur, le Toarcien supéiieur-

Aalenien moyen, l'Aalénien supérieur-Bajocien inférieur, le Bajocien moyen,

le Bajocien supérieur-Bathonien inférieur, le Batlionien moyen-Callovien

inférieur, l’Oxfordien moycn-Kimmeridgien inférieur, le Kimmeridgien

moyen supérieur, le l ithonique inférieur à moyen, le I ithonique supérieur

et le Vaianginien inférieur-Barrémien intérieur. De brèves descriptions des

assemblages à radiolaires sont données.

MOTS CLÉS

Radiolaires,

Jurassique,

Crétacé inférieur,

Taukha Terrane,

Sikhote-Alin,

prisme d'accrétion.

KEYWORDS

Radiolaria,

Jurassic.

Early Cretaceous.

Taukha Terrane.

Sikhote-Alin,

accretionary prism.

GEODIVERSITAS • 1999 • 21 (4)

675

Kemkin I. V. & Kemlcina R. A.

INTRODUCTION

Cherty rocks are important in the geological

structure of the South Sikliote-Alin. They com¬

prise up to 35% ol the sections of Mesozoic

accretionary prisms, lhat are among the main

structural units of tlie région. Flowever, paleon-

tology of these chertJâ is, în most cases, poorly

studied. Cherts hâve bccn descrihed Irom separa-

ce samples that allowed them to bc datcd accura-

tely to a period or an epoch. The ranges of the

microfaunal species in them hâve not been tra-

ced, Also, elemcntary biostratigraphic subdivi¬

sion has noL been constructcd and thercfore,

comparison and corrdation of the varions species

could not be carricd out. l’hc study of Pcrmian

chcrt dcposits is rclaiivcly more succcssfuh sincc

biostratigraphic subdivisions and zonal scalcs

hâve been proposed (Rudenko 1991), Sonie local

sections ofTriassic (Vololchin et ai 1990; Bragin

1991; Smirnova &: Lepeshko 1991) and Early

Jurassic cherts (Kemkin 6c Golozoubov 1996)

hâve also been studied, and laycrs with ddîcrcnt

microfaunal assemblages hâve bccn distingua

shed. The younger cheny formations hâve not

been broken down into clementary biostratigra¬

phic subdivisions with the exception of preÜmi-

nary data on Gorboushinskaya suite (Bragin

1993). Given below arc the results of the micro¬

faunal study of rhe most complète chcrt sections

and overlying terrigenous dcposits ot the Tauklia

Terrane, exposed on rhe Iclt bank of Roudnaya

River (south-east of Dalnegorsk Town).

GEOLOGICAL SETTING OL THE REGION

The Dalnegorsk Région is situated with in the

Taukha Terrane (Fig. 1), an Early Cretaceous

accretionary prism (Khanchuk étal. 1989;

Golozoubov et al. 1992; Kemkin ôc Klianchuk

1993). rhe prism structure is a complicated

combination of different-fades and different-age

formations. The Taiikba Terrane is composed uf

a repeated alternation of turbidite and olisiostro-

nie dcposits constiiuiing the matrix, and diffe-

rent-age accreted fragments of mostly

paleoceanic, rarely paleocontinental formations.

Section of the prism can be visualized as a

“multi-layered cake”, where relatively young

dcposits of rhe matrix alternate with more

ancient accreted formations.

The accreted fragments comprise extensive (up

to several cens of kilometers long) plates as well

as blocks and lumps of varying sizes within the

matrix of oli.sto.strome. Both plate and matrix

rocks were crurnpied together into assymetric

north-east irending iolds wiih a south-east ver¬

gence. Sonic plates can bo 500 m thick. Such a

thickness is a resuit of the tcctonic répétition (3-

5 rimes) of some parts of accreted formations. A

true thiclcness, for exampic, of dierty rocks does

not exceed 100 m. The contacts between plates

of the accreted fragments and the matrix (if they

are not broken by later deformations) afo .sedi-

mentarys distinct in litholog}'. Large places usual-

ly ûvcriic the olistostrome.

Baleoceanic accreted formations are represented

by siliceoûs (fragments of abyssal plains) and car-

bonaceous (fragments of paleoguyots) faciès.

These faciès are composed of rypîcal bedded-

cherts, daced from their dilfercni plates by

Middic Carboniferous to Lare Jurassic âge

(Rybalka 1987; Khanchuk et al. 1988; Bragin et

al. 1988; Rudenko & Panasenko 1990; Voiokhin

et ai 1990; Bragin 1993), and recl-lorming

limc.stones laying on high-litaniiiin alkaline

basalts. l'hc âge of the limcsione ba.sa] layers in

different plates and blocks ranges from Late

Dcvoiiian to Late Triassic (Nikitina 1971;

Vorobeva et ai 1978; Bersenev 1986; Budi et al.

1986).

The fragments of paleocontinenral formations

are repre.sentcd by blocks and lumps oi shallow-

marine (shelf) deposîts containing Mîddle-Late

Iriassic macrofauna, and by places of relatively

deep-sea Permian rocks composed of sandstones

and siltstoiies flysch alternation (Kemkin 1996).

RADIOLARIAN ASSEMBLAGES

Detailcd study of cherry formations from the

Taukha Terrane along rhe left bank of rhe

Roudnaya River (Dalnegorsk Town area) bave

bccn carricd oui. Phe cherts and overlying tuibi-

dites of the matrix form four tectonically repea¬

ted plates (Eig. 1). The most représentative

676

GEODIVERSITAS • 1999 • 21 (4)

Jurassic-Early Cretaceous biostrarigraphy

Fig. 1. — Tectonic scheme of the Sikhote-Alin Région and geological map of the investigated area. 1. Early Cretaceous olistostrome

formations of the accretionary prism matrix; 2. plates and blocks of Triassic-Jurassic cherts; 3, turbidite deposits of the matrix;

4. plates and blocks of Mîddle-Lale Trîassic limeslones; 5. high-tiianium alkaline basalts undertying limestones; 6. Early Cretaceous

shallow-marine (shelf) deposits; 7a, Late Cretaceous volcanites; 7b, intrusive formations; 8, Ouatemary deposits; 9, dislocations with

a break in continuity: 10. éléments of rock occurrence (sirikes and dips).

secrion of the cherts was discovered in the second

tectonic plate (l‘i^. 2) whcre they make up iis

lowcr portion. Wîthin the exposure^ tlic rocks

show monoclina] dtp lo chc soucheasc (dip azi-

muth, 130-140". angle 70-80"). l he cherts hâve

bedded texture thaï is cau-scd by thin (1-3 xnm)

clayey interbeds. rhickness of the cherr beds

varies from 1.3-2 to 3-5 cm, more rarely 7-

10 cm. The rocks arc broken by a séries of sicc-

ply-dipping, discoiuinuous dislocations of

northeast and submcridtonal uending, paraJlel or

at angle ro bedding. In the upper part of the sec¬

tion, the cherr>' formations change.s ro rerrige-

nous deposits, cherry mutlstoncs, nuidstones,

muddy siltstones and, lhen, flyscli alternation of

sili.stones and .sandstoncs that grade into massive

sandstoncs. Unloriunaiely, the comaci of cherts

and terrigenous rocks al tliis expo.sure Is œnipli-

cated by a laull, a.s cvldenced by ihe pre.sence of

boudinaged fragmenl.s of cherts in the contact

part of the cherly mudstone.s. However, in oihcr

places (for exainple, Korcy.skaya River area) we

observe a contormablc and graduai transition.

The conformable and graduai transition between

cherts and lerrigenous deposits is very important

bccausc ic indicates a smooth change of environ ■

ment of sédimentation from pclagic to marginal-

continental (cherr accumulation is cbanged at

the begining by the accumulation of fine and

then coarsc ceitigcnous matcrial). This évidence

fixe.s, ihus, the moment of approach of a given

pan of ihc oceanic plate to the zone of accrcüon.

AJl ihrcc Triassic and Lowcr Jurassic epoch.s have

bcen identificd in the chert units (Vololdiin et al.

1990: Bragin 1991; Bragin 1993) Accorcling to

Bragin (1993), Middie Jurassic is nor represenred

in lhe section due to the essentiel stmiigraphical

break in the Middie Juras.sic titne. The available

data on the Lace jurassic age of che cherts (Bragin

1993) arc not quitc correct, a.s tlic Latc Jurassic

Radiolaria have bcen separalcd 1mm the cherty

mudsiones bclonging to a transitional chert-io-

terrigenous packet. Lhe age of lhe tetrigenous

portion of the .sectioti has bcen determineci as

middie filhonian-Valanginian (Bragin 1993).

ïhe Triassic pan of the section is detaily subdivi-

ded into detailed zones by conodonts and radio-

larians (Volokhin étal. 1990; Bragin 1991) and

GEODIVERSITAS • 1999 • 21 14)

677

Kemkin I. V. &L Kemkina R. A.

0 25 50 m

X80

Fig. 3

X75"

cherty

mudstone

turbidite

Fig. 2. — Geological scheme illustrating the structure of chert-terrigenous successions of the second tectonic plate along the

Roudnaya River (Dalnegorsk Town).

is not discussed in chis paper. In this scudy the

Jurassic parts of the chetts and terrigenous rocks

hâve been sampled in great detail. l’hc micro-

faunal study show that the cherty beds of the

section contain Early, Middie and Late jurassic

radiolarians. The Lace Jurassic and Eaijy

Cretaceotus ones were fraind in terrigenous depo-

sits (Figs 3, 5). Aliogether, tvvclve successive

radiolarian assemblages have been distinguished

(Figs 3, 4). Short descriptions of thèse assem¬

blées are given below in ^scending order.

1. Parahuium longiconicuni assemblage was found

in cherts of decp-grcy to black in colour (samples

P-21, P-20, P-19). Spécifie composition of rhe

assemblage is not abondant (Fig. 3). This assem¬

blage conrains nassellarians such as Pambsuum^

Canoptum. Tricolocapsa and Parvteingula and

spumellarians — Tnactoma. Age diagnostic species

is Parahsuum longiconicum. l’hc geological range

of the assemblage is assigned to PHcnsbachian-

early Toardan. The lower âge boiindary is assu-

med to bc late PliensbacPiîan according to the

First appearance of the species-index (Sashida

1988). The upper boundary is restricted by the

lower onc of the upward following assemblage.

The as.scmblagc is compatable in âge and spécifie

composition (Fig. 4) with the assemblage of

Pamhsuum tiikarazawiiense zone (Sashida 1988)

and subzone 4 oïPamhsuum simplum zone (Hori

1990; Marsuoka et al. 1994), and lower part of

Trillus elkhornemis zone (Marsuoka 1995) repor-

red from Japan.

2. Hsnum altUe assemblage wa.s extracted Irom

violet-dccp-grey cherts (samplcs P-18, P-17).

The assemblage characterized by a relative diver-

sity of species (Fig. 3), with a prédominance of

Parahsuum and Hsimm. Some spumellarians such

as Triactoma and others are also found here. The

geological âge of rhe assemblage is early

Toarcian-middle Toarcian. 1rs lower boundary

was defined by the appearances of Hsuum ahilcy

Hsuum transiemisy Parvidngida nanoconica rhat

Jiavc been noted since early Toarcian (Hori &

Orsuka 1989; Hori 1990). riic upper boundary

is controlled by the upper assemblage and the

last appearance of Parahsuum longiconicum spe-

678

GEODIVERSITAS • 1999 • 21 (4)

Jurassic-Eariy Cretaceous biostratigraphy

cies (Sashida 1988). Age and the spécifie compo¬

sition of this assemblage are comparable wirh

thar of Mesosaturnalis hexagornis zone (Hori

1990; Matsuoka et al. 1994), and partially corré¬

lative wich rhe assemblage of Hsuum minoramm

zone (Sashida 1988) and upper parts ol Trillus

elkornensis zoai: (Matsuoka 1995) aiso reported

Irom Japan.

3. Purahsuum grande assemblage was foiind in

the identical violct-decp-grcy cherts (samplcs

P-16, F-15, 86-15). ’l'his a.ssemblage contains

abundant and diverse rcpic.sentacivcs ol nassclla-

rians such as Parahsuutn, Hsuunu and Parvi-

cingula, and spumcllarians such as Emiluvia.

Tetraditrimay Archacospongoprtouinu Xiphostilus

and others (Fig. 3). Age diagnostic species are

Parahsimm grande, Hsuum matsuôkai mxA Hsuum

hisuikyoense. The âge ol the assemblage is late

Toarcian-iniddie Aalcnian. According to the first

appearance of Parahsuum grande (Hori 1990),

the older age boundaiy was assumed. The top is

limitcd by the lower boundary of the upper

assemblage. The assemblage is comparable with

that of Parahsuum grande zone, and the lower

portion of Hsuum hisuihyoense zone (Hori 1990;

Matsuoka et ai 1994), as well as Laxtorum juras-

sicurn zone (Matsuoka 1995). AU zones bave

been identified in Japan.

4. Parahsuum hiconocosta assemblage was found

in deep-grcy cherts (samplc P-14). Parahsuum

and Hsuum predominate among the représenta-

tives chat are noi relatively numerous in this

assemblage (Fig. 3). l'hc gcological age of the

assemblage is late A;denian-early Bajocian. The

lower age boundary corresponds to the firsi

appearance of ihe spccies-indcx (Baumgartner et

ai 1995). fhc top is controlled by the lower

boundary oF the upper assemblage. The assem¬

blage is correlated with that of the Hsuum hisui-

kyoeme zone, lower part of the Unuma cchinatus

zone (Matsuoka et ai 1994), and upper parts of

the Lvctnruni jurasstcum xisnc (Matsuoka 1995).

5. Hsuum mirahundum a.ssemblagc was cxcractcd

from bluc-grcy cherts (samplcs P-13, P'12,

P-1 1). Thi.s as.scmblagc shows relative spécifie

diversity. Among the représentatives, nassella-

rians such a.s Hstiinriy Pnrahsuum, ParvicinguLt

and Tricolocapsa, as well as spumellarians ie

Emiluvia, Tripocyclia and others are prevailing

(Fig. 3). The geological range ot the assemblage

is assumed to be early-late middle Bajocian. The

lower boundary was determined by the first

appearance of Hsuum mirahundum (Baum-

gartner et al. 1995). The upper boundary is rcs-

rricced by the last appearance of such specics as

Parahsuum natorênsey Parahsuum grande,

Emilutàa splendtda. The boundary corresponds

to the cncl of middle Bajocian (Hori 1990:

Baumgartner et al. 1995). This assemblage is

comparable in age wirh that of the middle part

ol the Unuma echinatus zone (Matsuoka et al.

1994) , and lower parc of rhe Tricolocapsa plica-

rum zone (Matsuoka 1995) distinguished in

japan.

6. Hsuum matsuokai assemblage was found in

liglu-grcy chert.s (samplcs P-10, P-9, P-8).

vSpecifîc compositions of the a.sscmblage Ls cha-

racterized by the essential diVersiry of specics.

Among them, chcrc are nasscllarians: Hsuum-,

Transhsuuniy Parahsuum, Arhaeodiciyomitra,

Tricolocapsa, and spumcllaiians such as Aiesos-

aturnalh, Tritrahs, Ictraditrima and others

(Fig. 3). Age diagnostic sptccics are Tritrahs cas-

maUaemis and Hsuum matsuokai. The range of

the assemblage was dctccimned as. lato Bajocian-

early Baihonian. The lower age boundary is

based on the absence of charactcristic specics of

the end of middle Bajocian (see assemblage 5), as

weli as the presence of Tritrahs casmaliaensis cha-

racteristic of l;ue Bajocian (Ranrngarmer et al.

1995) . The upper boundary was determined by

the last appearance of Hsuum matsuokai that had

completed it.s évolution in the carly Baihonian

(Baumgartner et al. 1995). This assemblage is

correlated with that of the upper parcs of Unuma

echinatus et al 1994) and Tiicolocapsa

plicarum (Matsuoka 1995) zones.

7. Triactormr tithaniauum assemblage was (ound

in greenish-grey chert.s (sample.s P-7), 10 cm

below the bottoin ot the cherty niudstoncs.

Tricolocapsa and Stichocapsa predominate among

the représentatives that are not relatively nume-

TOUS in this xssemhlage (Fig. 3). The geological

age of the assemblage is identified as middle

Bathonian-early CaJlovian. The lower age boun¬

dary corresponds to the upper boundaty of the

previous assemblage and to the first appearance

of Triactoma tithonianum (Baumgartner et al.

GEODIVERSITAS • 1999 • 21 (4)

679

Kemkin I. V. & Kemkina R. A.

1995). The upper âge boundary is restricted by

thc last appearancc of Tntmhsuuni medium

(Baumgartner et al. 1995). The assemblage is

comparable in age to that of thc GtiexelLt nudata

(Matsuoka et al. 1994), and the Tricolocapsa

conexa (Matsuoka 1995) zones.

8. Archaeodictyomitra minoeiids assemblage was

cxcracted Irom the boudinaged fragments of cherts

(sample P-6) in thc contact zone of cherts and

cherry mudscones. This radiolarian assemblage

concains mainly nasseilarians and is characterized

by rich spécifie diversity. They are ArchaeU'

dictyomitra. Xitus, Mirifusus, îhtmm\ Sethocapsti-,

PseudodictyoMitra^ Stichaatfsu and others. The

range of the assemblage is middie Oxfordian-early

Kimmeridgian. Assumed lower age boundary is

from the first appearance of the species-index

(Baumgartner et al. 1995). The upper boundary

corresponds to the last appearance of Haliodicta

hojnosi (Baumgartner et al. 1995). The assemblage

is comparable in age with that of the upper parts

(if the Stylocapsa spiralis zone (Matsuoka 1995)

described in Japun. It should be noted (that wichin

the assemblage) ihere are several morphological

forms that are more common in Early Cretaceous

radiokrians (Figs 3, 5).

9. Pseiidodictyomitru okamurai assemblage was

found in green thecty mudstones (samplcs P-5,

86-14). The assemblage aisu contains numerous

and diverse radiolarian species (Fig. 3).

Prédominant ones arc Archaeodictyomitra and

Pseudodictyomhrâ. The range ot the a.ssemhlage is

middle-latc Kimmeridgian. The oldcr age boun-

dar)'^ is somewhat tcnlarive, bur the data on the

previous assemblage hâve been taken into

account. The upper age limit is restricted by the

last appearance of Pseudodictyomitra okamurai

(Baumgartner et ai 1995). The assemblage is

680

GEODIVERSITAS • 1999 • 21 (4)

Jurassic-Early Cretaceous biostratigraphy

4-0

ês-2S|S.S&

^ * §1*1 i 1 B

■So|p'®|aE

î? I « I

IÊI i -I t I I

“ §|ë

5 *

5>^fê

Parahsuum (ongiconicum

Hmi

Hsuum mirabundum

Pseudodictyomitra okamurai

Hsuum attile

Hma

Hsuum malsuokai

Xitus gifuensts

Parahsuum grande

fnactoma tithonianum

Pseudodictyomitra carprtica

Parahsuum hiconocosta

Archaeodictyomitra minoensis

C sp. Cecrops sp.

Fig. 3. — ütho- and biosiratigraphical column of the Jurassic portion of the chert section and overlying cherts terrigenous deposits,

enclosing radiolarian species and assemblage range aiong the section.

comparable in âge with char of Hsmwi maxwclli

zone (Mat.suoka 1995). Morphological features

of some speciês are more common m the Early

Cretaceous forms. 'l’hey aie ? Pscifdodictyomitm

nttdu and ? Pieudodicîyoftiimi Uptoconioi (f igs 3.

5) and also chatacteristk In this assemblage.

10. Xitus gifiiensis assemblage was also found in

green cherty inudstone.s (samples P-4, P-3).

Archaeodiîyoynitm and Xïtm prcdominaie among

the numerous radiolariuns of ihis assemblage.

vSomc spumellarians such as Tritrabs, Emiluvia

and PafUdttellium arc also found. The geologkal

range of the âssemblage is assumed as early-

middle Tichonian The lower âge boundary cor¬

responds 10 the flrst appearance Xitu^gijvensh

(Baumgartner et td. 1995). The upper boundary

is resiricied by the lower boundary ol the upper

assemblage. The assemblage is correlated with

that of the Pseudodktyomitra primitixm zone

(Maisuoka 1995) and also contains some species

similar to Psettdodictyomiti'a mida and Pseudo-

dktyonùtm leptoconica.

11. Pseudx)d\ctyomttm carpatica assemblage was

found in black mudsrnnes (samples P-1, 86-

16) very close to the contaa with green cherty

mudstoncvs. The assemblage is represented by

numerous and diverse radiolarians related to the

end of Jurassic and beginning of Cretaceous rime

(Fig. 3), Nassellarians such as Pseiulodictyomttm,

Archaeodictyoniitm^ Xitusy Thnnarla, Sethocdpsd

predominate. Spumellarians such as Tritrnhs,

Emiliivin, PantaneWtum and othcis arc also

contained. ITe range of ihc assemblage is latc

‘rirhonian. The lower âge boundary corresponds

to die iifsc appearance ol iheudodicvyomitrci car-

patica (Matsuoka 1992). The upper boundary is

GEODIVERSITAS • 1999 • 21 (4)

681

Kemkin I. V. & Kemkina R. A.

Age

Radiolarian zones and assemblages

Sashida1988

Hori 1990

Matsuoka

étal. 1994

Matsuoka

1995

This paper

Bar

Hau

Val

Ber

Trt

Kim

Oxf

Cal

Bat

Baj

Aal

Toa

Pib

Acanthodrcus canneîus

Ceavp^

Cecrops sp.

Pswàdodicyomfim

carpsGca

PsBiJdodtctyomitra

Pseutiodic^mHfa

_ _^9rpaftca

Xîtus gifuensis

Hsuum maxY/eili

Pssudi

Stylocapsa (?) spiralts

ArchaeodKtyomnrB

mlnoensts

GuexeHa nudata

Tncùtocapsa conaxa

Tr^ktonia tAhontantim

Unuma echinatus

Tricofocapsa p/*camm

Laxtorum (?) jurassicum

Hsuum hisuiHyoensa

Hsuum Msuikyoensa

LaKfofWTJ (?)/urassjcwm,

Hsuum matsuoka)

Parghsuum hiconocosla]

’HsiJum mlnoraïun

. Parahsuum

takarazawaense

Parahsuum grande

isosatumaksh BxtiODnôi]

PerHhsuum stmplum IV

ft gxBgonujj

rrillus eikhomansis

Rsüum aÏÏHS“

Pàrahufiun simpium

Parahsuum stmphm NI

Parahsuufn simplum

jParahsuum longicanicum

Parahsuum slmolum

Fig. 4. — Corretation table of Taukha Terrane and Japanese radiolarian zones and assemblages.

determined by the last appearance of

Archaeodictyomitra whioefisisy Ristola altissima

and Protunuma japonicus (Baumgartner et al.

1995). This assemblage contain.s the species

similar to Pseudodictyomitra nudti and Pseuda-

dictyomitra leptoconica. The assemblage is compa¬

rable in âge vvith tliar of the lower part of

Pseudod'tctyomitrâ varpatica zone (Matsuoka

1995) establishedin Japan.

12. Cecrops sp. assemblage was distinguished in

the black mudstoncs (samplc P-0) that is 40 m

above the horizon P-1 of the section. The assem¬

blage is charactcrizcd by diverse and abtindant

radiolarian species (Fig. 3). Most of tiiem hâve a

wide age intervni. However, rhe présence of

Cecrops .sp. and Sitchocdpsct ex. gr. altiforamimt

allows to déterminé range intcrval of the early

Valanginian-carly Barrcmian (Baumgartner et al.

1995). This assemblage is comparable in age witli

that of Cecrops septemporattis zone and lower parts

oïAcanthocircus carinatus uovïQ (Matsuoka 1995).

CONCLUSION

We hâve carried out detailed biostratigraphical

investigations. Twelve successive radiolarian

assemblages which characterize different-age

depo.sits of the cheri-iurbidicc section were dis¬

tinguished. Liglit assemblages arc included in the

chert portion ranging ftom late Pliensbachian to

early Kimmcridgian. le indicaccs that the chert

accumulation proces.s in Jurassic rime was conti-

nuous. The ptesence of Middie Jurassic radiola-

rians (of ail stages) di.spuie ihe presence of any

significant stratigraphical brealc in Jurassic tune,

dh WiLs previûusly reporicd (Btagin 1993). At the

samc time, somc chert portion, corresponding to

middlc CaJlovum-early Oxfordian time interval,

as wcll as some ol cheriy mudstones is absent

from chc section as a fcsult of later deformations.

In rbc vransitional packet of cherry mudstones

and in the terrigenous rocks, we hâve cstablished

cwo radiolarian assemblages in each, indicaring

Kimmeridgian-Tithonian and late Tichonian-

Early Creiaceous age of ihese dcposics correspon-

dingly. Tlicse data suggesr that one paleogeo-

dynantie environment of sédimentation was

rcplaced by anocher ai rhe end of Jurassic time,

and thaï chert accrccion took place in Early

Crctaceous time.

Cheriy formations analogous in age arc known

today among different accretionary prisms of the

Pacific margin of Asia, from Koryak plateau

682

GEODIVERSITAS • 1999 • 21 (4)

Jurassic-Early Cretaceous biostratigraphy

F«g. 5. — Some Jurassic and Early Cretaceous radiotanans from cherl-terrigenous seQüer>ce of Taukha Terrane A. Pârahsuum

cf. iongicomcum Sashida, P-17: B, H&uum a/We Hori & OtsuKa. P-IB. C. Patahsuum grande Hon & Vao, P-15; D, Hsuum sp. A.

P-14; E. Parahsuum cf. Uiconocosia Baumgarinef & De Wever. P-14. F, Hsuum cf. tmrabundum Pessagno â Whalen, P-13:

G. Hsuum matsuoka/ Isozaki S Mats^xia. P-8; H. Triacîoma Mhonianum Rust. P*7; I,. Trîtrâbs cf casmaliaensis (Pesagno). P-9,

J, Transhsuum medfum Takemnra, P-8: K. Archaeodictyotvnra minoensis (iVlizuiani). P*6: L. Hatiodictya (?) cf. tioinosi Riedel &

Sanfilippo, P-6; M Pseudodfctyomsira okamurai Mizutani^ P-6; N, P, ? Pseudodictyomitra aff. Nuda Shaat; N, P-6; P. P-4i

O. ? Pseudodictyomitra atf. Leptoconica (Foreman), 86-14, Q, R, XiTus gifuensrs Misulani, P-3; S, Tritrabs simplex Kîto & De Wever,

P-10; T, Stichocapsa ex gr. alîiforamina Tumanda, P-O; U, Pseudodictyomitra carpatica (Lozynyak), P-2; V, Cecrops sp., P-0. Scale

bars: 100 pm.

GEODIVERSITAS • 1999 • 21 (4)

683

Kemkin I. V. & Kemkina R. A.

(Vishnevskaya & [’ilutova 1996; Kemkin et al.

1996 and oihcrs) lo the fapanesc Islande (Hori

& Otsuka 1989; Hori 1990; Tcliikawa et al.

1990; Matsuoka & Yâo 1990; Mizutani étal.

1990; Matsuoka et al. 1994 and others)* This

face togecher with data on the prism âge is évi¬

dence ol the existence of a single acerctionary

System along the western boundary of the

Paleopacific in Late Jurassic^Early Crctaccous

time and ailows as to ourline general tendencies

of geological évolution of the Far East région at a

given rime interval.

It is interescing to note thaï our scudy has reco-

gnized among radiolarian assemblages (since

Oxfordian-Kimmeridgian time) the prcsence of

separare specimens widi morphological Kacurcs

characreristic in Teihys area for Early Crctaccous

(Valanginian and younger) forms. Thcy are ?

Pseudodinyomitra aff. ^uuia and ? Pseudo-

dictyomitm afl. lepumica range intervals which,

according to the currcntly available data

(Baumgartnci et al. 1995) arc early Valanginian-

Aprian and lare Barremian-Aprian, correspondin-

gly. It’s likcly rhat for diOerent rcason.s, ihese

morphological fcacures in radiolarians of the

Paleopacific area began Lo develop nuich earlier

rhan in rhosc of the Tethys area.

Acknowledgements

The authors express ihanks to Dr. S. Kojima

(Nagoya Univcrsicy, Japan) and Dr. Y. Taketani

(Fukushima muséum, Japan) for giving us an

opportunity to takc picrures of radiolarians

under scanning électron microscope, and Dr.

V. S. Rudenko (Far Easî Geological Institure. Far

Eastern Branch. Russian Acaemy of Sciences,

Russia) for consultations and discussions.

We are grateful to Dr. M. Faure (France) and Dr.

R. Ishiga (Japan) fo-r critical reading of the

manuscript and their constructh^e comments.

Spécial thanks are duc to Di. F. Spiller C. P.

(University ol New England Armidale, Australla)

for révision of the English text.

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zone of Sikhote^Alin (Primorye. Gornaya River

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Submitted for publication on 29 January 1998;

accepted on 27 July 1998.

GEODIVERSITAS • 1999 • 21 (4)

685

Combined radiolarian-ammonite stratigraphy for

the Late Jurassic of the Antarctic Peninsula:

implications for radiolarian stratigraphy

Wolfgang KIESSLING

Muséum für Naturkunde,

Invalidenstr. 43. D-10115 Berlin (Germany)

wolfgang.kiessling@rz.hu-berlin.de

Roberto SCASSO

Departamento de Geologia,

Ciudad Universitaria, 1428 Buenos Aires (Argentina)

Arnold ZEISS

Institut fur Paléontologie,

Loewenichstrasse 28, D-91054 Erlangen (Germany)

Alberto C. RICCARDI

Division Paleozoologia Invertebrados, Museo de Ciencias Naturales,

Paseo del Bosque, 1900 La Plata (Argentina)

Francisco A. MEDINA

CIRGEO, Velasco 847, 1414 Buenos Aires (Argentina)

Kiessling W., Scasso R.. Zeiss A., Riccardi A. C. & Médina F. A. 1999. — Combined radio¬

larian-ammonite stratigraphy for the Late Jurassic of the Antarctic Peninsula: implications

for radiolarian stratigraphy. in De Wever P. & Caulet J.-P. (eds), InterRad VIII,

Paris/Bien/ille 8-13 septembre 1997, Geodh/ersitas2) (4) : 687-713.

KEYWORDS

Radiolaria,

iimmoniies,

Late Jurassic,

Kimineridgian,

Tithonian,

bio.stratigraphy,

Antarctic Peninsula.

ABSTRACT

New biostraiigraphic dura From co-occurring radiolarians and ammonites in

Upper Jurassic sequences of the Antarctic Peninsula (Byers Peninsula on

Livingston Island and Longing Gap, Graham Land)> permit a revised and

more refined régional stratigrapliy. I he ncw data also allow a révision of the

chronostratigraphic assignineni of soine American radiolarian zones esrabli-

shed by Pcssagno and collaborators: the boundar)' of Zone 3-4 is assigned to

the latest Kimmcridgian, contrasting the former a^sjgnmenr to the carly/late

Tithonian boundar)'. The boundary between Subzone 4 beta and 4 alpha is

assigned co the carly Tithonian, but was usually correlared with the early late

Tithonian/latc late Tithonian boundary. The new chronostratigraphic dara

from Antarctica are used rogerher with recenr resuits of Baumgartner and

collaborators to revise the age a.ssignment of the North American Late

Jurassic radiolarian zones.

GEODIVERSITAS • 1999 • 21 (4)

687

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

MOTS CLÉS

Radiolaires,

Ammoniics,

Jurassicjue supérieur,

Kimméridgien,

Tithonicn,

biostratigraphie,

péninsule Antarctique.

RÉSUMÉ

Stratigraphie combinée de radiolaires et ammonites du Jurassique supérieur de la

péninsule Antarctique : implications pour la stratigraphie des radiolaires.

De nouvelles donnfe hiostraiigraphiques obtenues à partir de co-occurences

de radiolaires et ammonites dans le.s séries du Jurassrquc supérieur de la

péninsule Anrarcrique (péninsule Ryers sur l île de Livingston ci de Longing

Gap, Graham Land)t permettent de réviser et affiner une stratigraphie régio¬

nale. Les nouvelles donnée.s permettent aus.si une révision de.s attributions

chronosrratigraphiques de quelques zonations de radiolaires américaines éta¬

blies par Pe.ssagno ci ses coUaboraieurs : la limite de la zone 3-4 est assignée

au Kimméridgicn le plus tardifi contra^ant ainsi avec la précédente'assigna¬

tion à la limite Tîthonien prccocc-tardif. La limite entre la sous-zonc 4 beta

et 4 alpha est assignée au Tithonicn inférieur mais fut habituellement corré¬

lée avec la limite entre le.s parties inférieure et supérieure-du Tithonicn supé¬

rieur. I.es nouvelles données chronostiaitgraphtqiics de rAïuurcrique sont

utili-sée.s en même temps que les rcsuitais récents de Baumgartncr et .scs colla¬

borateurs pour réviser les attributions d’âge des zones à radiolaires du

Jurassique supérieur d’Amérique du Nord.

INTRODUCTION

Although Upper jurassic sequences with co-

occurring radiolarians and ammonites were

continuousiy reported in fhc lasf fcw ycars (c.g.

Pessagno et ai 1987a, b; O'Doglierty et al. 1989,

1995; Pujana 1989, 1991. 1996; Baumgarlnci et

al. 1995b; Zügel 1997), such findings can still be

regarded exccplional. Hencc, new sections yicl-

ding both radlolaiian and ammonite faunas are

of high value for the improvement ofbiostrati-

graphy.

Late Jurassic mud.sione sequences of ihe

Antarctic Pcninsula contain relatively wcll-preser-

ved ammonites and radiolarians at scveral locali-

ties. Two sections are dcscribcd in ihis paper.

The sections belong to the Anchorage Formation

(Byers Peninsula, Livingston Island) and

Ameghino (= Nordenslcjolcl) Formation

(Longing Gap, Ciraham Land), respectively.

Stratigraphically important macrofossils (ammo¬

nites, aptychi, bclcmnites. bivalves) as well as

microfossils (radiolarians) were found in the

same sections and somctinies even in ihe same

sam pies.

The ammonite tauna in the sequences is mainly

composed of cosmopolitan or Tethyan éléments

showing no significant dillercnces from Tethyan

or other eastern Pacific sites on a genus level.

Hence, ammonites allow a fairly straightforward

chronostratigraphic assignment.

The cxcdlcntly preserved radiolarian faunas reco-

vered hom carbonate concrctions exhibit a pro-

nounced Au.stral a.spect (Kie.s.s'Iing ëê Scasso

1996). Ncvetthclcss, they can bc linked to the

North American standard zonation (Pessagno et

ai 1993, 1994) and allow a detaiied biostrafigra-

phic subdivision. However, the chronostratigra-

phic radiolarian âges are aiways in slighr

disagreement with ammonite âges.

In ihis paper wc providc a reviscd chronostrati-

grâphic assignnient of the Kimmeridgian/

Tiihonian North American radiolarian zones

established by Pessagno et al. (1984, 1987b,

1993) and evaluate the applicability of other

radiohirian zonations in Antarctica.

GEOLOGICAL SETTING

l'he Antarctic Peninsula formed a separate plate

which was situated in Southern high latitudes

during Late Jurassic time (see review in Kiessling

& Scasso 1996).

688

GEODIVERSITAS • 1999 • 21 (4)

Stratigraphy of Antarctica

JVv'C UpperJurassic-Cretaceous arc magmatics ^ Occurrences of Upper Jurassic Mudstones

Fig. 1 . — Geological map of lhe northeastern Antarctic Peninsula (Graham Land). The studied localities are printed in bold.

This région is characterized by an almost conti- med partly on pre-existing continental crust

nuous magmaiic activity from the Early Jurassic (Hervé étal 1996).

to thc Miocene (Barker et al. 1991; Leat Back-arc of the Antarctic Peninsula volcaniclasdc

Scarrow 1994), sitnilar to the southemmost sédiments and anoxie radiolarian^rich mudstones

Andes. During the Jurassic period, thc eastward are supposed to unconformably overlay an oldcr

subduction of the Pacific Phoenix Plate led ro accretionary complex, the Triniry Peninsula

the development of a calc-alkaliue magmatic arc Group. The mudstone sequence belongs to the

(Antarctic Peninsula Volcanic Croup) whh voica- mainly Upper Jurassic Ameghiuo Formation

niclastic sequences in the fore-arc and back-arc (Médina & Ramos 1981; Médina et ai 1983)

areas. The magmatic arc is thought to hâve for- also known as Nordenskjôld Formation

GEODIVERSITAS • 1999 • 21 ( 4 )

689

Kiessling W., Scasso R., Zeiss A., Riccardi A. Sc Médina F.

(Farquharson 1982, 1983) which forms rhe basal

sedimentary infill of rhe Larsen Basin in rhe

northeasrern Anrarctic Peninsula (Macdonald et

al. 1988). The basin contains approximately

6000 m of epi' and volcaniclastic sédiments

deposited from the Laie jurassic to the Paleo-

gene. Ourcrops of rhe Ameghino Formation are

scattered along the eastern coast of Ciraham Land

(Fig. 1). They are either isoJ-ated by surrounding

ice-masscs or Idund in comploc tcctonic contaçt

to other rocks.

The Late Jurassic Anchorage Formation is the

chronostratigraphic équivalent oi the Ameghino

Formation in ihe lore-arc région (Pirrie &

Crame 1995). As in the Ameghino Formation

mudstones and tufTs prevatl, but additional sand-

stone beds are intercalatcd. 1 he Anchorage

Formation forms the base of a 1000 m thick

sequencc (Byers Group) ranging from the

Kimmeridgian to the Valangini.in (Crame et ai

1993). The Anchorage' Formation is only expo-

sed on Byers Peninsula, Livingston Island.

LOCALITY DESCRIPTIONS

Longinc Gap

Longing Gap is situated at the Nordenskjold

Coast (Larseii Inlet) of nonhern Graham Land

(Fig. 1). The area wichoui permanent ice cover

extends some A km in a north-south direction

and a maximum of 1.5 km in an casi-west direc¬

tion (Fig. 2) and Is surrounded by glaciers.

Longing Gap is the type locallty of the

Ameghino Formation and only rocks assigned to

the Ameghino Formation are exposed thene. *rhe

geological structure is a wide syncline with a

nearly east-west oriented axU. Beds dip to the

South at the northern margin of the exposure;

they lie horizontal in the Southern part,, and dip

gently lo che north at the southernmost margin.

Minor faults are présent, but no significant offset

was noriced.

The sedimentary succession consists of black

mudstones and gray tuffs, Both lithologies arc

tightly intercalatcd or mixed. Addidonally. cald-

te concrction.s are common throughout the sec¬

tion reaching 3 m in diameter. They occur in

mudstones as well as in tuffs, but mudstone

Ameghino Member

Longing Member ^

■ Ameghino Hut

/ Section for

- radiolarian samples

Moraine

Ammonite locaüty

Fig. 2. — Oulcfop of the Ameghino Formation at Longing Gap.

The profile line for radiolarian samples. important concrétion

levels and ammonite locations, and the âges provided by

ammonites are indicated.

concrétions are generally latger. At rhe base of

the succession mudstones predominate, while

towards the top tuff beds become incrcasingly

abundant. This trend lcd Whitham fie Doylc

(1989) to distinguish two members: a lowcr

Longing Member and a higher “Ameghino”

Member. Although there is a continuous transi-

690

GEODIVERSITAS • 1999 • 21 (4)

Stratigraphy of Antarctica

Radiolarian

samples

Ammonite

samples

030

K 57

Ranges of selected

radiolarians

K41

LG 20

020. 025.035. X6

LG 22

LG12, LG13, LG14, LG 25

LG 29. 013. 038. 046

LG2, LG3, LG 5. LG 26

LG 9, LG 10

LG 16

043, 044. 045

LG 4. LG 6, LG 7. LG 11

0 .

North American

radiolarian zonation

LJJ

Ammonite

chronozones

Spiticeras****

Koeneni***?

Blanfordiceras****

Densiplicatus’*?

Mendozanus***

VimineusVKossmatia’

Mucronatum*

Hybonotum*

Beckeri*

CH Interbedded tuffs and mudstones H Basaltic Sill

□□ Interbedded mudstones and tuffs — • Fault ?

Fig. 3. — Idealized lllhological column of the Ameghino Formation at Longing Gap. Important radiolarian samples, ammonite locali-

ties. selected ranges of radiolarian taxa, radiolarian zones and preliminary ammonite zones are shown. Ammonite samples from

transported blocks are indicated by a question mark. CrossStars after ammonite zones indicate: *, European standard zone;

Himalayan zone: ***, Argentlnean zone; ****, Antarctic zone. Due lolhe problems in recognizing middle Tithonian. we subdivide the

Tithonian sensu Gallico.

tion, the division proposed by these authors is

followed in this paper. Owing to the relatively

poor exposure quality of the succession it is diffi-

cult to déterminé the total thickness. Whitham

& Doylc (1989) hâve estimaied a thickness of

450 m for the Ameghino Formation at Longing

Gap, but Scasso èc Vülar (1993) mention

600 m. New gcodctic results Irom our ficld cam-

paign (SantisTeban 1997) indicate a total thick¬

ness of 580 m. The lower l.onging Meniber i.s

420 m thick, whereas the upper ‘"Ameghino”

Mcmber is 160 m ihick (Fig. 3).

The black mudstones in both members are lami-

nated or structureles.s. The tuffs are often graded

and show undulare bases due to loading. The

tuff layers are interpreted as pelagic deposits of

air-fall ashes, related to single volcanic events

(Whitham 1993). Intense silicification is fre¬

quent (Scasso et al, 1991). Mudstones as well as

tuff beds arc laterally continuons. Current sedi-

mentary structures are rare and no influence of

(storm) wave activiry îs évident. Slumps are very

rare and small.

The depositional environment of the Ameghino

Formation is assigned to an anoxie to dysoxic

basin, according to Farquharson (1983). Doyle

& Whitham (1991) and Whitham (1993).

Anoxie conditions prevaÜed e.specially in the

Longing Membcr; this is indicated by the often

lacking bioturbation and rare horizons with ben-

thonic tossils as wdl as by geochemical indicators

(Scas.so & Villar, 1993). In the “Ameghino”

Member moderately intense bioturbation

(Zoophycos, ChondriteSt Planolites) and a conse-

GEODIVERSITAS • 1999 • 21 (4)

691

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

100 ,

l-u_

coo

LU<

OC LU

CLCÛ

ÛC

! V \ \ VT _

C!»» oT 3

? Uhligites sp.. Berriasella sp. Berriasian

Spiticeras {Spiticeras)

cf. spitense (Blanford)

Berriasella sp., ? Blanfordiceras sp. late Tithonian-Berriasian

? Blanfordiceras sp.

late Tithonian?

Subzone 4 a

Radiolarians

Subzone 4 (3

Retroceramus haasti (Hochstetter) gr. Kimmeridgian

^^Tuffs

Sandstone and Conglomérâtes

Mudstones

Fig. 4. — Idealized composite section of the Anchorage Formation on Byers Peninsula (Livingston Island). Only radiolarians from

Zone 4 could be recovered. Macrofossll âges are based on fauna collected by Crame et al. (1993) at the base and own data for the

higher part ol the section. The late Tithonian âge for the upper part of the Anchorage Formation is based on new findings of

Blanfordiceras sp. and Berriasella sp.

quent destruction of litminarion indicate dysae-

robic conditions.

The Longing Member is more poorly exposed

chan the “Ameghino'’ Member, Only about one

fourth of the Longing Member is exposed in

place, whereas more than half of the “Ameghino”

692

GEODIVERSITAS • 1999 • 21 (4)

Stratigraphy of Antarctica

Member is well exposed. However, with rhe

exception ot somc small displaccmcnts due to

cryoturbation, most of the Joose blocks forming

the scree cover can bc considered in place. This is

indicated by wcarhered carbonate concrétions

ihat arc perlcctly traccd in the scree, 7'herelorc, it

was possible to gct a complété section of the

Anieghino Formation at Longing Gap.

The sequence contatris common macrofossils

(ammonites, belemnites, bivalves, aptychi, fishes,

driftwoüd) allowing a stratigraphie subdivision.

We emphasize on ammonites in this paper.

Although ihc microfauna is diverse as well

(radiolarians, sponge spiculés, foraminifera, paly-

nomorphs), wc exclusively rcler ro radiolarians

herein. The ammonites, like most other macro-

iossils, are parttcularly enrichcd in certain hori¬

zons, which are ollcn widcly separated.

Radiolarians are only well preserved in carbonate

coneretions. However, the concrétions are conti-

nuously distributed in the Longing Gap Section.

As a conséquence the radiolarian documentation

is more continuons than the ammonite docu¬

mentation.

Bvers Peninsula

The Anchorage Formation was defined by

Crame et ai (1993). It is composed ot dark gray

to black mudstones interbedded with sandstones

and tuffs. Its irue boundaries bave not been

observed. Although it is separated (rom rhe over-

laying Berriasian l’icsidcnr Beaches Formation by

a fault, faciès analysis indicatcs a transitional

change bens-een this two units.

Detailed mapping (Lopetrone 1997) allowed the

récognition of several Anchorage Formation out-

crops m faulr-bounded bloclts showing different

ficies associations. Crame et ai (1993) suggested

a minimum thickness of the composite section of

105 m. A composite section quite different and

difficult to match with the one of Crame et ai

(1993) re.sulteti from oiir work (Fig. 4), probably

as a conséquence of the .structural compicxity of

the area. The inlcgrated thickness of the

Anchorage Formation is close to 120 m inclu-

ding an uppermost sequence transitional to the

President Beaches Formation.

The whole sequence is composed of radiolarian-

rich mudstones with intercalations of tuffs and —

in contrast to the Ameghino Formation — sand-

stonc beds (sec Pirrie & Crame 1995, for a detai-

Icd description). The sandstonc beds reach up to

80 cm in thickness and show evidence of turbidi-

tic sédimentation. Carbonate concrétions occur

ihroughout the section. Flowever, ihcy are smal-

1er than at Longing Gap and many are silicified.

As in rhe Ameghino Formation thcrc is a shift

from parallel-laminatcd to intensely biorurbated

mudstones within the sequence.

Oui* composite section is composed of four inter-

vals, The lowermost exposure is about 1 1 m

dnck. It is separated Ifom the middlc part by a

fault with Lincertain offset. Fhis middle part is

about 55 m thick. A one meter ihick conglomc-

rate occurs at the top of this part of the section.

The upper two parts of the section reach a com¬

posite thickness of around 50 m and are predo-

minated by sandstones and conglomérâtes.

In contrast to Longing Gap. âge diagnostic

macrofossils are relatively rare on Byers

Peninsula. Driftwood, bivalves, belemnires, and a

few ammonites could be recovered. The carbona¬

te concrétions bcar very well preserved radiola¬

rian faunas in the middle section.

FAUNAL CHARACTERISTICS

Owing to the high paleolatitude of the Antarctic

Peninsula the fossils are expected to show biogeo-

graphical différences as compared with lower

paleolatitude sites. Since paleobiogeography bas

some impact on stratigraphie corrclaiion we

shortly discuss biogeographical affinitics of both

ammonites and radiolarians below.

Ammonites arc aftcctcd by the high latitude

dcpositional environment by their reduced diver-

siry and some morphological modifications.

With the probable exception of BLwfordiceras. ail

Antarctic généra are to bc found in Tcthyan sec¬

tions as well- There is no striking évidence for an

Austral ammonite province in the Tithonian

which could be équivalent to rhe Northern

Hemisphere Boréal provinces (Callomon in

Hillebrandt ei ai 1992, but sce also Enay ôc

Cariou 1997).

In contrast, the radiolarians display a pronoun-

ced Austral aspect, both in the Ameghino

GEODIVERSITAS • 1999 • 21 (4)

693

Kiessling W., Scasso R., Zeiss A., Riccardi A. &c Médina F.

Fig. 5. — Age diagnostic radiolanans Tram Byers Peninsula (Ll) and longing Gap (K. LG) A Bivallupus mexicanus Pessagno &

MacLeod, etched concrétion eut parallel to Oedding (K 20-1); B, Loopus primittvus (Matsuoka & Yao) (Ll 31). C. Tethysetta boesii gr.

(Parona) (K 44); D, Parvicinguia coleniani Pessagno S Btomô (K 25); E. Parviclngula exr.elsa Pessagno S Blome (LG 1);

F, Crucella theokattensis Baumgartner (K 14-t). G, Triirabs liiododactylus Baumgartner (Ll 31); H, Acaothôcircus fitriû&us Jud

(Ll 31): I. Valiupus tiopsoni Pessagno & Blome s./., very small specimen (Ll 44); J. Penspyndiuw ordinarium (Pessagno) gr. (K 6);

K, Haliodfctya i?) aniiqua (Rüst) s.i. (K 14*t); L, Acaenioiyfe pan/a Vang = Acaeniotyle umbilicata (Rüst) gr. (K 13); M, Sethocapsa

trachyostraca Foreman (K 13); N, Gongylothorax favosus Dumitrica (K 4); O, Suna echiodes (Foreman) s.l, (Ll 13). See Kiessling

(1999) for figures of additional âge diagnostic radiolarians. Scale bar: A, 76 pm; B, I, M, N. 50 pm; C-H, J-U O, 100 pm.

694

GEODIVEBSITAS • 1999 • 21 (4)

Stratigraphy of Antarctica

Formation and in the Anchorage Formation.

The faunas exhibit typical high latitude characte-

ristics as indicared by the prédominance of

Parvicingula/Praeparvicingtila (Fig. 5D, E). The

Antarctic fauna.s are especially similar to the

Southern Boréal Province as defincd by IVssagno

6c Blome (1986), Pessagno étal. (1993), and

Hull (1997). Borh the Austral Province and the

Southern Boréal Province hâve many species in

common and share fcacurcs such as the lluctua-

ting pantanclliid abundance and the high diversi-

ty of Parvicingula (Hull 1995; Kicssling 1999).

Compared wiih fâunas from équivalent latitudes

on the Northern Hemisphere. Pantarielliidae are

considerably more abundant (Kiessling 6c Scasso

1996). Typical Tethyan taxa such as Tritmhs and

Podocapsa are rare but présent. Vallupus hupsoni

and other vallupins are présent, which is very

useful for stratigraphie corrélation. Hsuum and

Perispyridhim arc as conimon as in ’lethyan sec¬

tions and can also be used for global corrélations.

However, the stratigraphically important

lethyan taxa Mirifiisus. kistola-. and Acanthoarcus

dicranacantbos (S'quinabol) are totally absent in

Antarctica which limits the corrélation with

Tethyan sections.

A sélection of stratigraphically important radiola-

rians is shown in Figure 5. A more compréhensi¬

ve taxonomie framework is provided by Kiessling

(1999).

STRATIGRAPHY

Former ammonite and bivalve data suggested an

âge range of Kimmeridgian/early Tithonian to

late Tithoniaii/Berriasian for the investigated sec¬

tions (Whirham & Doyle 1989; Crame et ai

1993; Pirric 6l Crame 1995). Our new matcrial

is essentially in agreemcat with previous désigna¬

tions. but wc are now ablc to pj-ovide a more

detailed stratigraphie subdivision.

The first stratigraphie subdivision of the Longing

Gap Section based on radiolarians was proposed

by Kiessling 6c Scasso (1996) and Kiessling

(1996). Referring to the North American stan¬

dard zonation the authors came co the conclu¬

sion chat the âge range of the Ameghino

Formation is early Tithonian to Berriasian. Our

new material shows that although the radiolarian

zonation of the sequence is stiJl valid, the chro-

nostratigraphic calibration nceds to bc revised.

The discussion of ammonite âges relies on com-

pari.sons with Antarctic, Argentincan, European,

and Himalayan zonations, whereas the radiola¬

rian zones are first exclusively compared with the

North American zonation ol Pessagno et al.

(1984, 1987, 1993, 1994) and Hull (1997).

Stratigraphy of Longing Gap

Ammonites (A. Zeiss and A. C. Riccardi)

The first ammonite from Longiag Gap, a Late

Jurassic Perisphinctes sp., was mentioned by

Bibby (1966). Further investigations were under-

laken by Médina & Ramos (1981, 1983),

Thom.son (1982), Farquharson (1983), Médina

et al (1983), Zeis.s (manuscripr 1985), Whitham

6c Doyle (1989), and Doyle 6c Whitham (1991).

New material was collected during the

Argentinean Antarctic field carnpaign (1993/

1994) by Scasso, Santisteban and Kiessling. Mosi

ammonites are difficult to identify, as incomplète

and crushed spccimens prevail; often only

impressions of crushed ammonites are availablc.

Therefore, many déterminations are obiained

not with the same securiiy as from better preser-

ved material; this should bc kept in mind when

using the déterminations beîow.

From base to top we can identify the following

macrofossils (horizons are numbered according

to the closest concrétion Icvcl, Fig. 3):

K 16 [LG 11 J. Virgataxioceras cf. setatohies

(Berckhemer 6c Hôlder) (Fig. 6F): the impres¬

sion of a crushed perisphincrid ammonite with

relativcly coarse ribs. Ribs prcdominantly bifur-

cating, but sometimes triflircating (“polygyrate'')

The ribbing .style rc.scmbles somewhat thaï of

“Perisphinctes'" uracemis (Berckhemer 6c Hôlder,

1959, pl. 7/35), but the ribs are branching a lir-

tle deeper near rhe niiddle of the flanks and rhe

secondaries are somewhat more inclined, Tluis,

the spccimen fits better to a paratype of

Virgataxiocerm setatoides (Berckhemer 6c Hôlder

1959, Fig. 30).

K 16 [LG 4]. Virgataxioceras cf. setatoides

(Berckhemer 6c Hôlder): an impression of a cru¬

shed Virgataxioceras. The specimen is rather close

to Virgataxioceras setatoides (Berckhemer 6c

GEODIVERSITAS • 1999 • 21 (4)

695

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

Fig. 6. — Age diagnostic ammonites from Longing Gap. A, ? Virgatosphinctes densisthatus (Steuer) (LG 20); B, Virgatosphinctes

aff. australis (Burckhardt) (LG 25), C, TarameHiceras cf. prolithographicvm (Fontannes) [LG 16(1)]; D, Aulaœsphinctoides (?) sp. juv.

[LG 16(2)]; E, Subplanitoides cf. oppeli Zeiss [LG 9(2)]; F, Virgataxioceras cf. setatoides (Berckhemer & Hôlder) (LG 11 ). Scale bar:

1 cm.

696

GEODIVERSITAS • 1999 • 21 (4)

Scratigraphy of Antarctica

Fi 6- 7 — Age diagnostic ammonites from Longing Gap

A. Neochetoceras (?) sp. [LG 9(1)); B, Kossmatia (?) et. tenuis-

triata (Gray) (LG 3); C. Virgatosphinctes altemecostatus

(Steiger) (LG 29), Scale bars: 1 cm.

Hôlder 1959, fig. 31). The shape and the ribbing

style agréé well. Différences are indicated by the

somewhat more rigid recticostate and denser rib¬

bing as well as by ihc branchirig point of chc ribs

situated a little deeper on our specimen.

K 16 [LG 6]. ? Vh’^aiûx/ocems cl. setatoides

(Berckhemer ^ Hôlder): a rather poorly preser-

ved specimen. Considering shape and ribbing

style it seems to belong to the above destribed

specics or to a rclated latc Kimmeridgian péri-

sphinctid. A similar specimen has been destribed

from the Antalo Limcstonc of Ethiopia (Jordan

1971).

K 17 [043]. Glocbiceras percevait (Fontannes);

Glochiceras cf. lilhographiciim (Oppel);

Taramelliceras n. sp,. ail. proluhographicimt

(Fontannes); l'orquiidsphinctcs hàbyensis Spath;

Lamellaptychxii lamellosus (Parkinson): ihis

sample contains a new species of the Itira-

mellicems proUthographicum/Glochket'as lithogta-

phiettm group. The peciiliar ribbing on the llank.s

of a large specimen is rather similar to

Taramelliceras hemiplenra. while ovcrall morpho-

logy, ribs, and uodes of the outermost part of the

flanks and the marginal and ventral région are

well comparable wîfh stronger ribbed variants of

the T. prolithographiciimlG. lithographicum

group.

A similar, hut smallct species ol the same group

is T. flandrini (Collignon I960, pk 147, fig. 583)

from (lie early Tithonian of Madagascar. 'Fhat

specics has a wider umbilicus, is stronger ribbed

and shows no nodes in the center of chc external

side.

K 17 [044]. Katroliceras sp., Retroceramus cf.

haasd (Hochsietter).

K 18 [045]- Tarciiuttisphinctes

K 18 [LG 16(1)]. Taramelliceras cf. prolithogra-

phicum (Fontannes) (Fig. 6C); an impression of a

partiy pteserved Taramellkerns. The outer part of

the flanLs is well observable. Thèse are ornamen-

ted with ftdcare ribs. The inner part of the ribs is

not strongly curveJ, the outer pan is curved for-

ward. The ribs bifurcate occasionally The ends

of the rilis are marked by smaU tubcrclcs. A row

of tubcrcles i.s aiso observed on the venter. The

ribbing style is characteristic for Taramelliceras

prolithographktim (Füiirannes). However, as we

cannoi observe the inner parts of the llanks and

the specimen is not complété, we déterminé it as

Taramelliceras cf. prolithographicum.

There is some affînity to T. cf rigidum as figured

GEODIVERSITAS • 1999 • 21 (4)

697

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

by Médina al. (1983, pl. 2e), but this détermi¬

nation docs not agréé with the description of the

species by Hôlder (1953) and his illustration of

the hoJotype.

K 18 [LG 16(2)]. Aul/icosphinctoides (?) sp. juv.

(Fig. 6D): this small specimen is difficult to

identify, as young spécimens ot the généra

Aulacosphincioidehy Katroliceras and Torquati-

sphinctes can be very similar and only the cross-

section could help ta distinguish them (d. Spath

1931). However, there is a rather good corres-

pondence between the shape of our specimen

and those of young Aulacosphhictouks as figured

by Spath (1931, pis 78/4, 79/7). Bearing in

mind the problems ineniioned above, specimen

is best identified as Aulacoaphwcioiclti (?) sp. juv.

K 29 [LG 9(l)j. Neoche-toceras (?) sp. (Fig. 7A): a

rather w'eU-presetved fragment of a compressed

oppeliid with narrow \imbilicus. The pour pré¬

servation of the suture does not allow to décide if

the specimen bclongs to the Haploccras subvltma-

tum group. As the ovcrall shapc is that of

Neochetoccras (sec Oppel 1863, pl. 69/3)» this

specimen can he assigned to Ncochvtocems (?) sp.

K 29 [LG 9(2)]. Snhplannoulcs cf. opp(4i Zei.ss

(Fig. 6E): an impression td a th nsely rihbed peri-

sphinctid fragment- A cast ol the .specimen is

very close to Stibplanitoides appeli Zeiss (1968,

pl. 8/2), As the venter is nor observable a déter¬

mination as Siihplanitoîdes cf oppeli is jusfified.

K 29 (LG 10, LG 27]. Neochetoreras (?) sp.:

several oppeliid specimens, crushed. SimKar

forms hâve been figured by Wliitham & Doyle

(1989, fig- 6e). Tliey agréé in shape with

Neochetoccras. In order to exclude tbc possibility

that they bclong to Pseudolissoceras, ihc poorly

preserved renrains oi siuurc-lines were closely

observed. In che end we are convinced that the

sutures suggest an assignment to Neochetocents

rather than to PseudoUssaceras.

?K 29 [LG 28]. Glochiceras sp.: another oppeliid

specimen. The widcr umbilicus suggests an assigiv

ment to Glochiceras rather than to Neochetoreras.

K 30 [LG 3]. Kossmatia (?) cf tenuistriata (Gray)

(Fig. 7B): fragment of a small ammonite. The

ribbing is rather fine and dense. The branching

point is situated in rhe upper part of the flanks.

On the inner part of the last whorl the seconda-

ries are bent forward. At the end of the shell the

specimen is somewhat damaged and the bend is

not well preserved. The decerminarion of such a

small specimen is difficult, OÊpcdally when the

ventral side can not be inspccicd. Some afiinity

exists to similar densely rihbed forms like

Kossmatia aff. temtisiriutu Gray (Thomson 1983,

fig. 3g) or somc Virgatosphinctes of the tennili-

neatm-btirckhardii group (cf. Indans 1954,

pl. 13/1, 4). Thcrc is al.so .some rcscmblance to

the inner whorls of a ^'Lirhacoirras sp,''j as figured

by Wliitham & Doyle (1989, fig. 6g) Judging

from the ribbing on the outer whorl, the forrn of

Whirham & Doyle does nor belong to Litha-

cocerasy but more likely ro forms like Fi-anconites

teriuiplicatus 7.ÇW (1968, pl. 11/4) Para-

bcrrutsella btondeti Zeiss (1968, pl. 12/2) is aiso

comparable to our form, but exhibirs a different

development of ribs on the outer whorl. Ail diese

forms corne from rhe upper part of rlie lower

Tithonian. The détermination as Kossmatia (?)

cf. tenuismata h therefore only one of .sec'eral

other possibilicies.

K 31 1013, 038a-e, 046, LG 12, LG 14,

LG 25, LG 29]. A 1 m thick bank with abun-

dant ammonites: ? Aulacosphifictoides sp.;

Haplocenn sp.; Oppeliidae indet.; ? Taramelliceras

-Sp.; Substj'eblites or Uhligites aft. kraffti (Uhlig);

ViïgatosphJrjcfes cf. and aff. amlescHsis (Douvillé);

Virgatosphiactes sp.; Virgatosphiactes (Lithaco-

ceras) sp.; Lamellaptychus cf. lamellùsus

(Parkin.son); Virgatosphinctes alternecostatus

(Steiger); Virgatosphinctes aff. australis

(Burckhardt).

[013]- ? Substreblites or Uhligites aff. kraffti

(Uhiig): a specimen of47 mm in diameter, very

involute and with fine falcoid ribbing. U looks

like the spccimens figured by Thomson (1979,

pis 2/i|, 3/d, f) under the above mentioned

names. However, détermination is doubtful sincc

the venter could not be ob.served and die ribbing

is srronger.

[LG 29]. Virgatosphinctes altcrnecostatus (Steiger)

(Fig. 7C): half of ihe ammonite is preserved. The

ribbing style is similar to V. denseplicatus nnunda

(Spath 1931, pl. 96/2), but ihc umbilicus is

more narrow. In ihis respea Perisphinctes" alter-

nccûstatus Steiger (1914, pl. 104/1) fies better.

This species seems to belong to Virgatosphinctes

representing an intermédiare form between the

698

GEODlVERSfTAS • 1999 - 21 (4)

Stratigraphy of Antarctica

denseplicatiis and communis group.

[LG 25]. Virgatosphinctes aff. australis

(Burckhardt) (Fig. 6B): a fragmentary specimen

of Virgatosphinctes witli a radier narrow umbili-

cus, but wirh more disrant, polygyrate and bifur-

catc ribs (cf. Indans 1954, pl. 20/6).

K 32 [LG 22, K 32]. Suhdkhotomoceras sp.; ?

Virgatosphinctes sp.

K 34 [020, 025^ 035, X8]- Virgatosphinctes

]^^Lithitcocerüs^^ IndansJ sp.; Aulacosphhictoides (?)

cf. patagoniensis (Favre in Tavera); Buchia cf.

hoebstetteri (Flemint^); Buchia sp.

[025]. A ulacosphinctoides (?) cf patagoniensis

(Favre in Tavera): a fragment of a rather large

pcrispliinctid. Fhc bifurcation point is çhanging

in height benveen the inner third and the outer

third of the flanks on the penultimate and outer

whorl. Ribs on inner whorl split up in half co

rwo thirds ofthe height of die llanks. l’iicrc is no

virgatotonie or polygyrate splitting of the ribs.

Single ribs are intercalaied e.specially on chc outer

half of the penuJiimate ând on the last whorl.

Since die specimen is fragmentary the assign-

meni to Auhicosphinctoides rcniains quescionable.

A désignation to ImpuUisphinctes could also be

possible, l'hcre is some affrnir)' rn speclmens

figurcd as ''Blanfordiceras patagoniense' (Favre)

Feruglio by Tavera (1970, pl. 3/8). However,

those forms are smaller, more coarscly ribbed,

and the liigh outer whorl of our specimen is

absent.

K 40-1 [LG 20]. ? Virgatosphinctes dertsistriatiis

(Steuer) (Fig. 6A): an impression of a densely

ribbed, virgatosphinctid ammonite wich a rather

narrow umbilicus. It has a good coiinterpart in

the specimen figured by ïndans (1954, pl. 21/5)

as V. densisty*iatus (Sieuei), but dicrc is aJso a dis¬

tinct affinity to undescribed forms of

Catutosphinvtes Lcanza & Zeiss (1992) from

Zapala, Argentiiia.

K 4l. ? Kawhiasphinctes cf. antipodus vScevens: a

fragment, broken at about die level of midflanks

or slighrly above. Only the outer half of che

flanks wich straight and slighdy prosiradiate rÜis

can bc observed. Any probable bilurcation point

of dic ribs should be situated deeper. Tlie flanks

arc similar to the outer flanks of Kawhiasphinctes

antipodus Stevens (1997, pl. 32/3) or Virgato¬

sphinctes aff. denseplicatus (Thomson 1979,

pl. l4/a). However, the lacter is more densely rib-

bed and does not fit well. The specimen is roo

poorly preserved for any more précisé identifica¬

tion.

K 57. Blanfordkeras cf wcaveri HowHert: a speçi-

men of 87 nim in diarneter with an umbilicus of

ca, 40 mm. The venter is not preserved; of the

last whorl only one quarter is preserved. The rib-

bing i.s similar to diat in specimens figüred from

Antarctica as Blanfordkeras u>taveri by I Inwlerr

(1989, pl. 2/5, 7), but our form is more evolute

and the ribhing is somewliac coarser. The same is

ULie in comparison with the specimen figured by

Krantz (1928, pl. 3/4) or Weaver (1930,

pl. 3/356-357). The ribs divide above midtiank

and are widely spaccd iti die last quarter of dic

whorl as iri Blanfordkeras watlichr Gray as figu¬

red by Steuer (1891-1892, pl. 16/1). ‘Fhcrc is

also sonie similarity co Blanfordkeras delgai

Collignon (I960, pl. 166/680).

[030]. Siibsteuroccras or Parodontuceras sp. 1 lie

specimen is comparable to the one figured by

Ülivero et al. (1980, pl. 1/2) ironi James Ross

Island II is also similar to Kossmatia carsensis

(Thom^son 1973).

[Al], Blanjhrdicerns d. weaveri Hewlett; rhis

ammonite stems from a moraine deposir above

the top of dic section. The specimen is compa¬

rable with ''Beriassella stihprivasensis' Kraniz {in

’Fhomsnn 1979, pl. 7/i). which was included by

Howlett in his new spccics B. weaveri. It is also

similar to ''Berriusella behrendsenr of Feruglio

(19.36, pl. 7/3-7, 9).

Stratigraphie subdivision based on ammonites

Mcdina &: Ramos (1981) and Médina et al.

(1983) describeJ ammonites from Longing Gap

that can be assigned to ihe catly lo middle

Kimmeridgian. Our new material did not

contain ammonites of this agc.

In our section, the firsr horizons with ammonites

occiir some 80 m above che base (K 16, K 17),

The.sc Icvcls bclong co ihe lare Kimmeridgian

Hyhonoticeras beckeri zone. The presence of rhis

sub.scagc is also demonscraccd by a specimen figu¬

red by Whitham & Doyle (1989, fig. 6c) as

Hyhonoticeras sp. This form appears to represenr

the microconch of a new species of Hyhonoticeras

{Hybonotella) which belongs to the group of

GEODIVERSITAS • 1999 • 21 (4)

699

Kiessling W., Scasso R., Zeiss A.. Riccardi A. & Médina F.

H. beckeri. The speeimen of Wlïitham & Doyle

can best bc comparée! with the inner whorls of a

macroconch figuied as " Hybonoticeras

hybonotiirn' hy Collignon (I960, pl. 132/494)

from tlic ‘■'Kinimcfidgicn moyen” of Madagascar.

However, the spccjes and âge assignmenr of

Collignon cannot be affirmed.

The presence of Submediterranean taxa

( Virgatûxiot'eras, Hybonoticems) in Antarctica may

be astonishing. However, Zeis.s {1971. 1979) has

shown thar rbese généra are widespread along the

eastern part of /Vfrica (Ethiopia-Tanzjinia). Those

forms probably immigrated together wiih Indian

taxa (cf. Howlett 1989) via the Malagassian sea-

way into the Antarctic Région.

The early Tithonian Nyboriolh'cms hybonoturn

zone is reached in concrétion Icvcl IC 18 as pro-

ved by charactcristic làramelUcenis .spccics. In the

middle part of the Longing Mcniber (K 29,

K 30-1) the ammonites may correspond with the

Mucronatum and Vîmineus zones of Sonthern

Germany. They are comparable with Sub-

planitokies^ Franconhes and to ihe Pacific genus

Kossmatia.

Higher in the section, somc 70 meters above the

former ammonite horizon, we fine! a typical

Virgatoiphirivtn fauna similar to that of the

Argenrinean Nenquen Basin (K 31-K 32). This

fauna is assigned to the latc early Tithonian

Mcndozünns zone in Argentina.

Virgatoiphinctei Ls picscnt up to level K 40-1. It

should be noied chat truc middle Tithonian clé¬

ments ol South America {Pseudolisscfceras and

Aidacosphmctes proximm) hâve not been discove-

red in Longing Gap so far. Reports from other

Antarctic localities are very doubtful. too.

However, the Antarctic Virgtttoiphimiei fauna

may aiso tcpreseni the middle Tithonian and

reach up even until the earliest laïc rithonian.

The Virgàtosphwctes-tlildoglochiceras assemblage

of Spiti was assigned to the middle Tithonian hy

Krishna et ai (1982) and Enay & Cariou (1997)

assigned rheir Virgdtüsplnticti's ics.sernblage lo the

late Tithonian. The laiter is charactcrizcd by

V. denseplicatus which is also known from

Antarctica (Ilowlett 1989). Il is especially remar-

kable that in the upper part of the

Virgatosphinctes beds of Longing Gap (K 34-

K 40) only densely ribbed forms predominate

which do not branch up in more than rhree

secondaries. The speetmen of K 41 cotild bc of

middle or late Tithonian âge (cf. Stevens 1997;

Enay Si Cariou 1997). We prehminarily assign

the bed.s above K. 32 to the earliest late Tithonian

Demiplicaïus zone. Eurther investigation are

neccssaiy to define the range of rhe

Virgatosphinctes fauna more precisely in the

Antarctic région.

The firsc occurrence of Blanfif^dicerns s,s. is noted

in concrétion level K 57 providing clear evidence

for late Tithonian. On zVIexandcr Island

(Howlett 1989) ihe Blan/ordiceras fauna includes

Lytohoplites weaverU a truc Lytohnpûtes. Spccics of

this genus hâve been found in Cliile (Biro-

Bagoczky 1984) in rhe Corongoceras alternans

zone, the second zone of rhe lace Tithonian in

South America. Ir corresponds approximately

with the zone tT ParauLtcosphincies tmniitorius in

Mediterranean Europe-, i.c., dic middle part of

the late Tithonian. This is ia agrcemenr with

Thomson (1979) and Howlett (1989) who

cons'idered the Bbmfordîceras zone as part of the

late Tithonian.

Some 30 m above K 37 lollow bed.s chat can

questionably bf correlated with the Argenrinean

Substruroceras koeneni zone. We can suppose the

Jurassic/Cretaceous boundary in these beds (cf

Zeiss 1986).

Near the top of the section a Berriasian âge is

suggested bv Spiticeras (Spiiiccras) according to

Whitham ÔC Doyle (1989).

Narth American radiularian zones at Longing Gap

The base of the Longing Gap Section is assigned

to Zone 3 as indicated by the presence of Caneta

hsui (Bessagno) and the absence of Valhipiu hop-

sont Pessagno Blome. Since neither Tnranta

s.s. nor Hsuum rnaxwelli Pessagno were found,

\vc présume that the basal part of the Longing

Gap Section bclongs to upper Subzone 3 alpha,

alihough the primary marker taxon Napora

burckhardti Pessagno, Whalen & Yeh was not

rccorded (- exclusively Terhyan marker taxon

according to Pessagno et ai 19S7b). The secon-

dary marker taxa Parvkhtgtda colemani Pessagno

&: Blome (Fig. 5D) and Hiuum mclaughlini

Pessagno & Blome are présent near the base indi-

cating Subzone 4 beta. However, the primary

700

GEODIVERSITAS • 1999 • 21 (4)

Stratigraphy of Antarctica

marker taxon Vallupus hopaoni was nor recorded,

although pantanelliids and everi vallupins are

common in some sampics and we hâve searched

for this specics inrcnsely. The lasi distinct hori¬

zon bcfore che evolurionary firsi appearance of

V hopsoni is K 14-K K 15. Above ihose samples

V. hopson'i is absent, but the sc-arcity ofother pan-

taneiliids indicates chat irs absence may be due to

paleoccanographic factors.

The base of Zone 4'Subzone 4 beta is well defi-

ned by the fîrst appearance of Vallupus hopsani in

sample K 2U-1. This is noted just above the first

Tithonian ammonites assigned to the Hybo-

notum zone; The firsi occurrence of Vallupus

hopsoni provides the most reliable datum in the

section. It will be dlscassed in détail below. Up

section V. hopsoni is continuously présent in

samples with a high total pantanelliid abundancc.

The top of Subzone 4 beta Ls marked by rhe last

appearance ol Perispyridium in concrétion K 29.

Perispyrtdhipi is represented by rv\^o ne^v species

within Subzone 4 beta (Kiessling 1999). It is

continuously rccorded in ail better preserved

assemblages. The lasc occurrence of Péri-

spyridium is noted between aminoiiiie a.s.scm-

blages assigned to the early diihoniaii

Mucronatum and zones, rcspectively.

Marker taxa in Subzonc 4 alpha and the suspec-

ted Zone 5 arc rare. The base of Subzorie 4 alpha

is characterized by abundant PantanelJiidae

including Vallupus hopsoni and the absence of

Perispyridiîim. The last occurrence ot K hopsoni

is noted some 20 m above the ammonite horizon

tliat lias been assigned to the late early Tithonian

Mucronatum zone, The upper boutidary of Sub¬

zone 4 alpha is poorly defined owing to the

absence of ptimaiy marker taxa. Ir is preliminari-

ly drawn between ihc last occurrence of Pannein-

gula coleniani Pèssagno & Blome and the first

occurrence of Wllliriedctlum ruesti (Tan Sin Hok).

The radiolarian âges are without major contra-

dicrions with regard to the zonation of Pèssagno

et al. (1993). However, die secondary and corpo¬

réal marker taxa Patvicingula çùlemaniy

Parvicingula joncsi Pèssagno s.l. and Hsuuw

mclaughlini s.l. occur slightly carlier than predic-

ted in Pessagnos zonation.

In summary, the Ameghino Formation at

Longing Gap ranges from the Kimmeridgian to

che early Bertiasian. The Longing Mernber

ranges Irom the Kimmeridgian to probably the

earliest laie Tithonian and the "Ameghino”

Mernber is assigned to rhe latc Tithonian to eatly

Bertiasian. The part of radiolarian Zone 3 expo-

sed at Longing Gap (top of Subzone 3 alpha) can

be a-ssigned to tbe Kimmeridgian. The base of

Zone 4 is likcly to coïncide with the base of the

lithonian or latest Kimmeridgian. The bounda-

ry between Subzone 4 beta and Subzone 4 alpha

is assigned to rhe middie part of the early

Tithonian (sensu Gallico). The boundary bet¬

ween Zone 4 and Zone 5 is less clearly deflncd at

Longing Gap. The occurrence of Spiticeras

(Spiticeros) approxlmately coincides with radiola¬

rian assemblages preliminarily assigned to

Zone 5. This would indicate chai the boundary

of Zone 4-Zone 5 agréés with the Jurassic-

Cretaceous boundary. A more detailed discussion

tollows below.

SïKAI IGRAPHIO SU.MMARY OF ByEKS PeNINSVU

RadioLmans

No radiolarians coald be extracted from rhe basal

section, but the middie section yielded several

exceptionally well preserved faunas (Figs 4, S).

Most of the productive samples can be assigned

to Subzone 4 beia, This is confirrned by the co¬

occurrence of Vulluptis hopsoni and Perispyrldhfm

near the ba.se of the fertile séquence (LI 44). Tlie

overlying concrétions lack Vallupinae (for paleo-

ceanographic rcasons) but contain Perispyridiunïy

thus indicating Subzonc 4 bet-a as w'ell.

Near the top of the middie section, a well-preser-

ved fauna (L1 35) concains Vallupus hopsonh but

lacks Perispyridiîim. This sample is, therefore,

assigned rn the hase of Subzone 4 .ilpha.

No âge diagnostic radiolarians could be extracted

from che upper section.

AmmoniteSy belemnites and bivalves

First âge diagnostic ammonites and belemnites

from the Upper ju rassie sequence wcrc listcd by

Tavera (1970) and Smcllie et ai (1980). SmclUc

et ai (1980) found indication for Kimmeridgian

(Hibolttes marwicki niarwicki Stevens and

Subplanites early Fithonian (Belenwopsis sto-

leyi Scevens) and latc Tithonian (Berriaiella cf.

hehrendseni Burckhardt). Without referring to a

GEODIVERSITAS * 1999 • 21 (4)

701

K 65

K 47

K 44

K 38

K 33

K 30b

lîW

K27

LG 1

K 24

K 20-1

K 18

kIs”

K 14-1

K13

K 12

K 8-1

ü 35

ü 13

TTÏT

Lt44

ü 48

Stratigraphy of Antarctica

section they gave a “balancée!” âge of early

Tithonian for the “mudstonc member".

Crame et al. (1993) found inocerams of the

Retroceramm htmsû (Hochscetter) group near the

base of tlie section stiggescing (but not proving)

Kimmcridgian. Ncar the top of their section

Crame et ai (1993) found an ammonite-bcleni'

nite assemblage with Tithonian affinities. We

could colicct BerrünelLt and ? Btanfordiceras 25 m

below the upper boundary of ihe exposed

séquence providing évidence for late Tithonian.

Spiticeras (Spiticents) cf spitense (Blantord) was

found in the overlaying President Beaches

Formation. No ammonites were discovered in

the radiolarian-rich intcrval.

In summary, the Anchorage Formation on Byers

Peninsula ranges ffom Kimmeridgian/Tithonian

to latest Tithonian. Radiolarians belonging to

Subzone 4 beta are stratigraphically doser to

what has been dated as Kjmmeridgian than to

the ifemV/WZ/i'bearing late Tithonian/Berriasian

(Fig. 4). The data .support the conclusion that

Subzone 4 beta should be completely assigned to

the early Tithonian» althouglt Utc cvidence is less

convincing chan at Longmg Gap.

LATE JURASSIC RADIOLARIAN

BIOSTRATIGRAPHY

The biostratîgraphic u.se of Laie Jurassic ladiola-

rians has only been recognized in cite past rwenty

years starring with Pe.ssagno (1977a). Sincc then a

number of Late Jurassic radiolarian zonations have

been proposed. Therc are basically four zonations

in use for different régions of the world.

1 . The North American zonation: this zonation

dates back to the work of Pessagno (1977a). It

was completely revised b}' Pessagno et al. (1984)

and refined latcr by Pessagno et al. ( 1987b, 1993,

1994). The most recent iipdare of the North

American zonation was provided by Hull (1997).

The chronosiracigraphic calibration of radiola¬

rian zones was esrablished using ammonite, cal-

pionellid and bivalve data.

2. The Tethvan zonation: a flrst zonation was

presented by Baumgartner et al. (1980) based on

unitary associations. This zonation was conside-

rably revi.sed by Baumgartner (1984), chrono-

stratigtaphically updated by Baumgartner

(1987), and rcachcd its current State by the com¬

préhensive contribution of Baumgartner et al.

(1995a). The chronostrarigraphic calibration of

radiolarian zones was esrablished by using

ammonite, calpionellid and caJeareous nanno-

fossil âges.

3- The “Japanesc” zonations: several Japanese

scientists deveJoped zonations which are mostly

applied to western Pacific sections, but are also

usefui in the Tethys. The mosi widely u.sed zona¬

tion ha.s been developed by Matsuoka Yao

(1986) which was updated by Mat.suoka (1992,

1995b). The chtonostratigraphic calibration is

partiy provided by ammonite and calcareous

nannofossil data, but mostly relies on corrélation

with dated Tethyan and North American radiola-

rian-bearing sequences.

4. The Russian zonations: zonaiioii.s of ihe

Caucasus Région and rhe Russian Far Easr were

proposed by Tikhomirova (1988) and Vish-

nevskaya (1993). The Juras.sic zones in the

Caucasus arc calibratcd by ammonites and apty-

chi, whereas the Russian Pacific margin is poorly

dated by Buch'ta sp Lace Jurassic radiolarian stra¬

tigraphy on the Russian platform is still in îts

infancy with only one preliminary zonation avai-

lable (Kozlova 1994).

As cxplained above, we mostly applied the North

American radiolarian zonation for dating our

radiolarian samplcs. The primary, secondary and

corporéal markets of Pessagno et al (1993) that

are présent in Antarctica are li.sted in Table 1.

The application of the new Unitary Association

stratigraphy of Baumgartner et ai (1995a) is

hampered by the scarcity of Tethyan taxa.

However, there arc several .specics that have been

used in Icthyan zonations as well ('Fable 1). Fhc

occurrences of .species discussed below arc indica-

ted in Figure 8, if they were traccd in more than

onc sample. Spccies occurring in only one

sam pic arc;

- LI i\'. AcUnthodreusfiirwsus]uà',

— K 8-1 : Saitoum pagei Pessagno;

— K 12: Provunuma japonicus Matsuoka & Yao;

- K 13: Sethocapsa trachyostraca Foreman;

GEODIVERSITAS • 1999 • 21 (4)

703

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

Table 1. — Anlarctic radiolarian taxa used in published zonations.

Radiolarian marker taxa used in Radiolarian species used in

the North American zonation the Tethyan zonation

(Pessagno état. 1984,1987b, 1993,1994) (Baumgartner étal. 1995a)

Bi\/allupus

Canota hsui (Pessagno)

Hsuum mclaughiiniPessagno & Blome s.l.

Orbiculiforma lowreÿonsis Pessagno

Parvicingula blowt Pessagno

Parvicingula oolemâfii Pessagno & Blome

Parvicingula excetsa Pessagno & Blome

Parvicingula jonesi Pessagno

Praeparvicinguta vera (Pessagno & Whalen)

Perispyridium

Tethysetîa boesit (Parona)

Vallupus hopsoni Pessagno & Blome

Acaeniotyle umbilicata (Rüst) gr.

Acanthocircus fvriosus Jud

Acastea diaphorogona (Foreman)

Angufobracchia biordinalis Ozvoldova

Tethysetîa baesü gr (Parona)

Crucelta theokaftensis Baumgartner

Emiluvia chica Foreman

Emiluvia hopsoni Pessagno

Emiluvia pessagnoi Foreman

Gongylothorax tsvosus Dumitrica

Haiiodiciya (?) antiqua s.l. (Rüst)

Homoeoparonaeiia etngans (Pessagno)

Hsuum sp. atl H cuestaense Pessagno

(= Hsuum mclaughiini s.l.)

Hsuum fefiformts Jud

Loopus primitivus (Matsuoka & Yao)

Napora pyramidalis Baumgartner

Perispyridium ordtnanum (Pessagno) gr.

Podobursa spinosas.)^ (Ozvoldova)

Podocapsa amphilroptera Foreman

Protunumn inponiaus Matsuoka & Yao

Saitoum pagai Pessagno

Sethocapsa /rac/iyos/raca Foreman

Suna achlodes (Foreman) s.l.

Triactoma moxicana Pessagno & Yang

Triactoma tithonianum Rüst

Tritrabs rhodudautyhs Baumgartner

Zhamoidellum ventricosum Dumitrica

- K 14-1: Haliodictyai^) antiqua (Rüst) s.l.;

- K 23: Orbiculiforma lawreyensis Pessagno;

- K 27: Podobursa spinosa (O/voldova) s.l.

We first discuss rhe value of the North American

zonation and subsequently try co link oiir data to

rhe zonation of Baumgartner et al. (1995a) and

Matsuoka (1995b). The Russian zonations are

not discussed, sincc their stratigraphie resolution

is either too coarse or ihey consider poorly defi-

ned species.

The North American radiolarian zonation

The major pitfall of the North American zona¬

tion is the rcfcrence to species absence in strati¬

graphie assignment. As zonal boundaries are

defined by first or last occurrences of marker

taxa, the reliability of their absence bas to be cri-

tically evaluated for cach section or sample. This

can bc achieved by observing the quantitative

distribution of marker ta.xa wirhin their range

and by judging the possibility that species absen¬

ce is mercly a rcsult of océanographie, diagenetic

or stochastic bias.

As discu-ssed above, wc can rccognize the North

American Zones 3 and 4, and probably zone 5 in

Antarctica. Zone 3 was originally assigned to the

early 1 ithonian, but it Iras been demonstrated by

Baumgartner et al. (1995a) that its base may

reach down to the middie Oxlordian.

rhe base of Zone 4 was originally (Pessagno et al.

1984, 1987) calibrated by corré.sponding closely

to the first occurrence of Crassicollana intermcdia

(Durand Delga) and laie Tithonian ammonites

in Mexico and by occurring below the Buchia

piocha zone of Jones et al. (1969) in California.

704

GEODIVERSITAS • 1999 • 21 {4)

Stratigraphy of Antarctica

Table 2. — Summary of modifications in the chronostratigraphic assignment of North American radiolarian zones resulting from our

new data.

Pessagno et ai.

(1977a, b, 1984,1987,1993)

This paper

Base of Zone 5

Base of Subzone 4 alpha

Base of Zone 4

Tithonian/Berriasian boundary

early late/late late Tithonian boundary

early/late Tithonian boundary

Tithonian/Berriasian boundary?

Early Tithonian (Darwini zone)

Kimmeridgian/Tithonian boundary

Ir was thus correlated wiih thc carly

Tithonian/lare Tirhontan (sensu Gallico) bounda-

ry. Recentlyj this boundary wai lowercd co the

late early Tithoniati (Pessagno pcrs. comm.

1997; Hull 1997).

The new résides from the Antarctic sections

demand a révision of ihc chronostracigraphic

calibration ftjr the base of Zone 4 and thc base of

Subzone 4 alpha given by Pessagno er ai (1993),

Before we do so» we hâve lo check the reliability

of OUI' radiolarian âges, especiallv referring to thc

marker taxa of Pessagno étal. (1993).

The base of Zone 4 was (vriginally (Pes.sagno ei

al. 1984) dePined by the first occurrence of

Acanthocircus dicranacanthos and Vallupns hop-

soni. Since A. dicranacanthos is absent in

Antarctica» due to the high paleolaritude, the

first occurrence of che pantanelliid Vatlupus bop-

soni (Fig. 51) is crucial in our discussion. The

Austral characrer ot the radiolarians requires cau¬

tion in the interprétation of thc first occurrence

date of this spccies. Since the abundance (or pro-

bability of détection) of thc pantanelliid sub-

family Vallupinac is correlated with thc ovcrall

abiindance ot PantaneUiidae, it is very unlikely to

dctect Vallnpus hopsoni in standard residues

(about 1 g in thc Antarctic material), if pantanel-

liids make up Icss than 5% of a radiolarian

sainplc. This hict may bc partly responsible for

the erroncous corrélation of Pessagno et ai

(1993)- The abundance and diversity of panta-

nelliids was thought to decrease rapidiy with lati¬

tude in che paleolatitudinal mode! of Pessagno &

Blome (1986). Although pantauellüds siun up to

50.1% in one sample from Longing Gap, their

abundance is .strongly flucruating in Antarctica,

In Longing Gap (Fig. 3) rhe first occurrence of

Vallupus hopsoni is noied in a sample (K 20-1)

with 12.1% total pantanelliid abundance. The

samples taken frorn just 2 and 3 m below (K 18,

19) contain a rich radiolarian fauna» but yield

fcw pantancJIüds. Only the samples K 14-1 and

K 15 providc firm evidence for an âge older than

vSubzone 4 beta. They contain diverse and abun-

dant pantanelliids (15-6 and 13.8%, respcctively)

and even sonie vallupins, but no Vallupus was

detected. Our last firm ammonite évidence for

the Kimmeridgian is from between K 15 and

K 18, but our first evidence of Tithonian stems

from thclevcl of K. 18. I hus thc first appcarancc

of Vallupus hopsoni is only rcliablc within a 40

thick intcrval separating K 15 and K 20-1.

Although we do have ammonite évidence for

early Tithonian below K 20-1 (Hyhonotum

zone), we cannot rcjcct a latc Kimmeridgian âge

for rhe base of Zone 4.

The last occurrence of V. hopsoni has been used

a.s a corporéal marker within Subzonc 4 alpha. At

Longing Gap concrétion Icvcl K 33/34 is thc last

horizon containing this spccies. This horizon is

dated as middlc/latc 1 ithonian and is probably

équivalent to rhe Windhaiisenkeras internispino-

sum zone of Axgcntina. Although we are not able

to provide firm evidence for this zone in

Antarctica (see discussion above), the présence of

hopsoni in rhe W. internispinosum zone w;ei

established by Pujana (1991, 1996) in Argentina.

In the Southern Alps, Subzone 4 alpha with

V hopsoni was recorded în che lare middle to ear-

liesr late 3 ithonian Chitinoidella zone (cf.

Kiessling 1995).

Perispyridium (Fig. 5J) is the only other primary

marker taxon in Zone 4 that is présent in

Antarctica. Its last occurrence marks che top of

Subzone 4 beta. The last occurrence of rhis genus

provides a reliable datum, since Perispyridium is

common ihroughout its stratigraphie range (with

two exceptions) and suddenly disappears in the

GEODIVERSITAS • 1999 • 21 (4)

705

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

Primary Marker

Taxa

Secondary and Corporéal Marker

Taxa

BERR.

early

Zone 5

Subzone 5A

Parvicinguïa jonesi

NVINOHIII

early late

Zone 4

Subzone 4a

1 Ristola procera

Ristola altissima X

^ VaUupus hopsoni^

^arvicingula excei

Hsuum metaugh.

Parvicinguia colemani

Isa

Ijfjj Orbiculif. lowreyensis

Subzone 4p

Perispyridium ^

Acanthoc. dicranacanthos^

^ T

P. colemani

^ Parvicing. jonesi

KIMMERIDGIAN

_ _ _

early late

Zone 3

Subzone 3a

Napora burckhardti

ï_Ÿ

Subzone 3p

Mirifusus guadalupensis T

1 Turanta J

Hsuum maxwelli

OXFORDIAN

early middle late

- Mirifusus baileyi

Caneta hsui

^ Parvicinguia t^wi

Zone 2

Subzone 2a1

Loopus

Subzone 2a2

Parvicinguia s.s. ^

Fig. 9. — New chronostfatlgraphic assignmentot the radiolarlan blostratigraphy ot Pessâgno (1977b), Pessagno et al. (1984, 1987,

1993, 1994, 1996). Our data allow a modification ol the Zone 3/Zone 4 boundary and the boundary between Subzone 4 alpha and

4 beta. The lower zones were modified foUowIng Baumgartner et al. (1995a. fig. 13). Marker taxa lhal are présent in Antarctica are

printed in bold, In this figure we use the Tithonian sensu Gallico as do Pessagno et ai: however it should be noted thaï subzone

4 beta ends betore the middle Tithonian sensu Gerlh.

sequence. However, there is a relatively thick

interval with only sparse radiolarian faiinas above

the last record of Perispyridium in K 29. The first

radiolarian sample with a sure absence of this

genus is K 30b, which is only a few meters below

the first record of the latest early Tithonian

[sensu Certh) Mendozanus zone. Hence, the top

of Subzone 4 beta i.s as.signcd to the late carly

Tithonian [sefisu Gcrth = early early Tithonian

sensu Gallico).

According to Pe.ssagno e/ al. (1987). the last

occurrence of Parincingula colemani is noted in

the upper part of Subzonc 4 alpha (corporéal

marker taxon). In Longing Gap, the last samplcs

with P colemani s.l. are above the level with first

evidence of bcrriasellid ammonites indicating

late Tithonian. Above the last occurrence of

P colemani no primary marker taxa (with the

exception of Parvicingtda joncsi Pessagno) of the

Nnrth American zonation are présent. However,

Hull (1997) used the la.st occu trente of lïsuum

mclaugblini as a secondary marker to define the

top of Zone 4. This species ts présent ncar the

rop of the Longing Gap Section (K 65) which is

assigned to the Berriasian. This would indîcate

chat the top of Zone 4 should be assigned to the

early Berria.sian, consistent with new resuirs of

Pessagno étal. (1996). However, a relatively great

faunal change is noted in Antarctica from K 60

onward, approximately consistent with the

706

GEODIVERSITAS • 1999 • 21 (4)

Stratigraphy of Antarctica

Jurassic-Creraceous boundary. Since no primary

marker taxa are présent, wc tcntatively corrclate

rhe Zone 4'Zone 5 boundary with the Jurassic-

Cretaceoiis boundary and ihc first occurrence of

Williriedellum ruesti (Tan Sin Hok) as figured in

Kiessling & Scasso (1996j pl. 2/14).

Considering the staiemcnts abovc, wc can revise

the chronostraiigraphic assignments of the North

American radiolarian zonation (Table 2, Fig. 9).

We arc currently not able to affirm whar led ro

the erroncoüs chronostracigraphic assignment of

the zones and subzone.s discusscd abovc. They

may partly be duc to the coniplcx lectonic ser-

tings of both Mexico and California.

Evidence (-rom other areas

rhe new chronostracigraphic assignment of the

Zone 3-Zonc 4 boundary is supported by new

data from Gerntany,

Recent investigations in the Upper Jnrassic of

Southern Gerrnany produced a very well-pre.ser-

ved and diverse radiolarian fauna in the

Mdrnsheim Formation (Zügel 1997) including

V hopsoni. The Mornsheim Formation is correla-

ted with the upper part of the Hybonoticeras

hybo)iotu)n zone (Zeiss 1977) équivalent to an

early early Tichonian âge. In his ongoing work,

Zügel (pers. comm. 1997) coiild recover V. hop¬

soni aiso in the cherr-bearing limestones of

Schamhaiipten (Bavaria, Southern Gerrnany).

The locality is curnently -assigned to the upper-

most Kimmeridgian (Bausch 1963).

In summary, the data from Gerrnany do support

an oldcr age for rhe Zone 3-Zone 4 boundary.

We can thus conclude that V. hopsoni Hrsi

appears vety close to rhe Kimmeridgian/

Tichonian boundary. Other reports (Matsuoka

1992, Chiari et ai 1997) on the first occurrence

of V. hopsoni do also support chis interprétation,

althoLigh they are nor directiy correlated with

ammonite data.

Zonation or Badmgariner Erwz. (1995b)

We hâve discusscd above chat the applicabilicy of

the 'Fcchyan unnary association zonation (UAZ)

is rcstricred owing to biogcographic différences.

Additionally, there is a general trend from assem¬

blages containing Tethyan taxa at the base to

assemblages with a higli degree of endemism al

the top in chc Ameghino Formation. However, a

limitcd comparison is possible, if we sum up ail

our samples from the zones and subzones of ihc

North American zonation. Three of the new uni-

tary associations of Baurngartner et al. (1995a)

werc expected to occur in Antarctica:

— UAZ l ] ‘ late Kimmeridgian-early Tithonian;

— UAZ 12; early-early laie Tithonian:

— UAZ 13; laieÿt 1 ithonian-carlicst Berriasian.

We will show below ihat UAZ 10 is unexpected-

ly also présent at Longing Gap.

At Longing Gap, our samples from Zone 3, Sub¬

zone 3 alpha (K 2'K 1 5) contain the Tethyan

taxa Acaenwtyle mnhilicata gr. (Fig. 5L), Acustea

diap h or Q go na-> Angu lob racchia bio rd i nalis^

Archaeodictyomitra minaemisy cyucelld theokajifu-

sis (Fig. .5F), Gongylothorax Javo^us (Fig. 5N'),

Haliodictya (?) antiqna s.l. (Fig. 5K), Hsuum sp.

atf- //- rnestiiensc, Napora pyramidulis. Péri'

spyridturn ordhiarium gr. (Fig. 5]). Prottoiuma

japonieuhy Saitoum pagei, Sethocapsa trachyostrara

(Fig. 5M), Triûctoma îiiexira^iOy and Zhamoi-

dellum ventricosnm. This assemblage was not

observed in the Tethys and trying to appty the

UAZ 95 Icads to ci^ntradictory rcsults. Triactoma

niexicana (samples K S-l, K 13) is prcdictcd to

range not higher than UAZ 9, but Acaeniotyle

umbïliaiut {.samples K 6, K 12, K 13. K 14-1) Is

not supposcd to occur before UAZ 10. It is likely

that the total range of T. mexicana is poorly défi*

ned in the UAZ considering the zonal as.sign-

menr oi T. niexicana ta vSubzone 4 beta by

Pessagno et al. (1989) and ics occurrence in

LIAZ 12 in ihc Southern Alps (c£ Kiessling

1995). Congylothorax favosus is not reporred

above UAZ 10 according to Baumgartncr et al

(1995a). d'bis specics was fbund unly at the very

base of the section (K 2, K 4) which may actually

be assigiied to UAZ U). The .samplc.s above K 4

are assigned to UAZ 10-11. dhcre arc not suffi*

cicni l'erhyan radiolarians to prcciscly define the

LIAZ of Baumgartner et al (1995a). However,

rhe application ofthe unpublished 127 UA range

charr on the lurnped zone 3 fauna resulrs in a

firm corrélation with UAZ 10 (Guex, pers.

comm. 1998). Tnactoma mexicana ranges up to

UAZ 11 in this recomputing.

GEODIVERSITAS • 1999 • 21 (4)

707

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

Within Subzone 4 beta thc loJlowiag Taxa used

by Baumgartncr et ûl. (1993a) are présent in

Antarctica: Acafzthocirrus furiosm (Fig. 5H),

Acastea diaphorogondy Angulobracchia hiordlnalisy

Emiliivict chicdy Rmiltivid peisagnoi s.L.

Gorgarisiitm sp., HùmoeoparonaelLt êlegavsy

Hsuum aff. cuestaedsc, Usuam feliforrnh (onJy

detected in James Ross Island). Loopusprimitivm

(Fig. 5B), Nnpora ppuynidulhy EeHspyrldium

ordinarium gr., Podoburui sphwuj s.l,, Podocapsa

amphitreptera s.l., Suna cchiodes .s.l. (Fig. 50),

TriactornU tithoniiWtmiy Iritrahs rhododaciylus

(Fig. 50.

Again, there are some contradictions applying

the unitary âs.sociation zonation. Gorgum'ium

ranges from UAZ 3-8 according lo Baumgartncr

et al. {Î995a), whcrcas Hsuum feliformis \s

rhoughr to occur not earlier than UAZ 13.

Leaving aside these problenutic taxa would rcsidt

in a correlarion wirh UAZ 10 for the assemblage,

as defined hy A. furinsus (UAZ 10-20) and

H. elegam (UAZ 4-10). However, H, ekgafis only

occurs up to the middie part nf Subzone 4 beta

at Longing Gap. Above the Ust occurrence of

H. elegtms the assemblage would be assigned to

UAZ 10-11- Again, the application of thc

127 UA range chart hclp.s to define the corréla¬

tion more precisely. Gucx (1998, pers. conim.)

States thac thc lumped Subzone 4 beta launa per-

fectly corrclares wirh UAZ 11.

Only a iVw Terhyan taxa were ('ound in the

assemblages assigned to Sub/one 4 alpha and

Zone 5: Gorgamïum sp., Hsuuni af£ cuestaensvy

Tethysetta hœsiï gi. (Fig. 5C), Triactoma tithonia-

num arc présent indîcating UAZ 10-13. A more

exact corrélation is not possible. Thus rhe pré¬

sence of UAZ 12-13 cannot be proved in

Antarctica.

The stratigraphie corrélation of the North

American zones with the UAZ can be controlled

by new data iVorn Europe (Kiessling 1995;

Chiari ci ni 1997-, Zügel 1997). V hopsoni was

reported irom UAZ 10 (Chiari étal, 1997) to

UAZ 12-13 (Ziigel 1997, cf Kiessling 1995,

1996). Two sainples from the Southern Alps bear

V. hopsoni atid lack Perhpyridimn and can chus be

assigned to the base of Subzone 4 alpha. The

sample from Ronce Serra near Fonzaso (see

Kiessling 1996 for localicy description) is from

the rransitional intcrval berween the

Ammonitico Rosso Superiore and the Maiolica

whiclî has hecu assigned to the lare middie to

earliest late Tithonian Chiünnidella zone by

Grandesso (1977). This simple (PS 13) contains

many species that make their first occurrence in

UAZ 13: Emiliivia chtca decussata .Steiger,

Obesacapsula ruscoensis umbriensis }ud,

Paronaella (?) tiihulata Steigen Pynnnhpongia

barmsteruensis (Sçeiger), and Syringocapsa ampho-

rella (Jud). On the other hand, species like

Syringocapsa spinellifera Baumgartner and

Williriedclliim crystallinum Dumttrica arc a.lso

présent, These hâve their last occurrence în

UAZ 12 and UAZ 11, re.spcctivcly. Thcrclbre,

PS 13 is preliminarily assigned to UAZ 12.

In summarv" thc total range of U hopsoni is from

UAZ 10 to at Icast UAZ 12. Tlie related torm

VallnpiL^ jafwnuiis has been shown by Matsuoka

(1998) to range up to thc early Berriasian

(UAZ 13). UAZ 10 radiolarian assemblages can

bc obsciwcd frojTi the base of the Longing Gap

Section (Kimmeridgian) up to a horizon thaï has

been dated as early Tilhonian by ammonites.

Baumgartner et al. (1995a) indicared a laïc

Oxford!an-early Kimmeridgian âge for UAZ 10.

Although Baumgartner er///. (1995a: 1033) pro¬

vide good évidence for this âge, the âge of the

succeeding UAZ 11 is much less well defined.

Considering rhe rcsults above, we can conclude

thac UAZ 10 ranges up to ai least ilie latest

Kimmeridgian Beckeri zone. The new corrélation

of UAZ 10-13 with thc North American zona¬

tion and their clironoso'angraphic assignaient are

indicaied in Figure 10.

Zonation of Matsuoka (1995b)

The comparison with Matsuoka (1995b) is ham-

pered by che rarher coarse stratigraphie résolu¬

tion of Matsuokas Latc Juras.sic zonation. Only

rhe Pseudodictyoniitra priwitiva zone can be tra-

ced in Amanctica, owing to the absence of other

age-diagnosiic taxa, l'his intcrval zone is defined

by the last occurrence ol Hsuum W{4.xu>elli at its

base and the first occurrence of Pseudodictyoniitra

carpatica (Lozynyak) ai its top. It is supposcd to

range from the early to the middie Tithonian.

708

GEODIVERSITAS • 1999 • 21 (4)

Scratigraphy of Antarctica

NORTH

TETHYAN

AMERICAN

ZONES

(UAZ 95)

BERRIASIAN

i Q

1 O

_co

4 a

TITHONIAN

°§-

l’a

-1

k 5

KIMMERIDGIAN

3 a

Fig. 10. — Corrélation of the North American (Pessagno et al.

1993) and Tethyan (Baumgartner et al. 1995a) zonations for the

Kimmeridgian/Tithonian Inlerval.

According lo Matsuoka (1995a, fig. 3)i the

/?priniitivii zone ranges trom the ba.se ol Zone 3

CO the top of Subzone 4 beta. Con.sidering our

resuirs and the eorrclation chait of Baumgartner

et al. (1995a, Hg. 13) this would imply a total

range ol the P pYtrn'nhM zone from rhe middle

Oxfordian to early 'J'ithonian. However, as rhe

last occurrence of Hsuum maxwelU is noTcd

within upper Subzonc 3 alpha according to

Pessagno et al. (I993)i we suggest thar rhe

Pmidodictyomitm primitmi zone starts in rhe lare

Kimmcridgian. Since Psnuiodkîyomitra carpatica

is absent due ro biogeographical dilferenccs, the

top of rhe Pseudoditîyomiim prlmttiva zone can-

not be defined.

Although the total range of Loopiis prîmitiinis

(= Pseudadrayumiîra pritaitiva) is uncerrain

according to Matsuoka (1995b) its major occur¬

rence is dcfinitely within the I^eudodiciyomitra

primitiva zone. At Longing Gap and Livingston

Island, primitivus is found in Subzonc 4 beta

and at the verv base of Subzone 4 alpha, les first

occurrence coincidc-s with the first occurrence of

V hopsoni and iis lasr occurrence is noted slighrly

above the lasr occurrence of Perispyridium. This

agréés with a latest Kin^meridgian to probably

middle Tirhonian âge and is consistent with

Matsuokas chronostratigraphic assignment for

the Pseudodictyomitra primitiva zone.

CONCLUSIONS

New paleontological data from two Upper

Jurassic localides on the Ancarctic Peninsula allow

the élaboration of a combined ammonite and

radiolarian strarigraphy, providc a high stratigra¬

phie résolution and allow to révisé current chro-

nostradgraphic calibrations of radiolarian zones.

The Ameghino Formation ai Longing Gap

ranges from the Kimmcridgian ro ihe early

Berriasian, vvhereas the Anchorage Formation at

Byers Peninsula ranges from rhe Kimmcridgian/

Tirhonian to the latest Tithonian. Zone 3>

Subzone 3 alpha. Zone 4, Sulrzones 4 beta and

4 alpha and probably the base of Zone 5 could

be traccd at Longing Gap, whcreas on Byers

Peninsula only Subzone 4 bera assemblages are

well cstablished.

The chronostratigraphic calibration of Zone 4

and its subzones as used in the North American

radiolarian zonation (Pessagno ci al. 1993) is

reviscd herein. The base of Zone 4 is assîgncd to

ihe Kimmeridgian/Tithonian boiindary interval

and ihe base of Subzonc 4 alpha is located within

the early Tithonian.

The North American radiolarian zones can be

correlated with the unitary associadon zonadon

(Baumganner et ai 1995a). Uppermosr Zone 3>

Subzone 3 alpha correlates with UAZ 10 and the

base of Zone 4 agrées with LIAZ 11 in Antarc¬

tica. Higher up in ihe .scquences no corrélation

with the UAZ 95 is possible owing ro increasing

biogeographical différences. Evidence from ihe

Southern Alps suggests that Valltipm hopsoni

ranges iip co at least UAZ 12.

The itïterval zonation u.sed by Pessagno et ai

(1993) ha» rhe adrantages lo be applicable to tro¬

pical as well as high latitude sertings and lo rely

on only a few âge diagnostic radiolarians,

However, rhe absence of market taxa bas lo be

carefully proved, in order ro overcomc prcsemi-

tional, paleoceanograplfic and stochastic biascs.

With the chronostratigraphic correcdons in this

paper and thosc of Baumgartner et al. (1995a),

wc hope that the Nojth American zunadon can

now bc applicd everwhere wirhout contradic¬

tions. A major task for the future will he the défi¬

nition of the Zone 4-Zone 5 boundary with the

aid ofhigh latitude radiolarians.

GEODIVERSITAS • 1999 • 21 {4)

709

Kiessling W., Scasso R., Zeiss A., Riccardi A. & Médina F.

Acknowledgements

This study is a coiitribunon to IGCP 381 (South

Atlantic Mesozoic Corrélations). Excellent logis-

tic support in rhe field was provided by the

Instiruto /\nr3rtico Argenrino. Financial lunding

was provided by the Gennan Research

Foundation and the Studicnstiitung des deut-

schen Volkes. We thank Mrs. B. Leipner and

Mrs. C. Sporn for rhe préparation of Silicon casts

and photographs of ammonites.

Spela Gorican and Jean Guex reviewed rhe

manuscript and provided important suggestions

that helped to improve the manuscript conside-

rably. Jean Guex is especially tlianked for his help

CO defmc the UAZ of the radiolarian assemblages

more accurately.

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Submitted for publication on 24 Eebmary 1998;

accepted on 24 June 1998.

GEODIVERSITAS • 1999 • 21 (4)

713

Preliminary radiolarian biostratigraphy across

the Jurassic-Cretaceous boundary

from northwestern Turkey

Figen A. MEKIK

Department of Geology and Environmental Geosciences,

Northern Illinois University, DeKalb, Illinois 60115 (USA)

figen@geol.niu.edu

Hsin Yi LING

Department of Geology and Environmental Geosciences,

Northern Illinois University. DeKalb, Illinois 60115 (USA)

jlingl @ gateway.com

Sevinç ÔZKAN-ALTINER

Marine Micropaleontology Research Unit, Department of Geological Engineering,

Middie East Technical University, 06531 Ankara (Turkey)

altiner@rorqual.cc.metu.edu.tr

Demir ALTINER

Marine Micropaleontology Research Unit, Department of Geological Engineering,

Middie East Technical University, 06531 Ankara (Turkey)

demir@rorqual.cc.metu.edu.tr

Mekik F. A.. LIng H. Y.. Ôzkan-Altiner S. & AHiner D. 1999. — Preliminary radiolarian bio¬

stratigraphy across the Jurassic-Cretaceous boundary from northwestern Turkey. in De

Wever P. & Caulet J.-P. (eds), InterRad VIII, Paris/Bierville 8-13 septembre 1997,

Geodiversiias2A (4) : 715-738.

ABSTRACT

rhis is the first study from Turkey where radiolarians from calcareous

sequences of che Sakarya Continent are tesred in the délinéation of the

Jurassic'Creraceous boundary. The Sakarj'a Continent, which comprises rhe

Southern parc of northwest Turkey, was a Jurassic-Early Cretaceous carbona¬

te platform micro-continent distant from terrcstrial sedirnem influx. Jt was a

site of pelagic carbonate déposition wiih abundant calcareous and siliccous

microfossil input. Among 44 mcasured stratigraphie sections of die jurassic-

Lower Cretaceous deposits of rhe Sakarya Conrinent, four continuous sec¬

tions (MK, KEL, AÇ, ÇD) which encompass the Tithonian-Berriasian

boundar)' were selected for study. However, due to poor préservation and

calcification of radiolarian faunas» only seaion KEL produced rich and well-

preserved radiolarians. This section is 600 meters in thickness and spans rhe

upper Tithonian-lower Berriasian interval. In addition to radiolarians, sec-

KEYWORDS

Radiolarians,

Jurassic-Cretaceous boundary,

northwest Turkey,

calpionellids,

calcareous nannofossils.

GEODIVERSITAS • 1999 • 21 (4)

715

Mekik F. A., Ling H. Y., Ôzkan-Altiner S. & Altiner D.

tion KEL contains abundanr calpionellids, calcareous nannofossils, bcnthic

foraminifera and calcareous algae. The upper part of this stratigraphie section

is made up of rhe Sogukçam Limestone which lithologically resembles the

Bianconc and Maiulica ^ormarions in the Umbria-Marche Région ol Iialy.

The besü préservation and richest radiolarian faunas were observed from the

Sogukçam Limestone in section KEL. This is significanc becatise niany radio-

larian studies as well as studies on magneiostratigraphy, calcareous nannofos¬

sils and calpionellid biostratigraphy in the l ethyan realm hâve been carried

out on the Biancone and Maiolica formations. The rapid sédimentation rate,

pelagic microfacies and well prc.served non-calcified radiolarian faunas make

section KEL idéal for the invesrigarion of the Jurassic-Cretaceous boundary

with radiolarians. The corrélation betsveen radiolarian faunas and co-occur-

ring calpionellids and calcareous nannofossils in section KEL can be compa-

red with sîmilar biostratigtaphic studies from the Bianconc and Maiolica

formations in Italy. The calcareous nannofossils ïn section KEL somerimes

attain rock forniing abundance, and rhe first appearancc of nannoconids as

well as their First abundance peak arc rccognizcd in this section. Throughout

the présent study, the boundary bccwecii Calpionellid standard zones A and

B is considered as the Tichonian-Berriasian boundary. l*he close sampling

interval, 15-20 meters. provides excellent resolution in documenting the First

occurrences of numerous Cretaceous radiolarian species. l'hese First occur¬

rence datum points for radiolarian taxa are nor concurrent. Due to the leFi-

ned résolution oF dating, a stepwise appearance of Cretaceous radiolarian

Faunas in section KEL is clearly obser\^ed; however, radiolarians do not deli-

neate the Jurassic-Crctaceous boundary because a marked synchronous Fau-

nal turnover docs not exist.

RÉSUMÉ

Étude biostratigraphique préliminaire des radiolaires à travers la limite juras¬

sique-crétacé du nord-ouest de la Turquie.

Cette étude est la première de Turquie où les radiolaires ont été analysés

pour décrire la limite jurassique-crétacé dans des séquences calcaires du

continent de Sakarya localisé dans la partie sud de la Turquie nord-occiden¬

tale. Le continent de Sakaiya. a été une plate-forme isolée dans le jurassique

et Crétacé inférieur et un lieu de depot des carbonates pélagiques contenant

des microFossiles calcairCvS et siliceux abondants. Parmi les 44 coupes strati-

graphiques qui ont été mesurées dans les dépôts jurassiques et crétacés du

contineni de Sakarya. quatre coupes (MK. KEL, AÇ. ÇD) traversant la limi¬

te tithonique-berriasien ont été choisies pour cette étude, Néanmoins, à

cause de la mauvaise présersation cr de la calciFicarion de l.i faune de radio¬

laires, seule la œupe KEL a produit des radiolaires bien préservés et abon¬

dants. L’épaisseur de cette coupe est de 6Ü0 mètres pour Fintervallc du

Tithonien supérieur-Berriasien inférieur. En plus des radiolaires, la coupe

KEL contient en abondance des calpionelles, des nannofossilcs calcaires, des

foraminiferes bcnchiquc.s et des algues calcaires. La partie supérieure de cette

coupe est représentée par le Calcaire de Sogukçam qui ressemble par sa litho¬

logie aux formations de Biancone et Maiolica dans la région d'Ombrie-

Marche, en Italie. La faune de radiolaires la plus riche et la mieux préservée a

été retrouvée dans le Calcaire de Sogukçam de la coupe KEL. Cette observa¬

tion est importante parce que plusieurs études sur les radiolaires comme sur

716

GEODIVÊRSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

MOTS CLÉS

Radiolaires,

limite jurassique-crétacé,

Turquie du nord-ouest,

calpionelles,

naniiofossilcs calcaires.

la magnétostratigraphie et la biostratigraphie des nannofossiles calcaires et cal-

pionelles, dans le domaine de la féthys, onr été efïcctiiccs sur les Formations

de Biancone et Maiolica, Le taux de sédimentation élevé, le microfaciès péla-

gique cr la Faune de radiolaires non-calcifiée et bien préservée rendent la coupe

de KE,L idéale pour décrire la limite jurassique-crétacé avec les radiolaires. La

corrélation entre la faune de radiolaires et la présence conjointe de calpionelles

et de nannofossiles calcaires dans le meme matériel en Turquie peut erre com¬

parée avec les études biostratigraphiques similaîres des formations de

Biancone cr Maiolica. Les nannofo.ssiles calcaires dans la coupe deviennent

parfois le constituant majeur de la roche et la première apparition des nanno-

conides ainsi que leur première acme y ont été reconnues. La limite entre les

zone.s standards de.s calpionelle.s A et B est considétee comme la limite du

Tithonien et Bérriasien dans cette étude. L échantillonnage serré de 15-

20 mètres a fourni une résolution parfaite pour dotumenier la première appa¬

rition de plusieurs espèces de radiolaires. Ces pmmières apparitions ne sont

pas simultanées. Grâce à la résolution fine des dacafions par cchanrillonnagc

serré, rapparirion graduelle de la faune de.s radiolaires crétacés a été nettement

observée dans la coupe KEL ; néanmoins, les radiolaires ne décrivent pas la

limite jurassiquc-crctacc puisqu’un changement synchronisé important

n’existe pas dans la faune de radiolaires.

INTRODUCTION

Radiolarians are diverse and abiindant in Upper

Jurassic-Lower Cretaceous sequences across the

World. They hâve been studied intensively in the

past thirry years from North America (Pessagno

&c Blome 1982, 1990; Pessagno et uL 1984; Yang

& Pessagno 1989; Hull 1995, 1997). Europe

and rhe Middle East (Baumgartner ôc Bernoulli

1976; Baumgartner 1980, 1984, 1987; Steiger

1992; Jud 1994; O'Dogherry 1994;

Baumgartner /?/. 1995a; Kicssling 1995, 1996;

Dumirrica et al. 1997), Japan (Nakaseko &

Nishimura 1981; Aita ^ Okada 1986; Maesuoka

& Yao 1986; Aita 1987; Marsiioka 1995a, b, c;

Yang & Matsuoka 1997) and Southern high lati¬

tudes (Baumgartner 1992, 1993; Kiessling &

Scasso 1996).

The main purpose of chis study is to compare

radiolarîan biostrarigraphy with bîozonations of

calpioncllids, calcareous nannofossils and other

calcareous microfossils (e.g. algae and benthic

foraminifera) across the Jurassic-Cretaceous

boLindary on samplcs from northwest Turkey,

near Ankara. Out objectives are: (!) reporting

rhe radiolarian assemblage Irom this boundary

for ihe firsi cime from Turkey; (2) investigaiing

the chronostratigraphic ranges of our radiolarian

faunas; (3) correlating our radiolarian biostrati-

gxaphy with that of co-occurring calcareous

microfossils.

The study area is located in rhe Southern part of

northwest Turkey near the towns of Kozluca,

Kabalar and Akia»! (Fig. 1) which lie northwest

of’furke/s capital, Ankara. Alcincr et al. (1991)

studied ihc straiigraphy and paleogcographic

évolution of this région whcrc the Llppcr

Jurassic-Lower Cretaceous successions occupy

approximarely 120.000 square kilometers.

Altiner et al (1991) rneasured 44 stratigraphie

sections from these successions in which four

sections were reported ro contain radiolarians,

These four sections arc AÇ (by Akta^), KEL (by

Kozluca), MK (by Kabalar) and ÇD (by The

Ismet Pa§a railway station) (Fig. 1). Among these

four sections, only section KEL produced well

GEODIVERStTAS • 1999 • 21 (4)

717

Mekik F. A., Ling H. Y., Ozkan-Altiner S. & Altiner D.

Fig. 1. — Géographie map of sîudy area {modified after Altiner étal. 1991) illustrating locations of radiolarian bearing stratigraphie

sections (AÇ, ÇD. KEL, MEK).

preserved radiolarians. le is also the thickest of

these four ÿiictions (600 m for the iipper

Tithonian and Berriasian interval) and provides

superior résolution for marking the Jurassic-

Cretaccous boundary duc to ics high to very high

sédimentation rate.

Within a tectono-stratigraphic fraraework, the

Southern part of norihwcstcrn Turkey contains

the deposits of a Mesozoie micro-continent, the

Sakarya C'ontintMit (Fig. 2). The Sakarya

Continent was a Jurassic-Cretaceous carbonate

platform micro-contincnc iimidsi the branche.s of

the Neo-Tcthys (îjengor &: Yilmaz 1981). Dtiring

the Tithonian-Bcrriasian interval, the Sakarya

Continent was distant Irom terresttiaJ scdiment

influx and henue a site ol carbonate déposition.

This micro-coniincnt rifred away from

Gondwanalaiid in the Jurassic and moved north-

ward CO eventually colhdc wiih Eurasia

(Rhodope-Pontide Fragment in Fig. 2) by the

end of the Lare Creraceous (^engôr 6c Yilmaz

1981). Today, the Sakarya Continent is a part of

Turkey and bound to the Rhodope-Pontide

Fragment in the north by the Invra-Poncide

Suture and to tlie Tauride and Kirçehir Blocks in

the South by the l/mir-Aakara Suture (Fig. 2).

These sutures are ophiolilc belts remaining Irom

the closure of the branches of Neo-Tethys.

LITHOLOGY

Section KEL (600 meters in rhickness) contains

the Tithonian-Berriasian pelagic limestone depo-

.sits ol the Sakarya Continent. The rhickness of

the scctioti, its pclagic microfacics and rich

micfolos.sil content of radiolarians, calpionellids,

calcareoiui nannofbssils, benthic loraminifera and

calcarenus algac, make ît Idéal for the examina-

rion of the Jurassic-Cretaccous boundary.

Calcareous nannofossils in tins section occasio-

fuilly attain rock-forming abundance. Located at

Koziuca, northwest ol Beypazari, section KEL

consists ol the Yo.sunlukbayiri Formation in its

lowcr portion (samplcs 24-36) and the

Sügiikçam Limestone in its iipper part

(sample.s 2-23) (Altiner cr^/. 1991) (Fig. 3).

The Yosunlukbayiri Formation is a thick caldrur-

biditic sequence. The upper pan of this forma¬

tion, outeropping in section KEL, Ls composed

ol fine detxitic limextones containing six distinct

olistostrome levels. The uppermost detritic

limestone beds contain Zoophycus as wclt as

abundant calpionellids and calcareous namiofos-

sils (Altiner et///. l99l;Ôzkan 1993a. b).

The Yosunlukbayiri Formation is graciually over-

lain by the porcelaneous rnicrites ol the So^kçam

Limestone in the area. The lower part of the

718

GEODfVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

Fig. 2. — Map of Turkey illustrating lectono-stratigraphic units (modified after §engôr 1984). SC. Sakarya Continent; RPF, Rhodope-

Pontide Fragment: TB, Tauride Block; KB. KIrçehir Block; EAAC. East Anatolian Accretionary Complex; AP. Arabian Plate.

So^kçam LLmesionc (KEL 2-24) is characterized

by thin, medium or chickly bedded, somcrimes

silicified, whire ro cream micritic limesrones bea-

ring chert nodules and intercalaced with fine tur-

bidite layers (Altiner et (iL 1991). The So^ikçam

Limesrone lithologically resembles the Bianconc

and Maiolica formations in the Umbria-Marchc

Région in Italy (Farinacct et al. 19813, b; Altiner

et al. 1991). The Bianconc and Maiolica forma¬

tions hâve been extensively stndied for calpioncl-

lids, calcareous nannofossils and magneto-

stratigraphy (e.g. Lowrie & Channcll 1983; trba

& Quadria 1987; Channcll et ai 1987, 1993) as

vvell as for radiolarian.s (e.g. Baumgartncr 1984;

Jud 1994; Ü’Dogherty 1994). The strong litholo¬

gie similarity between the Sogukçam Limcstonc

and the Maiolica and Bianconc formations is due

to rheir déposition in the .same océan, during the

samc tinte interval, and under similar conditions

as submerged carbonate platforms disrant front

terrestrial sédiment influx (sec Altiner et ai 1991).

For this reason the radiolarian biostratigraphy we

présent hefc and its corrélation to calpionellid and

calcareous nannofossil biozonations previously

establishcd for the same .section (K£l.) Ls signifi-

canr as a corrélative example from Turkey to the

previous studies in Italy.

THE JURASSIC-CRETACEOUS

BOUNDARY

The Jurassic-Cretaceous boundary is one of the

most problematic System boundarics because the

‘l'ithonian doe.s noi hâve a stratotype, the lowcr

parts ol the Berriasian tend to lack lossils Jn

many parts of Western Europe, and ihe bounda¬

ry does not correspond to any major faunal or

floral turnover (Hoedcmackcr 1987; Oloriz &

Tavera 1989; Romane 1991; Pessagno et al,

1997). Ammonites (Kemper et al. 1981;

Hoedemaeker 1991), Buchia (Zakhanov 1987;

Pessagno et a.L. 1987a, b; Hoedcmackcr 1991;

Pessagno et at. 1993), calpioncllid.s (Le Hcgarat

ôc Remanc 1968; Allemann et ni 19'7|; Rcmane

1964, 1983, 1986; Remane et al. 1986; Cecca et

al. 1989) and calcareous nannofossil.s (Thiersteiti

1975; Coopet 1985; Bralower 1990; Bown &

Ùzkan 1992; Ozloui 1993a. b) hâve been utiü-

zed in biostratigraphically maridng rhis bounda¬

ry. Ammonites, which are tradicionally

considered che basis ol .standard and high resolu¬

tion biostratigraphy, bccome strongly provinciali-

zed during the Tithonian-Berriasian interval,

This provincialism créâtes problems in corréla¬

tion between the Tethyan and Boréal realms

GEOOIVERSITAS • 1999 • 21 (4)

719

Mekik F. A., Ling H. Y., Ôzkan-Altiner S. & Akiner D.

KEL Section

ZONATION

"ce

_a3

Lithology

Fossils

CO CO

•O ^

s N

0)0 T-

geesg

CO c

O S

b O)

ü<‘*"

CO .

3 '

I Ü)

^ O CO ^

^ O -SS

O c.^ s

O g

CÛ

>05

20 -t

U 0

@ ^

25 4

C/3

^ U

uSXSTjf^

V U

120

■90

•60

■30

0 m

.CO

: CO

•i CD

CO c

CO (0

CD 5S:

O O

J O

: O

.CO

' CO

-c

.CÜ.

CO c

3 C

C CD

O C

^ P

O-E

g-S

à CO

CD '

.CD

CO ,

e:c:

.otj

Slope breccia or olistostrome I ItI I Siliceous limestone

l: ‘ :i;i: l Fine detritic limestone (calciturbidite) h~ i ~ ' i Porcelaneous limestone

0 Trocholina U Calpionellidae ^ Sponge spiculé ^ Belemnite V” Saccocoma

U Chitinoidella ^ Radiolaria ® Ammonite Aplycus Zoophycus

Fig. 3. — Calpionellid, calcareous nannofossil, and benthic foraminifera and algae biozonations on stratigraphie section KEL. Rich

radiolarian assemblages were recovered from the numbered samples in the figure.

720

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

(Jelecsky 1984; Zeiss 1984, 1986; Remane 1991;

Pessagno et al. 1997). According to Pessagno et

al. (1997) calpionelÜds arc diachronous with

longer ranging zones in North America rhan in

Europe. However. .since Turkey is located in

Eurasia, and since calpionellid biozones are well

established in Europe (Allenunn et al. 1971;

Trejo 1980; Remane êt al. 1986; Altincr ôe

Ôzl^n 1991; Pop 1994a,b: 1996; Grün & Blau

1997), calpionellid zones arc used to mark the

boundary in ihis study.

Le Hegarat & Remane (1968) placed the

Jurassic-Cretaceous boundary wirhin Calpionel¬

lid standard zone R in the stratotype ot the

Berriasian. For ihis reason, Altincr & Ozkan

(1991) also placed the boundary in zone B in

section KEL HoweVer, since the boundary bet-

ween Calpionellid standard zones A and B also

corresponds to the boundary between the

Duraa^ites and Euxinus ammonite zones, the

Jurassic-Cretaccous boundary svas accepted as

the limit between Calpionellid standard zones A

and B at the Colloque (Anonymous 1975), and

by Cecca et al, (1989). Other rc.searchers

(Jeletsky 1984; Channell ôz Grandesso 1987;

Ôzkan 1993b; Grün & Blau 1997) consider chc

limit between Calpionellid standard zones A and

B as the Jurassic-Cretaccous boundary as well.

On the other hand, Tavera et ai (1994) stated

thar the boundary berween Durangites dtwà Jacobi

ammonite zones dnes not correspond to the limit

between Calpionellid standard zones A and B in

the Vocontian Région (sec also Oloriz & Tavera

1989) but rather to a levcl within Calpionellid

standard zone A We also consider the Jurassic-

Crctaceou.s boundary to correspond to the limit

between Calpionellid standard zones A and B in

section KT.l. based on the consensus reached at

the Colloque (1975) and many subséquent

publications accepting ihis limit as the Jurassic-

Cretaceous boundary. Therefore, the limit ber¬

ween Calpionellid standard zones A and B in

section KEL falls between samples 20 and 21

(Fig. 3).

The development oF a magnetic polarity urne

scale for the Jurassic-Cretaceous boundary (Ogg

& Lowrie 1986; Ogg et al. 1991) and the corré¬

lation of chis time scale with biozonations of cal-

careous nannofossils (Bralower et al. 1989),

calpionellids (Channel Grandesso 1987) and

radiolarians (Jud 1994) are important advances

in the multidisciplinary délinéation oF rhis boun¬

dary. According co Ogg (1992) the boundary is

defined as the base of the reverse polarity chron

M I8R and Bralower et al. (1989) correJate the

base of M 18R with the boundary between

Calpionellid standard zones A and B.

The following is a brief discussion on compari-

son of radiolarian biozonations across the

Jurassic-Cretaceous boundary from North

America (Pessagno 1977a; Pessagno étal. 1987a;

Pessagno & Blomc 1990; Pessagno et al 1993;

Huil 1997), Europe (Baumgartncr 1980, 1984,

1987; Steiger 1992; Jud 1994; Baumgartner et

al. 1995b: Dumitrica et al. 1997) and Japaa

(Maesuoka & Yao 1986; Aica 1987; Matsuoka

1995a. b, d; Yang & Matsuoka 1997) which

illustrâtes problems of provincialism and dia*

chroneity among radiolarians;

North America, Originally the top of zone 4 was

defined as the Jurassic-Cretaceous boundary

(Pessagno 1977a; Pessagno et ai 1984, 1987b,

1993; Pessagno ôc Mizutani 1992). Rccently the

uppermo.st part of .subzone 4a hus been revised

and is considered to bclong to the Lower

Cretaccous (Berriasian). This boundary within

subzone 4a coïncides with the tops of the

Durangites (ammonite) and the Buchia fitochü

zones (bivalve) (Pes.sagno et ai 1997). Ir should

be nored here that originally Pessagno (1977a)

and subseqtiently Pessagno et al. (1984, 1987b,

1993) considered the la.st occurrence.s of RistoLi

altisshna and Ristola prneera (priniary marker

taxa) for defining rhe top of zone 4 (and

subzone 4a). Parvicingula colemani bccomcs

exrincr slighrly bclow thîs level. The datum

where Parvicingula colemani becomes extinct falls

within the Pseudodictyomirra carpatica zone of

Japan (Yang & Matsuoka 1997).

Europe. Baumgartncr et al. (1995b) utiJize uni-

tary associations among radiolarian taxa to

construct radiolarian biozones (UAZ 95). Each

biozone is defined by a group of radiolarian taxa

that only co-occur in that zone. When UAZ 95

is compared with North American zones

(Pessagno et al. 1993), diaclironism between the

zones is évident. Discrepancies between fîrst

appearance data of some taxa berween Europe

GEODIVERSITAS • 1999 • 21 (4)

721

Mekik F. A., Ling H. Y., Ôzkan-Altiner S. & Altiner D.

Fig. 4. — Chronoslratigraphic dlslnbution of radiolarian fauna in section KEL. Symbols on stratigraphie section are the same as in

Fig. 3.

and North America as wcll as radiolarian provin-

cialism during the Late Jurassic-Early Cretaceous

interval hamper the corrélation of radiolarian

biozones beeween North America and Europe;

howeven in somc récent studies rhis corrélation is

becoming incrcasingly doser (Hull 1997).

Japan. The evolutionary Hrst ap[)earance of

Psetidodïcvyomitra carpatica from Loopus prirniü-

vus (= Pmidodictyomitra primnivui) defines the

boundary between the Loopus primliitnis and

Pseudodictyomiîi'a carpatica zones. This boundar}'

is in the latest Tithonian and ir is approximately

one million year older than the Jurassic-

Cretaceous boundary in both Japanese Island

sections and in the western Pacific deep océan

basin (Matsuoka 1995a, b; Yang & Matsuoka

1997).

RESULTS AND DISCUSSION

Section KEL was previoiisly studied for its cal-

pionellids (Altiner Ôz Ôzkan 1991), calcareous

nannofossils (Ôzkan 1993a, b) and bcnthic fora-

nünilera and calcareous algae (Altiner 1991). In

the présent study, we compare these previously

cstabÜshed zonation.s for die same section with

our radiolarian biosrratigraphy. Section KEL was

reported to contain abondant radiolarians in 28

of 40 samples from rhin section examinations

722

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

(Ozkan 1993a). Howevcr, well-preserved and

rich radiolanan faunas could only be obtained

from thc uppcr part of the section that corres¬

ponds to thc So^ukçam Limestonc in section

KEL. In thc lower part of the section radiolarian

préservation is poor and hence recovery is very

low. Radiolarians are recovered from sampics in

section KEL assit^ned to Calpionellid standard

zones A2 (KEL 25-26), A3 (KEL 20-24), B

(KEL 19-5) and C (above KEL 4) (Altiner

Ozkan 1991) (Fig. 3). Altiner Ozkaii (1991)

aiso report ihe présence ol Duvalia tithonica

(belemnite) in subzone A2 whosc range is known

to be from late Tithonjan to carly Berriasian

(Ehxihhs zone). We wilt flrsr discuss calcareous

microfossil blostratigraphy for section KEL.

Biostratigraphv of co-occurring

CALCAR£OU.S MICROFOSSILS

The Jurassic-Cretaccous boundary is considered

as the boundary between Calpionellid standard

zones A and B which corresponds to the location

between samples 20 and 21 in section KEL

(Fig. 3). This boundary falls within the upper

pan of the Aikrostaurtis chinuius calcareous nan-

nofossil zone in section KEL and it Ls impossible

to delineate with Altiner s (1991) foraminiferal

and algal zonation where his Protopeneroplis iro-

changiilata zone (zone III) transgresses the boun¬

dary (Fig. 3).

1L\DI0LAK1AN BlOSTRATlGRAmV

Due to thc poor préservation of radiolarians in

the fine detritic Umestones ol die Yosunlukbayiri

Formation, the initial occurrencevS of the majori-

ly of Cretaceous radiolarians in section KEL

begin near thc base of thc So^ikçam Llmestone.

In section KEL, the first appearance of nannoco-

nids as a group is observed in sample KEL 21

(Fig. 4) from which well-preserved radiolarians

could not be extracred. The Jurassic-Cretaceous

boundary corresponds lo the firsr occurrences of

Dicerosatunialis dicranacamhou Dcinatus diarn-

phidius^ Pyramispongia harmsteinemiu Acaeniotyk

diaphorogontiy Archneodictyomitra apiariumy

Thanarla sp., Htilesium (^) sp., Emihiina pessa-

gnoi and Alievitim nndidosuvi in this section.

Also, thc first occurrences ol Sàitoum sp.,

Angulobracchia portnianni s.L, Acanthocircus mul-

tidentatiiSy Becus triiingulocentrum, Triactomn

tithonianum and Tethysetta colvmna correspond

to rhe First peak in nannoconid abundancc as

defined by Ozkan (1993a, b) (Fig. 4) in section

KEL. As a general pattern, thc initial occurrences

of Cretaceous radiolarians throxighour the sec¬

tion arc not abrupt, but stepwisc, emphasizing

that a major radiolarian faunal turnover does not

exLst across thc Jurassic-Cretaceous boundary in

northwest Turkey..

The chronostratigraphic distribution of radiola¬

rian taxa within section KEL (Fig. 3) does not

compiy with any of the established radiolarian

zonations in North America or Japan. This is

due to rhe lack of biostradgraphically index spe-

cies sucK as Psrudodictyômirra aupatica^ RistoU

procera or Pankcinpila calernani in our samples.

The taxa we describe herein (e.g. Mieinum regu-

lare^ Dicerosatutnalh dicranacanthoSy Mirifusus

diauat’y Tethysetta boesUy Deviatîn diamphidiuSy

Pantanellmm berriasianuni, Hsunm rarkosmum)

enables us to correlate section KEL with Jud's

(1994) biozone D2 and UAZ 95 zones 13 and

14 (Baumgartner er/z/. 1995a).

SYSTEMATIC MICROPALEONTOLOGY

The supra-generic classification for radiolarians is

based on, for the most part, Dumitrica’s (1995)

classification. The synonymy lists contain only a

few représentative studies.

Subclass RADIOLARIA Muller, 1858

Order POLYCYSTINA Ehrenberg, 1838

enietid, Riedel, 1967

Suborder NASSELLARIA Ehrenberg, 1875

Family ARCitAFOÜICrYOMITRIDAB

Pessagno. 1976

Genus Archaeodictyomitm Pessagno, 1976

Archaeodictyomitra apiarium (Rüst, 1885)

(Fig. 5B)

Lithocampe aptarium Rüst, 1885 {fide ]\xày 1994):

314, pi. 39(l4),fig. 8.

GEODIVERSITAS • 1999 • 21(4)

723

Mekik F. A., Ling H. Y., Ôzkan-Altiner S. & Altiner D.

Fig. 5. — A. Hsuum raricostatum Jud (KEL 18): B. Archaeodictyornitra apiarium Koctier (KEL 7); C, Archaeodictyomitra sp. cf.

A. minoensis (Mizutani) (KEL 7); D. Thanaiiasp. (KEL 16); E, Stichocapsa sp. aff. S. altiforamina Tumanàa (KEL 4); F, SviniUium

depressum (Baumgartner) (KEL 20); G. Tethysetta sp- cf T boesii (Parona) (KEL 18); H. Teihysetta columna (Rüst) (KEL 16);

I. Mirifusus dianae (Karrer) (KEL 17): J. Ristola alUsstma altissima (Rüst) (KEL 18), K, Tethysetta ovoldala Dumitrica (KEL 11);

L, Loopusyangi Dumitrica (KEL 25). Scale bar: A, 55 pm; B, E, K, 45 pm; C, H, 65 pm; D. G, 40 pm; F, 50 pm; I, 120 pm; J, 75 pm;

L, 70 pm.

724

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

Archaeodictyomitra apiara- Pessagno 1977a; 41, pl. 6,

figs 6, 14. — Bnumgartnet 1984: 758, pl. 2 figs 5-6.

Archdeodict\mnitrn üpiarium—K.oc\\cr 1981 {fide]uà^

1994): 56; pl. 12, fig. 13. - Jud 1994: 62, pl. 3,

figs 10, 11. - Baumgarincr et al. 19ÿ5a: 98, pl. 3263,

figs l-7(H). — Dumicrica et uL, 1997: 38. pl. 7, fig. 7.

Occurrence. — Samples KEL 5-20; from Jurassic-

Cretaceous boundary to boundary between

Calpionellid standard zones B and C.

Archaeodictyomitra sp.

cf. A. tnitioeasis {MïzuVdni, 1981)

(Fig. 5C)

Occurrence. — Sainples KEL 5-7; from upper por¬

tion of Calpionellid standard zone B to boundary bet¬

ween zones B and C.

Genus Thanarla Pessagno, 1977b

Thanarla sp.

(Fig. 5D)

Occurrence. — Samples lŒL 7-20; from Jurassic-

Cretaceous boundary to upper part of Calpionellid

standard zone B.

Family HSUUIDAE Pessagno & Whalcn, 1982

Genus Hstium Pessagno, 1977a

emend. Talcemura, 1986

Hsuum raricostatum\\\à^ 1994

(Fig. 5A)

Hsmim raricostatum Jud, 1994: 81, pl. 12, figs 3-5. -

Baumgartner et al. 1995a: 286, pl. 3591, figs 1-3. -

Dumitrica et ai 1997: 46, pl. 10, fig. 1.

Occurrence. — Sample KEL 18; in Calpionellid

standard zone B.

Family ParviCINGUI.IDAE Pessagno, 1977a

Genus M/r/yî/^wj Pessagno, 1977a

Mirifiisus dianae (Karrer, 1867)

(Fig. 51)

Lagena dianae Karrer, 1867 (fide ]\xà, 1994): 365,

pl. 5, figs 8a. b.

Mirifiisus duinae - Dumirrica & De Wever 1991:

553-557, Egs 1, 2a, b. - Dumitrica et al. 1997: 52,

pl. 11, fig. 8.

Mirifiisus dianae minor — Baumgartner 1984: 772,

pl. 5, figs 11, 14. — Jud 1994: 84, pl. 13, fig. 2. —

Baumgartner ///. 1995a: 314, pl. 3286, figs 1-5.

Occurrence. — Sample KEL 17: in Calpionellid

standard zone B.

Genus Ristola Pessagno & Whalen, 1982

emend. Baumgartner, 1984

Ristola altissima altissima

(Rûst, 1885)

(Fig- 5J)

Lithocampe altissima Rüsr, 1885 (ftde Pessagno,

1977a): 315 (45), pl. 40» fig. 2.

Parvicingula altissima - emend, Pessagno 1977a: 85>

pl. 8, figs 9-10.

Ristola altissima (Rüst) - Baumgarincr 1984: 783,

pl. 8, fig. 3, non figs 4, 9. - Dumitrica et al. I997i 52,

pl. 11.% 5,?7.

Ristola ahisstma altissima — ]\a6. 1994: 101, pl. 19,

fig. l. - Baumgarrncr et al. 1995a: 472, pl. 3241,

figs 1-5(H).

Occurrence. — Sample KEL 18; in Calpionellid

standard zone B.

Genus Svinitzîum Dumitrica, 1997

Svinitzium depressum

(Baumgartner. 1984)

(Fig. 5F)

Pseudodictyornttra depressum Baumgartner, 1984: 782,

pl. 8, figs 2» 7, 8, ]].

Wran%ellium depresmm - Baumgartner et al. 1995a:

632, pl 3284, figs 1 -5.

Svinitzium depressum — Dumitrica et al. 1 997: 53,

pl. 11, figs 11, 17.

Occurrence. — Samplc.s KEL 7-23; from

Calpionellid standard zone À subzone 3 to zone B.

Genus Dumitrica, 1997

Tethysetta sp. cf. T. boesii

(Parona, 1890)

(Fig. 5G)

Occurrence. — Sample KEL 18; in Calpionellid

standard zone B.

GEODIVERSITAS • 1999 • 21 (4)

725

Mekik F. A., Ling H. Y., Ozkan-Altiner S. & Altiner D.

Remarks

The broken nature of che specimen makes a positive

assignment of the présent spccies to 7*. hoesii diffîculr.

Family SethocapsiuAE Haeckel 1881

Genus Gongy/othorax Foreimn, 1968

emend. Dumurica, 1970

Tethysetta columna (Rüst, 1898)

(Fig. 5H)

Gongylothorax sp.

(Fig.6E) '

Lithocampe columna Rüst, 1898: 63. pl- 18, fig. 5.

ParvicinguLi columna -Jud 1994: 116, pi. 23, fig. 17.

Tethysetta columna - Dumitrica et ai. 1997: 49, pl. 11,

figs 13-15.

Occurrence. — Sample KEL 16, in Calpionellid

standard zone B.

Remarks

This species ditfers from Wrangellium columna'

rium Jud, 1994 by having threc rows of pores per

chamber.

Tethysetta ovoidala Dumitrica, 1997

(Fig. 5K)

Tethysetta ovoidala - Dumitrica étal. 1997: 50, pl. 50,

figs 21,22.

Occurrence. — Sample KEL 11; in Calpionellid

standard zone B.

Family PSEUDODICTYOMITRIDAE

Pessagno, 1977b

Genus Loopus Yang, 1993

Occurrence. — Sample KEL 25; in Calpionellid

standard zone A subzone 2.

Genus Sethocapsa Haeckel, 1881

Sethocapsa funatoensts hlxiAy 1987

(Fig. 6A)

Sethocapsa funatoensis fS\{Ay 1987; 73^ p]. 2, figs 6a-7b;

pl. 9, figs 14-15- - Baumgartncr et al. 1995: 494,

pl. 3070. figs I-5(H).

Zhnmoideluim funatoensis — Hull 1997: 132, pl. 38,

figs 13, 15.

(Occurrence. — Sample KEL 7; in the upper part of

Calpionellid standard zone R

Sethocapsa leiostraca Foreman, 1973

(Fig. 6D)

Sethocapsa leiostraca Foreman, 1973; 268, pl. 12,

figs 5-6. — Jud 1994: 105, pl. 20, fig. 5. -

Baurngartner étal. 1995a; 498, pl. 3062, figs 1-5(H).

Occurrence. — Sample KEL 14; in Calpionellid

standard zone B

Loopus yangi Dxxmm'icdiy 1997

(Fig. 5L)

Loopusyangi — Dumitrica et al. 1997: 31, pl. 5, figs 8,

Occurrence, — Sample KEL 25, Calpionellid stan¬

dard zone A suhzone 2.

Family Théo PERI UAE Haeckel, 1881

emend. Riedel, 1967 emend. Takemura, 1986

Genus Stichocapsa 1 laeckel, 1881

Stichocapsa sp. cf. S. altiforamina

Tumanda, 1989

(Fig. 5E)

Occurrence. — Sample KEL 4; just below the

boundary between calpionellid zones B and C.

Family Sponcocapsulidae

Pessagno, 1977a

Genus ObesacdpsuU Pessagno, 1977a

Obesacapsula cetia (Foreman, 1973)

(Fig. 6B)

Sethocapsa cetia Foreman, 1973: 267, pl. 12, fig. 1;

pl. 16, fig. 19.

ObesacapsuU cetia — Baumgartncr 1992 : 325, pl. 12,

fig. 1. - Jud 1994: 87, pl. 13, fig. 11. - Baumgartncr

et ai 1995a: 342, pl. 3203, figs 1-4(FI).

Occurrence. — Samples KEL 7-23; from

Calpionellid standard zone A subzone 3 co upper part

of zone B.

Family WïllIRIEDELLIDAE Dumitrica, 1970

Genus Cryptamphorella Dumïmcz, 1970

726

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

Fig. 6. — A. Sefhocapsa funatoensis Aita (KEL 7); B, Obesacapsula cetia (Foreman) (KEL 23). C. Tricolocapsa sp. (KEL 25);

D. Sefhocapsa Jeiostraca Foreman (KEL 14); E. Gongylothorax sp. (KEL 25): F. Cryptamphorella sp. (KEL 25): G. Tricolocapsa

campana Kiessling (KEL 18); H. Zhamoidellum sp. cf. Z ventricosum Dumitrica (KEL 18): I. Deviatus diamphtdius (Foreman)

(KEL 20); J, Deviatus diamphidius (Foreman) (KEL 16); K. Praeconosphaera sphaeroconus (Rüst) (KEL 18); L, Àcaeriiotyle diapho-

rogona Foreman (KEL 16); M, Acaeniotyle diaphorogona Foreman (KEL 16); N, Triactoma tithonianum Rüst (KEL 16). Scale bar: A,

D. 65 pm; B, L, 100 pm; C, E, F, G. 35 pm; H, 40 pm; I, K, 60 pm; J, 75 pm; M, 80 pm; N, 105 pm.

GEODIVERSITAS • 1999 • 21 (4)

727

Mekik F. A., Ling H. Y., Ozkan-AItiner S. & Altiner D.

Cryptamphorella sp.

(Fig- 6F)

Occurrence. — Sample KEL 25; in Calpionellid

standard zone A subzone 2.

Genus Tricolocapsa¥{^ccVc\, 1881

Tricolocapsa campana Kiessling, 1995

(Fig. 6G)

Tricolocapsa campana Kiessling, 1995; 338, figs 7/1-4

Occurrence. — Sample KEL 18; in Calpionellid

standard zone B.

Tricolocapsa sp.

(Fig. 6C)

Occurrence, — Sample KEL 25; Calpionellid stan¬

dard zone A subzone 2.

Tktmxs Zhamoidelhim Dumiirica, 1970

Zhamoidellum sp. cf. Z, ventricosum

Dumitrica, 1970

(Fig. 6H)

Occurrence:. — Samples KEL 14-18; in

Calpionellid .standard zone B.

Family POUEPIDAE-De Wever, 1981

Genus Saitoum Pessagno, 1977b

Saitoum sp.

(Fig. 7K)

Occurrence. — Sample KEL 16-2; from middle of

Calpionellid standard zone B to zone C.

Family Amphip\'NDACIDAH Riedel, 1967

Subamily SyrjngocaPSINAE

Forcman, 1973

Genus Podobursa Wisniowski, 1888

Podobursa sp.

cf. R multispina Jud, 1994

(Fig. 7L)

Occurrence. — Samples KEL 2-18; from

Calpionellid standard zone B to zone C.

Rlmarks

Poor préservation prevents the positive identifi¬

cation of this form as Podobursa multispina.

Podobursa polyacantha (FischÜ, 1916)

(Fig. 7H)

Theosyringtum acanthophorum Rüsr var. polyacanthus

Fischli, 1916 {jfde Baiimgartner et al., 1995a): 47,

fig. 41.

Pniinhuna iJolyaùintlM — Baumgartner et al. 1995a;

424, pl. 3174, figsl-4(H).

Occurrence. — Sample KEL 7; in upper part of

Calpionellid standard zone B.

Suborder SPUMELLARIA Ehrenberg, 1875

Superfamily ActinomMACEA Hacckel, 1862

Family Leugdnidac Yang &: Wang, 1990

entend. Dumitrica. 1995

Genus Acaeniotyle Foretnan, 1973

Acaenîotyle diaphorogona

Foreman, 1973

(Fig. 6L, M)

Acaeniotyle diaphorogona Foreman, 19’^3: 258, pl. 2,

figs 2-5- — Thurow 1988: 396, pi. 9, fig. 8. -

Baumgartner et ai 1995a: 50. pl. 3090. figs 1-6.

Occurrence. — Samples KEL 5-20; from the

Juras.sic-Crctaccous boundary to upper part of

Calpionellid standard zone B.

Genus Praeconosphaera Yang, 1993

Praeconosphaera sphaeroconus

(Rüsu, 1898)

(Fig. 6K)

Conosphaera sphaeroconus Rü.st, 1898: 13, pl. 4, fig. 8.

Praeconosphaera sphaerocoHits - Yang 1993: 105,

pl. 17, figs 2, 6, 12, 16, 23. — Dumitrica et ai 1997:

21, pl. 3. fig. 3.

Occurrence. — Samples KEL 7-23; from

Calpionellid standard zone A subzone 3 to upper part

of zone B.

Family Paneanelliidae Pessagno, 1977a

emend. Pessagno & Blome, 1980

728

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

Fig. 7. — A, Dicerosaturnalis dicranacanthos (Squinabol) (KEL 16); B, Dicerosaturnalis dicranacanthos (Squinabol) (KEL 7):

C, Acanthocircus sp. aff. A. minimus (Squinabol) (KEL 2); D. Acanthocircus muttldentatus (Squinabol) (KEL 7); E. Pantanellium ber-

riasianum Baumgartner (KEL 16); F. Pantanellium sp. (KEL 18); G. Archaeospongoprunum patricki Jud (KEL 20); H. Podobursa

polyacantha (FIschli) (KEL 7); 1, Emiluvia omanensis Kiesslïng (KEL 16); J, Emiluvia pessagnoi Foreman (KEL 20); K, Saitoum sp.

(KEL 5): L. Podobursa sp. cl. P. multispina Jud (KEL 18). Scale bar: A. 70 pm; B, 160 pm; C, 105 pm; D, 95 pm; E, 50 pm; F. H.

60 pm; G, 90 pm; I, L, 80 pm; J. 155 pm; K, 35 pm.

GEOOIVERSITAS • 1999 • 21 (4)

729

Mekik F. A., Ling H. Y., Ôzkan-Altiner S. & Alciner D.

Subtamily PANTy\NFLUlNAE

Pessagno, 1977a

emend. Pessagno ik. Blome, 1980

CtenUN Pantanellium Pessagno, 1977a

emend. Pe^sagno & Blome, 1980

Pantanellium berriasianum

Baumgartner, 1984

(Hg. 7E)

Pantanellium (?) berriasianum Baumgartner, 1984:

776-777, pl. 6, figs 14-15.

Pantanellium berriasianum — Jud 1994: 89, pl. 15,

figs 5-6. - Baumgartner et al. 1995a: 368, pl. 3280,

figs l(H)-2.

Occurrence. — Simples KEL 7-12; txom lower to

upper pan of Calpionellkl standard zone B.

Pantanellium sp.

(Fig. 7F)

Occurrence. — Samples KEL 2-25; from

Calpionellid standard zone À subzone 2 to zone C.

Rkmark-S

Poor preservarion hinders further identification

of this spécimen.

Family XlPHOS TYLlOAE Haeckcl, 1881

emend. Pessagno & Yang,

in Pessagno et al.., 1989

Genus TriactomaK\i?>i, 1885

Triactoma tithonianum Rüst, 1885

(Fig. 6N)

Triactoma tithonianum Rüst, 1885 {fide Baumgartner

étal., 1995a); 289, pl. 28, fig. 5. - Jud 1994: 115,

pl. 23, figs 10-11. — Baumgartner et al. 1995a: 52,

pl3097, figs 1-3 (H)

Occurrence. — Sample KEL 16; in Calpionellid

standard zone B.

Superfamily Pyi.ONIACEA l laeckel, 1881

emend. Dumitrica, 1989

Family OrbicULIFORMIDAE Pe.ssagno, 1973

emend. Dumitrica, 1995

Subfamily Emiluvunah Dumitrica, 1995

Genus Emiluvia Foreman, 1973

Emiluvia omanensis Kiessling, 1995

(Fig. 71)

Emiluvia omanensis Kiessling. 1995: 330, figs 6/5-8. -

Dumitrica et al. 1997: 27, pT. 4, figs 2, 4.

Occurrence. — Samples KEL 7-16; in Calpionellid

standard zone B.

Emiluvia pessagnoi Foreman, 1973

(Hg- 7J)

Emiluvia pessagnoi Foreman, 1973: 262, pl. 8, fi^. 6.

Emiluvia pessagnoi s.l. - Jud 1994; 77, pl. 10, figs 1,

2. - Baumgartner et al. 1995a: 206, pl. 3066, figs 1,

2 .

Occurrence. — Samples KEL 20-21; on Jurassic-

Cretaceous boundary.

Family'F ritrabid.ae Baumgartner, 1980

Genus Deviatus Li, 1986

Deviatus diamphidius (Foreman, 1973)

(Fig- 61, J)

Paronaella (?) diamphidia Foreman, 1973: 262, pl. 8,

figs 3,4.

Foremanella diamphidia ■ Baumgartner 1984: 765,

pl. 6, fig. 18.

Deviatus diamphidius — O'Yio^hexiy 1994: 345,

pl. 64, fig. 14. — Dumitrica et al. 1997: 28, pl. 4,

fig. 3.

Deviatus diamphidius diamphidius — Baumgartner et

al 1995a: 172, pl. 3112 Jigs

Occurrence. — Samples KEL 2-20: from lower part

of Calpionellid standard zone B to zone C.

Genus Baumgajtner, 1980

Tritrabs ewin^ ÿt. (Pessagno, 1971)

(Fig. 8B)

Paronaella (?) ewingi Pessagno, 1971: 47, pl. 19,

figs 2-S.

Tritrabs ewing s.l. — Baumgartner et al. 1995a: 606,

pl. 3l Id^ figs 1-8(H).

Trip a bs ewingi 1994: 116, pl. 23,figsl2-13.

Tritrabs ewsngi — Dumitrica et al. 1997: 27, pl. 4,

fig. 1. -Hu!l 1997: 4, pl. 19, fig. 9, 12.

Occurrence. — Sample.s 2-7; from upper part of

Calpionellid standard zone B to zone C.

730

GEODIVERSITAS • 1999 * 21 (4)

Radiolarians from NW Turkey

Fig. 8. — A, Halesium sexangufum Pessagno sensu Steiger (KEL 7); B, Ttitrabs ewingi gr. (Pessagno) (KEL 18); C, Halesium irre-

gularis Steiger {KEL 16); D, Angulobracchia (?) porvnanni s.l Baumgartner (KEL 16); E. Halesium (?) sp. (KEL 20); F, Paronaella (?)

sp. cf. P. tubufata Steiger (KEL 7); G. Paronaella (?) sp. et. P tubulata Steiger (KEL 7); H. Pyramispongia barmsteinensis (Steiger)

(KEL 20); I, Paronaella (?) tubulata Steiger (KEL 7); J, Becus triangulocentrum Dumitrica (KEL 16); K, Alievium nodulosum

Dumitrica (KEL 20); L, Alievium regulare (Wu & Li) (KEL 18). Scale bar: A, 120 pm; B, 155 pm; C, 85 pm; D, 145 pm; E, 110 pm; F,

90 pm; G, J, 75 pm; H. I, K, L. 65 pm; K. 105 pm.

GEOOIVERSITAS • 1999 • 2l (4)

731

Mekik F. A., Ling H. Y., Ozkan-Altiner S. &c Altiner D.

Superfamily SatURNAI.IACEA

Dcflandre, 1953

Family SaturNAI.IüAK Dcflandre, 1953

SubFamily Saturnalinae Dcflandre, 1953

Genwh Acanthocifeus Squinabol, 1903

Acanthocircus multidentatus

(Squinabol, 1914)

(Fig. 7D)

Satumalis muitifivntatm Squinabol, 1914: 298, pl. 23

[4], figs lu 12,

Acanthocircus rnultidencatus ~ Pessagno 1977b: 32,

pl. 2, figs 15, 20. - O’Dogherty 1994: 255, pl. 44,

figs7'10.

Occurrence. — Samplcs KEL 7-16: from lower to

upper part of Calpioncliid standard zone B.

Acanthocircus sp.

afî. yl. minimus (Squinabol, 1914)

(Fig. 7C)

Occurrence. — Samples KEL 2-23; from

Calpionellid standard zone À subzone 3 to zone C.

Remarks

Our spccimcn ditfers from A. ellipticus

(Squinabol, 1903) and A hispinns (Yao, 1972)

by its smullcr size and narrower ring, h more cio-

sely resemblcs rninhnus (Squinabol, 1914)

although it bas à moie rectangular outline and

flatter ring,

Genus Dicerosaturnalis

Dumitrica & Jud, 1997

Dicerosaturnalis dicranacanthos

(Squinabol, 1914)

(Fig. 7A, B)

SaturnalîS dicranacanthos Squinabol, 1914: 289,

pl. 22, fig,s4-7;pl. 23,fîg. 8.

Acanthocircus dicranacanthos — Ï^OTcmzti 1975: 610,

pl. 2D, figs 5-6. - Hull 1997: 29, pl. 9, fig. 3, 4.

Acanthocircus rrizonalis dicranacanthos - Baumgartner

étal. 1995a: 72, p!. 3087, fig.s 1-8(H).

Dicerosaturnalis dicranacanthos — Dumitrica et al.

1997: 18, pl. Uflg. 15.

Occurrence. — Sample KEL 2-21; from Jurassic-

Crctaceous boundary to Calpionellid standard

zone C.

Superlamily SponGODISCACEA

Haeckel, 1862

Family CAVA.SPONGIDAE Pessagno, 1973

Qcnxxs Pyretmispongia Pessagno, 1973

Pyramispongùt barrnsteinensis

(Steiger, 1992)

(Fig. 8H)

Nodotetraedra bartnsteiuensis Steiger, 1992: 33, pl. 4,

figs 9-14.

Pyramispongia barrnsteinensis — Baumgartner et al.

1995a: 464, pl. 6109, figs 1-4. - Dumitrica et al.

1997: 26, pl. 4, fig. 12.

Occurrence. — Samples KEL 2-20; from Jurassic-

Crecaccous boundary to Calpionellid standard

zone C.

Family PaTULIBRACCHIO/VE Pessagno, 1971

emend. Baumgaitner, 1980

Genus Angidohracchia Batmigartner, 1980

Angulobracchia (?) portnianni s.l.

Baumgartner, 1984

(Fig. 8D)

Angulohracchia (?) portrnanni Baumgartner, 1984:

757, pl. 2, fig. 3-

Angîdobraccma (?) portmanni s.l. - Baumgartner et al.

1993a: «8, pi.6I2U figs 1-4.

Angttlobracchia (?) portrnanni - Dumitrica et al. 1997:

30, pl 4, fig. 16.

Occurrence. — Samples KEL 7-16; from lower to

upper part of Calpionellid standard zone B.

Genus Halesium Pessagno, 1971

emend. Baumgartner, 1984

Halesium sexangtdum

Pessagno, 1971 sensu Steiger., 1992

(Fig. 8A)

Halesium sexangulum Pessagno, 1971: 25, pl. 1, figs 5-

6 ; pl. 2, figs 1-6. - Steiger Î992: 47, pl. 11 figs U 2.

Occurrence. — Samples KEL 2-7; from upper part

of Calpionellid standard zone B to zone C.

732

GEODIVERSITAS • 1999 • 21 (4)

Radiolarians from NW Turkey

Halesium irregularis

Steiger, 1992

(Fig. 80

Halesium irregularis Steiger, 1992: 47, pl. 11, figs 3-5.

Occurrence. — Sample KEL 16; in Calpionellid

standard zone B.

Halesium (?) sp.

(Fig. 8E)

Occurrence. — Samples KEL 9-20; from Jurassic-

Cretaceous boundary to uppcr part of Calpionellid

standard zone B.

Genus ParonaellaVes,sà%no^ 1971

emend. Baumgariner, 1980

Paronaella (?) tubulata

Steiger, 1992

(Fig. 81)

Paronaella (?) tubulata Steiger, 1992: 45, pl. 10,

fig. 10. - Jud 1994: 91, pl. 15, figs 18-19. -

Baumgartncr 1995a: 400, pl. 5183, figs 1-5 (H).

Occurrence. — Samples KEL 2-7; from upper part

of Calpionellid standard zone B to zone C.

Paronaella sp.

cf. P, (?) tubulata 1992

(Fig. 8F, G)

Occurrence. — Samples KEL 2-7; from npper part

of Calpionellid standard zone B to zone C.

Family PSEUDOAULOPHACIDAE Riedel, 1967

emend. Dumicrica, 1997

Gcwws Alievium Pessagno, 1972

Alievium nodulosum Dumitrica, 1997

(Fig. 8K)

Alievium nodulosum Dumitrica, 1997: 224, pl. 3,

fig. 9.

Occurrence. — Sample KEL 20; on Jurassic-

Cretaceous boundary.

Alievium regulare (Wu & Li, 1982)

(Fig. 8L)

Praeconocaryomma regulare Wu & Li, 1982 : 65, pl. 1,

figs 1,3.

Alievium helenae - Schaaf 1981; 431, pl. 7, fig. 9;

{non) pl. 10, fig. 2a-b. - Baumgartner et al. 1995a:

80, pl..5228, figs 1,3.4, non 2,5.

Alievium rtgulare - Dumitrica 1997; 221, pl. 2,

figs I2'l4; pl. 3 figs 1-3, 5.

Occurrence. — Samples KEL 2-23; from

Calpionellid standard zone À .subzone 3 to zone C.

Genus Bectis Wu, 1986

Becus triangulocentrum

Dumitrica, 1997

(l*ig. 8J)

Becus triangulocentrum Dumitrica, 1997: 216, pl. 1,

figs 8-9; pl. 2, figs 1.2,4, ?3, ?5, ?6.

Alievium belenae — Baumgartner et al. 1995a: 80,

pl. 3228 (/>w), fig. 2, non 1-4 = Alievium regulare^ 5 =

Becus helenae.

Occurrence. — Samples KEL 16; in Calpionellid

standard zone B.

Remarks

Our specinien diflers from Becus helenae (Schaaf.

1981 ) by having three nodes at ihe centêr of the

circle of nodes on each side. It ditfers from

B. gcmtntttusA^u, 1986 by having rwelve nodes

composing a circle rathêr than niuc. It mute clo-

sely resembles B. triangulocentrum Dumitrica,

1997 by having rwelve nodes making up a circle

on cach face and by having diree nodes in the

central area insidc the circle.

Family SPONGlJRIOAE Haeckel, 1862

Genns Archaeospongoprunum Pessagno, 1973

Archaeospongoprunmn patricki

M, 1994

(Fig. 7C)

Archaeospongoprunum patricki ]\xày 1994: 63, pl. 4,

figs 2-4. — Baumgartner et. al. 1995a: 110, pl. 5042,

figs 1 (H)-4. - Dumitrica étal. 1997: 21, pl. 2, fig. 3.

Occurrence. — Samples KEL 2-23; from

Calpionellid standard zone À subzone 3 to C.

GEODIVERSITAS • 1999 • 21 (4)

733

Mekik F. A.. Ling H. Y., Ôzkan-Altiner S. & Altiner D.

CONCLUSIONS

The résolution of radiolarian bioevents incrcases

with the fine sampling interval in section KEL

(15-20 meters) and the stepwise initial occurren¬

ce of Cretaceous radiolarian taxa Ls acccncuatcd.

This graduai appcarancc of the taxa is probably

an artifact of selccth'c prescrv^ation becaiise taxa

such as Alieinum rvgidjire, Dicerosatimialis dicra-

nachanthos, Deinattts dianiphidlus, Acaeniotyle

diaphorogonas ArvhueQdlcïyomitra apïarium,

Emiluvia pessagnoiy htntànellium berrulsianumy

and Hstium rartcosiitttany among oihers, appear

at chrono.stratigraphically lower Icvels in other

European sections (sec Baumgartner e^aJ. 1995a)

than they do in section KEL (Fig. d). Sélective

préservation, the lack of a sudden change/turn-

over in radiolarian fauna at the Jurassic-

Cretaceous boundaiy and only two samples from

the latest Tithoniari inukc the dclincation of the

Jurassic-Cretaceous boundary impossible in sec¬

tion KEL at this timc. Ucspite preservational

problems, a typical Tethyan radiolarian fauna

consisting of 33 généra and 36 spccies are illus-

trated from Turkey for the (Irst lime.

Acknowledgements

We wish to thank Dr. P. Dumitrica for his kind

and constructive review of an earlier version of

this manuscript. We also thank Dr. L.

O’Dogherty for his thorough icvicAv and

thoughrful suggestions which grcatly improvcd

our paper. Many thanks arc also due to Dr. A.

Ohler for her careful corrections of syntax, espc-

cially wirh German spellings. Mr. M, Howland

and Ms. Dian Molsen (both from Northern

Illinois Llniversity) kindly helped with preparing

the figures and plates.

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738

GEODIVERSITAS • 1999 • 21 (4)

Late Cretaceous (late Campanian-early

Maastrichtian) radiolarian biogeography;

a review

Osamu TAKAHASHI

Department of Astronomy and Earth Sciences, Tokyo Gakugei University,

Koganei-shi, Tokyo 184-8501 (Japan)

takahasi @ u-gakugei. ac.jp

Takahashi O. 1999. — Late Cretaceous (late Campanian-early Maastrichtian) radiolarian

biogeography; a review, in De Wever P. & Caulet J.-P. (eds), InterRad VIII, Paris/Bierville

8-13 septembre 1997, Geodiversitas 2^ (4) : 739-750.

KEYWORDS

Late Cretaceous.

radiolarians,

Tethys,

Atlantic,

Pacific,

oceanic circulation.

ABSTRACT

Some characteristic species of Late Cretaceous radiolarians from central

Japan and the world are discussed. With respect to the relation berween

radiolarian distribution and latitude, Amphipyndax enessefft Foreman,

Theocampe abschnitta (Empson-Morin). Myltocercion acineton Foreman, and

Dictyomitra Limelltcostata Foreman were restricted to the low to intermediate

latitudes. LHhomelma héros Campbell & Clark, Lithomelissa hoplites

Foreman, Theocampe altamontemis (Campbell &: Clark), and Stichomitra

livermorensis (Campbell & Clark) would tend to be cosmopolitan; however,

only in the circum-Pacific région, they were apparently confmed to northeas-

tern Asia, northwestern North America, and the Antarctic. The existence of

the distribution of the Late Cretaceous radiolarians could be explained by

oceanic circulation patterns and it was important in determining Late

Cretaceous provincial boundaries of radiolarians.

GEODIVERSITAS • 1999 • 21 (4)

739

Takahashi O.

MOTS CLÉS

Crétacé supérieur,

radiolaires,

mer mésogéeunÇ)

Adanrique,

Pacifique,

circulation océanique.

RÉSUMÉ

Biogéographit des radiolaires du Crétacé supérieur (Campanîen supérieur-

Maastrichtien inférieur) : bilan.

Quelques espèces caractéristiques du Crétacé supérieur du japon central et

du monde soni discutées. Tenant compte des distributions paléolatitudi-

nales, il apparaît que Amphxpyndax enesseffi Foremaii, Theocampe ahschnitta

(Empson'Morin)j Myllocercian adneton Forcman, and Dirtyomirra lamellico-

stata Forcman sont restreints aux basses latitudes ou intermédiaires, alors que

Lithomelîssa héros Campbell ÔC Clark, Lithomelissu hoplites Foreman,

Theocampe altamontensis (Campbell &: Clark), and Stkhojmtra livemorensis

(Campbell 6c Clark) tendraient à être cosmopolites. Néanmoin-s, dans les

régions drcum-Pacifique,. ils sont apparemment confinés au Nord-Est de

l’Asie, au nord-oufcsrdc l'Amériquedu Nord et à l’Antarctique. L’existence de

cette distribution au Crétacé supérieur pourrait être expliquée par des cou-

ranrs océaniques qui ont dércrminé le.s limites des provinces fauniques de

radiolaires à cerre époque.

INTRODUCTION

Radiolaria are effective indicarors of various

oceanic environments; paleoceanographic,

paleoecologic, bathyinetric, etc. Since Haeckel

(1887), many paleobiogeographic studies of

radiolarians hâve been donc during the past

100 years. However, most hâve been restricted to

the Cenozoic (c.g., Casey 1971; Goll &

Bjorkiimd 1971; Petrushevskaya 1971). and very

litrie has been published on radiolarian paleobio-

geography from the Mesozoic. Pessagno (1976)

establishcd a radiolarian zonation for the Upper

Cretaceous portion of the Créât Valley sequence

of Northern California and stated that radiola¬

rian spedes common to the Upper Cretaceous

strata of the lechyan, Boréal, and Austral Faunal

Provinces are eurybarhic and would rend to be

more cosmopolitàn. However, commencing with

the study of Empson-Morin (1984), Upper

Cretaceous radiolarians hâve been appreciated as

valuablc biogeographic tools. She described the

Upper Cretaceous radiolarians as effective envi-

ronmental indiçators showing variations in res-

ponse to deptb and/or latitude.

Recently, a preliminary study by Takahashi ôé

Ishii (1993) stated that the Upper Cretaceous

(late Campanian-carly Maastrichtian) strata of

central japan include two characteristic radiolar¬

ian faunas. I hâve noticed in the Late Creta¬

ceous Northwestern Pacific Océan an example

showing two parallel distributions of characteris¬

tic radiolarian feunas; the similarity of the nor-

thern Northwestern Pacific fauna and the lack of

similarity of the Southern Northwestern Pacific

fauna to species of the California Upper

Cretaceous (e.g., Campbell & Clark 1944).

LATE CAMPANIAN TO EARLY

MAASTRICHTIAN RADIOLARIANS

FROM CENTRAL JAPAN

GEOLOGIC SETTING AND RADIÜL/VRIAN FOSSILS

OF THF Shüya Formation, northurn central

Jafan

The Shoya Formation (Watanabe 1958) is expo-

sed in an area approximatcly 0.5 km wide and

4,5 km long, and located 100 km northwest of

Tokyo (Fig. 1). It con.sists ofthrcc fining-upward

cyclic sequences of marine sedimentary rocks

about 600 m in total thickness, lacking pelagic

iruerbeds. The lower and middlc parts of each

sequence are composed of poorly-sorted, black,

medium- or fine-gtained sandstone, which grade

upward into welLsorted, bedded, dark gray sand¬

stone. The upper part of cach sequence is com¬

posed of alternations of mudstone and .sandstone

with dark gray, siliceous mudstone. The siliccous

mudstone frequently contains thin (several milli-

740

GEODIVERSITAS • 1999 • 21 (4)

Late Cretaceous radiolarian biogeography

SapporoT

km 500

36'’N-

35°N-

Shoya Formation

Vladivostok,

■i

40'

IO Séoul I

36-N

Kobûtùke Group

LEGEND I

I I T erliary & Quaternary-

Late Cretaceous déposits

Eariy Cretaceous déposits

Jurassic déposits

[,-<<] Jura.-Ôret. metàmorphic rocks

rf4%Fukuoka’'^

;akâ

Tokyo

135°

140°

139^E

140°E

Fig. 1. — Index map of the study

area showing the position of the

Shoya Formation and the

Kobotoke Group in central Japan.

mcters) layers of interbedded, greenish-gray, tuff-

aceoiis mudsrone or ruff. Some sajîdsrone units

contain abondant, yet poorly preserved molluscs,

including Spon^iyltu Jfiponicus, Cûr/iium{})j

Ostreûy other pelecypods, brachiopods, and corals

(Amano &c Marui 1958). Based on cectonic

configuration, litho- and bio-facies, rhc Shoya

Formation is interpreied as a typical forearc

sequcnce at the eastern margin oF rhç Asian

Continent (Ishii &C Takahashi 1993).

Radiolarian fossils were encountered in the dark

gray or black siliceous mudstone parts of the

strata. The radiolarian assemblage conrains

17 species belonging to 10 gênera (Table l),

some of which are shown in Fig. 2A-S. The

assemblage rarely containcd Arnphlpyndax tylolm

Foreman and ^4. enesseffi Foreman, and is charac-

terized by chc occurrence of Lithomelissa héros

Campbell Ôc Clark, L. hoplites Foreman,

Theocampe altumontensis (Campbell & Clark),

and Stichoniitra livermorensis (Campbell ôc

Clark).

Geolocuc settjng and radiolarian fossils

OF l’HF Kobotoke Group, Southern central

Japan

The Kobotoke Group (Makino 1973; Sakai

1987) is exposed in an area approximately 10 km

wide and 70 km long, and located 50-100 km

wesr of Tokyo (Fig. 1). It îs composed of rhyth-

mically alrernating beds (severai centimeters

thick) of fine- to medium-grained arkosic sand-

stone and black mudstone, occasionally inclu¬

ding cliert and lime.stone blocks and

conglomerate lenses in the mudstone dominant

part. The chert is mosrly red and rhyrhmically

bedded and the limesfone is dark gray in color.

The conglomerate is composed of pebbles of

limcstone, chert, sandsrone, and mudstone

within a sandy matrix, and they are found in

small bodies sporadically scartered in the sand-

stone layers.

The strata show normal graded bedding and are

steeply dipping northward in a monoclinal struc¬

ture, nevertheless, the geological âges of the South¬

ern beds are younger than those of the northern

beds (Ishii et ai 1990). These Icatures, the over-

all younging towards the south by répétition of

the strata wirhln imbricate thrusts, suggest a

typical strata distribution for an accretionary

prism (Ishii ôt Takahashi 1993).

Radiolarian fossils were encountered in the sili-

ceous, dark gray or black mudstone parts of the

strata. The radiolarian assemblage contains

11 species belonging to 6 généra (Table 1 ), some

of which are shown in Fig. 3A-M. The assembla¬

ge is characterized by the prédominant occur¬

rence of Amphipyndax tylotus Foreman and

GEODIVERSITAS • 1999 • 21 (4)

741

Takahashi O.

Table 1. — Occurrence and relative abundance of radiolarians of the Shoya Formation and îhe Kobotoke Group. Radiolarian abun-

dances are categorized as common (C) and rare (R). Plus (+) means presence. but recognized with such difficulty that no estimate

of abundance could be made.

Taxon

Shoya Formation

Kobotobe G.

Sh-1

Sh-2

Sh-3

Sh-4

Sh-5

St-2

Amphipyndax alamedaensis (Campbell & Clark)

A. enesseW Foreman

A. plousios Foreman

A. stocki (Campbell & Clark)

A. tyhtus Foreman

Archaeospongoprunum salumi Pessagno

—

A. stocktonensis Pessagno

Comuteita caliiornica Campbell & Clark

Dictyomitra andersoni (Campbell & Clark)

D. lamellicostata Foreman

D. multicostata Pessagno

Eribotrys anax Foreman

Lithomelissa héros Campbell & Clark

L. hoplites Foreman

Myllocercion acineton Foreman

“

Praeconocaryomma dauerhafta (Empson-Morin)

Pseudoaulophacus floresensis Pessagno

Rhopalosyringium magnificum Campbell & Clark

Saturniforma brionesensis Pessagno

sciadiocapsid

StichomiTra asymbatos Foreman

—

S. livermotonsis (Campbell & Clark)

Theocampe ahschnitta (Empson-Morin)

T. altamontensis (Campbell & Clark)

Theocapsomma amphora Campbell & Clark

—

A. enessefft Foreman, and also characterized by

the occurrence of Theocûmpe ahschnitta

(Empson-Morin), Dictyomitra lamellicostata

Foreman, and Myllocercion acineton Foreman.

AGEASSIGNMENT

The rwo radiolarian assemblages from the Shoya

Formation aitd the Kobotoke Group hâve somc

différences tn thcir componcnts. Howevcr, thcse

assemblages contain common and/or individual

typical species of the Amphtpyndax tylotus zone

(Foreman 1977; Sanfilippo & Riedel 1985). For

example, the first appearances of Lithomelissa

hoplites and Theocampe ahschnitta are included

near the base of the A. tylotus zone. The top of the

zone is defined as the Maastrichtian/Danian

boundary recognized by the last occurrences of

A. tylotus, L. hoplites, and Dictyomitra Ltmellicosta-

ta (Foreman 1968, 1977; Sanfilippo & Riedel

1985). Wirh respect to the othct species, the first

appearances of Lithomelissa héros, Theocampe alta-

montemis^ and Myllocercion acineton are

Campanian (Pessagno 1976; Foreman 1978;

Taketani 1982; Empson-Morin 1981; Sanfilippo

& Riedel 1985), whereas Stlchomltm liiermorensîs

first occurs in the Coniacian (Moore 1973). The

final occurrences of these species also correspond

to the top of the A. tylotus zone at the

Maastrichtian/Danian boundary (Foreman 1968,

1978; Sanfilippo &: Riedel 1985).

742

GEODIVERSrrAS • 1&99 • 21 (4)

Late Cretaceous radiolarian biogeography

Fig. 2. — Late Campanian-early Maastrichlian radiolarian fauna from lhe Shoya Formation, northern centra) Japan. A, Amphipyndax

tylotus Foreman; B. Amphipyndax enesseffi Foreman; C. Amphipyndax alamedaensis (Campbell & Clark): D, Amphipyndax stocki

(Campbell & Clark); E, Stlc^omkra livermorensis (Campbell & Clark): F. Dictyomitra multicostata Pessagno; G. Drclyomitra anderso-

ni (Campbell & Clark): H, Lithomelissa haros Campbell & Clark; I. Lithomelissa hoplites Foreman; J, Theocampe altamoniensis

(Campbell & Clark): K. Theocapsomma amphora Campbell & Clark; L, Rhopalosyringium magnificum Campbell & Clark;

M, Cornutella californica Campbell & Clark; N, gen. sp. indet.; O, Sciadiocapsid gen. sp. indet.; P, Saturniforma brionesensis

Pessagno; Q, Orbiculiforma sp.; R, Archaeospongoprunum saiumi Pessagno; S, Archaeospongoprunum stockîçnensis Pessagno.

Scale bars: 0.1 mm

Therefore, rhese spedes of both assemblages reco-

vered from the Shoya Formation and the Kobo-

toke Group represent the Amphipyndax tylotus

zone which is indicative of a range from the late

Campanian to the early Maastrichtian in âge

(Foreman 1977, 1978; Sanfilippo & Riedel 1985).

GEOOIVERSITAS • 1999 • 21 (4)

743

Takahashi O.

Fig. 3. — Late Campanian>early Maastriçhhan radiolarian faunafrom the Kobotoke Group, soufhern central Japan A. Amphipyndax

tylotus Foreman; B, Amphipyndax enesseffi Foreman; C, Amphipyndax alamedaensis (Campbell & Clark): D. Amphipyndax stocki

(Campbell & Clark); E, Dictyomitra multicostata Pessagno; F, Diciyomitra ancfersom (Campbell & Clark); G, Dictyomitra lamellicosta-

ta Foreman: H. TTïeocampe abschnitta (Empson-Morin); I. Theocampe sp.; J. f^hopafosyringium magnificum Campbell & Clark:

K. Myflocercion acineîon Foreman; L, Pseudoaulophacus ftoresensis Pessagno, M. Archaeospongoprunum sp. Scale bars: 0.1 mm.

PALEOBIOGEOGRAPHIC

DISTRIBUTIONS OF LATE CAMPANIAN-

EARLY MAASTRICHTIAN RADIOLARIANS

Selected pairings of the assemblages from the

Shoya Formation and the Kobotoke Group were

compared by means of a similarity index (Jaccard

CoefFicicnt; Table 2). The results show that the

pairings between the Kobotoke Group (St-1 and

St-2) and the Shoya Formation (Sh-1, Sh-2, and

744

GEODIVERSITAS • 1999 • 21 (4)

Late Crecaceous radiolarian biogeography

Table 2. — A matrix of similarity values (Jl: Jaccard index) for

comparisons of radiolarian assemblages from each sample.

Shoya F.

Kobotobe G.

Sh-2

Sh-4

St-2

Sh-1

0.38

0.44

0.29

0.36

Sh-2

0.40

0.41

0.50

Sh-4

0.28

0.26

St-1

0.78

Sh'4) yieldcd somewhat lower values rhan did

pairings from vvirhin each one. Namely, each

assemblage is characrerized by different species.

For example, the assemblage from the Shoya

Formation is characterized by the occurrence of

Liihomelissa héros Campbell ^ Clark, Litho-

melissa hoplites boœman. Theocampe altamonten-

sis (Campbell & Clark), and Stichoniitra liver-

motensh (Campbell & Clark), whereas the one

from the Kobotoke Group is characrerized by rhe

occurrence of Theoaimpe abschnitta (Empson-

Morin), Dictyornina lani&llkosuiîn Foreman, and

Mylloctrcion adnttvn Foreman.

Radiolarians from each sample occiir in ihe same

.siliccous mudstone lithofacie.s. and the rock

samplcs wcrc carcfully caken from non-foldcd,

non-overcurned, and non-metamorphosed parts.

Furthermore, in spite of varied sraces of préserva¬

tion, each radiolarian assemblage has ics own

characterisnc species, although the number of

skclctons may differ. d'hus, it is suggested ihat

the différences in coniponencs berween the two

Lace Crctaceous radiolarian assemblages may

bave been caused largely by oceanic environ¬

ment. In chis stüdy, 1 artempr to distinguish che

paleobiogeographic distributions of the seven

characteristic species of the radiolarian faunas,

and examine rhe différences in components and

their possible cau-ses from their worldwide distri¬

butions in Lite Crctaceous timc. The loailicics of

radiolarians are jllustrated in Figs 4, 5.

Lithomelissa hoplites (Fig. 2J) was reported from

California (Foreman 1968), the mid-Atlantic

Océan (Foreman 1977), New Zcaland (Hollis

1997), and Southwest Japan (Yamasaki 1987).

Lithomelissa héros (Fig. 21) was reported from

California (Campbell & Clark 1944; Foreman

1968; Pessagno 1976), New Zealand (Flollis

1997), and the mid-Atlanric Océan (Foreman

1978). Lithomelissa sp. were reported from the

northeast coast of New Zealand (Ballance et al.

1989; Hollis 1997), Southwest japan (Yamasaki

1987), and Hokkaido (Iwata & Tajika 1986).

Theocampe altamontensis (Fig. 2K) w^as reported

from the northeasr coast of New Zealand

(Ballance et al. 1989; Hollis 1997), rhe South

Atlantic Océan (Foreman 1977). the Antarctic

Océan (ling & Lazarus 1990; l.ing 1991),

California (Campbell & Clark 1944), Southwest

Japan (Muramatsu 1986; Yamasaki 1987), and

the Bering Région (Vishnevskaya 1986).

Stichoniitnt liverrnorejisis (Fig. 2F) was reported

from California (Campbell & Clark 1944;

Forernan 1968), the Bering Région (Visbnev-

skaya 1986), the Antarctic Océan (Ling 1991),

New Zealand (FloHi.s 1997), .Southwest japan

(Suyari 1986; Yamasaki 1987), and Hokkaido

(Iwata & Tajika 1986, 1989). Amphipyndax enes~

seffi (Figs 2C, 3C) was reported from the mid-

Pacific Océan (Moore 1973; Fimpson-Morin

1981), California (Pessagno 1969), the mid-

Atlantic Océan (Foreman 1977, 1978; Empson-

Morin 1984), Southwest japan (Suyari &

Hashimuio 1985; Muramatsu 19S6; Suyari

1986; Yamasaki 1987)» and Hokitaido (Iwata &

Tajika 1989). The occurrence from FIokkaido

(Iwata Tajika 1989) is the northernmost limit

of the range of A. enesseffi in the World.

Theocampe abschnitta (Frg. 31) was reported from

the mid-Pacific Océan (Empson-Morin 1981)

and Southwest japan (Muramatsu 1986;

Yamasaki 1987), Mylloeercion acincton (Fig. 3E)

was reported from ihe mid-Pacific Occan

(Empson-Morin 1981), California (foreman

1968), New Zealand (Hollis 1997), and the mid-

Atlantic Occan (Foreman 1978). Diçtyomitra

lamellicostata (Fig. 3H) was reported from the

mid-Atlantic Océan (Foreman 1977, 1978),

California (Foreman 1968), New Zealand

(Hollis 1997), and Southwest Japan (Suyari Se

Hashimoto 1985; Suyari 1986).

With respect to the relation between radiolarian

distribution and latitude, Amphipyndax enesseffi,

Theocampe abschnitta, Myllocerçwn acineton, and

Diçtyomitra lamellicostata were restricted to rhe

low to intermédiare latitudes except for New

GEODIVERSITAS • 1999 • 21 (4)

745

Takahashi O.

Fig. 4. — Distribution of Stichomitra llvermorensis (Campbell & Clark). Uthomelissa sp. (including L héros Campbell & Clark and

L. hoplites Foreman), and Theocampe altamontensis (Campbell & Clark) in the late Campanian to eariy Maastrichtian. Data are from

Campbell & Clark (1944). Foreman (1968. 1977). Pessagno (1976), Empson-Morin (1984). Muramatsu (1986), Iwata & Tajika (1986,

1989), Vishnevskaya (1986), Yamasaki (1987). Ballance et ai (1989). üng & Lazarus (1990), Ling (1991), Hollis (1997), and présent

research. This map has been synthesized from Barron et ai (1981). Smith et ai (1994), and Roberts & Kirschbaum (1995).

Fig. 5. — Distribution of Amphipyndax enessefff Foreman. Theocampe abschnitia (Empson-Morin), Myllocercion acineton Foreman,

and Dicîyomitra lamellicostata Foreman In the late Campanian to eariy Maastrichtian. Data are from Pessagno (1969), Moore

(1973), Empson-Morin (1981,1984), Suyari & Hashimoto (1985), Muramatsu (1986), Suyari (1986), Yamasaki (1987), Iwata & Tajika

(1989), Takahashi et ai (1989), Ishü et ai (1990), Hollis (1997), and présent research.

746

GEODIVERSITAS • 1999 • 21 (4)

Late Cretaceous radiolarîan biogeography

★ Amphipyndax enesseffi • Theocampe abschnitta a Myiiocercion acineton ■ Dictyomitra famellicostata

Fig. 6. — Relâlionshtp between Gordon's (1973) oceanic circuiation and the global distribution of lhe ses/en characteristic radiolarian

species. Amphtpyndax enesseffi, Thtfooampe aPschniffa, Myiiocercion acineion, and Dictyomitra lameflioostata were restrlcled lo the

low to intermodiale latitudes. Llidomelissa héros, Uthomelissa hoplites, fheocampe atiamnntensls. and SUchomitra Iive/rnorensls

would tend lo be codcnopolitan. howevef. ooly in the cimunvP^fânr région, they werw epparently confined to northeftstem Asie, nor*-

thwestem North America, and the Antarctic. In lhe fethys Sea and Atlantic Sca. therc wore more longitudinal channols which permil-

ted mlxing of lheir water with highei UtitudQ wdter. Intermediate tn high intitude radlolanans, theretore, reach much forther south to

lhe Tethyan and central Atlantic régions alOng lhe sPHways on the Leurasia. In contrasi. citculation in lhe norlhern Pacific Océan

dur'ing the Late Cretaceous was dominated by a clocKwise gyre. It made possibly contrasling distributions ot radiolanans in this time.

Zealand (Hollîs 1997)- Lithomelissa herosy

Lithomelissa Psoplites, Theocampe ait amont émis y

and Stichomitra livermorensis would tend to be

cosmopoiitan. Howevci, only in lhe circum-

Pacific région, they werc apparently confmed to

northeastern Asia, norrhwestern North America,

and the Anrarctic. Thar is, the paleobiogeogra-

phic distributions ol the particular species of

Late Cretaceous radiolarians seem to hâve reflec-

tcd water-masses or theif conditions.

Température is presumably a laritudinal compo-

nenr (e.g., Petrushevskaya 1971). Factors other

rhan water depth and température such as

nucrieni levels and water chemistry undoubtedly

controllcd radiolarian distribution and abundan-

ce (e.g., Anderson 1983)^ many of diese factors,

however, are also relatcd to water depth and tem¬

pérature (Pessagno 1976). Among fossil orga-

nisms, the clearly latitudinal distribution of

foraminifera in Cretaceous rocks indicates the

importance of température (e.g., Caron 1985).

T^mmonoids also seem to be influenced by tem¬

pérature as they are .separable into Tethyan (ixo-

pical) and Boréal assemblages (e.g., Obata &

Matsulcawa 1988). If the faunal distributions of

radiolarians are duc co différences in température

of the water masses, the distribution is possibly

influenced by the current Systems. Not only do

currents sepatate biogeographical régions, but

the currents themselves contain characteristic

radiolarian fiunas.

Using analogies with the modem world and évi¬

dence of past climates, Gordon (1973) recon-

strucîed global océan currents for the Late

Cretaceous. Fig. 6 shows the relationship be¬

tween GordonS (1973) oceanic circulation and

the global distribution of the seven characrerisric

radiolarian species.

Any discussion of Lace Cretaceous paleoenviron-

ments first rcquires a description of land-sca dis¬

tribution. which was significantly different from

the présent (Barron H ai 1981; Smith et al.

1994). Global marine transgression progressed

during Late Cretaceous time (e.g., Payton 1977).

GEOOIVERSITAS • 1999 • 21 {4)

747

Takahashi O.

The Tethys Sea and the Atlantic Océan wcre

broad at this rime, and thcre were more longitu¬

dinal channels (the norrhern Tethys and north-

ern Atlantic longitudinal seaways) which

permittcd inixing of iheir watcr vvîth highcr lati¬

tude watcr, not neccssarily at rhc surface of chc

water column. The circumpolar West Wind

Drift would hâve canscd cool currents to enter

the Norrh American mid-continental seaway and

the European shelf \eas (Gordon 1973)*

Intermediate lo high latitude radiolarians, thcre-

fore, reach much farther south to the Tethyan

and central Atlantic régions aJong the seaways on

the Laurasia. It was proved by bimodal radiolar-

ian faunas lound at the Latc Crctaccous Tethyan

and mid-Atlantic régions, and was clearly asso-

ciared wirh the Late Cretaceous transgressive

phase. Pessagno &c Blome (1986) referred to

Cordons model as being applicable to the

Middlc Jurassic world occanic circulations. They

also recognized the mixing ol warm and cool

watermasscs at the Tethyan and Atlantic régions

in that cime.

In contrast, circulation in the norrhern Pacific

Océan during the Lare Cretaceoies was domina-

ted by a clockwise gyre (Gordon 1973), with a

warm current (Paieo-Kuroshio Curreni) Howing

north on ils western inargin whcrc Amp/jf/))fNd^ix

enesseffî, Theocampe abschmttas Myllacercïon ad-

neton, and Dlctyormtrn Inmellicosmm rhrived, and

a cool current (Paléo-California Current) flowing

south on the eastern margin where Lithomelhsa

herosy Lithomdissa hoplites, Theocampe altamoN-

tensis, and Stichomitra livermorensis wcre success-

ful. Around ihc Japancsc Islands, two occanic

currents may have existed; one from ihc north-

ernmosr Pacific Océan and the othet from the

Equator. They crosscd cach other at the présent

position of the japanese Islands.

Acknowledgements

I gratefully acknowledgc the help of W. Kiessling

and F. Cordey who rend earlier drafts ol this

manuscript. I am indebted to H. Okada and

A. Ishii for cheir invaluable contributions and

criticism. Y. Ogawa and M. Matsukawa are thank-

ed for their helpful discussions during the course

of this study.

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Ling H. Y. & La^a^us D. B. 1990. — Cretaceous

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Muramatsu l'. 1986. — Late Cretaceous-earliesr

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Radiolarian fossils firom the Masutomi Group, sou-

GEODIVERSITAS • 1999 • 21 (4)

749

Takahashi O.

thwestern part of the Kanto Mountains, central

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Submitted for publication on 29 January 1998;

accepted on 24 July 1998.

APPENDIX

Sample localities

Figured specimens will be deposited in the Tokyo Gakugei University. The following sample num-

bers, Sh and St, refer to samples from the Shoya Formation and the Kobotoke Group, respectively.

For St-1, see Loc. 8 in Takahashi et al. 1989; Loc. 12 in Ishii et al. 1990.

Samples Géologie setting

localities

Sh-1

Sh-2

Sh-3

Sh-4

Sh-5

St-1

St-2

Siliceous dark gray mudstone

Siliceous black mudstone

36°13’07”N,

36°13’07”N. 138°35’04”E

36*^13’07”N, 138“35’04”E

36M2’5rN. 138"35’04”E

36°12’5rN, 138°35’04”E

35°53’39”N, 138^3riO”E

35°46’06”N, 138°54’33”E

750

GEODIVERSiTAS • 1999 • 21 (4)

Permian Albaillellaria (Radiolaria)

from a limestone lens at the Arrow Rocks

in the Waipapa Terrane (Northland, New Zealand)

Atsushi TAKEMURA & Tami MORIMOTO

Geoscience Institute, Hyogo University of Teacher Education,

Yashiro-cho, Kato-gun, Hyogo 673-14 (Japan)

takemura@sci.hyogo-u.ac.jp

Yoshiaki AITA

Department of Geology, Faculty of Agriculture, Utsunomiya University,

Utsunomiya 321 (Japan)

Rie S. HORI & Yasushi HIGUCHI

Department of Earth Sciences, Faculty of Science, Ehime University,

Matsuyama 790-77 (Japan)

Bernhard K. SPÔRLI

Department of Geology, University of Auckland.

Auckland (New Zealand)

Hamish J. CAMPBELL

Institute of Geological and Nuclear Sciences,

Lower Hutt (New Zealand)

Kazuto KODAMA

Department of Geology, Faculty of Science. Kochi University.

Kochi 780 (Japan)

Toyosaburo SAKAI

Department of Geology, Faculty of Agriculture, Utsunomiya University,

Utsunomiya 321 (Japan)

Takemura A., Morimoto T., Aita Y,, Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J.,

Kodama K. & Sakai T. 1999 — Permian Albaillellaria (Radiolaria) from a limestone lens at

the Arrow Rocks in the Waipapa Terrane (Northland, New Zealand), in De Wever P. &

Caulet J.-P. (eds), InterRad VIII, Pahs/Bierville 8-13 septembre 1997, Geodiversiias2^ (4) :

751-765.

GEODIVERSITAS • 1999 • 21 (4)

751

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

KEYWORDS

Radiolaria,

Albailltllaria,

PermiJIi.

New Zealand,

Waip^a Tcrmnc.

Follkucidlui,

Arrow Rocks,

new spcck*^

ABSTRACT

Well-preserved Permian radiolarians are présent in a limestone lens at Arrow

Rocks in the Wliangaroa Area within Waipapa Terrane, New Zealand. This

fauna conrains eighr species of albaillellarians» six species cl genus

Follkucullus and wo of Pseudoalbaillella, and is Lare Middle lo Early Late

Permian in âge. In the Whangaraa Area, bAsalti» are probably as old as

Middle Permian. whilc cherts arc mosily Latc Permian. AJthough the radio-

larian launa frum Arrow Rocks cuinains twn new species oFFoUicucuUus, this

fauna can nevcnheless bc assigncd a low-Iatitude origin. Two new species»

Folliamillus iphuiricfd and Follkucullus luhangaronetisis, arc described.

MOTS CLÉS

Radiolaire,

Ibaillellarides.

Permien,

Nouvelle Zélande,

Waip^a Tcnane,

Follicticiillm^

Arrow Rocks,

nouvelles espèces.

RESUMJÉ

Albaillellaridés (radiolaires) permiens d'un banc calcaire à Arrow Rocks dans la

Waipapa Terrane (Nouvelle Zélande septentrionale).

Des radiolaires permiens bien conservés ont été trouvés dans un banc calcaire

a Arrow Rock.s dans la région de Whangaroa de la Waipapa Terrane,

Nouvelle Zélande. Certe faune conrienr huir espèces d'albaillcilaridés, six

espèces du genre FolUcucitllns et deux de Fseudoalhuillclliiy et est d'âge

Permien moyen à début Permien supérieur. Dans b région de Whangaroa,

les basaltes sont probablement aussi anciens que le Permien moyen, alors que

le.s chens sont principalement Permien supérieur. Bien que la faune a ladio-

laircs à Arrow Rocks contiennent deux nouvelles espèces de F'ollicucullus,

cette faune peut néanmoins être considérée comme de basse latitude. Deux

nouvelles espèces, Follkucullus sphaericus et Follkucullus whangarodensis. sont

décrites.

INTRODUCTION

Our knowledge of Permian radiolarians has

significantly incrcascd since Oimiston

Babcock (1979) described genus Follicucullus

from Guadalupian scquence.s in West Texas.

After this pioneering research, taxononty and

biostratigrapliy ol Permian launa devejoped

rapidly in the Llnited States, Russia and Japan

(e.g., Holdsworth dé Jones 1980^ Ishiga & Inioto

1980; Takemura & Nakaseko 1981; Ishigâ cl al.

1982a, b; Nazarov & Ormiston 1986; Ishiga

1986). Most of this Work was. however, doue in

the northern hemisphere, and most Permian

radiolarians recorded from the Southern hémis¬

phère are from New Zealand.

Permian radiolarians are known froni only a fcw

fossil local itie.S in New Zealand, one of which is

Red Rocks near Wellington m Torlesse Terrane

(Fig. 1), where Grapes et al. (1990) reported

Middle Permian radiolarians from bedded chert.

The other localities are concenrrated within the

Whangaroa Area in the northern Waipapa

Terrane. Révérai radiolârian locâlines of bedded

chert and limestone hâve been reported from this

area, géologie âge of which ranges fa>m Middle

to Late Permian (Caridroit & Ferrière 1988;

Adachi 1988; Takemura et ai 1998).

We have made geological and biostratigraphic

surveys in the Whangaroa Area ( 1995-1996), and

liaVc alrcady reported the occurrence of Permian

and Triassic radiolarians from this area. At Arrow

Rocks, an almost conçinuous section from basait

with limestone, bedded chert to siliceous mudsto-

ne is exposed, Well-preserved radiolarians are |)re-

senc in a lirnesrone lens within spiliric basait, the

âge of which is Middle to Late Permian

(Takemura et al. 1998). This fauna includes seve-

ral albaillellarian species of the généra

Follicucîillus Ormiston &; Babcock, 1979 and a

752

GEODIVERSITAS • 1999 • 21 (4)

Permian Radiolaria from Arrow Rocks, New Zealand

175°E

Fig. 1. — Index map of the North Island, New Zealand, showing the distribution of terranes (Aita & Spôrli 1992) and the location of

the Whangaroa Area, as well as Red Rock near Wellington.

GEODIVERSITAS • 1999 • 21 (4)

753

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

few of Pseudoalbaillella Holdsworth àc Jones,

1980. We describe albaillellarians of this fauna,

including two newspecies ofgenus Follicucullus.

GEOLOGICAL SETTING, STRATIGRAPHY

AND METHOD

Basement of New Zcaland North Island consists

mostly of five lirJiostratigraphic units, Murihiku,

Dun Mountain, Waipapa, Torlesse and Mata

River Terranes {Aita & Spôrli 1992; Fig. 1).

These terranes becomes younger in geological

âge from west to cast, and the lattcr three,

Waipapa. TorJesse and Mata River, aie Mesozoic

accretionar)^ complexes.

The Whangaroa Area (Figs 1. 2) is situated at

about 90 km northwest of Whangarci in

Northland. This area belongs to the northern

part of Waipapa Terrane, which is composed

mostly of terrigenous clastic rocks associated

with spilitic basait, chcrt and argillites.

Geological âge of the northern part of this terra¬

ne is Permian to Triassic, based on radiolarians

and fusulinids (Aita & Spôrli 1992; Takemura et

ai 1998).

The Waipapa Tcrranc rocks in the Wliangaroa

Area consists of massive to thick bcddcd sandsto-

ne (greywackc), spïlicic basale, bedded chcrt,

green siliccous mudstone (argillite) and liniesto-

ne lenses within basait (Fig, 2). Prior to this

study, more chan six locahnes of Permian fossils

were known from chert and limestone in this

area. Radiolarian fossils show Middle to Late

Permian âge from five locaiitics (Caridroit &

Ferrière 1988; Adachi 1988; Takemura et al.

1998). L.cvcn &: Granr-Mackie (1997) dcscribed

fusulinids from limesTonc Icnscs at Wherowhcro

Point (Fig. 2), the samc locality from which

Hornibrook (1951) reported fusulinids. Thcy

concluded that rhe hisulinid fauna belonged to

Yabeina-Lepidolina zone and thcrcforc is part of

the Midian Stage of Tcthyan Rcalm. They al.so

mentioncd the paleogeographic relationship of

this fauna with casteni Asia. At Mahinepua

Peninsula about 5 km cast of the Wherowhcro

Point, very wcll-preserved Ttiassic radiolarians

occur in the phosphatic nodules within green

siliceous mudstone (Aita & Bragin 1999).

rhe material studied in this p;tper was obrained

at Arrow Rocks (Oruatemanu Island), a small

island located wirhin Whangaroa Bay, north of

Whangaroa Harbour (Fig, 2). The Grid

Référencé for Arrow Rocks, based on the New

Zealand 1:50,000 topographie map, îs P04 &

Q04/837895 corresponding to latitude

34'^59.7Ti and longitude I73°46.8^E. On this

small island, we hâve observed a 135 m thick

seemingly continuous section composed of spili¬

tic basait witb limestone layers, bedded chert,

and red, maroon and green siliceous mudstones.

Takemura et al. (1998) made a preliminary

report on the lithostratigraphy of this scqucnce,

and divided it into cight lithological unirs

(Fig. 3). Ficld observation of lithologics and

thickness in these units in ascending order is as

the foUows:

— Unir 1: spilitic basait with limestone lenses,

31.5 m;

— Unit 2: bedded chert, 11 m;

— Unit 3: alternation of cbert and black shale,

1 m;

— Unit 4: red siliceous mudstone and red chert

with manganese-rich layers, 6.6 m;

— Unit 5; red siliccous mudstone with chin red

chert, 17.2 m;

— Unit 6: maroon chert and siliceous mudstone,

29.5 m;

— Unit 7. alternation of maroon and green sili¬

ceous mudstone, 11.2 m;

— finit 8: green siliceous mudstone with vitric

tuffs, 27 m.

Within this sequence, we observed no significant

faulting excepr between Units 2 and 3.

Boundaries bciwecn the units descrihed above

arc conformable and appear to represent cond-

nuoLLs déposition.

Takemura et ai (1998) report the occurrence of

Late Permian Radiolaria including AUniillella tri-

angularis Ishiga, Kiro âc Imoto, 1982 and

Hegleria sp. in a bedded chert sample (ARR-7)

within Unit 2. The horizon of ARR-7 lies about

10 m above that oi ARR-1 (Fig. 3). Triassic

radiolarians such as Pareyitacttnta (Dumitrica,

Archaeosemafitis (Dumitrica, 1978) and

forms belonging to genus Glomeropyle (Aita &

Bragin 1999) are présent in siliceous mudstones

within Units 6 and 8.

754

GEODIVERSITAS * 1999 • 21 (4)

Permian Radiolaria from Arrow Rocks, New Zealand

spititic basait chert

green sifioeous massive

shale sandstone

Fig. 2. — Pemiian and Triassic fossil localities in lhe Whangaroa Area. X. fossil localilies. Perntian radiolarians from limestone

and bedded chéri at Arrow Rocks (Takemura et af. 1998 and this study); 2. Permian radiolanans from bedded chert al Kairawaru

Bay {Caridroit & Ferrière 1988; Adachi 1988); 3. Permian radlolarians from limestone and chert at west of Mahinepua Peninsula

(Takemura et al. 1998); 4, Triassic radiolarians from phosphate nodules in green argillite at the Mahinepua Section (Alla & Bragtn

1999); 5. Permian fusulintds from limostones at Wherowhero Point (Hornibrook 1951; Leven & Grant-Mackie 1997).

The material treated in this study is a limestone

lens (ARR-1) wichin Unit 1. The unit includcs

four red, pale red or white limestone layers, 0.7

ro 2 m thiclc, intercalated wichin basalts, which

are usually green grey lo green coioured, massive

or showing pillow structure, or .sometimes are

fragmentai. ARR-1 is a purple grey coioured.

laminated limestone lens, situated at about 24 m

above the base horizon. This lens is intercalated

just below lhe uppermost red limestone laycr

within Unit l (24-26 m. Fig. 3).

ARR-1 coniains numerous radiolarian shells, but

they hâve been altcrcd bv CàCO^ so rhat we

obeained no or very few residues by extraction

using diluted hydrochloric, nitric or aceric acids.

As a resLilr nf this^ ir was decided to process the

sample using diluted hydrofluoric acid (HF, 1 to

3%) for about 20 hours. We successfully recove-

red residues inckiding radiolarians by chis pro-

cess, but the préservation was nor good enough

for détermination of spccics. The samc sample

was then again processed by diluted nitric acid

(HNO 3 , 1 to 2%) for up to 24 hours. After this

step, we were able ro obtain well-pre.scrved

radiolarian shells. Although otlier acids such as

hydrofluoric, hydrochloric or acetic acids were

tried lor the second step after HF, the best pré¬

servation was achieved by using nitric acid.

RAHI01.AR1AN FAUNA FROM ARROW

ROCKS AND GEOLOGIC AGE

OF BASALT-CHER'r SEQUENCE

IN THE WHANGAROA AREA

The limestone Ions sample (ARR-1) contains wclk

pre.ser\cd albaillellafian fauna. The fauna includcs

six spccies of genus Follicuçtdlm and cwo of genus

PseudoiübailUlh (Figs 4, 3). Ishiga (1986, 1991)

established Permian radiolarian zonation bascd on

die ranges of albaitlellarîans from mosfly bedded

chert seqtiences in Southwest lapan. His zonation

is applicable for the ARR-1 tauna, bccause many

albaillellarians from our sample were alrcady

included within Ishigas zonation.

Among these albalJlc!lartan.s wiih conicaJ shells

investigated by Ishiga (1986, 1991), Pseudo*

albailleUa fuiifornn^ (Holdsworth 6c Joncs,

1980), P aft. longicomis of Ishiga et aL (I982a)>

FoHicHcullus scholasticus Ormiston âc Babcock,

1979 and F. porreetns Rudenko, 1984 (= E jûpo~

nicm of Ishiga 1991) arc présent in our sample

ARR'l. Because both FoUicucidlus monacanthm

Ishiga & Imoto, J 982 (Ishiga et al. 1982b) and

spccics ot genus NeoalbaiUella Takemura 6c

Nakaseko, 1981 are absent in thi.s .sample, wc

correlate this fauna with Follicucullus scholasticus

zone of Ishiga (1986).

GEODIVERSITAS • 1999 • 21 (4)

755

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

Unit 8

Unit 7

Unit 6

Unit 5

Unit 4

Unit 2

Unit 3

-^ARR-7

-^ARR-1

Unit 1

Fig. 3. — Summarized géologie column of the Arrow Rocks. A, fold zone; B, siliceous mudstone; C, bedded siliceous mudstone and

chert; D, alternation of black shale and chert; E, bedded chéri; F, tuff; G, limestone; H, spllitic basait. ARR-1 and ARR-7 are the hori¬

zons where Permian radiolarians occurred (Takemura étal. 1998).

756

GEODIVERSITAS • 1999 • 21 (4)

Permian Radiolaria from Arrow Rocks, New Zealand

Following Ishigas zonation, rhe uppec limits of

the ranges of Psetidodlbaillella fitsiformis and

P. aff longivornîs are wichin Follicucullus mona-

canthus zone or lowcr. However, occurrences of

thèse cwo spccics in ARR-l are fe\v and they are

usually less weU preserved than Folïmtadlm. Ir is

possible that these two species might be rewor-

ked, or that the ranges might be longer than thaï

suggested by Ishig^s (1986) zonation.

The fauna in ARR-l can bcalso correlatcd to the

Follicucullus japonicus zone of Ishiga (1991)

because of the co-occurrencc of F. porrectus {-

F. japonicus) and F. scholasticus^ and because of

the absence uf F. rnonacanthus^ F. charveti

Caridroit ^ De Wever, 1984, F. hipartitus

Caridroit ôc r>e Wever, 1984 and NeoalbaiUdla.

According to the corrélation ol radiolarian zona-

lion wiili fusulinid and conodont zonations by

Ishiga (1986, 1990, 1991), the géologie âge of

Follicucullus scholasficus zone and F japonicus

zone is in the vicinity of rhe bonndar)' berw-een

Middle and Lace IVrniian.

Résides thcsc species, Kozur (1993) described

Cariver dorsoconvexus (herein treated as a species

of the genus Folliciiadlt4s) from Upper Permian

sequencc in -Sicily, Jraly, F sphaeriais n. sp. was

figured by Küwahara (1997) as Follicucullus sp.

A, which is présent in bedded chen of GA sec¬

tion in GujO'Hachiman Area, central Japan

These samples are wichin Neoalbatllella optima

and N. ornithoformis zones, indicating a l.are

Permian âge. The ranges of dicse two species,

Follicuadhis darsoconvexiis and F. sphaericus ii. sp.,

however, ,are not ctarified yet. Phcrelore, we

regard the géologie âge ol our samplc ARR-I as

Late Middle or EatJy Latc Permian.

lakcmiira et al. (1998) reporred Permian radto-

larians from a üniestone Icns (MAH-5) ai the

west end ol Mahinepua Pcninsiila (Fig. 2).

MAH-5 corUiiins Follicucullus porrectus Riidcnko

and Pseudoidhaillella (?) sp. T'hcy correlatcd this

samplc with ihc F monacantbiis zone ol Ishiga

(1986), and with the F japoniais zone of Ishiga

(1991), bcoiusc ol the absence ol other species

ol Follicucullus. The géologie âge ol this sample

is aiso neaj- the Middle/Late Permian boundary.

Rcccmly l.even & Granc-Mackic (1997) descri-

bed fusulinids from some limestone lenses within

spilitic basait at Wherowhero Point (Fig. 2).

These fusulinids Include Lepid^/litm shiramensis

Ozawa, 1925, Ncoschwagerina margaritue

Depmt, 1913 and Yabtina glvLma (Yabc. 1906),

and the fauna was correlatcd with the Yabeina-

Lepidoliiia zone. Leven & Grant-Mackic (1997)

regard the géologie âge of these fusulinids as

Midian, and mosi samples probably as Early

Midian. The Midian stage corresponds to the

Capitanian and late Wordian in Norch America

(Leven 6c Grant-Mackie, 1997) and Ishiga

(1990) correlatcd the fusulinid Yabcina-

Lcpidolina zone with chc radiolarian FolhcucuUus

numacanrhus and F. scholasficus zones.

Thus, the chrcc llmcstonc samples within spilitic

ba.salts from uorchern New Zealand show similar

géologie âges. Bedded chcris arc sometimes asso-

ciated with these basalts and arc characicristic of

océan floor sedimentary scquciices. indced, at

Arrow Rocks, bedded cherts comformably overlie

spilitic basait (Fig. 3). The âges of these cherts

are reporred Irnm rhree localitie.s in the

Whangaroj Area (Caridroit &C Ferrière 1988;

Adachi 1988; Takernura et al. 1998) to bc about

Lare Permian. Thcrelore, the âge of océan Iloor

sequencc represented by basait and cherr in the

Whangaroa Area is Middle to Late Permian.

The radiolarian fauna from Arrow Rocks

contains two new species oï Folltcncnllu^y

R sphaericus n. sp. and F. whangaroaensis n. sp.

The former was already figured by Kuwahara

(1997) from Japan, but the larier lias not hecn

reporied yei. These two species are cotnmon élé¬

ments within thi.s fauna, and they may reflecl a

significant faunal diflcrcnce in albaillcllarian dis¬

tribution between New Zealand and northern

hémisphère rcgion.s.

Leven &L Grani-Mackie (1997), however, aIso

maintained that the lusulinid launa Itom

Wherowhero Point showed a clear affînity with

those in the castern Paleotethys and Panthalassa

région, and that Üicse limestone blocics had been

moved from the original site of déposition.

Becau.se the radiolarian-beai ing limestones which

wc describe herein show similar géologie âge as

these fusulinid lime.srones, and because they ail

oceuf within a restricted area, the radiolarian

fauna from these samples musi originare from

near the région where the fusulinids were deposi-

ted. Therefore, the radiolarian fauna from Arrow

GEODIVERSITAS • 1999 • 21 (4)

757

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

Rocks originated in a low-latitude area of Middle

to Late Permian timc.

SYSTEMATIC DESCRIPTION

The following description was madc by rhe first

author, Takemura A, The type specimens are

deposited ar Hyogo University of Teacher

Education.

Subclass RADIOLARIA Müllcr^ 1838

Order Poi.YCYS'I lNA Ehrenberg, 1838

miend, Riedel, 1967

Suborder ALBAILLELLARIA Dcflandre, 1953

eintntd. Holdswonh, 1969

Family Ai^BAILLELLIDAE Deflandre, 1952

emend. Holdswonh, 1977

Remarks

Cheng (1986) classified Albaillellaria Into two

groups, Albaillellacea and Eoilicucullacea, based

on rhe presence of a cross-bar, Ehis criterion is,

however, applicable only for verv well-pre.served

specimens, and we cannot observe such fragile

parts in most Permian samples.

Kozur (1981, 1993) and Kozur Mostlcr

(1989) described many généra for Permian

albaillellarians with conical shells. His classifica¬

tion seems to be so minute that sornetimes we

cannot make genenc assigtiment. In this paper,

the first author thorefore adopis four généra for

Permian albaillellarians, Albaillella Dcflandre,

1952, Psiudücilbctilhllü l loldsworth & Jones,

1980, F(dlkui'u/ls4s Oïm\stvn & Babcock, 1979,

and NeaaibailLUa Takemura & Nakaücko, 1981,

same as Ishiga & Imoto (1980), Ishiga (1982)

and Ishiga et al. (1982a, b).

Genus Folliciicullus

Ormiston Ôd Babcock, 1979

Foliicucullus Onvàsxon &r Babcock, 1979: 332.

Kozur Mostler, 1989: 181-182.

Cariver Kozur, 1993: 108-109.

LadsusY^oaxi, 1993: 109.

Type SPECIES. — Follicucullus ventricostis Ormiston &

Babcock, 1979.

Rkmarks

Mosi Permian taxonomie works followed rhe ori¬

ginal définition of Genus Follicucullus made by

Ormiston &: Babcock (1979). Only Kozur &

Mostler (1989) and Kozur (1993) divided ihis

groupv with descriptions of three new' généra.

However, rheir divusion are so minute thaï we

cannot use rhem to assign a genus ro poorly pre-

served specimens. Tberefore, for this paper, the

autlroi regards rhcwsc thrcc gênera as junior syno-

nyms of the genus Follicucullus.

The author generally follows ihe spécifie division

of Follicucidlus csrablishcd by Ishiga (1991), who

lumped forms of this genus into six specics from

Permian sédiments in Japan. *l'he>' are F mona-

canthus Uhiga Imoro, 1982 (Ishiga et al.

1982b), F. ventricosus Ormiston Babcock,

1979, F. charveîi Caridroit De Weven. 1984,

F. scholasticnc Oïxy\hxon ôc Babcock, 1979,

F/fometus Rudenko, 1984 (= F. japonicus Ishiga,

1991) and F. bipartitus Caridroit &: De Wever,

1984. Other than these forms, three species

A darsocortvexus (Kozur, 1993), F. sphaericus

sp. and R whangaroaensis n. sp. were distingui-

shed in ihe sample ARR-1.

Follicuculltu scholasticus

Ormiston & Babcock, 1979

(Fig. 4A, R)

Follicucullus scholasticus Ormiston & Babcock, 1979;

333-334, pJ. l.figs 1-5.

J'ollicucHlius scholasticus Ormiston & Babcock mor-

phorj'pe I - Lshiga 1985: 180, 181, pl. I, figs 15-21.

KEMARKS

Ishiga (1984) proposed rwo morphotypes wiihin

this species. F scholasticus morphotype I bas

simple conical shell without undulation and it

resembles forms described by Ormiston &

Babcock (1979) under the name of this species

(Ishiga 1985). In this paper, ihc author follows

Ishigas taxonomy and F. scholasticus is used for

forms with simple conical shell without undula¬

tion.

Kozur & Mostler (1989) proposed a new genus

hhigaconus for Follicucullus forms without shell

undulation. However, the distinction of this spe¬

cies and R porrectus is sornetimes difficult because

758

GEODIVERSITAS • 1999 • 21 (4)

Permian Radiolaria from Arrow Rocks, New Zealand

Fig. 4. — A, Follicucullus scholasticus Ormiston & Babcock, 1979; B, Follicucullus scholasticus Ormiston & Babcock, 1979;

C. Follicucullus porrectus Rudenko, 1984; D, Follicucullus porrectus Rudenko, 1984; E, Follicucullus ventricosus Ormiston &

Babcock, 1979; F, Follicucullus ventricosus Ormiston & Babcock, 1979; G, Follicucullus dorsoconvexus (Kozur, 1993);

H. Follicucullus dorsoconvexus {Kozur, 1993); I, Pseudoalballlella fusiformis (Holdsworth & Jones, 1980); J, Pseudoalbaillella aff.

longicornis Ishiga & Imoto, 1980. Scale bars: 100 pm.

GEODIVERSITAS • 1999 • 21 (4)

759

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

the undulation or tripartite division of shells is

often unclear.

Follicucullus porrectus

Rudenko, 1984

(Fig. 4C, D)

Follicucttllus porrectus Rudenko» 1984 — Beljanskij,

Nikitina Rudenko 1984, pl. 8, figs3* 10.

Follicucullus scholasticus Ormisron & Babcock mor¬

photype Il - Ishiga 1984: 430, 431, pi. 1, figs 1-8.

Follicucullus japonicus Ishiga, 1991: 108-111, pl. 1,

figs 1-22, pl. 2, fig. I.

Remarks

In this paper, rhe author uses this species name

for intermédiare foems between F. scholasticus

and F. ventrkosus. Therc arc much variations ol

shell shapes within rhîs spccies trom samplc

ARR-l, saine as described by Ishiga (1991). Such

variation.s .seem ro be couünuous Irom simple

conical shapc of F. schoLmicus ro clearly tripartiie

F. ventricosus wirh inflaied sphcrical pseudo¬

thorax. Therefore, it is somerimcs difFicult to dis-

tinguish this species from die other cwo species.

FoUicuetMus tfe7itncosm

Ormiston & Babcock, 1979

(Fig. 4E, F)

Follicucullus iferirricosus Ormisron & Babcock, 1979:

332-333> pl. 1, figs 6-14.

RKMARK-S

Ishiga (1991) made a compari.son between

R porrectus (= F. japonicus) and F. ventricosus

under the dc.scripcion of the former species. He

used the widrh/lengrh ratio (W/1 ) of shells,

strongly inflated pseiidothorax and existence of

groove (sinus) on pseudorhorax as criteria to dis-

tinguish these two species

F ventricoms of the présent scudy lias strongly

inflated and subspherical pseudorhorax and a

distinctly tripartite conical shell. However, there

is usually no groove on rhe dorsal sidc of pseudo¬

thorax as seen in F. dorsoconvexus. The author

tcntativcly include tripartite forms without

grooves on subspherical pseudothorax wîthin

F ventricosus in iliis paper. Tlie dillerencc be¬

tween this species and F. porrectus is only the

degree of inflation of rhe pseudorhorax, and the

variation between rhem seems to be continuous.

Folltcuctillus dorsoconvexus

(Kozur, 1993)

(Fig. 4G, H)

Cariver dorsoconvexus Kozur, 1993: 109, pl. 1, figs 15-

17, 19.

Remahks

Ktjzur (1993) proposcd a new genus Cariver for

Follicucullus species wich curved shell and apertu-

re perpendicular to che shell axis. If we adopc

such minute generic divi.sioii, wc can assign

gênera only for well-prcscrved specirnens.

F dorsoconj^exus rcscmblcs to /: ventricosus. Both

two species hâve tripartite shell wich inflated

pseudoabdomen and sinus on ihe dorsal sidc of

the shell. The aperrurc is somecimes nor cxactly

perpendicular to the shell axis, because the dorsal

side of the shell wall becomes shorter (Fig. 4G).

Follicucullus sphaericus

Takemura, n. sp.

(Figs 5A-F, G)

Follicucullus sp. A. — Kuwahara 1997, pl. 2, fig. 8.

Follicucullus (?) sp. - Takemura et ai 1998, pl. 1,

fig. 13.

Types. — Holotypc HUTE-R-4024 (Fig. 5A), para-

types HUTE-R-4()25 (Fig. ^B) and HUTE-R-4026

(Fig. 5D).

Etymoi.OCY. — The .species name was derived from

the characteristic .shapc of this species.

MF.ASUKEMFNTS. — Lcngth of shell, 260-350 pm;

iength of upper conical part, 120-180 pm; widch of

shell, 160-230 pm; width of the base of upper conical

part> 50-110 pmrmeasured in 28 spécimens.

De^scuiimion

Imperforate and smooth shell composed of two

parts, upper conical part and lower part with

flattened hcmi,spherical shape. The upper conical

part slcndcr, and straight or .sometimc.s slightly

curved dorsally. The lowcr portion of tins conc

olten slightly inflated. The inflated and curved

lower part large with smooth surface and

760

GEODIVERSITAS • 1999 • 21 (4)

Permian Radiolaria from Arrow Rocks, New Zealand

Fig. 5. — A, Follicucullus sphaericus n. sp , right laleral view, holotype (HUTE-R-4024): B, Follicucullus sphaericus n. sp.. left latéral

view, paratype (HUTE-R-4025): C, Follicucullus sphaericus n. sp., a broken specimen showing the inner surface of the intlated lower

part, a hook-shaped Irace of the Inner wall can be observed, D. Follicucullus sphaericus n. sp., right latéral view, paratype (HUTE-R-

4026); E, F, Follicucullus sphaericus n. sp.. apertural view of parily broken specimen, a tube-like ventral spine arises upward trom

the edge of bended wall; G, Follicucullus whar}garoaensis n. sp., right laleral view, holotype (HUTE-R-4027); H, Follicucullus whan-

garoaer)sis n. sp.. left latéral view, paratype {HUTE-R-4028); Follicucullus whangaroaensis n. sp., ventral view, paratype (HUTE-R-

4029). Scale bar; A. B, D, E. G-l. 100 pm; C. 83 pm; F, 20 pm.

GEODIVERSITAS • 1999 * 21 (4)

761

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

Upper part

Lower part

Fig. 6. — Schematic diagram of FollicucuHus sphaericus n. sp. The inflated lower part of the Shell is so strongly curved that the aper-

ture opens upward. WIthin the inflated lower part, the Shell wall of ventral side is curved and tumed upward. Then, both dorsal and

ventral spines aiso extend upward.

showing a semicircular shape in latéral view. Two

apertures présent on the lower part. A large aper-

ture situated at the ventral side of the upper

conical part and opening upward. This large

aperture subelliptical in shape and tapering dis-

tally hom the upper part. One more small aper-

ture opening at the distal end of the shell in

welhpreserved specimens. This smalJ aperture

teardrop-shaped and opening loward the ventral

side of the shell, with srnall dorsal spine or flap

originating the lowet end of this aperture. Insidc

the shell wall of the inflated and curved lower

part, the ventral side of the shell wall of conical

part strongly curved and turned upward. Tube-

like ventral spine extending upward from the

center of the turned end of the wall.

Remarks

In the broken specimen (Fîg. 5C), the trace of

the shell wall could be observed on the inner sur¬

face of the lower inflated part of the shell. The

trace is smoothly continuous from the upper

conical part and somewhat inflated within the

lower part, which resembles the inflated pseudo-

thorax of F. porrcctus or F. ventricosus. Then, the

trace is curved -strongly and turned upward.

Frorn the turned end of this wall, cylindrical

tube-like spine is arises upwanl inside the shell

wall (Figs 5E, F, 6). This skeicton is homologous

wirh a ventral spine or flap of other FollicucuHus

spccies. A small dorsal flap aIso exists helow the

small aperture on the distal part of the lower

shell.

The upper conical part often shows slighr infla¬

tion on its lower portion similar to the pseudo-

thorax oi F porrectus or F. ventricostL^. Therefore,

the upper conical part of F. sphaericus n. sp. is

homologous either with the apical corn jlone or

with both apical cône and upper pseudothorax of

the other FollicucuHus species. The lower shell

762

GEODIVERSITAS • 1999 • 21 (4)

Permian Radiolaria from Arrow Rocks, New Zealand

shape of this new species was formed by the

strong bcnding and inflating of the pseudothorax

and pseudoabdomen of the other species like

F. porrecws or E dorsoconvexus.

R sphaericus n. sp. differs from ail the other spe¬

cies of Follicucidluî in its flattened hemispherical

and curved shell shapcv its aperture opening

upward, and boih ventral and dorsal flaps arising

upward. The characterisric shape of this species

resembles that of PscudonlbfliLlelLz bulhasa Lshiga

(Ishiga 1982: 335, pl. l, figs 8-13, 16, 17). Ihe

strongly intlated and curs^cd pseudoabdomen of

P. bidhosa is quite similar to the lower part of

F, sphaericus n. sp., except for a small flap of the

former species. F sphaericus n. sp. does not hâve

pseudothorax and wings observed in Pseudo-

alhaillella, P. bidhosa ranges from Laie Carboni-

ferous to Early Permian in âge, and there should

be no direct phylogcnetic relationship berween

these two species. /T sphaericus n. sp. should be

cvolvcd frorn the other Follicucullus species like

F porrectus or F. dorsoconvexus.

Follicucullus whangaroaensis

Takemura» n. sp.

(Fig. 5G-I)

Follicucullus — T-ak&mnx^ et ai 1998. pl. 1, fig. 14.

Types. — Holorvpe HUTE-R-4027 (Fig. 5G), para-

type HUTE-R-4028 (Fig. 5H) and HUTE-R-4029

(Fig. 51).

Etymology. — The species name is after Whangaroa

Area in Northland, New Zealand, where Arrow Rocks

is located.

Measurements. — Lcngth of sheil, 240-330 pm;

length of apical cône, 130-180 pm; width of shell, 70-

110 pm; width of the base of apical cône, 60-70 pm;

measured in 12 specimens.

Description

Impcrforate conical shell slightly curved ventral-

ly, and undulated at the lower part with two dis¬

tinct inflated rings. Apical cône wirh smooth

surface and with a length more than half of the

total shell. Apical cône slightly flattened laterallv

and curved ventrally. In some specimens, vague

ring-like inflation observed at the lowest part of

apical cône. The lower part of the shell distinctly

undulated in dorsal or ventral view. Two rings

inflared laterally berween apical cône and apertu-

ral région, with circular shape in transverse sec¬

tion. Distinct furrows existing berween the two

rings, and berween the lower ring and inflated

apertural région. In dorsal or ventral view, shell

distinctly undulated becau.se of ihe.se ring.s and

furrows. A vague furrow may dlvide apical cône

and the upper ring, ’Fhesc furrows not présent or

becoming weak at the dorsal and ventral sides of

this ring région. The outline of the shell not

undulated distinctly in latéral view. The aperru-

ral région, the Jowermost part of conical shell,

inflated like rings. Two small spiiics or flaps, dor¬

sal and ventral ones, arising obliquely downward.

Remarks

F ivhangaroaensis n. sp, differs from the other

species ol Follicucullus by its banded lower shell.

This kind of rings has never been observed in the

other FoUicucullus spedes. The author included

this new species wiihin genus Follicucullus becati-

se of the similârity of its shell .shape to other

Follicucullus^ sucii as F scholassicus or F. pofreetns.

The ring région of this species may correspond

with inflated pseudothorax of rhe other species.

Similar structure ta this undulated shell with

rings was observed in the pseudoabdomen of

Pseudoalbaillelld globosa Isliiga & linoio (Ishiga

et al. 1982b). P. globosa has cite ring and inflated

apertural région below the spherical pseudo¬

thorax with two wings. The author considers

that there is no direct phylogcnetic relationship

between thcsc two species.

Genus Pseudoalbaillella

Holdsworrh & Jones, 1980

Pseudoalbaillella Holdsworth & Jones, 1980:

284. - Ishiga, Kîto & Imoto !982b: 274, 275.

1‘YEE Si'ECIES. — Pseudoalbaillella scalprata

Holdsworth & Joncs, 1980.

Remarks

Ishiga & Imoto (1980), Ishiga (1982) and Ishiga

et al. (1982a, b) assigned this genus for Late

GEODIVERSITAS • 1999 • 21 (4)

763

Takemura A., Morimoto T., Aita Y., Hori R. S., Higuchi Y., Spôrli B. K., Campbell H. J., Kodama K. & Sakai T.

Paleozoic albaillellarian.s wirh conicaK usually

imperforate and tripartite shelU and with two

wings on thc inflated pseudoahdomen. The

aurhor follows thcir taxonomy of this genus.

Pseudoalbaillella fusiformis

(Holdsworth & Jones, 1980)

(Fig. 41)

Parafollîcucidlusfitstfonvis Holdsworth & Jones, 1980:

285, Figs D, E.

Pseudoalbtullella fusiformis (Holdsworth &

Jones) - Ishiga, Kiro & Imoto 1982b: 275, 276, pl. 4,

figs 10-12.

Remarks

Most specimens of this species exrracted from

ARR'l are more or less broken. The préservation

of this species seerns to be wor.se than thar of

Follicucullus.

Holdsworth &: Joncs (19S0)‘ dcscribed this spe¬

cies as ParafoUiaictillxis fusiformis and they regar-

ded thc existence of a ring-like prepseudo-

abdominal segment as a criterion ol lliis genus.

However, some spécimens irom ARR-1 hâve no

ring on their pseudoabdotnent

Pseudoalbaillella aff. longicomis

Ishiga & Imoto, 1980

(Fig. 4J)

Pseudoalbaillella sp. afF P. longicomis Ishiga &

Imoto - Ishiga, Kito & Imoto 1982a: 18, pl. 3,

fig. 11; 1982b: 275, pl. 2, Figs 1-7.

Remarks

Most specimens of this form are broken and

their préservation is usually poon The total shape

and size of this form b almost same as the upper

hall of P. fusiformis.

Ackno wledgemen ts

We thank Peter, Judith and Jonathan Hall of

Tauranga Bay Motel for their kind help to our

survey. We thank Drs Jean-Pierre Caulet and

Patrick De Wever for their great effort in organi-

zing InterRad VIIl Meeting at Paris and to edit

this volume. We also thank Dr Martial Caridroit

for reviewing our manuscript. This research was

supported by Monbusho grant-in-aid (No.

07041085) for rhe International Scientific

Research Program 1995-1996.

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36: 272-281.

Kozur 11. 1981. — AJbaillellidca (Radiolaria) aus dem

Uiucrperm dos Vonirals. Geologisch-Palâontolo-

gische Mineilungm Innsbruck 10: 263-274.

— 1993. — Upper Permian Radiolarian.s fmin the

Sosio Vallev j'Vrca, Western Sicily (liaJy) and from

the Uppermost Lamjr L.irncstone of West Texas.

Jh. Geol B.^A. 136: 99-123.

Kozur H. & Mostlcr FL 1989. — Radiolarien und

Schw^ammskleren aus dem Cntetpcrm des

Vo rurals. Geologisch-PalHoutologische Minr/lungen

InnsbrttcF Sonderband 2: 147-275.

Kuwaluira K. 1997. — Llppcr Permian radiolarian

biostratigraphy: Abundance zones of Alhaillella.

News of Ùiakü Micropaleotmlo^sis, Spécial Volume

10; 55-75 (in Japanese wirh English anstract).

Leven E. Ja. & Grant-Mackio J. A. 1997. — Permian

fusulinid Foraminifera from Wherowhcro Point,

Orua Bay, Northland, New Zealand. Nnv Zealand

Journal ofGeology and Geophysics 40: 473-486.

Muller j. 1858. — Über die Thalassicollcn, Poly-

cystinen und Acanrhonietren des Mittelmceres.

Abhandfungcn der KHaii^lichen Akademie der

WJsscfbùhapen zu Berlin, ]Zt\rc: 1858: l-62_

Nazarov B. B. & Ormiston A. R. 1986. — Radiolaria

frorn the Laie Palcozoïe of the Southern Lhal.s,

LJSSRand West Texas, USA. Micrapaleontology 31:

1-54.

Ormiston A. R. &i Babcock !.. C. T.E'V. — Follicu-

cullns, new radiolarian genu.s from the Guadolupian

(Permian) Limar Limestone of the Delaware Basin.

Journal of Paleontology 53; 328-334.

Ozawa Y, 1925. — PaTconiological and straiigraphical

studios on tlic Permo-C3rbt>iiiroTous limestone of

Nagato. Pan 2, Paleonrolog)’ journal of the College

oJ Science, InipchaJ Ijnh'tr.siry of Tokyo 45: 1-90.

Riedel W. R. 1967. — Proruzoa (Subclass Radiolaria),

in Harland W. B, ei al. (cd.s), The Fossil Record, The

Geolagtcal Societ)' of London 291-298.

Takemura A.> Aita V-, Hori R. -S., fiiguclii Y., Sporli

K. B.» Campbell H., Kodairta K. & -Sakai T.

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phy of the Arrow Rocks, and géologie âge of the

norrhern parr of rhe Waipapa Tertane. New

Zealand. News of Osaka AiicropaleontologistSy

Spécial Volume, 11; 47-57.

Takemura vV. bc Nakaseko K. 1981. — A new

Permian radiolarian genu.s from the Tamba Bclt,

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the Palaeontoiogical Society of Japan, New Sériés

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Yabe H. 1906, — A conrrihuiion ro rhe genus

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Univensity ofTokyo 21: 1-36.

Submittedfor pîiblication on 24 February 1998;

accepted on 1 July 1998.

GEODIVERSITAS • 1999 • 21 (4)

765

Remerciements/Acknowledgements

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Références bibliographiques

Denison R. H. 1978. — Placodermi. in Schultze

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Marshall C. R. 1987. — Lungfish: phylogeny and

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Schultze H. P. 1977a. — Tlie origin of the tetra-

pod limb within ilic rhipidistian fishes:

541-544, in Mccht M. K., Goody P. C. Ôc

Hecht B. G. (cds), Aiajor Patterm in Vertebrate

Evolution. Plénum Press, New York and

London.

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References

Denison R. H. 1978. — Placodermi, in Schultze

H. P. (ed.), Handbook of Paleoichthyology^

Volume 2. Gustav Fischer, Stuttgart, 128 p.

Marshall C. R. 1987. — Lungfish: phylogeny and

parsimony, in Bemis W. E., Burggren W. W.

& Kemp N. E. (eds), The Biology and

Evolution of Lungfishes, Journal of Morphology

1: 151-162.

Schultze H. P. & Arsenault M. 1985. — The pan-

derichthyid fish Elpistostege: a close relative to

tetrapods? Paleontology 28: 293-309.

Schultze H. P. 1977a. — The origin of the retra-

pod limb within the rhipidistian fishes:

541-544, in Hechr M* K., Goody P. C. &

Hecht B. C. (eds), Major Patterns in Venebrate

Evolution. Plénum Press, New York and London.

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1999 • 21 (4) suite

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Zoological Record

geodiversitas

http://www.mnhn.fr/publication/

Kiessling W., Scasso R., Zeiss A., Riccardi A. C. & Médina F

687 • Combined radiolarian-ammonite stratigraphy for the Late Jun

implications for radiolarian stratigraphy

Mekik F. A., Ling H. Y., Ôzkan-Altiner S. & Altiner D.

71S • Preliminary radiolarian biostratigraphy across the jurassic-Cretaceous boundary from

Turkey

Takahashi O.

739 • Late Cretaceous (late Campanian-early Maastrichtian) radiolarian biogeography; a review

V. :

Takemura A., Morimoto T., Aita Y., Horl R. S., Higuchi Y.,

Spôrli B. K., Campbell H. )., Kodama K. & Sakai T.

751 • Permian Albaillellaria (Radiolaria) from a limestone lens at the Arrow Rocks in the Waipapa Terrane

(Northland, New Zealand)

geodiversitas

http://www.mnhn.fr/publication/

InterRad VIII, Paris/Bierville 8-13 septembre 1997

edited by Patrick de Wever & Jean-Pierre Caulet

De Wever R & Caulet J.-P.

SOI • Introduction

Aita Y. & Bragin N. Yu.

503 • Non-Tethyan Triassic Radiolaria from New Zealand and northeastern Siberia

r ^

Bak M. & Bak K.

S27 • Corrélation of the early Albian-late Turonian radiolarian biozonation with planktonic and

agglutinated foraminifera zonations in the Pieniny Klippen Belt (Polish Carpathians)

Bragin N. Yu. & Krylov K. A.

539 • Early Norian Radiolaria from Cyprus

Bragina L. G.

571 • Cuboctostylus n. gen., a new Late Cretaceous spicule-bearing spumellarian Radiolaria from Southern

Sakhalin (Russia)

Braun A. & Budil P.

581 • A Middie Devonian radiolarian fauna from the Chotec Ümestone (Eifelian) of the Prague Basin

(Barrandian, Czech Republic)

Cortese G. & Bjorktund K. R.

593 • Radiolarians from the cyclic Messinian diatomites of Falconara (Sicily, Italy)

Danelian T.

625 • Taxonomie study of Ordovician (LIanvirn-Caradoc) Radiolaria from the Southern Uplands (Scotland,

u.K.) _ r

Ishida K.

637 • Radiolarians as tracers for provenance of gravels in Lower Cretaceous molasse (Outer Zone of SW

Japan)

Kamata Y.

657 • Lower Triassic (Spathian) radiolarians from the Kuzu area (Tochigi Préfecture, central japan)

m ^

Kemkin I. V. & Kemkina R. A.

675 • Radiolarian biostratigraphy of the jurassic-Early Cretaceous chert-clastic sequence in the Taukha

Terrane (South Sikhote-Alin, Russia)

Publication trimestrielle, décembre 1999. ISSN : 1280-9659

N’ d'inscription à la commission paritaire des publications et agences de presse ; 0902 B 0140S

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