Corrélations stratigraphiques

de la plate-forme européenne

dans le cadre du Programme Péri-Téthys

(Introduction générale)

Stratigraphie corrélations of European platform in the trame

of Peri-Tethys Programme (General Introduction)

Sylvie CRASQUIN-SOLEAU & Patrick DE WEVER

Une synthèse géologique des données disponibles

concernani les bassins et les systèmes pétroliers

installés sur les plates-formes qui bordent (ou

sont incluses dans) les chaînes téchysicnnes est

actuellement possible car ;

1. D’une part de nombreux géologues ont

récemment soutenu des thèses de doctorat

autour de la Téihys et de nombreux travaux de

synthèse ont été effetnués par differentes équipes.

Le plus souvent, seuls les concepts ont donné

lieu à publication alors que les donneex qui les

fondent ne sont pas aisément accessibles ; mais

elles sont disponibles en exemplaires à très faible

tirage et peuvent être analysées.

2. D’autre part, de nombreuses données indus¬

trielles sont légalement abordables (en général

dix ans après leur acquisition). Un certain

nombre ont été publiées dans un Mémoire du

Muséum national d'Uistoire naturelle (Peri-

Tethys Memoir 2, tome 17ü, 1996).

3. Enfin, l’ouverture des pays qui furent à écono¬

mie planifiée et accèdent à l’économie de marché

est de plus en plus nette ; les informations

deviennent accessibles et sont susceptibles d’être

compilées avec celles d’autres pays.

Cet état de fait permet l'établissement d’une syn¬

thèse de bassins. Cela nécessite :

1. De réunir les équipes qui disposent de Tinfor-

It is now possible to synthesize the available data

from basins and lheir associated petroleum

Systems which border (or are included in) the

Tethyan chains because:

1. Numerous geologiscs bave recenriy undertaken

doctoral thesis in régions arotind Terhys and

numerous synrbetic works bave been realized by

different teams. Often, only ihe concepts bave

been published and the data on which these

conclusions arc based, are not easily available.

2. Many data derived from induscry are legally

available, in general ten years after tbeir acquisi¬

tion. Some of rhese data bave been published in

a “Mémoire du Muséum national d’Histoire

naturelle” (Peri-Tethys Memoir 2, tome 170,

1996).

3. The conntries which previously had planned

économies hâve begun to be more opened to

market forces and those data are becoming more

accessible and can now be synthesized with those

of other countries.

Tbis situation allows the synthesis of basins in

terms of tbeir petroleum sj'stems. Tbis nécessi¬

tâtes:

1. The création of teams which bave at tbeir fin-

gertips che data which were not available furmerly.

2. To détermine a chronological scale and a com-

mon vocabulary between the different cultures.

GEODIVERSITAS • 1997 • 19(2)

169

Crasquin-Soleau S. & De Waver P.

mation (données de base des thèses, données

tombées dans le domaine public.., ).

2. De déterminer une échelle chronologique et

un vocabulaire communs aux différentes cul¬

tures. Les corrélations stratigraphiques sont

actuellement un élément prioritaire à toute ten¬

tative de synthèse associant les trois lamilles de

données évoquées ci-dessus.

L’idée du travail est d’examiner le comportement

des bassins sédimentaires péri-iéthysiens à la

lumière des réseaux de contraintes successifs asso¬

ciés à la fin de forogenèse varisque, à l’ouverture

de la Téthys puis à sa fermeture entre TEurasie et

l’Afriquc-Afabic.

Le Programme Péri-Téthys concerne les régions

comprises, au nord en Europe, entre l’AtJantique

et l’Oural, au sud, en Afrique-Arabie-Moyen

Orient jusqu’à l’océan Indien. Le présent travail

concerne uniquement les bassins épi-cratoniques

au nord de la Téthys.

La synthèse finale se présentera sous forme d’un

atlas de vingt-deux cartes paléogéographiques et

de leurs légendes. L’essentiel portera sur les

paléoenvironnemencs et le .synchronisme des

objets et des étapes physiques.

L’initiative de ce Programme provient d’Europe

occidentale ; le Programme Téthys (1989-1993)

a conduit à une synthèse de l’océan téthysien et

de ses maires d'Amérique cennale au travers des

chaînes alpines et himalayennes jusqu’aux

Philippines, pendatn 2^0 Ma (du Permien termi¬

nal au lorconicn). Au noyau de base, où les géo¬

logues français étaient largement représentés, se

sont joints au cours du Programme de nombreux

géologues européens.

Le Programme Péri-Téthys associe à ce noyau

des équipes importantes de divers pays d’Europe

occidentale (Italie, l^lys-Bas, Allemagne, Suisse,

Belgique, Royaume Uni...) et des géologues de

chacun des pays oii sont conduites les études.

Aujourd'hui que les t>pportuniiés scientifiques

sont facilitées entre chercheurs des pays de l’Est

et de l’Ouest, des solutions à de nombreux pro-

At the présent rime, rhe problcm of stratigraphi-

cal corrélations is rhe critical aspect for ail

arrempts which try to synthesize rhe rhrec types

üf data mentioned above.

The work purposc is co c.xatninc chc behaviour of

Peri-Tcthyan sedimentary basîns in the light of

the framework provided by the end ot the

Variscan Orogeiiy, the opening of the Terhvs and

finally its clos^ure between Eurasia and the

Arabian-Afncan plates.

The région covered by the Peri-Tethys

Programme has been limitcd in the north, in

Europe, to the région between the Atlantic

Océan and the Urals and in the sourh, in Africa

Arabia-Middlc East as far as Indian Océan.

The présent work is dealing only with the basins

to the north of the Téthys.

The final rcsults will be presenred in an atlas of

csventy-two palaeogeographical maps, with their

legend. These maps will include palaeoenviron-

menral interprétations. Synchtonism of objects

will be examined as far as possible.

The initiative for this Programme dérivés from

Western Europe: rhe Terhys Programne (1989-

1993) led to a synthesis of the Terhyan Océan

from rhe margins of Central America via rhe

Alpine chain.s and ihe Himalayas to the

Philippines diiring 250 million years (end

Permian to Torconian). During the Programme

scveral European geologists hâve been added to

the initial cote which was dominated by rhe

French. The Peri-Tethys Programme has added

many teams working in such countries as Italy,

the Neiherlands, Germany, Switzerland,

Bclgium... This group has conracred geologists in

other countries where there were relevant studies.

Now thac scicntific cxchangc is easicr between

Eastern and Western worke/s the solutions to

many .stratigraphie problems may be lound

through joint projects and enablc rcsearchcîs to

compile a more complète fossil record and allow

interested \VQrker-s to dçvclop models thaï will

facilitate more accurate interprétations of gcolo-

170

GEODIVERSITAS • 1997 • 19(2)

blêmes stratigraphiques pourront être apportées

par le biais des projets communs et permettre

aux chercheurs d’établir des inventaires plus

complets et par là significatifs, puis d’établir des

modèles qui faciliteront des interprétations affi¬

nées des bassins géologiques. Notre objectif est

de faire des analyses biostratigraphiques des bas¬

sins un outil plus performant à la fois pour les

chercheurs fondamentaux et appliqués. Des syn¬

thèses taxonomiques et stratigraphiques existent

aujourd’hui pour des régions téthysiennes, mais

souvent aucune corrélation n est possible avec des

aires géographiques orientales sous influence

boréale. Cette lacune dans nos connaissances

est due à la fois aux domaines paléogéogra¬

phiques différents (Boréal vs Téthysien) et au fait

que la plupart des données boréales de l’Est

avaient été acquises dans les pays de l’Est où les

méthodes et les moyens techniques étaient diffé¬

rents.

gical basins. The goal is to make biostratigra-

phical basin analyses a more usefui tool both for

industry and for academies.

Taxonomie and stratigraphie synthèses are publi-

shed from Tethyan régions but often no corréla¬

tion is possible with geographical areas which

were under Boréal influence. This gap in our

knowledge results from different palaeogeogra-

phic domains (Boréal vs Tethyan) and the fact

that much of the Boréal data was acquired in eas-

tern countries where methods and technical

means were different.

GEODIVERSITAS • 1997 • 19(2)

171

Moscovian and Artinskian rocks in the frame

of the cyclic Permo-Carboniferous deposits

of the Garnie Alps and related areas

Gian Battista VAI & Corrado VENTURINI

Dipartimento Scienze Geologiche,

Via Zamboni 67, 1-40127 Bologna (Italy)

Vai G. B. & Venturini C. 1997. — Moscovian and Artinskian rocks in the frame of the cyclic

Permo-Carboniferous deposits of the Garnie Alps and related areas, in Crasquin-Soleau S.

& De Wever P. (eds), Peri-Tethys: stratigraphie corrélations. Geodiversitas 19 (2) :

173-186.

KEVWORDS

Palaeogeographic maps,

guidclincs,

Icgcnd,

low and iiigli Ircquency cycles.

lectonics,

eustaiism,

parasequenccA,

Gzhelian,

corrélation,

Southern Alps,

Adriatic Sea,

ABSTRACT

Guidelines and legend for rhe Moscovian and Artinskian maps to be produ-

ced within the Peri-l ethys Programme are presenced. An updared review of

rhe most important composite .scction.s exposed in different parts of the

Garnie Alps and drillcd in the northern Adriatic Sea is presented. The sec¬

tions spanning a large part of the Mid-Lare Garboniferous co terminal

Permian tinte interval are corrclaied so as to show the major .sediinenraiy

cycles and rhe main régional ircnd.s of icctonic vs eu.staric .sea level changes.

High frequency cyclidty is aiso siimmarizcd in rerms of parasequences, espe-

cially for the Gzhelian stage, although the entire Pontebba Supergroup

(Moscovian to Artinskian) was known for many décades as a classic cyclic

sédimentation area.

MOTS CLÉS

cartes paléogéographiques,

directives,

légende,

cycles à faible et haute fréquence,

recion ique,

eu.statismc,

paraiéqueiitX'S,

Czhelieii.

corrélation,

Alpes méridionales,

mer Adriatique.

R^UMÉ

Le schéma directeur et la légende des canes du Moscovien et de l'ArtinsIden

qui seront réalisées dans le cadre du Progiammc IMri-Téthys sont proposes.

Nous présentons ici une révision des coupes composites les plus importantes

des Alpes Carniques et des forages du nord de la Mer Adriatique. Les coupes,

qui s’étalent sur une grande partie du Carbonifère moyen-supérieur au

Permien terminal, sont corrélées et montrent les principaux cycles sédimen-

taircs ainsi que les modifications lectono-eusrariques majeures. Une cyclicité

haute fréquence est également résumée en termes de paraséquences, surtout

au Gzhelien, bien que le Super-Groupe de Pontebba (Moscovicn-Aninskicn)

soit connu depuis plusieurs décennies comme une région à sédimentation

cyclique.

GEODIVERSITAS » 1997 • 19(2)

173

Vai G. B. & Venturini C.

FOREWORD

Beforc entering rhc copie of this paper, an intro¬

duction is needed to provide the aim, legend,

and guidelines according to which the présent

and the following stratigraphie contributions

(Pasini & Vaij Di Stefano Gullo, Cassinis,

Cassinis ôc Ronchi, Vai, Geluk, ail in iliis volu¬

me) have beeti subinitied lo ihe hoc working

group, in view of ihe compilation of chc palaco-

geographic maps of rhc Moscovian and

Artinskian wkhin the ainis and chc scope of the

Peri-Tethys Programme (PTP). Further contribu¬

tions are expecied and welcome.

Guidemnrs

The contributions provide original and/or upda-

ted stratigraphie rough data on the Moscovian

and/or/io Artinskian time slices in the different

areas within ihe scopc of the PTP, mainly as spot

columnar sections, with the aim to acr as valida¬

tion data points for rhe following map recons¬

truction:

1, The Moscovian Map, focusing ihe Age inter¬

val (abour 3)2-305 Ma) and includtng additio-

nal information iip to rhe top of the

Carboniferous (abour 296 Ma)

2, The Artinskian Map, focusing the

Artinskian f Bolorian Age inrerval (about

280-273 Ma) and including additional informa¬

tion down to rhe base of the Perniian (about

296 Ma).

The Moscovian Stage is used here as roughly

represented by the Aljutovelta aljutovica to

Fusulitia cylindrica fusulinid zones, by the

ïdiognathotdes marginodosus to ïdiognathodus

obliquuS'Neognathodus roimdyi conodont zones,

and by the Paralegoceras to Wellerites ammonoid

zones.

The Artinskian + Bolorian Stages are used here as

roughly corresponding to rhe Chalaro-

scbwagerina solitu» Pamhintt, Ch. (-'Pseudo'

fïisuUna") viilgiirh, Aihellinii dyhrenfurthi and

Alisellina parvîcostaui fusulinid zones, lo the

Streptogmithodus artitukiemis^ Sioeetog>iathus whF

tei, Neôstieptog}iathodî4s pcquopensu and N. leono-

vae conodont zones, and are characterized by the

new fusulinid généra Mesosihubenella,

Toriyamaia, Pracsknnierelln, DarvdselLt and by

the ammonoid généra Artinskia. KitrgalUes,

Almites, Cardiclla^ Paragathiceras. ArUtoccraîoides,

Pseudogastrioceras. The selccted lare early Petniian

time bas some advantages: it has a duration

almosr similar ro that ot the Moscovian; it is clo-

sely équivalent of the Chinese Chihsian and

ptaciically overlap with the Yachcash-Boloi* fau-

nal step of Leven (1993) comprised between the

top of Sakmarian and the base of Kubergandian;

it minimizes rhe imprécision deriving from the

poor corrélation and définition level of indivi-

dual stages involvcd.

le is preferred to receivc contributions coordina-

red in a .set of sections by couniry or group of

coLinities (such as e.g.: France, Bclgium, UK,

Ciermany, Poland Hungary, Austria + Tchekia,

Bulgaria t Rumania, foimcr Yugoslavia, Turkey,

Creece, Iraly Spain, NW Africa, I.ybia, Central

W Africa, Middle F.ast ^ Arabia, Iran,

Russia + Ukraiaa, Kazaldistan, a.s.o.). Flowever,

.submissions provided by independent indlvi-

duals or rescarch groups are also M^clcome.

The contributions consist mainly of a set oïspot

columnar sections (.stratigraphie columns), possi-

b!y correlaied on a stratigraphie chart (scc fi.

Ziegler 1988), possibly accompanied by location

and/or simplified gcological maps. and illustrared

by a concise cxplanatory text. ITie text shall not

excecd ten doublc-spaccd typed pages (or five

printed pages). Columnar sections, corrélation

charts (one or more if needed) and locafion/geo-

logicai maps must be drawn on A4 .sized .sheets

allowing final print réduction up to 50%. Each

iiidividual map drawing must contaln a graphie

scale.

Columnar sections are to be drawn and correla-

ted on rime/space (chronosiraiigraphic) dia-

grams. The thickness of the different litho-

stratigraphie units will appear from separace

labelling in a .side-column and from the text. The

vertical axis of chc columnar sections (time) will

adopt the geologicul cime .seule shown in the next

heading.

Each individu;d columnar section (represenring a

rrtie spot-like section expostd in tlie field or

drilled by a well, or a composite section whose

174

GEODIVERSITAS • 1997 • 19 (2)

Cyclic Permo-Carboniferous of the Garnie Alps

Table 1. — PTP time scale for the Carbonrferous and Permian

Periods (âges of the lower boundary in millions years).

Early Triassic

Induan

251 Ma

Changxingian

255

Dhzulfian

259

Midian

264

Murgabian

269

Late Permian

Kubergandian

273

Bolorian

275

Artinskian

280

Sakmarian

288

Early Permian

Asselian

296

Gzhelian

301

Late Carboniferous

Kasimovian

305

Moscovian

312

Middie Carboniferous

Bashkirian

323

Serpukhovian

328

Viséan

345

éléments are included within the résolution

power of a point on a 1:10 000 000 scale niap -

which is about a circle of 1 km radius) should

consist of a main column :md a few side-coliims.

The main column should ’melude lithology,

lithostratigraphic units, and dcpositional envi-

ronments. The side-columns should include data

on thickness, unconformitics, rectonic, magma-

tic and mctaïnorphic events, rectofacies and

orher addîtional information (sec legend). The

location of cach section within a résolution

power of 1 km of radius should bc identified hy

means of ifs latitude and Longitude figures.

If graphically possible, tlie columns should inclu¬

de the data on boih ihe Moscoviun and the

Artinskian (plus possibly the intervening inter¬

val) on the samc sheei (aiso by using the long

side of the A4 shcei).

Drawings should besubmitred m both color and

black and whitc (BW) versions, one for the sake

of the future map compilation, the other for the

immédiate purpose of prinring the volume. To

speed Work, il is suggested lo label with number

(see legend) the different units in rhe BW version

and to fin them by hand colors for the color ver¬

sion.

The structure of the legend mainly conform to

the previous onc used in Dcrcourt et ûl. (1993)

with some intégrations derived froin Zieglcr

(1988), Sassi Zanferrari (1990) and Vai

(1991). It seems particularly usefui to include

whenever possible in the maps the isopach

corttours or the margins of tlic main basins of the

latc Carboniferous (and Moscovian if available

separatcly) and of chc carly Permian (plus

Artinskian if available separatcly).

In the présent stage, the basic legend type fur

borh the stratigraphie columnar sections and tlie

rclated geological maps (îf available) is reporred

in Appendixes 2 and 3 re.spectively.

When addirional subdivisions and symbols are

needed, they hâve to bc added by the contribu-

tors in their own legend sheets, preferably

conforming to rhe use by rhe authors reported

above.

PTP INTl.RVAL IIMH SCALli

The numcrical time scale for Carboniferous and

Permian chronologie classification down to stage

level tentatively adopted for the purposes of the

PTP ha.s a simple pragmatic meaning lo enable a

coinmon frame fur communication among diffe¬

rent conrtibutors. However, a.s a matter of f'act

the présent scate of chronométrie calibration of

rhe conventional stratigraphie scale in the time

interval concerned is largely unsarisfactory as

appears from the very large error bars (from 3 to

9 Ma) affccring jndividual stage, sériés and Sys¬

tem boundarv âges (Odin 1994). lispccially pour

is the knowledge about the Dinanrian or

Mi.ssissippian subsysrem. The latc C^arboniferous

is mainly dated from continental successions not

evcniy relatcd to the marine oncs. A further limi¬

tation dérives from rhe still pool level of formally

defîned standard chronostrarigraphic subdivi¬

sions (G5SP) in rhis rime interval. Pcople invol-

ved are close to an agreemenc for the rwo System

and some subsysrem boundaries but hâve nor yct

paid any attention to the stage boundaries.

In such a condition, oiir aim was firsi to hâve a

reliable frame of reasonahie duration of stages,

regardless of précisé boundary âges, and second,

CO maintain a possible conrinuiry' with the rime

scale used in ihe previous Teihys Program.

Thcrctorc, the numcrical scale adopted here

(Table 1) was based mainly on the time scale by

GEODIVERSITAS • 1&97 • 19(2)

175

Vai G. B. & Venturini C.

Ross et ai (1994), aireajy uscd in Baud et ai

(1993), as a prcliminary ouiput ot rhe rime scalc

by Menning (1995). Some modifications hâve

bcen derived frorn Claoué-l-oi\g et ai (1995 and

pers. comni.), Roberts et al, (1995) and Irom

actempts at the besr fit with Harland et al.

(1990) and Odin(1994).

It is hoped that this first group of contributions

prompt other interestcd specialists to provide

soon updated informations for those other coun-

tries which are relevant for the compilation of an

accurate map reconstruction.

LATE CARBONIFEROUS AND EARLY

PERMIAN OF THECARNICAl.PS

l’he lato Moscovian lo latc Artinskian (x./.)

Ponrebba Supergroup represents a classic area for

late Palaeozoic stratigrapliy acting as a bridge

connecting the continental Permo-Carboniferous

sequence of Western Europe and the marine one

of the Russian Plaiform, the Lirais and Middie

East to Asia (peri'Terh)'an and Tethyan rcalm).

In fact, in the area including at leasr rhe Garnie

AJps, the Karawanken, the ouier Dinarides and

the northern Adrialic Sea both faciès interfinger

conspicously, providing excellent tools for eco-

stratigraphic corrélations (Kahler Prey 1963;

Selli 1963; Kochansl^-Dc\'^ide 1965).

Within the trame of the easccni Southern Alps,

the Pontebba Supergroup (Venturini et al. 1982)

represents u superb exposure of à pose 1 lercynian

cover (episuturui basin) sealing, with sharp angu-

lar unconformity, the scvercly thrusted

Hercynian (Palacocarnic) Chain and its shallow

cpimetamorphic équivalents of the Comelico

basement (Vai 1976; Castcliarin 6c Vai 1981; Vai

& Coeozza 1986). The basal unconformity of

the Pontebba Supergroup is well exposed over an

area some liundreds of square km, although it is

intersected by large Meso^oic extensional faults

and Alpine thrust faults. Sucli faults are widely

spaced froin each other to enable large blocks

showing che primary Hercynian basin/cover rela-

tionship preserved (Castellarin & Vai 1981). Ehe

western corrélative of the Pontebba Supcrgi*oup

is represented by the continental clastics of late

(Harbonifcrous (to Permian) age sealing rhe

Southalpinc crystalline basement in the

l.ombardy lakc région, Orobic, Giudicaric and

Alto Adige areas. Rccent rcsearch on physical

stratigrapby, cnvironmenral interprerarion ,ind

palaeoclimatic évolution bas provided the basis

for a berter understanding also in terms of

sequence stratigrapby and sedimentary history

(Venturini 1990, 1991: Krainer 1992).

CvCLia iY, SliQULNCES AND IRKNDS IN

Il 11-- P]‘:ra'U>Gakhoniklrüus Pontebba

Supergroup (Figs 1-3)

Local autocyclic and teclonic processes as well as

over-regional cycles hâve been recognized in the

sedinientury (laiierii.s of rhe Ponrebba

Supergroup. Derailed descriptions and columnar

sections showing rhe cycles are found in récent

papers (e,g. Venturini 1990, 1991; and espccially

Massari et al. 1991), although cyclic sédimenta¬

tion was ako stressed by previous aurhors.

As .1 whole, rhe Pontebba Supergroup is viewed

as a lare Hercynian cranstensional pull-apart

basin-filh consistent with both the post tectonic

relaxation of the very short emersion of the

Palaeocarnic Ghain (Vai 1976) and the late

Carboniferous^early Permian trans-Variscan

meg;tshear (Arlhaïul ik' Marte 1977). It forms a

composite sedimentary cycle defined by the

Hercynian (Garnie) non cnnformity ar rhe base

and the mid-Permbn (Saalic) disconformity ar

the top. This sedimentary c)T:le is notabJy dis¬

tinct trom the Permo-Triassic cycle and following

ones by its smaller extent and different architec¬

ture in response to a difierent stress régime.

The most prominent character of this Permo-

Carboniferous sedimentary cycle is lhat it is

composed by a qiiite regular sériés of cyclothems

having a mean ibickness ol about 30 m. Almost

the samc type of modal cyclothem is recognized

in two different sedimentary environments. One,

dominated by marine carbonate deposits (Pizzul

and Auernig Formations, see below), starts with

an unconformity by which progradation and

shallow-marine course silicoclastic depo.siis rest

on ramp sédiments, a transgressive finc-grained

highly fosslHferous clastic layer is closcd by a

limestone horizon followcd by shallowing

upward clastic sédiments. The other one, domi-

176

GEODIVERSITAS • 1997 • 19(2)

Fig. 1- —Third and fourth order lithocycles îrom !he Carbonilerous and eariiesl Permian ot the Garnie Alps, Key: LST-TST-HST. low stand, transgressive and high stand Systems

tracts; MFS. maximum tlooding surface; B, Bombaso Formation; the second column îrom lefl shows the stratigraphie subdivision according to the Austrian authors. Notice scale

change trom pan 1 lo pan 2 ot the section. See aiso legends in Appendixes 1,2 and 3.

Cyclic Permo-Carboniferous of the Garnie AIp;

Vai G. B. & Venturini C.

nated by more or less continental silicoclastics

(Corona and Carnizza Formations), starts with

superimposition of fluvial conglomérâtes on del-

taic to Coastal plain muddy sédiments followed

by fine-grainecl transgressive clastic ramp depo-

sits and highstand fine silicoclastic marine bands.

It follows ihat ihe upper Carboniferous cyclo-

thcms ol thc Garnie Alps can be described as

high-frcquency small-scale séquences in terms of

sequence strarigraphy and dcpositional s)'stcms.

Furthermore, the alternation of cither carbonate

or silicoclastic biindics suggests a climaiic modu¬

lation ot bigbcr rank cyclicity in respect to thaï

involved in tbe génération of cyxlothems.

A similar, although more irrcgular and Icss stu-

died cyclicity'. is shown in almost ail remaining

late Carboniferous to early Permian Formations

except tbe Trogkolcl Limestone (and related

units, see below).

Both larger and smallcr-scale cycles recognized in

the Pontebba Supergroup are closely similar to

tbe classical PerniO'Carboniferous cyclothems of

North America, the Russian Platform, Western

Europe and Africa (or to cheir internai subdivi¬

sions in formations and members). As an

example, one can compare the impressive corres-

pondence bepA^een the four Gzhelian formations

of the Garnie Alps (Pi//ul, Coronar Auernig and

Garnizza) and the corresponding four Gzhelian

‘‘horizons” of the Russian Platform (Ross & Ross

1988: 234; izart et al. 1995). On thc otiier band,

similarly impressive is thc almost perfcct match

between twenty-slx cyclothems of tbe upper

Gzhelian in the Garnie Alps (Fig. 1) and the

iwenty-one unîis ot ibe voughiy corresponding

Virgilian in Kansas (Ross & Ross 1988: 233).

The twenry*tvvo cycles recognized within thc

Gorona, Auernig and Carnizza Formations

(Massari et al. 1991) added ro the three out of

the four cycles known in the ‘T.ower”

Pseudoschwagerina Fonnaticjn (Homaiin 1969)

altogether rougldy correspond lo the upper half

of the Gzhelian, lasting as a whole stage about

5 Ma The ratio closely approximates thc magic

figure of 100 ka, whicb is thought lo be tbe for¬

cing orbital (short excentricity) factor of many

dcpositional cycles the glacial Pleisiocene

climatic-controiled paired Emiliani isotope

stages ).

The cyclostratigraphic analysis of the Upper

Carboniferous succession of the Pramollo Basin

(' Auernig group" and its basal immature clascics,

reierred to as Bombaso Formation) deserves

some additional rcmarks.

1. The Bombaso Formation is hetcropic with

both the Meledis Formation and the Imver part

of the Pizzul Formation (Venturini 1990, 1991).

Thl.s l.s an eflect of the Kasiinovian synsedimen-

lary tecionics, resubing in thc uplift ol a narrow

Horst exposed to érosion. It lincd up with the

basin axis spÜrting ir into two separared and

independeni Graben.

2. During late Gzhelian limes the north-eastern

Grahe, thaï is the well known area of Auernig,

Garnizza and Gorona Montain.s, was affcctcd by

strong lecionic sub.sidence. l'he sédimentation

rate remarkably increased as compared to the

previous Kasimovian-eaily Gzhelian figures

(Venturini 1991).

ft follows thât> for a correct anaivsis of thc cyclic

upper Gzhelian succession, interfering of pos¬

sible tcctonic puises must be carefully discounted

from the effects of the glacio-custaric oscillations.

’T'hf. Pkrmo-Carboniferc'jus Pontebba

SUITKCROUI* (Fig. 2)

For a betrer understanding of the palaeogeogra-

phic meaning of the Moscovian and Arrinskian

rocks exposed in tbe Garnie Alps, a summary

about its almost continuou.s succession ranging

(rom late Moscovian to enrly Kubergandian (in

thc castern area) is uscful.

The sequence starts with the fine clastic ro carbo¬

nate mairily basinal Meledis Formation not

conformably overlaying rhe Hercynian chain.

The Meledis Formation often rests on a chin

basal carbonate breccia body (Malinfier Fforlzon)

and in some areas is latcrally replaced by fault-

scarp related plygenic breccias and immature

coarse-grained siliciclaslics (Pramollo Mb)

naincd, as a whole, Bonibaso Forniaiion

(Venturini 1990). The Meledis and Bonibaso

Formations span from thc late Moscovian

(Mjackovian) to thc Kasiniovian {hotriticites to

Moritiparus Zones). They are followed by the late

Kasiinovian to early Gzhelian (Tritieites, Jigtdites

and Üaixiua Zones) Pizzul Formation, composed

of outer shelf limestones and pelires alternating

178

GEODIVERSITAS • 1997 * 19(2)

Cyclic Permo-Carboniferous of the Garnie Alps

Fig. 2. — Lithostratigraphic subdivision of the Upper Carboniferous of the Garnie Alps. Key: AU. Auernig Fm; B, Bombaso

Formation: Cor. Corona Formation: PS. INF., “Low^er Pseudoschwagerina” Formation; V.D., Val Doice Formation; the fifth column

from left shows the stratigraphie subdivision according to the Austrian authors. See aiso legend in Appendixes 1, 2 and 3.

with coasial-deltaic coarse-grained da.sucs.

The Corona Formation of latc Gzhelian

{Daixina and Pseudofusulinn-Rugosofusulina

Zones) follows wirh fine-grained open shelf

pelites (and a single limestone layer in the distal

area) alternaiing wirh alluvial plain to deltaic

conglomérâtes and sandsrones (inclucling some

thin coal seems). The drastic decrease in carbo¬

nate productivity, withoul major change In phy-

siographîc conditions of the basin, suggest a

marked cemperate to cooi climatic oscillation.

This formation Ls charactcrizcd by 30 to 40 m

thick cyclothcms (parasequences).

The following Auernig Formation, of late

Gzhelian âge (Pseutlufusulind'Rugasoftist^Iina

Zones) is composed by outer shelf marine carbo¬

nates and pelites alternating with coastal-deltaic

coarse-grained clastics. Fhis formation is charac-

terized by cyclothcms (parasequences) of mean

thickness of abour 20 m (range 15 to 40 m).

The Carnizza Formation closes the late Gzhelian

(Ps^fudofiisulinû-Rugosofusulijia Zones) and is

made by outer shelf pelites and subordinate

limesrones alternating with coarse-grained sand-

stones and quartz conglomérâtes of deltaic envi¬

ronment.

The "Lower” Pseudoschwagerina Formation of

latcst Gzhelian to Asseiian âge (Schiuagerinn

Zone) is composed of massis'e to bedded shal-

Jow-water limestuncs inrerlayeted by fuie-grained

marine silicoclastic .sedirnents. Four cyclothenis

hâve bêen recognized (Homann 1969) and

recently ànalysed (Samankassou 1995). The Val

Doice Formation of Asseiian âge {Schwagerina

GEODIVERSITAS • 1997 • 19(2)

179

Vai G. B. & Venturini C.

Zone) is dtîminared by terrigenous deposits with

minor limesTone intercalations (Üke in most of

rhe late Carboniferous) reprcsencing delta to pro¬

delta sequences.

Traditionally, ibe Carboniferous/Permian boun-

dary was placcd bctwccn ihe Carnizza and ihc

“Lower" Pseudoschwâgerina Formations. More

recently a position inside the ‘‘Lower” Pseiido-

schwagcrina Formation ac the base of thc

Occidemoschivagerim alpina Zone was suggested

(Kahler & Krainer 1993). Lately, Davydov &

Kozur (1995) bave proposed an even higher

place at the base of thc Val Doice Formation

(Grenzlandbànkc). Waiting for furcher taxono¬

mie précision wc adopt here a boundary place

still wiihin ihe “Lower” Psendoschwagerina

Formation inside the not yct investigated inicr\'al

above samplc SKI 15 ol^ Kahler & Krainer

(1993).

The “IJpper” Rseudoschwagerina Formation of

late Asselian to early Salcmarian âge {Zellia Zone;

Forke 1995) is composed of alternating massive

reefal and bedded partly marly inner shelf limes-

tones.

The following Trogkofel Limesrone (Sakmarian,

Robustoschivagerina and Pseudoschwâgerina

Zones) and the following related l'ressdorler

Limestone (early Artinskian, Painirhia Zone) and

Coccau (= Goggau) Limestone (niid to late

Artinskian, Muellina Zone) represent as a wholc

a reef-compicx ol shcll and shelf-edge environ¬

ment, vvhich has been compared with the

Capitan Reef of Texas (Fl ügel 1981).

The Moscovlmsî oi- vhe Carnic Alps (Fig. 3)

Only the late Mjackovian siibstage of the

Moscovian is ccrtainly represented In the early

lithostratigraphic units not conformably over-

lying the sevcrely foldeti and thrusted

Palaeocarnic Chain. The lowermost tiisulinids

foLind above the nneonformity are représentative

of the Protrhicites Zone and inclnde Eostajfella,

Paraendoihyrcu crinoids, brachiopods, echinoid-s,

molluscs, bryozoans, trilobites and phylloid plus

dasycladacean algac (Kahler &; Prey 1963; Selli

1963; Pasini 1963. 1974. Vai cr al. 1980;

Venturini 1990). Fhe stratigraphie unies bearing

this fauna are the Malinfrcr Horizon (matrix),

the Meledis Formation and its latéral équivalent

Pramollo Mb (matrix) which hâve been referred

to above. Consistent with the above dating are

also macrofloral and palynomorph data. In fact,

ferns (Netmipteris ex gr. ovata = grand'ewyi) of

Cantabrian âge (late Moscovian to early

Kasimovian) occur ai the top of the Mclcdis

Formation (Vai et ai 1980). Also the palyno-

morphs of thc lowermost Bombaso Formation

(Francavilla 1966), dated at thc Wesefalian B or

so (early Moscovian), are consistent with the âge

of the finit fusulinids. h suggests also a possible

earlier Moscovian onset of che pust-tectonic sédi¬

mentation of the Pontebba Supergroup.

The major faunal affinities arc found benveen

Carnic Alps, thc Dinarides and thc Russian

Plaitorm to Lirais. Floral rclacionships are inore

close with the Cantabrian région than with

NW Europe. Rccenr finding of Kasimovian

conodonts suggests close affiniry with Chinese

clementvS (Perri 6c Spallecta, pers. comm,; see also

Forkç 1995).

Thi Artinskian of thf Carnic Ai.ps (Fig. 3)

On top of the 150 ro 400 m thick Trogkofel

Limesrone (a complex sysrem of Tubiphytes buil-

dups) of Sakmarian âge, in places of the * middic”

Permian rcef-complex, -somc limestone masses

escaped the Saalic uplift and érosion, showing

remnants ot the Artinskian stage is.

The lower Artinskian is represented direerly by

the Tressdorler Limestone (15 m thick). ft is

made ul maiuly brecciated .shalluw-water limes¬

tone with both extraforrnaiional (reworked from

the underlying Trogkofel and ‘TJpper” Pseudo-

schwagerina Formation) and autoclithonous

components rich in Mizzin, other algae, g.asCro-

pods, fusulinids, other foraminitera, pelrnato-

zoans and bryozoans. It contains scimetimes

Praeparafusulina lutugini which is an eicment of

the Russian Pseudofiisulina lutugini Zone. A quire

Fjg. 3 — Stratigraphie corrélation of the main Moscovian to

Artinskian coiomnar sections ot the Southern Alps (exposures)

end lhe Adnaitc Sea (subsorface) and their interprétation {chro¬

nométrie calibration ot lhe dîronostraligraph'c scale conlorms to

thaï discussed in the tirst peut of the paper). Key: A, Auernig: B,

Bombaso; B.T., Tarvisio Breccia: C.S., Sesio Conglomérats; M,

Meledis; Piz, Pizzul; T-TROG, Trogkofel: R. Rattendorf- V.G..

Va! Gardena; Bell.. Bellerophon. See iegend in Appendixes 1,2

and 3 for other symbols.

180

GEODIVERSITAS • 1997 • 19 (2)

CARBONIFEROUS \ PERMIAN

middiê üpptr _. Lowêf 3!

Cyclic Permo-Carboniferous of the Garnie Alpi

Vai G. B. & Venturini C.

effective pre-lare Kubergaridian érosion is sugges-

ted by rhe frequent occurrence of Tressdorfer-

and Trogkofel Limestone block.s in tbe late

Kubergandian ro Murgabian Tarvisio Breccia

(Fig.3)-

The upper Artinskian is repre.senled by the

Coccau Limestone. ’) bis Ls a light grcy massive

shallow-watcr limestone qiiitc similai to the pre-

vious two lormations. ]n its upper part a rich

fusulinid ftuna from the Pseudofiisnlina vulgaris

Zone, including Pamirina dtirvasica^

Mmojaporiella elofigata 3iX^A NagatoelU aff. onentis

is found, suggesring an âge from Artinskian to

early Bolorian or carly Kungurian, at the very

base of the Misellma Zone (Kahler l‘}y2).

The Artinskian or thf Northern

Adriatic Sea (Fig. 3)

The âge assigned to the Coccau Limestone above

was confirmcd recently from the Amanda 1 well

drilled by AGIP about 30 km F. of Venice

(45”24’47”N - 13”00’38"E). The Permian,

beneath the mid ‘iViassic Latcm.ar Formation

(late Anisian-Ladinian), was encoimtercd from

6840 to 7305 m depth (Sartorio & Rozza 1991).

It is rcpi-esentcd from the top by:

1. The Amanda Formation, dark to reddish

maris, clay, silty sand.slones wiih palynomorphs,

some carbonate intercalations with fusulinids

{Kahlerina pnvhythtca of rhe Neoschivagerina

Zone), foraminifera and algae {Ttthipdjytts) and

fine brcccias represenring the laie Permian (possi-

bly late Kubergandian lo Murgabian).

2. 'Fhe 'Jarvisio Breccia, composed of reworked

clasts from the underlying Coccau (= Goggau)

Limestone and a red claycy matrix, deposited in

a subaerial environment.

3. The 175 m rhick Coccau Limestone, represen-

ted here mainly by sliallow-waier plaiform rud-

stone and grainstone faciès, including rich

fusulinid fauna (I):tudofust4limu Pmeparafmulina,

Acerimi'bwagerina, A'îiscllifia)', toraminifera, algae

(Tubiphytes, AfchaeoUthoporclUPs bryozoans, bra-

chiopods, pclmatozoans, bivalves, ostracods and

rare Belkrophon. The core taken from the middie

part of the formvttion was assigned to the

Misellifid claudiiie Zone of ihc latest early

Permian (Chihsianskian or équivalents).

Finai RHMARK.S

The corrélation chart in figure 3 shows two

major stratigraphie cycles easily traced along the

entire western Adriatic and eastern Souihalpinc

areas. The flrsi one, represented by the Pontebba

SupergroLip, starts with the late Moscovian and

lasfs at Icast up to the entire Artinskian and part

of the Bolori;m. It is mainly marine, wkh conti¬

nental clastic suppiy strongly dccrcasing upwards

and dominated by western provenance.

Thala.ssocratic conditions ciilminate with the

early Permian. cspecially Sakrnarian to

Artinskian, It is followed by a remarkable, gene¬

ral although differeniial upllfc and érosion,

occLirring sonietimes during llie late Bolorian to

Kubergandian interval. How much the relative

uplih is to be relaied to a concurrent eustatic sea

levcl drop could bc argued only upon establish¬

ment of more rcUable sea Icvcl curves for the

Pcrmi.in. The second cycle begîns with the early

Murgabian spanuing the Penno-Triassic bounda-

ry, except for the Venetian Gull area showlng late

Permian/carly Ttiassic uplift, This is a broadly

transgressive cycle dominated by the Mood plain

Val Gardcna Formation cvolvlng to the

Bellcrophon sebkhas and shelf. This trend is

quite concrasting with rhe more common world¬

wide Permian régression.

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Appendix 1: Keyto fossil and sedimentary structure symbols

FOSSILS SEDIMENTARY STRUCTURES

^ Acritarchs, Chitinozoa

^ Gastropods

^ Bioturbation

Algae

Graptolites

jiz Large scale cross bedding

4* Insects

Smal) scale cross bedding (r: ripple)

^iî^Amphibian.s

(s> Nannofossils

= Parallel bedding

X Bivalves

^ Orthocones

= Lamination

Q Brachiopods

c?- Ostracodes

Channel

^ Brachiopod spine

(g) Palynoflora

^ Slump

Y Bryozoans

^ Plantae (wood)

Tempestite

^ Charophytes

JcT Planlae (leaves)

4- Radiolarians

Conodonts

^Reptiles

9 Corals

ô Sponges

4 Crinoids

A Sponge spiculés

* Echinoderms

Stromatoporoids

Fishes

^ Tetrapod fool prints

Fish teeth

Trilobitcs

A Foraminifera (benthic)

y Vertebrate teeth

® Foraminifera (planktic)

ç =3 Vertebrate bones

A Foraminifera (indet.)

Shells indet.

^ Fusulinids

'^/Bioclasls indet.

184

GEODIVERSITAS • 1997 • 19(2)

Cyclic Permo-Carboniferous of the Garnie Alps

APPENDIX 2: COLUMNAR SECTION LEGEND

MAINCOLUMN

DEPOSITIONAL ENVIRONMENT

1 *1 1

Continental, Lacusthne

orange

1 6 1

Shallow carbonates

gold yeliow

1 2 1

Evaporites

pink

1 7 1

Pélagie rise

olive green

1 3 1

Deltaic

pale yeliow

1 0 1

Deep carbonates

light blue

1 4-5 1

Shallow marine clastics

green

Erosional hiatus

1 3 1

Deep marine clastics

blue

[n]]

Non-depositional hiatus

1 *10 1

Deeper marine clastics

brown

□

Lackof data

^ ^ ^ Breccia

O. Sand, conglomerate

• O • ° l

LITHOLOGY

s=silicoclastic

Turbidites v=volcanoclastic

c=carbonate

Sand

Sand, silt, shale

Organic shale

Dolomite

Carbonate, sand

I pspackstone

w’^aîTkB'Ju.nc,

msmuctstone

I « jj ReefaI carbonate, bindstone

> l-W

Sulphate

Halite

Coal

Carbonate, shale

A A Chert, radiolarite

Pélagie carbonate

|X xl Volcanics

Nodular carbonate

Ti |7| Volcanoclastic deposits

ï - Shale, some carbonate

Shale

Erosion, unconformity

C'^ Concrétion (Fe: iron, etc.)

O Colite

P Phosphate

B Bauxite

Pa Paleosol

• Cil, gas

SIDE-COLUMN

Low / High angle unconformity

R W Rift/Wrench induced

I F Inversion, folding

TR RE Transgression, régression

U C Régional uplift/collapse

M* + Metamorphic, volcanics, intrusives

GEODIVERSITAS • 1997 • 19(2)

185

Vai G. B. & Venturini C.

Ai’Pendix 3; Map legend

DEPOSITIONAL ENVIRONMENT AND MAIN LITHOLOGY

] Mainly continental clastics orange

{c=coarse;fsfine; Nacustrine, d=desertic, lateritic)

I 7

Pélagie rise

olive green

Lj_

] Evaporites pink

(t^and clastics; c^and carbonates)

L8_

Deeper marine carbonates

light blue

Lj_

] Deltaic shallow marine, mainly sands

pale yellow

Ll_

Deeper marine clastics

blue

] Shallow marine, mainly shales

pale green

Deeper marine, mainly sands

(turbidites) lîghtbrown

La_

L6_

] Shallow marine, carbonates and clastics

green

] Shallow marine, mainly carbonates

gold yellow

Basins floored by oceanic

lithosphère dark blue

TECTONIC SETTING AND LITHOSPHERIC TYPE

1 Inactive fold belt

Normal

□a

Foreland

Normal lithosphère

1 12

1 Anorogenic craton

lithosphère

Thin

lithosphère

Foredeep basin

1 Rift

Active fold belt

Thick lithosphère

1 Oceanic lithosphère

dark blue

VOLCANIC ACTIVITY

I 15 I Basaltic plateau

dark red

I 16^1 Porphyric plateau

light red

★

☆

Anorogenic

Orogenic

AUXILIARY SYMBOLS

Fault, wrench, normal

Basin margin

Major thrust fault

1 active, 2 inactive

Direction of clastic influx

B and A subduction

1 active, 2 inactive

—

ümit of palaeoenvironment

Accretion wedge

11111 ■ I ■

Continental slope

Major anticlinal axis

Isopach of the. (stage)

Active sea-floor spreading

axis and transform fault

As above, with magnetic

anomaly

186

GEODIVERSITAS • 1997 • 19(2)

Review and updating of the Moscovian to

Artinskian marine rocks in peninsular Italy

Mario PASINI

Dipartimento Scienze délia Terra,

Via La Pira, 1-50121 Firenze (Italy)

Gian Battista VAI

Dipartimento Scienze Geologiche,

Via Zamboni 67, 1-40127 Bologna (Italy)

KEYWORDS

Bashkirian,

Vereyan,

Kashirian.

Podolskian,

Bolorian,

Kubergandian,

fusulinids,

conodonts,

corals,

Tuscany,

Lucania,

Apulia,

Apennincs.

Pasinj M. & Val G. B. 1997. — Review and updating of the Moscovian to Artinskian marine

rocks in peninsular Italy, in Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigra¬

phie corrélations, Geodiversitas 19 (2) : 187-191.

ABSTRACT

New and previous data on the niainly marine Carboniferous to Permian

sequence of the Apennine Chain and its foreland in Italy (especially Tuscany

plus Lucania and Apulia) are summarized. Of spécial interesi is the restored

corrélation between a shallow-water carbonate platform and the related basin

with turbidites and olistostromes, pointing to the Hcrcynian outer foredeep

tectofacies.

MOTS CLÉS

Bashkirien,

Vareyen,

Kashirien,

Podolskien,

Bolorien,

Kubergandicn,

fusulines,

conodontes,

coraux,

Toscane,

Lucanie,

Apulie,

Apennins.

RÉSUMÉ

Nous résumons ici les données, nouvelles et anciennes, qui concernent des

dépôts, principalement marins, du Carbonifère au Permieades Appennins et

de son avant-pays italien (particulièrement la Toscane, la Lucanie et

LApulie), On notera tout spécialement rétablissement dhme corrélation

entre des carbonates de plate-forme peu profonde et les turbidites et olisto-

stromes liées au bassin adjacent, qui illustrent la tectonofaciès de l’avant-fosse

hercynienne externe.

GEODIVERSITAS • 1997 • 19(2)

187

Pasini M. & Vai G. B.

Moscovian and Arcinskian units are emphasized

here within the frame of Carboniferous to

Permian sequence of rocks.

MOSCOVIAN (Fig. 1)

Fossiliferoiis marine sedimentary rocks datable to

the Moscovian outcrop only in a narrow area of

the northern Apennines, becween Siena and

Grosseto (Monticiano-Roccastrada area,

Tuscany). Two main sequences hâve been sépara-

ted (Cocozza et ai 1987); a northern onc along

the Farma river and a scrnthern one in the San

Antonio mine area.

The Farma river sequence, becween Contrada

Carpineca and 170 ra a.s.l., near Ie.sa (43°5’N -

11°16’E) includes: (1) rhe Risanguigno forma¬

tion containing Devonian silidfied limestone

(Bagnoli & ’Fongiorgi 1980); (2) a chert forma¬

tion (lyditic radiolarites) of possible Dinantian

3geî (3) the Carpineia formation (Cocozza et ai

1974) of late Visean to Moscovian âge; and (4)

the Farma formation (Cocozza et ai 1974) of

late Bashkirian to late Moscovian âge. This

sequence, severely tecronized and largely ovcrtur-

ned, is uncontormably overlain by the Permo-

Triassic Verrucano Group (Cocozza et al. 1974;

Conti et al. 1991). Of major interest are the

Carpineta and Farma formations.

The Carpineta formation, mainly shaly and silty

with brachiopods, bivalves and plant débris,

contains olistolitfoc intercalations ai limestone

rich in erînoids, algae and loraminifera.

Brachiopods suggest a late Viséan to early

Namurian âge (Pasini & Winkler-Prins 1981) as

well as the Archaediscidae found in the sandy-

silty layers (Pasini 198()b), Fîowever, the forami-

nifera Irom the limcstones suggest a late

Bashkirian to early Moscovian âge (Pasini 1978,

1980a).

The Farma formation is a thin bedded silîcoclas-

tic turbiditc with few interposcd limestone olis-

tostromes and olistoHths. Limestones contained

in the lower part ot the formation and probably

identical to the San Ajitonio limestone formation

(see below) hâve been dated to the late

Bashkiriaii'late Moscovian (Podolskian to

Mjackovian substages) by Ferrari et al (1977)

and Pasini (1978, 1980a). More prccisely, Ferrari

et ai (1977) reported two different foraminiferal

faunas from the limestone olistostrome.^j and

from a loosc dark limestone houlder: rhe First

onc, with Profusulinella and Pseudostajfèlla, was

assigned to the zone 22 (or slightly younger) of

Marner, which is late Bashkirian to early

Moscovian; the second one was tematively assi¬

gned to the late Moscovian: Corals [Spirophyllum

rntiltilamellatum de Groot) and conodonts

(Idiognathodus delicatia Gunnell) yicldcd in the

sajnc houlder were assigned an early Moscovian

and a late Moscovian âge respectively.

Limcstonc.s from the upper part of the

Formation show Pustella praetypica Safonova of

the Podolskian substage (late Moscovian). The

Farma formation is more than 500 m thîck

(Conû et ai 1991).

The San Antonio mine sequence is located near

Casai di Pari (Grosseto) (43"3’N - 1 riTE) and

include. (1) the Carpineta formation (lacking

olistolichic inclusions herc); (2) the San Antonio

limestone formation, 200 m rhick, of late

Bashkirian to early Moscovian âge; (3) lhe paleo-

sol horizon with bauxite; and (4) rhe Spirifer

shales (Cocozza 1965) of late Moscovian

(Mjackovian) lo early Cantabrian âge, which are

exposed for 2 m only,

The San Antonio limestone formation is a dark

to black, shallow-water, bioclasric limestone,

partiy dolomitized, It contains algae and forami-

nifera with fusulinids {Ozawaiaella ex gr.

O. ginndis Putrja)) of early Moscovian (Vereyan

to Kashirian) âge.

The Spirifer shales contain Pseudostajfella cf.

sphueroideu (Hhr.) and brachiopods of latest

Moscovian-earliest Cantabrian âge (Pasini

1980a).

The Farma sequence is entirely basinal and

shows a systematic deepening of the sedimentary

environment. The San Antonio sequence sug-

gests an almost steady outer shelf environment

with a short émersion disconformity in the late

Moscovian. Large parts of the cwo sequences are

cime overlapping- Both contain the

188

GEODIVERSITAS « 1997 • 19(2)

Moscovian to Artinskian marine rocks in Italy

Pseudoendothym-Pseudostajfella association which

supports a close relationship aiso suggested by

olistostromes and olîsroliths supplied from the

shclf to the basin.

ARTINSKIAN (Fig. 1)

Clear fossil evidence of marine Artinskian rocks

in peninsular Italy was only found in the well

PC/33b (42“50'5n"N - ir4r30"E) drilled by

ENEL Co* on the Mt. Amiata (southern

Tuscany). This well cored fossiliferous carbonate

layers, containing fusulinids from — 3Ô24.40 to

— 3028.40 m beneaih the surface. ’Fhe cote was

made up of fivc cléments, the deeper of which

included Praeparafusidina cf. lutugini (Schellw.)

;tnd Eopolydiexodina sp.; therefore it was referred

to the P lîii-iigini Zone ot the Artinskian. Higher

éléments of the cote, however, yielded fusulinids

assigned to the généra Cancellina, Yangkieniu and

Pseiidodolwliria, which hâve been referred to the

Kubergandian.

The cored interval thus seems to represent a

condensed Artinsldan to Kubergimdian sequence

(Pandeli & Pasini 1990). Fhe lack of fossils

within the drilled deeper levels prevent an assess-

ment of the total thickness ol the Artinskian

sédiments.

The Palacozoic sequence found in the well

PC/33b is composcd by the “A”, “B” and “C”

formations (Fig. 1), among which the “B” for¬

mation is viewed as a tectonic wedge of pre-

Viséan âge within the “A” formation. This

Fig. 1. — Mid to late Carboniferous. mainiy Moscovian, stratigraphie sections in Southern Tuscany and their interprétation (left); late

early Permian stratigraphie section from the Southern Tuscany subsurface and their interprétation (right). See Vai & Venturini {this

volume) for legend; F. fault.

GEODIVERSITAS • 1997 • 19 (2)

189

Pasini M. & Vai G. B.

sequence îs unconformably overlain by the (?)

Triassic Verrucano Group, and was inrerpreted as

a reverse-recumbent fold or a complex pile of

Alpine cecronic wedges (Conti et al. 1991).

RELICS OF THE MARINE PERMIAN

This is a revicw of subsurface, poorly exposed, or

indirect évidences of Permian marine rocks in

peninsular Italy.

Poorly exposed marine sedimenrs of probable

Artinskian âge are represented by small carbonate

lenses with rare fusulinicts {Parafiistilina of eaxlier

type) (Bodechtel 1964; Kahler 1969), crinoids

molluscs brachiopods and plant débris enclosed

in the mostly marine Rio Marina formation of

Westfalian/Stepbanian ta early Permian âge, Elba

Island (42"49'N' 10“26T.;Vai 1978).

Rare relies of uppermost Carboni ferons to lower-

most Permian with fusulinids and algac have

been found as clasts within the middlc Triassic

Mt. Quoio Formation, Verrucano Group, Sou¬

thern Tuscany (43°6’N - 11®12’E; Engcibrecht et

ai 1988).

Other relies are found in the middle Triassic Mt.

Facico Formation, Southern Apennines, near

Potenza (40”28'N - 15°42'E: 40“12’N - 15^50 Tî

D onzelli & Crescenti 1970). Fusulinids and

smaller foraminifera of late Permian

(Murghabian to Dzhulfian âge) are cuntaincd in

resedimented conglomérâtes in the lower part of

the formation (Païr/anelli-Fratoni et al. 1987;

Ciarapica et al. 1990). Rare Artinskian fusulinids

(Pamirina darvasica Leven) are also found besides

rhe late Permian micrtjfauna (Pasini, unpubli-

shed data).

A possible source area for the Mt. Fâcito resedi¬

mented Perrnian conglomérâtes may be found in

the poorly fossiliferous cutrings from the

4581-4698 m interval drilled by Conoco in the

Gargano 1 well in 1984 (4P5Û’46”N -

15“24*30'’E). It is composcd of lighr grcy limes-

conc containing fusulinids of late Carboniferous

to Permian âge undcilying a thick Jurassic and

Triassic sequence.

Consistent with the above assumption îs also the

late Permian of rhe Apulia subsurface. A mainly

continental alluvial plain sédimentation of late

Permian âge (équivalent to the Southalpine Val

Gardena Formation) containing some Coastal

lagoonal carbonate deposits in the latest Permian

was drilled hy Agip in the Puglia 1 well

(4P3’30"N- 16'’5*30”E).

The dan discussed siiggesr a coherenr picture of

a mainly marine foredeep to foreland deposits

punctuaring the Carboniferous to Permian inter-

val in rhe wide palinspastic space hidden in the

présent Italian peninsular area.

REFERENCES

Bagnoli G. & Tongiorgi M. 1980. — New fossiliferous

Silurian (Mt. Corchia) and Devonian (Monticiano)

lavets in the [ usean Paleozciic. Me^notie délia Soeietà

Geofogka Italiana 20:301-313.

Bodechtel j. 1964, — Stratigraphie und Tektonik der

Schiippenytmê F.lbàs. (leolo^hche Rundschati 35:

25-41.

Ciarapica G.. Cirilli S., Pan’/anelli Fratoni R.,

Passer! L. & Zaninerti F. 1990. — The Monte

Facito Formation (Southern Apennines). Bollettino

délia Società Geolo^ica Ittdkina 109: 135-142.

Cocozzii T. 1965. — Il Carhonifero ne) grnppo

Muniicvano-Roccasirada. Rkerea Sdentiflca 35(11):

1-38.

Coeozza T.. Lazzarotto A. 6i Vai G. B. 1974. —

Flysch e mplassa crcinici dcl f orreiuc Farma

(Toscana). Beliettino délia Soeieiti Geologka Italiana

93: 115-128.

Coeozza T., Dccandia F., Lazzarotto y\., Pasini M. &

Vai C. B. 1987. — I he marine carboniferous

sequence in Southern Tuscany: Its bearing for

Hercynian palaeogeography and icciofacies, in

Fluçgel H. W. et al, (ed.s), Pre-Variscan and

V.iriscan evefu.s in the AIpine-Mediterranean

mountain belts. Mhteralia slovaca Mona^tanhy:

135-144.

Conti P.. Cosiancini A., Dccandia F. A., Elier F. M.,

GattigUo M., Lazzarotto A., Mecoheri M.,

Pandeli E., Rau A., Sandrelli 1^, Fongiorgi M. &

Di Pisa A. 199T. — Strutuind haine nî ihe Tuscan

Paleozoic: a review. Bollettino délia Società

Geologka Italiana 110: 523-541.

Donzelli G. Crescenti II. 1970, — Scgnala/.ionc di

una microbiofacies permiana, probabilmenie riina-

neggiau. nella fbrmazione di M. Faciro (l.utania

occidenmlc). Bollettino délia Soeietà Naturalisti

Nanolt 79: 59-75.

F.ngclbrccht H., KJemm F). D, fid Pasini M. 1988. —

Preliminar)' notes on the tectonics and Üthotypes of

rhe *"VeiTucano s.l/' in rhe Monticiano area (Sou¬

thern Tuscany, ïialy) and ihe finding ol Fusulinids

within the M. Quoio Formation. (Verrucano

190

GEODIVERSITAS • 1997 • 19(2)

Moscovian to Artinskian marine rocks in Italy

Group). Rivista Italiana Paleontologia e Stratigrafia

94: 361-382.

Ferrari A., Perri C. & Vai G. B. 1977. — Middle

Carboniferous corals and conodonts from the

Hercynian Farma “MassiP (Tuscany, Italy).

Giornale di Geologia 42: 133-164.

Kahler F. & Kahlcr G. 1969. — Einige südeu-

ropàische Vorkommen von Fusuliniden.

Mitteilumen der Geobçischen Gesellschaft in Wien

61:40-60.

Pandeli E. & Pasini M. 1990. — Fusulinidi permiani

nella successione metamorfica de! sottosuolo dcl M.

Amiata, Toscana méridionale (Italia). Rivista

Italiana di Paleontologia e Stratigrafia 96: 3-20.

Panzanelli Fratoni R., Limongi P., Ciarapica G.,

Cirilli S., Martini R., Salvini Bonnard G. &

Zaninetti L. 1987. — Les Foraminifères du

Permien supérieur remaniés dans le « Complexe ter-

rigène » de la Formation triasique du Monte Facito,

Appennin Méridional. Revue de Paléobiologie 6 :

293-319.

Pasini M. 1978. — Edmondta scalaris (MlCoy, 1884)

e Phestia cf. attenuata (Fleming, 1928) nclla forma-

zione Carpineta (Palcozoico superiore délia

Toscana méridionale). Rivista Italiana di

Paleontologia e Stratigrafia 84: 849-864.

— 1980a. — I Fusulinidi délia Valle del torrente

Farma (Toscana Méridionale). Memorie délia

Società Geologica Italiana 20; 323-342.

— 1980b. — Gii Archacdiscidi delPalFioramento di

Poggio aile Pigne nclla Vallc del Farma (Toscana

Méridionale). Mernorie délia Società Geologica

Italiana 20: 343-346.

Pasini M. & Winkler Prins C. F. 1981. —

Carboniferous Brachiopods from the locality

Poggio aile Pigne in the Farma Valley (southern

Tuscany, Italy). Rivista Italiana Paleontologia e

Stratigrafia 86: 459-468.

Submitted for publication on 5 April Î996\

accepted on 11 October 1996.

GEODIVERSITAS • 1997 • 19(2)

191

Permian deposits of Sicily: a review

Pietro DI STEFANO & Maria GULLO

Dipartimento di Geologia e Geodesia dell’Università di Palermo,

Via E. Toti, 91, I-90128 Palermo (Italy)

Di Stefano P. & Gullo M. 1997. — Permian deposits of Sicily: a review, in Crasquin-Soleau

S. & De Wever P. (eds), Peri-Tethys: stratigraphie corrélations. Geodiversitas 19 (2) :

193-202.

KEYWORDS

stratigraphy,

palcogeograpliy,

Perm ian,

western Sicily.

ABSTRACT

The complcx rccronostratigraphic setting of the Permian rocks of Sicily is

outlincd in the lîght of rhe large mas.s of new stratigraphie and paléontologie

data recently collecred by several researcher groups. The Permian deposits

occur mostiy as rectonic mélanges imbricated in che thrust pile forming the

Sicilian fold and thrust belr. AIso Mesozoic and Tcrtiary unconipctcni rocks

can bc found in thcsc méLtnges. Scvcral lithostratigraphic unies werc difïcrcn-

riated among thèse mosriy siliciclastic and clasric-carbonatc deep-water depo¬

sits, spanning in âge from Kungurian up to Changxingian. The Permian

deposits arc regarded as rhe originary sediraentary substraie of the deep-water

mcsoccnozoic domains of Sicily. Fossil associations, faciès and âges of these

deposits are consistent with the existence ofa wide and persistent deep-water

basin located along ihc Africa margin sincc, at least, the early Permian cime

and connected to the main Tethyan domains.

MOTS CLÉS

stratigraphie,

paléogéograph ic,

Permien,

Sicile occidentale.

RÉSUMÉ

L’arrangement tectonostratigraphique complexe du Permien de la Sicile est

défini à partir de nombreuses données stnuigraphiques et paléontologiques

récemment coIIccicc.n par différents groupes de chercheurs. Les dépôt-s du

Permien surviennent le plus souvent comme des mélanges tectoniques, avec

quelquefois des roches mésozoiques et tertiaires, imbriqués dans des piles

d’unités tectoniques formant la chaîne sicilienne. Plusieurs unités lithostrari-

graphiques, principalement constituées de dépôts silicoclastiques et clas-

riques-carbonatées de mer profonde, datées du Kungurien au Changxingien,

ont été différenciées. Ces dépôts constituent le substrat sédimentaire des bas¬

sins méso-cénozoiques de la Sicile. Les associations de fossiles, le faciès sédî-

mentaires et l'âge des terrains permiens indiquent l’existence d\in bassin

ample et persistant, localisé le long de la marge africaine dqDuis, au moins, le

Permien inférieur et relié avec les principaux domaines téthysiens.

GEODIVERSITAS • 1997 • 19(2)

193

Di Stefano P. & Gullo M.

INTRODUCTION

In the Sicilian fold and chrust belt strongly tecto-

nized PermianOViassic deep-water deposits occur

as either duplexes or mélanges imbricated with

tectonic unit.s of basin-derived Mesozoic and

Tertiary rocks. A large amount of ncw stratigra¬

phie data was collected in this last decade from

these deposits, poorly exposed in tlic Lcrcara

région and in rhe Sosio Valley (Catalano, DI

Stefano àC Koziir 1988, 1989, 199] and réfé¬

rencés therein, 1992; Senowbari-Daryan & Di

Stefano 1988; Ko/ur 1989a, b, 1991a,'b, 1993a,

b; Kozur àc Mostlcr 1989; Di Stefano 1990;

Flügel, Di Stefano 6^ Senowbari-Daryan 1991

and références therein; Gulky & Kozur 1992).

Some new liihostniligraphic units were difteren-

tiated. New Lower and Middie Triassic rock

unies werc described fiom the Sosio Valley. AIso

the stratigraphie and palcocnvironmental évalua¬

tions of the famous Sosio Limestoncs

(Gemnicllaro 1887*1899) were revised (Di

Stefano 1990; Flügel et 1991).

Figure 1 is a simplificd structural sketch-map of

Sicily showing the location of chc géologie section

in figure 2 and of the stratigraphie columns in

figure 4: a = Lercara-Roccapalumba-Vican area;

b = Sosio area.

GEOLOGIC SETTING

The Permian rocks from the Lercara and Sosio

Valley areas are incorporated in the Sicanian

thrust .System, an external element of the Sicilian

chain (Catalane et ai 1993, 1995). Fhis tectonic

élément consists of basin-derb^ed thrust sheers

thaï are arranged wirh an overall foreland vergen¬

ce and minor batk thrusts (Sicanian units in

Figs I, 2). The Sicanian thrust System is buried

in central Sicily beneath a ihick allochthon

consisting of delorrned foreland and satcllice-

ba.sin deposits of Neogene age and outerops

again in ea.stern Sicily in the Mouni Judica area.

It overthru-sts souihwards more external plat-

(orm-derived tectonic units (Saccense-Hybican

units) as 'well ns the dcfbrmed syntecfonic covers

(Fig. 2). The Sicanian thrust sheets are derived

from ihe deformation of a sedimenury nntlti-

làycr, consisting of up to 2000 m of Upper

Paleozoic to Tcitiary deep-water deposits daac

accumulated in a Southern Tethyan domain loca-

STRUCTURAL DOMAINS OF SICILY

AND ADJACENT AREAS

I I Exlensional areas

plin - Ouflle»no 7 voCs«iK»s

j. . .| Ko6<io-Ca‘«b'*^)e niiil»

r*-^ MaghfeDwnftnoSoumem

I_1 Ap€orir«8 Chain

I ^ I ; ‘ j Mainiano 2onB&o< Die

' -1 pRiagMn ann Aana qkicka

TRAPANI ^ wPîSÎ

£■

‘ETNA'.'

CATANIA

P'a^pcene oeposüs

MO'PlMCsn»

synorogentc deposits

CalaPro - Peloritani

Siciüdi units

n|igo.Miocene

f tyieh urils

Plaiidrm (Panormide) umts

Siop« to basin (Ime^se) unjte

Piatlofm • seamount

(Tiapanesa-Saccensey units

Slopatotiasin (Sicanian) units.

ai MmozoiC'T ertiary

b) PermotnassiC

ÏmS Foreland unltâ

Plio-Oiialernary vDicanites

Fig. 1. — Main structural domains of the central Mediterranean area and structural sketch of Sicily (modified from the Structural

Mode) of Italy sheet No. 6).

194

GEODIVERSITAS • 1997 • 19(2)

Permian deposits of Sicily

Fig. 2. — Interprétative géologie section across the Rocca QusamOra'Sicani Mountains area baseO on surtace data (location in

Fig. 1}: TP, Trapanese umts (Late Tnassic MIocône); NF. Numidian Rysch units (Late Oligooene Early Miocene): SI. Sicanian units

(Late Triassic-Early tertiary), PT. PeiTnlan-Carnian units; SC. Saccense units (Late Tnassic^MIocene); TE. Oligo-Mrocene, mostly

terrigenous, deformed covers. The thick allochthon of Permian-Carnian deposits dipping below the Rocca Busambra Unit repre.sent

the westward extension of lhe Lercara structure.

tcd along ihe African margin (Sicanian Basin,

sensu Di Stefano 1990, Catalane et al. 1991).

Becausc of the Ncogene compression rhis multi-

layer was detached Irom its original (unknoAvn)

substrate. According to Catalane et al. (1993,

1995). it was deformed into fliree different

duplex stacks consisting of Palco/.oic-Carnian.

Late Triassic'Paleogeoc and Neogene rocks res-

pectively.

In the Lercara area the Permian rocks occur in a

large antifonnal structure, up to 3000 m thick,

consisting of Permian and Triassic rock sliccs

alternating, in places, with thin .slices of Miocène

clays. The extension at depth of the structure i.s

documenteti by .scismic and exploration well data

(Roccapalumba I well, Caflisch & Scbrnidi di

Friedberg 1967)- The repeated imbrication of

Permian and Iriassic rocks in lhe Lercara struc¬

ture provides evidence of a duplc?^'iype deforn^a-

tion in the Permian to Carnian interval ot the

Sicanian sedimentary mulcilaycr. d hc firsi defor¬

mation of the Sicanian allochthons is gcncrally

considered to be no older than Tortonian

(Mascle 1979; Caralano & D’Argenio 1982)

even though a possible older âge (Lower

Miocene) for the duplex accrerion was suggested

by Virale & Giambrone (1992). The Lercara

structure is inflected northwards below

Numidian Plysch units as well as Trapanese plat-

form units and overthrusts southwards more

external Sicanian allochthons (Fig. 2). The

upward-arching and emplacement of rhe structu¬

re is due to later (Pliocène) transpressional defor¬

mation a.s indicated by the involvemcnt of the

Upper Ibrtonian-Lovvxr PÜoeene syntcctonic

covers in arching as well as in breaching thrusts.

In the Sosio area the well-known Permian lime-

stone rnegablocks (Gemmellaro 1887) were

considered sedimentary klippen in Carnian beds

(Masclc 1979)- Wc now bellcve that the Permian

ro Carnian rocks outeropping in tbis area, com-

prisiag tbe Permian to Middie Trias.sic deposirs

desenbed by Calalano et ai (1988, 1991), are

part of a tectonre mélange (herç indicated as

So.sio mélange), which is related to the Neogene

compressit)n and imbricated in tbe Sicanian

rhrusi pile (Fig. 2). 'Fhis mélange^ up to 500 m

thick, indicates décolUfïient or Hoor-thrusts along

which the Lace Iriassic-Tcrtiary sequences hâve

been detached from tlie Peimian-Triassic .substra-

le. It overthrusts the Oligo-Miocene deformed

Cüver of a lower unit and is overlain by a duplex

structure composed of Upper Triassic-Eocene

cheriy limestones.

Besides the Lercara and So.sio areas, siliciclastic

deposits of supposed Permian âge, containing

cléments of algal-oolitic liniestoncs, were descri-

bed in the Cozzo Rasolocollo area, south of

’lcrmini Imerese (Broquet 1968). Until now no

hiostratigraphic data confirming a Permian âge

hâve been obcained from rhese rocks. They form,

together with Carnian //^/o^'/W-bearing maris

and calcilutices, a thick allochthon crossed by the

exploration well Cerda 1 for about 3300 m.

According to Rocco ^ Giartosio (1961) evidence

of Permian rocks could be fbund only In the dee-

pest part of this well.

Permian and/or Lower Triassic rocks could .tlso

hc présent in the suhsurface of the Hyblean fore-

land, in souih-ca.stern Sicily, as suggesied by

magnetic and gravimétrie data (Blanchi et al.

1989).

GEODIVERSITAS • 1997 • 19(2)

195

Di Stefano P. & Guilo M.

PERMIAN LITHOSTRATIGRAPHIC UNITS

The stracigraphic reconstruction of the Permlan

successions from the Lercara and Sosio areas is

ver}^ diflîcult due to:

1. The strong deformation affecting these mostly

incompétent rocks.

2. The poor exposurcs: only a fcw small and dis-

continuous sections can bc obscrved.

3. The faciès types, which consist of mostly silici-

clastic/carbonate turbidires containing a large

mass of reworked lithoclastic and bioclastic

material.

4- The lack of stratigraphie relations among rhe

different lithologie units, the contacts gcnerally

being tectonic.

Aware of the above limitations which bave led to

debate about the âge of the siliciclastic rocks of

the Lercara area Ruggieri & Di Vita 1972;

Cirilli et al. 1990), wc recognize the following

lithostratigraphic units, whose thickness is quitc

impossible to be estimate. In figure 4 wc hâve

preferred ro présent the different rock units in

separate columns, but we believe they belong to

different deposirional areas of a single sedimenta-

ry basin. The Permian chronostratigraphic scalc

of Kozur ( 1989a, c) is used, tenrarively correlated

with rhe proposed time scale adopted for the

Peri-Tcthys program and map.

KUNGURiAN Flysch (Cacalano étal 1991)

This is the oldest Permian lithostratigraphic unit.

It was recognized in the Rtxcapalumba, Lercara

and Vicari areas and consists of a thick package

of deep-water siliciclasnc curbidites characterized

by reddLsh shalcs, siltstoncs and micaccous sand-

stones displaying Bouma divisions, flûte cast.s

and Nemtes ichnofacies. '1 he sandsrones contain

abundani quartz and muscovite and subordinare

biotite, feldspars and rare zircons (Broquei

1968). A Latc Ariinskian-Kungurtan âge of ihese

deposits is supported by conodoms (Catalano et

al 1991). Calcareous turbidites are frcqucntly

interbedded. They consist of skcletal-lirhoclastic

grainsrone.s/packstones with fusulinids,

Tîibiphytrs sp., Ardmeolithopordla dasyclada-

cean algae {Miizia sp., Epimastopora sp.) and

sponge fragments.

Magmatic rocks (diabases and lamprophyres) are

présent in the flysch deposits. Also a small lacco-

litic body coivsisting of a sodic-differentiated

alkaJi-syenitc is présent in the Torrente Margana

area, about 10 km West of Lercara (Vianelli

1970). No âge déterminations of these magmatic

rocks are available. They could also bc younger

than Permian

Intercalations of coarse calcareous debrites in the

siliciclastic turbidites also occur in places. A large

spectrum offacies-types can be recognized in the

debnre éléments. Shallow-water pcbbles and

boulders consisting of ^^orv^d Yuhiphytes bound-

scones, TubiphyteslArdiaeolithopoYellü bindstones,

phylloid algae boundstones, Afez/Æ-fusuiinid

grainstones-packstones, and crinoidal pacicstones

are commonly found (Senowbari'Dàryan & Di

Stefano 1988), A Lower Permian âge of these clé¬

ments is indicated by algal assemblages and fusu-

linid.s as Psetidofusulinn (Leema) hraffti

Schellwien and P. vutgaris SchclKvicn (Flügcl et

ai 1991).

Large boulders' of deep-water dark-grcy ammo-

noid'brachiopod'Crinoidal bcaring waekestone-

packstonc arc also présent, in tinclcar rclation-

ships with the flysch deposits. Conodonts of

Chihsiaji age wcrc found associated to aJbaillella-

cea radiolarians, ammonoids, scolccodoncs. Üno-

produettd brachiopods and trilobites (Catalano

étal 1991).

Younger Permian rock packages are exposed in

lire Sosio Valley area, along the Torrente San

Calogcro (Catalano et al 1988, 1989, 1991,

1992) as well as in the famous limestone mega-

blocks.

San Cai.oghro Flysch

The oldest unit recognized in this area is a flysch

consisting of gtey to blackish pyritic shales and

siltstones with intercalations of micaceous sand-

stones and hyhrid arenites. This unit is well

exposed along the riglu bank of rhe Torrente San

Calogero. The age ol this unit, hased on cono¬

donts, is Lüwermost middle Permian (Guilo

1993) . In the Torrente San Calogcro section

similar deposits appear as a chaoiic clayey mass

containing sandstone blocks. The age of the

clayey matrix is the sanie of the flysch deposits

on the basis of conodonts (Catalano et ai 1991).

Scattered small éléments of dark grey calcilutites

196

GEODIVERSITAS • 1997 • 19 (2)

Permian deposits of Sicily

wirh circumpacific radiolarians of Early

Kungurian âge suggest chat these deposits hâve

bcen affected by synsedimentary sliding and

rcworking (Olistostrome Unit sensu Catalane et

al. 1991).

RuPE DEL Passo di Burgio Limestones

Stratigraphically younger deposits consisting of

whice ro grey ammonoid-bearing caJciluiites wirh

intercalations of reworked skeletal calcarenites

are found in the Rupe del Passo di Burgio block.

A Wordian âge of these deposits is supported by

the rich fossil association characterized by

ammonoids, holoturian sclerites, ostracods, cri-

noid ossicles, fusulinids and conodonts

(Gemmellaro 1887-1899; Müller 1956; Bender &

Débris and landslldes (Recent)

Gypsiterous maris and evapohtee (Upperl

Torionian * Messintan) *

(Middlel

71 Sandy crays and olobigerinid maris

—I Larrgnian - SerravaiTian)

Sandy ctays and giauconitic arenites (Oligocène |

• Lower Miocene) '

Globigertnid limestones *Scagtta‘ (Lowerl

Crelaceous • Eocene)

Pélagie limestones and radiolarites (Jurassic) |

Cherty limeelones (Upper Carnian • Rhaetian) |

Maris and catdluiites (Camian)

Bedded cberts, nodular limestones and maris |

(?Anisian • Ladinian]

l~ ''miJnl SIliciclastrc d^osils (Permian) and (a)

( ■ ■— M J undifferentiated Permian and Triassic deposits

Sosro limestone blocks (Permian); a) Pietra di

Salomooe. b) Rupe del Passo di Burgio. c) Pietra

dei Saracini, d) Rupe di San Caiogero

HIgh angle faultsj

, Axis of syncline

Fig. 3. — Géologie map of the Palazzo Adhano area.

GEODIVERSITAS • 1997 • 19(2)

197

Di Stefano P. & Gullo M.

StoppcI 1965; Catalano et ai 1991, Kozur

1993a). The Rupe del Passo di Burgio

Limestones can be inrerprered as hemipelagic

carbonates deposited in a distal slope area in

which skelctal material, produced in an adjacent

platform, was transportcd downslopc by tiirbi-

dity currencs and grain flows. Animonitic limcs-

tones of Wondian âge are a)so dcscribed from the

Passo di Burgio area, south of the Pietra dei

Saracini hlock (Ko/.ur 1995).

WORDIAN ClAYS

Ycllow ro grey clays with Wordian conodonts are

found in die Sosio Valley in a small outcrop close

to the Rupe del Passo di Burgio (Catalano et al.

1991).

Pietra di Salomone Limestones

These deposits characterize the most famous and

fossil-rich limestone block outcropping in the

Sosio Valley and two smaller blocks présent

along the Torrente San Calogero valley, known as

Pietra dei Saracini and Rupe di San Calogero

(Fig. 3). Aitcr Gcmmcilaros careful descriptions

(1887-1899) many paleontological studies were

carried out on these limeMones, prcviously regar-

ded as reeJ limestones (see référencés în Mascle

1979 andin et al. 1991).

Recent sedimentological and stratigraphie contri¬

butions indicate that the Pietra di Salomone

Limestones are composed by generally poorly

defined thick and, in places, graded beds of coarse

calcareoLis breccias, aliernating co skeletal packs-

tone/grainstone beds (Di Stefano 1990; Flügel et

ai 1991). The latier deposits prevail in the upper

part of the Pietra di .Salomone bli»ck giving ruse

ro a fining-up sequencc. The maximum ihick-

ness of these deposits is esiimatcd at about 70 m.

The breccia éléments consist of placfoi m-slope

derived carbonates. Reef-derived boundstones/

rudstones prevail bur aiso floaistones and grains-

tones are commonly observed. Sponges,

TnhiphyteSy Archaeolitbopm'ella. phylloid algae,

richthofenid bnichiopod.s are the main frame-

building organisms, associated to highiy-diverse

fossil assemblages comprising fusulinids The age

of most of the éléments ranges from the

Artinskian ro the Djulfiaii. A Late Pemiian age

of the matrix is suggested by fusulinids and

conodonts occurring with a large mass of rewor-

ked Middie Permian faun.as (Flügel étal 1991).

The Pietra di Salomone Limestones represent

debrite and turbldife sédiments deposîted in a

basc-oTslopc position. These rocks lormed car¬

bonate aprons that could hâve been accumulated

adjacent to or interlayered with the Red Clay

Unit (sec below).

Red Ctj\Y Unit (Catalano étal. 1991)

This is ihe youngest Permian unit présent in the

Sosio area, outcropping along ihc Torrente San

Calogero and between the Rupe dcl Passo di

Burgio and the Pietra dcl Saracini locniities

(Gullo ^ Kozur 1992). It consists of red clays

containing fine grained silicidastic and carbona¬

te lurbidires. A ricli pelagic fossil content occurs

in the red clays, consisring of tircumpacific

radiolarians, paleopsychrosplieric osrracods and

conodonts. It iudicates a L.ate Permian (Djuliian

to Changxingian) age (CataJano et al. 1991;

Gullo 5c Kozur 1992; Ko/ur 1993h)- The calca-

rcous turbidites mostly consist of .skeletal grains-

tones/packstones with abundant foraminîlers

(Reichetina sp.)j Anhaeolithaporella/Tubiphytes

fragments and conodonts of Lare Permian age

(Fig. 3).

PALEOGEOGRAPHIC IMPLICATIONS

Faciès associations and âges of the Permian depo¬

sits from western Sicily couplcd with the palin-

spastic re.storarion ol the chrust pile forming

\ve.sicrn Sicily segment of the Apenninic-

Maglircbian chain, are consistent with the exis¬

tence of a widc and persistent deep-water basin

along rhe Africa margin since, at least, the Early

Permian lime (Catalano et al 1989, 1991; Di

Stefano 1990, Rerntiulli étal. 1990; Robertson et

al 1991, Blentlinger et al 1992; Kozur 1993b;

Vai 1994). Siliciclastic turbidites, ns-sociatcd with

carbonate turbidites and debrices formed the

sedimentary lÜI of this basin during the Permian.

Sballow-water skeletal material and pUtform-

slope carbonate.s of well-dared Early, Middie and

I.ate Permian age.s were almost continuousiy

transported downslopc into the basin, indicuring

the existence of a mixed terrigenous/carbonate

198

GEODIVERSITAS • 1997 • 19(2)

GEODIVERSITAS * 1997 • 19(2)

Western Siclly

Konjr(1BaS|

IGCP Tethyen

scaie

CHANG»NGIAN

CHAMGXINGIAN

DJUUHAM

CUULRAM

AaAOEH'AN

MIOIAN

CAPITANIAN

MUnClABIAN

WOftDIAN

KUeEflGAN-

OiNIAN

KUBEHGAN-

CXNIAM

CHtHSIAN

BOLORIAN

KLINGURIAN

’ \

AnTtMSKUM

ARTINSKIAN

SAKMARlAN

SAKMARIAN

ASSELIAN

LITHOSTRATIG«APHY

UTHCHjOGV BXNOAftieS

I nocc«p«lurTt»- So«io Smio

LTCara [ SanCateoyo Muèblolci

Woidm

I Oaw

îll

I Ut

♦ IjT t_

I UT \

IliT

niT

F08S11. CONTENT

« 0^

Cl«r. |C»r>*ii| Sln.»i9[up«

POSSILS

ki0 TracMtossil

O Aigu

£* Fuiutinids

^ l^adBUKans

^ Spnnpi tpiciAS

V Bnozoarw

• Corail

5 SpgngM

9 Braehupodi

tUÎH0l.0GŸ SEDIWENTARY

FEATURES

2 Bivalves

^ Gaslropods

^ NauMotds

4 Ammonites

£ Tniobiies

If Crinoide

f Echinodemttj

^ Conodonts

A A A

Brecaa»

[E3

Sands

Olistolilhs

TufbUrtBe

c carbonate Blolur-

Calcarenaee,

Mnds

R Red

— Planer

PejMic

carbonates

lamnaiiw»

[SI

Bhales

lainmalion

Œ2

MsgmaUKs

r Ripple

i y Fining

IUT

tecionic

V opward

boündaries

T^T, Bouma

Tecionic Uagmatic evenia

^ Eaternsional

PALEOENVIRONMEWr

r 1 Daeper nianne dastics

Y///} Deoper rT«r:;te carbonates

Fig. 4. — Permian lithostratigraphic units of Sicily.

Permian deposits of Sicily

Di Stefano P. & Gullo M.

shelf area at ihe margins of this basin. Part of ihe

clastic carbonares coulcl aiso hâve derived from

seamount areas inside the basin.

As assumed by Catalane et aL {1991 ), the occur¬

rence of circumpacific deep-water faunas in the

Permian deposiis of western SicÜy suggests à

connection of the basin to the Pcrnïian Tethys.

The most reliable castward connection oP this

basin wirh the oceanic Perhys was through the

present-day lonîan basin. This implie.s a sépara¬

tion of the Adria block from the Gondwanian

margin already în rhe Permian (Vai 1994),

Remnants of this basin toward the easi are found

in Crete (Krahl et ni 1986; Ko/.ur 6c Krahl

1987), Kurdistan (Vasieek &c Kulinrann 1988)

and Oman (Blendinger 1988; Blendingcr et ai

1992).

The Southern edge of the Permian ba.sin of Sicily

was represented by the siliciclastic-carbonatc

platform of Tunisia. Herc Middie and Upper

Permian deposits, wirh an upward régressive

trend, arc wcll known, reaching a thickness ot

6000 m. Faciès distribution shows a transition

from a rcef coniplcx belt to deep-water shaly

faciès rowards the Noich (Toomey 1991).

Remnants of the norrhern .shelf area uf the

Permian basin ot Sicily could be represented by

the reworked fusulinid limestones from the

Lagonegro basin of the Southern Apennines

(Donzelli & CTescêmi 1970).

The crustâl characters of the Permian basin of

Sicily are unknown siuce in the Sietlian chain the

sedimentary coVers are rcgionally decached from

their original substraie whilc oceanic crust is wcll

known in tfie easiern prosccution of rhe basin

{e.g. in Oman, Bèchennec 1988).

The Permian basin could fiave represented either

the Southern passive margin of the Permian

Tethys or a rifting along the Gondwanian margin

connected to the rnain Tethyan domains

(Catalane et ai 1989, 1991), Crustal extension

along the Gondwanian margin could aiso hâve

been induced by Tare Paleoxoîc mega-shears bet-

ween Gondwana and Laiiru.ssia (Ricou 1994; Vai

1994). The Permotriassic deep-water deposits of

Sicily predate, at rhe l.ate Carboniferous-earliesr

Permian time, the extensional phase afifecting the

Gondwanian margin since the oldest recognized

lithostratigraphic unit is a flysch of Kungurian

âge and llms older syn-rift deposits must hâve

originally nnderlain the flysch sequence.

Ackn owledgm en ts

The study was supported by grants from the italian

Consiglio Nazionale dclle Ricerche

et. 95.00389.et 05. We thank A. Baud and

S. Crasquin-Soleau for the carefui review of the

manuscript.

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Subrnitted for publication on 5 April Î996\

accepted on 11 October 1996.

202

GEODIVERSITAS • 1997 • 19(2)

Review on continental Permo-Carboniferous

deposits in italy

Giuseppe CASSINIS

Dipartimento di Scienze délia Terra, Via Ferrata 1,27100 Pavia (Italy)

KEYWORDS

sedimentary conrinental deposits,

volcanic products,

plutomc bodies.

(late)-posrHercvnian

metamorpKism,

tectonosedimentan' cy cles,

Upper Carbonilerous^

Permian,

Tnassic p.p.,

Southern and western /\Jps,

Tuscan^.

“Calabro-Peloritan Arc

Cassinis G. 1997. — Review on continental Permo-Carboniferous deposits in Italy, in

Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigraphie corrélations,

Geodiversitas 19 (2) : 203-216.

ABSTRACT

The paper présents a short, but up-to-date review of the late Paleozoic to

Triassic continental deposits of a large part of Italy. These deposits generally

crop out in northern Italy, from the Dolomites to the western Alps, in some

central and maritime 7.oncs ol Tuscany, and, miich further South, iri Calabria

and NE Sieily. Since the tecronics of these régions arc highiy cornplcx, the

stratigraphie schemes drawn up in figures 2, 3 only show the most complété

and significant licliological successions. From the rcsults, it Is worthy of note

that the (late)~püstHercynian continental sequences under discussion can

generally bc divided into rwo main cectonosedimentat)' cycles, The lowcr

cycle consisrs borh of alluvial-lacusrrine siliciclastic deposits and of calcalkali-

ne acidic-to-intermediate volcanic products. On the whole, this cycle ranges

from Late Carboniferous to Late Permian times. In the Alps. the overlying

cycles includes rhe well-known Verrucano-Val Gardena clastics> which are

still Permian in âge. However, the Apenninic Verrucano is younger, gcncr-

ally pertaining to the Middle Triassic.

GEODIVERSITAS • 1997 • 19(2)

203

Cassinis G.

RÉSUME

Ce papier présente un bref résumé, qui est une mise à jour des dépôts conti¬

nentaux d’Italie du Paléozoïque au Trias. Ces dépôts affleurent généralement

en Italie du Nord, des Dolomites aux Alpes occidentales, dans quelques

zones centrales et maritimes de Toscane, et plus loin vers le sud, en Calabre

et dans le NE de la .Sicile, La tectonique de ces zones étant très complexe, les

schémas stratigraphiques (Figs 2, 3) ne montrent que les successions litholo¬

giques les plus significarives et les plus complètes. Cependant, dans cette

revue, de nombreuses données sur les dépôts du Carbonifère et du Permien

concernent les régions voisines. A partir de ces résultats, il est intéressant de

noter que les séquences (tardi-) post-hercyniennes peuvent généfalement être

subdivisées en deux cycles tcctonosédimciu.iires principaux, l-c cycle inferieur

consiste à la fois en des dépôts aüuvlo-lacusires silicocla.stiqucs et en pmduits

de volcanisme pour la plupart intermédiaire i acide caico-alcalin. L’ensemble

de ce cycle s’érend du Carbonifère supérieur au Permien tardif. Dans les

MOTS CLES Alpes, le cycle .susjacenc inclut les dépôts détritiques du V'errucano et de Val

Paléozoïque supérieur à Trias, Cardena, d âge encore permien. Le Verrucano apennin, est cependant plus

Italie. jeune, et appartient généralement au Trias moyen.

After the recionic-metamorphic evernts of the

Hercynian orogeny, tlie pre.sent north-western

part of Italy, which ranges approximately from

the eastern Dolomite Alps to Southern, Coastal

Tuscany, togerher wirh the “Calabro-Petoriran

Arc*’, represented primarily continental domains,

where siliciclastic and/or magmatic deposits

developed in various ways, right up to the dia-

chronous Triassic marine Transgression.

UPPER CARBONIFEROUS

Well-documentcd Upper Carboniferous succes¬

sions, wbich lie unconformably on the

Hercynian crystalline basement, crop ont in

some sectofs of the Icalian Alps (Como-Maggiore

région, western Liguria) and in rhe northern

Apennines (Mts. Pisani, Jano village), and extend

lo fairly adjacent régions. *l*hey generally mark

the beginning of a cycle, where the annexed

deposits aiso include rhe Permian (Italian

I.G.C.P. 203 Group 1986; Cassinis et ai 1988).

Southern Alps

The scactered, strip molasse outerops of Manno

and Logone, which lie unconformably on the

Hercynian crystalline basement of the South

Alpine segment, are rich in fossil plants, and

constitute the hesc-known example of the central

sector of this cliain, Jongmans (1960) idcntified

Linopteris neuropteroides^ Pccopteridium-,

Sigdlari(icph\illitmy Cordaites cf homssifolhis in rhe

former localiry, near Lugano, and classiPied the

fiera as middie ot B-C Westphalian; Venzo &

Maglia (1947) ascribed the lutter deposits of the

Alpe Logone to Westphalian C, on the basis of

the présence of Calamites spp., Pecopteris

plumosUy Linopteris ncuropteroides, Lepidodendron

wehhthniy abundant Sigitbnae and other plants.

Nearby, however {e.g. in Bedero, on rhe eastern

side of Lake Maggiore), the presence of scarse

Stephanian clastic strata and small anthracite

lenses has also heen generally recognized.

To the wesc, in rhe South Alpine lower crust of

the Ivrea Zone, the LP-HT granulitic sériés, with

basic and ultrabasic rneta-intrusives, date back to

about 300 Ma {e.g. Pin & Vieizeuf 1983; Pin

1986).

Western Al.ps

Within the boundaries of rhe extensively meta-

morphic western Alps, and as far a> rhe l.igurian

segment, the inner lower Aasrroalpine domain of

the Sesia-Lunzo Zone shows rhe intrusion of a

number of (late)-postHercynian granitoid and

mafic-igneous bodies. Possible Carboniferous

204

GEODIVERSITAS • 1997 • 19(2)

Continental Permo-Carboniferous deposits in Italy

and Permian detrital sédiments, accompanied by

intermediate-to-acidic calcalkaUne volcanics, are

also recorded in rhe Dent Blanche nappe, near thc

Switzerland-ltaly border (Ayrton et al. 1982). In

the Pennine areas, both internai scctors (Mount

Rosa, Gran Paradiso, Dora Maira) and external

sectors (Briançonnais, Gran S. Bernardo) seem ro

be widely characterized by Carboniterous and

Permian clastic sédiments, which are still associa-

ted with volcanic rocks. (Late)'posrHcrcynian

Fig. 1. — Map location. Big latters: stratigraphie sections showed in Figs 2, 3. A. Val Fersina Section; B. Tregiovo Section; C, Val

Trompia Section: 0, Val Seriana Section; E, Mallare Section: F. Case Tuberto Section; G, Mt Pisanl Section; H- lano Section; I. Elba

Section; L. Argeniiaho Section, Numbers: locatities cîted in lhe text- 1, Rio di Pusteria, 2. Bressanone; 3. Mt. Ivigna, 4. Giogo délia

Croce; 5. Cima d'Asta; 6. Val Sugana area; 7, Val Fersina area: 0. Düsso bel Sabion; 9, Basse Giudicane area; 10. Val Biandino; 11,

Alpe Logone; 12, Manno; 13. Lugano; 14, Cuasso al Monte; 15, Varese; 16, Montorfano; 17. Baveno; 18, Roccapielra; 19, Bieila; 20.

Ivrea; 21. Mt Rosa, 22 Matterhorn {Cer\/ino). 23 Dent Blanche area; 24, Aost-a; 25, Passo del Gran San Bernardo: 26, Mt. Bianco;

27, Passo det Piccolo San Bernardo, 26, Gran Paradiso: 29. Dora Maira area; 30. Cima dell Argentera; 31, Ormea. 32. Mallare. 33,

Case Tuberto; 34, Aipi Apuane area; 35, Siena, 36, Lardereilo; 37, Monticiano, 38, Roccastrada; 39, Mt Leont; 40, Mt. Amiata: 41,

Mts. Romani; 42, Mt. Facito; 43, Longobucco; 44, Sila area; 45, Rovale; 46, Serre area; 47, Aspromonte area; 48, Mts. Peloritani

area.

GEODIVERSITAS • 1997 • 19(2)

205

Cassinis G.

intrusives, including granitoids and subordinate

gabbro-diorilic bodies, aiso crop our.

Upper Faleozoic units in the tfelveric (or Dau¬

phinois) Zone s.L ot ïhe western Alps occur in

the upper Val d’Aosca and in surrounding Swiss

and French territory. Huge intrusions (e.g. Mr.

Bianco granité; 316 Ma, Bussy et ai 1989) took

place dui'ing Carboniferous rimes. Along rhe

Italian slope of the Argentera massif, a fcw

Wesephalian-Stephanian rock-sequences, lying

unconformably on the basement,, crop our loc-

ally. Radiometric age-dating of rhe Argentera

central cote granité and other rocks (286'

293 Ma, according tu Ferrara & Malaroda

1969), which inrrude ihe pre-Wesiphalian meta-

morphic complex^ is largcly in agreernent with

the âge suggested by the afbre-mentioned Upper

Carboniferous cover.

In the western Ligurlan Alps, rhe Upper

Carboniferous is well-known, and again consists

of continental mctavoltanics and inetasediments

(Cortesogno et al. 1988). In the extenial

Briançonnais (Fig. 2), the (Late)'postHercynian

sequence, which rescs unconformably upon a

pre-Namurian crystalline basement, commences

with some detrital deposirs and calcalkaline rhyo-

litic ignimbrites, which are also widespread in

the internai sectors. Graniric dikes, and subvolca-

nic and intrusive graniioid bodies, which are

probably connected with this early magmaric

phase, occurred at different cru-stal levcis. Laler

on, fluvial to lacastrine, coarse- to Pine-graincd,

clastic sédiments and local graphiric lenses, as

well as rhyolitic and andesiric eruptive products,

were deposited wichin faulr-bounded basins,

which persisied up to Lare Permian cimes.

Among these sedimentary unies, rhe Ollano

Formation (Fig. 2), at mosr 1000 m rhick, repre-

sents the latéral équivalent of the Frcnch

“Houillère” Zone. Morcover, the ubiquitous

andesiric, tuffaccous and lava flow products (E/e

Formation), which characterize rhe Late

Paleozoic middie volcanic épisode of the

Ligurian Briançonnais domain, display a subal-

kaline potassic sériés with calcalkaline affinity

(Cortesogno et al. 1992). A number of fo.ssil

plants, idcjidfied as Pecopteris plumma dentatas

Sphenopterb schatzlarensis^ Imparipteris (Neuro-

pteris) obliqua, etc. (Bloch 1966), classified the

afore-mentioned deposirs as upper Wesrphalian-

htephanian (Cerro et al. 1969) and possibly

slightlyyoungcr Permian (Vanossi 1991).

API‘NNINUS

In rhe Apennines, Llppcr Carbonilcrous outerops

are well-known in the north-eastern Pisan Mts.

and ncar Jnno, south of the Arno River, In the

former area (Fig. 3), the San Lorenzo .Schists

consist of black silty shales, with graphiric layers,

which gradually pass, in the uppermost part, to

coarse-graincd sédiments, which can he as much

as 300 m thick, and arc rich in plant fossils ran-

ging from Wcscphalian D (?) to Early Permian

(Remy in Rau & Tongiorgi 19/4). Pclccypods,

ostracods and insects aIso occur. The cristalline

suhstraie should occur below this unit.

The (Late)-postHercvnian. weakiy metamor-

phosed, lower sequence ol Jano (Fig. 3), south of

Vblterra, is c.ssenrially made up of alluvial-dcltaic

sandstorie and dark-grey shales, which are a lew

dozen inerers thick, and incliide plant remains

and shallow marine organi.sm.Si such as crinoids,

pciecypods and possibly hrachiopods (lano

Formation). The flora has bcen identified by Vai

ik. Francavilla (1974) as belonging to rhe

Scephanian A.

Marine influences were aiso reponed for the

Island of Elba, where a Permo-Carboniferous,

recronized and slightly mcramorphic succession

of dark-grey detrital sédiments and graphiric

levels crops out ncar Rio Marina, aJong rhe cas-

rern coast (Fig. 3). Thc^e rocks yicid pelecypods,

crinoidsv echinoids, hrachiopods, lusulinids

[refeired to as ParafusuUrta (Bodechiel 1964;

Kahler & Kalilcr 1969)] and plant rcmains. Vai

(1978) suggested that thèse fossil-bcaring heds

range from near the Westplialian-Sccphanian

boiindary to the Early Permian. The unit bas

been interprered as a prograding deltaic deposit.

Furiher south, the Mr. Calamira Schists perhaps

represent a more metamorphic équivalent ol the

Rio Marina Formation (Vai 1978).

Fig. 2. — Some selGcted and schematic Upper Carboniferous-

Permian continental successions in ihe Italian Alpine régions

(localities in figure 1). Abbreviations; VGS, Val Gardena

Sandstones; VE. Verrucano Lombardo- Vertical distances not

time or thickness-related. Géologie time scale from Odin & Odin

(1990).

206

GEODIVERSITAS • 1997 • 19(2)

LOCATION

Cfu»EllTO

TKECIOVO

SERIANA

DI BATTISTINI

ETAL. >988

OIOBBI ET AL.

1981

VANOSSI ET AL.

1*91

iTguTlfcTiU-,

SEDIMENTARY STRUCTURliS CD «mcretion (F« irx)»»,

O gypsum, C cwboMtc)

Z/y large scale ctobs stratification

/ ... * palaeosol

^ -/ small scaJe cross stratincabon

(r tipplc*)

parallel strati6catioo

lamtnaiioQ 1. cooonental teciMmiPâmed.

f fim-gniBed, I tenisaifie)

SC7 chanoci

3. deltaic shailon'

-v-<r mud cracks manne

FOSSIL CONTENT

^ plants

^ palynofloras

<0? tetr^KxJ footprmts

fusulinids

^cnnoids

O brachiopods

X bivalves

^echiDodenns

l ^-^l conglomerates-brcccias

[ J [T| érosion and/or

' -l—L-L. non déposition

undifYereniiated andcsitic to rtivolilic lî

' (volcanoclastic deposits locally)

i" rhyolitte volcanoclastic deposits

(ignimbrites. tufTsi

11 /, 1 1 rtiyodaciiic volcanoclasùc deposits

I (ignimbrites. tufTs)

ENVIRONMENT

erosional surface

unconfarmity

^ A chens

carbonate nodules. letues^ etc.

coarsc sandstones

> bioturbafion

S. shalldw marine

Continental Permo-Carboniferous deposits in Italy

Cassinis G.

Along the Tuscan Marenimn, tn the south-

eastern Argentario promontory, the Triassic

Verrucano cla^tic clepositi untonformably ovcriie

weakiy metamorphosed grey and black sandsto-

ne, which alternâtes with prévalent, black, carbo¬

nate shales (Argentario Sandstones; Fig. 3).

Scattered conglomcrâtic and quart^itic layers aLso

occur. Vai (1978) pointed out tlic local presence

of crinoid temains and suggested a shallow mari¬

ne environment for tliese deposits. Fhc âge bas

been teiuaiivcly identified by l.a/v.arotto et al.

(1964), and by Gasperi & Gelmini (1973), as

Late Carboniferous. l'urther East, in the nearby

Romani Mts., prévalent .sandy, phyllitic, mono-

tonous rocks, generally relerred to as

Carboniferous and/or Permian, trop out again

beneath the Verrucano s.l. (Coeoz/a et al. 1974;

Gasperi &; Gelmini 1975; Az/aro et al. 1976).

However, according to Mcccheri (in Conti et al.

1991), thèse rocks vvere probably aftected by the

Hercynian Sudetian phase,

Widespread and thick Paleo/.oic sequences are

also présent in sevcral deep wells in the geother-

mal fields of cenrral-southern Tuscany. In the

Larderello area, Llter & Pandeü (1990) related a

sériés of dark, grey-black phyllitcs, with quartzii-

ic intercalations, to the Upper Carboniferous

deposits présent eisewhere m the région CSan

Lorenzo Group” in Bagnoli étal 1979). South-

east of Mount Amiata, in the Piancastagnaio

area, the 'J'rias.sic Verrucano ovcrlies 2U00 m of

graphitc-rich phyllites, metasandstonc and meta-

gray^ackes (tormarion A, Eltcr & Pancieli 1991),

which locally yicid crinoids, brachiopods, calca-

rcous algae and other fossil rcmains. They may

bc corrclated to the turbiditic karma Formation

of the Montici.ino-Roccastrada massif, which

was identified by Coeozza et al. (1987) as late

Bashkirian-Moscovian in agc.

In light of the above, the Late Carboniferous pic-

turc of the Apcniiinc continental domains shows

no évidence of intense magmatic activity. By

contrast. chis activity was constsrcntly présent in

the Alps and rhe “Calahro-Peloxitan Atc”.

Moreover, it i.s worth mentioning chat in South¬

ern Calabria, as in ihe Ivrea Zone, mafic-igneous,

basic bodies occurred, around 300 Ma, during a

granulite-facies iiietamorphisni.

PERMIAN

The Permian System of the continental domains

under discussion may be, for the most part,

divided Lato cwo groups or cycles. The lower

cycle, which is connected with the previous one

of Late Carboniferous âge. consisrs of prévalent

dctficic and volcanic depo.sits, wherea.s the upper

cycle generally includes the Verrucano-Val

Gardena red clastics. However, the Apenninic

Verrucano pertains to Triassic rimes. Moreover, a

marked unconformity, which is associated with a

gap of uncertain duration, séparâtes rhe lower

group from the stratigraphie cover.

SOUjHi-KN Al.PS

In rhe South Alpine région, the lower group is

made up of calcalkaline. intermédiare and acidic

volcanics which alternate, in sonie suike-slip or

pull-apart basins (Cassinis & Perotti 1994), with

alluvial and lacusrrine piliciclastic deposits.

Intrusive, largely calcalkaline graniroid rocks,

which arç concentrated in the area wesc of Lake

Maggiore and along and near important rccconic

lines {c.g. the Giudicarie, Pusteria and Vaisugana

hncs), are also attributed to the samc igneous activ¬

ity, From West to east, the Biella-Valsessera, AJzo-

Roccapietra, Moitarone-Baveno, Montorfano,

Cuasso al Monte, Val Biandino, Mt. Sabion, Mt.

Croce, Ivigna, Bresvvanone and Cima d'Asta pluto-

nic masses represent the best-known examplcs, and

generally hâve an intrusion agc of around 275 Ma

Moreover, in the western South Alpine scctor, it is

worrh noting chat calcallcdinc mafic-to-intcrmcdi-

atc bodies intruded bcforc, during and afeer the

granité batholith emplacement ol the so-called

‘‘Sérié 4<?i î-aghi'\ which i.s teci(,)nically juxtaposed

to the lower crustal Ivrea-Verhano Zone (Ginbbi

Origoni et al 1988). Among tbese bodies, an appi-

nitic .suite predates rhe uplift and érosion of the

Hercynian bcit and the intrusion of the granité

pkitons (Boriani et al. 1988).

In the BolzanO'Trcnto and Varcsc-Lugano areas,

the igneous. extrusive covet is generally represen-

ted by voluminous sequences of up to 1500-

2000 m in iliickne.s.s. On the basis of an ideali/ed

.stratigraphie succession (Di Battisiini et al.

1988), the Bolzano-Trentü Southern plateau is

divided from base to top into:

208

GEODIVERSITAS • 1997 • 19(2)

CARBONIFEROUS

Fig. 3. — Some selecled and schematic Upper Carboniferous-Permian stratigraphie successions in the Tuscan areas. Localities and legend in figures 1,2 respectively. Vertical dis¬

tances not time or tbickness-related. Géologie time scale from Odin & Odin (1990).

FOSSILSl

Cassinis G.

1. A “Lowtrr Group” composée! ot (basaltic)

andesitic lavas, trach}Thyolitic lavas, rhyodaciric

ignimbrites, dacitic'rhyodaciric lavas and, again,

andesitic lavas.

2. A more homogeneous “LJpper Group” compris-

ing rhyodacitic ignimbrites, daciric-rhyolitic

lavas, and rhyoliric ignimbrites (Fig. 2).

Early Permian volcanism is indicated by Rb-Sr

biotite isochron, which ranges from 276 ± 2 Ma

to 267 ± 2 Ma (Barth et al. 1993). and by

congruenr biotite mode! âges estimated from

rhyodacitic ignimbrites irt the Power and Upper

Groups (D’Amico & Del Moro 1988). and rhyo-

litic ignimbrites in the Upper Group (D’Amico

étal. 1980).

The igneous, eftusive. calcalkaJine succession of

the Ganna area, near Vaiese. is made up, from

base to top, as follows (Bakos et al. 1990);

1. Rhyodacitic and rhyolitic tutfs which are

intercalated with rhyolitic ignimbrites; rhe upper

part consists of alternating luyets of cUstics:

2. Clastic and syn-volcanic epiclastic rocks

(mainly composcd of occasionally thick pyro-

xene-biotice bearing, andesitic to dacitic lava

flows) with overlying rhyodacitic tuflfe and rhyo¬

litic ignimbrites with udfs;

3. Tiiffs> Ignimbrites and lavas of rhyolitic to

rhyodacitic composition.

In the Varesc-Lugâno area, the lop of the afore-

mentioned leucogranitic Cua.sso al Monte or

Ganna stock intrudes into this section. Hunziker &

Zingg (19S0) suggesred, on the basis of available

Rb-Sr whole-rock isotope data on some rhyolitic

volcanites of the Val Sesia and Lugano région,

thac the volcanic activity occurred some

278 ± 3 Ma ago. Moreover, .Stille ôe Bullerri

(1987) poînted out that the best âge estimate of

the Lugano volcanites is given by a Rb-Sr miner¬

ai isochron of 262 ± 1 Ma

Gcnerally speaking, rhe hypothesis of an Early

Permian and, In some places, a Latest Carboni-

ferous interval for this post-orogcnic volcanism,

agréés fairly well with ihe available paleoniologi-

cal data coming from the intervening sedimenr-

ary basins, /-f- rhe well-known fossiliferoiis

Orobic, C-oilio and Tregiovo fault-bounded

basins ol the central South Alpine (Fig. 2).

However, the macro and microfloral ;LSsemblages

of the typical Collio and Tregiovo beds, espe-

cially tbe oncs pertaining to the latter unit, gene-

rally cnable us to attribute ihem lo late Early

Permian and early Late Permian times (see the

Remys and Doubinger /;/ Cassinis et al. 1995;

Fig. 2). In particular, tlie palynomorphs recogni-

zed in the Tregiovo Formation, which include

Lueckisporites virkkiae, Corisaccites alutas,

Cmeisatrites vansulcatns, Pamvesicaspom splendens

and other fonns, would seem to indicaie the pré¬

sence of Upper Permian, including the Kazanian

deposits- Thereforc. the overlying, calcalkaline,

rhyolitic ignimbrites appcar tu testify that the

volcanic activity of this are.i (and probably of a

vast part of chc South Alpine segment) ended

during younger Permian cimes, before lhe dépo¬

sition of the prc-Triassic Vcrrucano Lombardo

and of rhe more or less coeval Val Gardena

Sandstonc. V^ithin a general stratigraphie Frame¬

work, the more récent investigations on the

tetrapod footprints found in the.se basins

(Ceoloni et al. 1987; Conti et al. in press) also

toncord with this dating.

Therelore, in the South-Alpine segment, the

Vcrrucano-Val Gardena redbeds, which un-

confonnably ovorlie the above-mentioned depo-

sits and step down onio the Hercynian basement,

pertain to the Upper Permian younger cycle. This

clastic liibosome is generally missing from Lake

Como to the western extremity of the chain.

WESILRN Ai.I'S

Along the western Alps, the Flercynian basement

of the iower vVu.stroalpine domain underwent a

Permo-Carboniferous H F-LP rnetâmorphism

chat was duo to a geothermal anomaly. which in

turn was caused by the asiheno.shere upwelling

and gave rise to granulitic Faciès. This substrate

includes gabbros and granitoids, vvhose âges are

not aiways well dcfincd, which crop out in chc

Dent Blanche (Matterhorn gabbro, c.250 Ma;

Dal Piaz et ai 1977) and other ncarhy snialler

klippens. Sedinients and volcanics below the

Upper Permian Vcrrucano clastics, as well as

(lare)-postHercynian granitoids, bave .dso bcen

indicated in some Pennine atcâs of chc chain.

In the Ligurian Alps, the présent pre-Piedmont

Zone (Fig. 2) is locally characterized by the

Lower Permian, meta-volLanicla.stic Aimoni

Formation of the Melogno “porphyroid” Group,

210

GEODIVERSITAS • 1997 • 19(2)

Continental Permo-Carboniferous deposits in Italy

which is unconformably cappcci by the younger

prc-Triassîc Vcrrucano. At the same time, the

Briançonnais area (Fig. 2) was afFected by wide-

spread, thick, calcalkaline, rhyoliric and suhordi-

nacc rhyodacuic ignimbrites. together with

pyroclasticü (the so-called aiore-mentioned

Melogno porphyroids); in the uppennost part,

however, Cabella n ai (I98*S) found évidence of

the onset of a sub~.ilkaline porassic composition

in the Ormea area. In the Helveric (Dauphinois-

Provençal) Zone o( the Argentera massif, the

Permian continental deposits are extensively

dcvcloped, wuh a thickness of almosr 2000 m on

the French slope.

In the western Alpine domain, the above-

mentioned deposits of rbe lower cycle are un-

conformably overUin by the Verrucano clastics of

the Upper Permian cycle,

Apknninhs

According to Bagnoli et ai (1979), Permian vol-

canism probably occurred In ilic western Apuane

Mrs. of Tiiscany, as intlicated by rhyolitic cla.st.s

in the basal part of the Middie Trias.sic

Verrucano. This magmatic activity is aiso sup-

ported by the presence of sorne granltic block.s

(308 ± 10 Ma to 287 ± 10 Ma, Eberhardt et al

1962) in.side the Ligurian allochthonoiis structur¬

al unies, rhesc unies hâve been interpreted as

crustal fragments, partially derived (rom the

Tuscan continental margin (F.lter etlü. 1966).

Further south, in somc areas of tlic Prsan Mts.,

ihere are red hreccias and conglomérâtes, the so-

called Asciano Formation, which arc up to 80 m

ihick and of undefincd âge, Fhese clastics, inter¬

preted as scarp-foot alluvial deposits (Rau &

Ibngiorgi 1974), lie citlier on rhe San I.orenzo

Formation oj- dircctly on the Hercynian meta-

morphic basement (Fig. 3). The presence of red.

rhyolitic clasts in vhe ovcriyiiig, basal Verrucano,

a feaiure not previou.sly observed in the Asciano

Formation, susses chat volcanism was probably

active dtiring Permian times, ahcr the Asciano

was deposited, but bcforc the Middlc Tnassic

Verrucano.

South of the Amo River (F1g. 3), ma.ssive poly¬

génie detriud deposits ( Forri Formation) and

porphyric products (partly interpreted as acidic

volcanics) overlie the lano Formation. Although

the dating of both iinits Ls uncertain, il is likcly

tbat the porphyric products are Permian. The

Triassic Verrue,ino crops out unconformably

above this section, with internicdiatc, purple,

carbonate-bearing siltstones occurring locally.

In the Larderello geothermal area, the presence

of clastic units, such as the Mts, Pisani Asciano

Fm. and the redbeds (including cJascs of acidic

volcanics) of the so-called Castclnuovo

Sandstone, which rescmbles ihc Val Gardcna

Fni. of the Dolomite Alps, seems to indicatc a

wider Permian comincnial domain. Morcover, in

the Moiinr Amiata geothermal field, below the

Triassic Verrucano, wells levcal a Palcozoic, meta-

morphic .md tectoniscd clastic séquence, where a

carbonate levcl with Latc Permian tusul-

inids, such as Praeparajuititiaa ci. luîigin 'u

Polydiexoelimi {nopolydiexodina}) cl. shabalkinh

Camellina sp., Parafnsultna sp., Psedojttstdina sp.,

etc,, occurs at the transition between vhe so-

callcd formations A c C (Elter & PandcÜ 1991).

According lo Pasini (1991). the whole associa¬

tion indicates the Cancellina Zone (Kubergan-

dian): in addition, ihe presence of Pmeparu-

jusidina links this finding to thaï oi Bodcchtel

(l‘)64) in the Island of Flba, and aIso to the

Artinskian oi the Southern Alps. Thus, fiom the

above it may bc hyporhesized that a great part of

formation C (about ^00 m drilled) is Permian in

âge (Conti et ai 1991).

On the Island of Elba (Fig. 3), che upper pan of

the Rio Marina Formation, which includes allu-

vial-deltaic and marine sédiments with

Pamfusu/imt sp., bclongs to rhe Early Permian.

Continental, clastic deposits, bcncath the Tnassic

Verrucano, have aiso been attribured, at Icast par¬

tially, to the same âge in the Argentario and

Romani Mts. (Fig. 3).

Farther cast, in Southern Tuscany, benveen the

Montagnola Senese and Mt. Leoni, the Upper

Paleozoic scquencc is essentially characterized by

the presence of marine conditions.

In the Southern Apennincs (Basilicata), mainly

Upper Permian (Murgabian-Dzhulfian sJ,) car¬

bonate clastics occur in tlic lower part of the

Triassic Mt. Facito Formation. A continental

régime at the end of the Permian (Dorashamian)

may be presumed, as we have no data co prove

otherwise.

GEODIVERSITAS • 1997 - 19(2)

211

Cassinis G.

The “Calabro-Peluritan Arc”, which is rhc resuit

of at least six different composite microplates ot a

former Hercynian basement (Vai 1991). reintro-

duces continental domains. The metamorphic

SLibstratc was gcnerally intrudcd by granitoids;

however, a Pcrmo-Carbonifcrous cover is lacking

or unknown. In thc Longobucco structural

block, granodiorites and youngcr AbSiO;^ - bcar-

ing granités, of 284 + 14 Ma (Wicland 1978)

occurred betore the déposition ot Verrucano-typc

red clastics, relerred to by Baudclot a ûL (1988)

as the top of the Triassic. lo rhc south. ncar

Rovale, gabbrc)ic and dioritic bodies with Rb-Sr

biotite cooling âges of 2/0-280 Ma (Caggianelli

et al. 1991), as well as other close granodiotitic

rocks, are eut by porpbyriric gnmitic dikes and

plugs. According to Campana et ai (1991), in

the Serre-Capo Vaticano areas, the radiomctric

age-darings of calcalkalinc granitoids, which

range front tonalités to granodiorlrcs-monzo-

granites, with minor quartz diorires/gabbros,

hâve been esrimated as approximately

270-291 Ma. In the Aspromonre block, the

time-span of some peraluminous intrusions

wirhin thc Hercynian metamorphic basement

ranges berween 282 and 286 Ma [in Spallecta &

Vai 1990).

In the above-ciied areas, the sédiments related to

the Verrucano belong to thc Triassic. The Tuscan

deposirs lie unconformably on chose of the lower

cycle, or .step down dircctiy over the Hercynian

metamorphic subscrarci and are generally ascrilted

to Mid-Triassic rimes. Although the Apcnninic

Verrucano is nor generally as young as the

Carnian. récent dating of rhc Longobucco and

Longi Verrucanoes in thc '‘Calabro-Pcloiitan Arc"

as latest Triassic (Baudclor et al. 1988) places an

outside limir on rhc diachronism of the deposit.

SlClLY

In north-east Sicily, the Mts. Peloritani block

includes some granitoids, which date from

293 ± 9 M;i, and are situated within a strongly

deformed crystalline subsrrace and below a Triassic

Verrucano-like clastic unit (ui Spallecta &: Vai

1990). As in Basilicata, the western secror of che

island dispbys bighiy fossiliferous Permian marine

deposirs, the basement pf which is unknown

GENERAL REMARKS

In the record o( continental domains in Italy

from Carbonilerous through to Triassic we can

recognize several sedimentary and/or tectonic

cycles as well as orher events.

In some Alpine régions a first main cycle began

in the Lare Carboniferous, where jc is documen-

ted by the Westphalian-Srephanian deposirs of

the Como-Maggiore area, of the western Liguria

(Viozene) and of orher localities. This cycle

continued, in a seemingly more widespread

fashion, into various ievels of the Permian, up to

rhe onset of che so-called Verrucano rock-units,

which belong to rhe upper part of this System.

In some placer of the central South Alpine sector,

as in the Collio and Iregiovo basins, rhe macro-

and microfloras présent generally enable us to

attribute che above cycle to the lace Early

Permian and, in particular regarding the

Tregiovo beds. also to slightly youngcr Late

Permian times. However, as thc Permo-

Carboniterous sedimentary and volcanic succes¬

sion of rhe Alpine région is subjected to

consistent and rapid géométrie changes, it is pro-

blematic and ohen impo.ssiblc to achieve exten¬

sive conelattons of rhe local data. Purther

difficulries arise owing to thc présence of strati¬

graphie di.sconttnuiiies. Phesc unconforrnities

are not only confined to the houndaries of this

lower cycle but al.su occur inside its vertical and

latéral development, and mark rhe présence of

gaps ol various but as yet unknown time-dura-

tion.

As indicaied earlier, in the Alpine continental

areas, ihc Verrucanoes and, lo the east, the more

or less coeval Val Gardena Sandsiones (logether

with some underlying conglomeratic units, such

as rhe Daone Cgi. in thc Giiidlcane area) mark

the beginning of another Permian upper cycle.

Palaeonrologic data (plants, palynomorphs, tetra-

pod footprints) and thc stratigraphie position of

the \'al Gaidena redbeds, which pass laterally and

vertically to thc Upper Permian shallow-marine

Bcllerophon Formation, generally ascribe che

above unies to Latc Permian. The overlying Lower

Triassic Werfen Formation and its latéral équi¬

valents unquesrionably confîrra iliis attribution.

In the Tuscan Apennines, the stratigraphie

212

GEODIVERSITAS « 1997 • 19(2)

Continental Permo-Carboniferous deposits in Italy

schemes and other data in rhe texi indicare the

persistence of the aforementioned older cycle.

Howcver> as in lano and Elba, the continental

deposits show some Late Carboniferous to Early

Permian shallow-rnarinc intercalations, which

testify to a former irrcgular landscape of the

région, Moreover, the Upper Permian cycle has

noc, as yct, bcen recorded in this area. According

co the stratigraphie successions oi figure 3, the

Verrucano deposits cssenrially deVclopcd during

Middle Triassic times. As a conséquence, the

présence at P.ta Biancâ, ncar La Spezia, of pré¬

valent Anisian and Ladinian marine deposits

(Martini er ni 1986; Passer! 1988), which rest

unconformably over rhe ï"îercynian crystalline

basement, leads us tt» relaie ilie overlying

Appenninic Verrucano to a cycle évolution which

does noc coïncide with rhat of rhe Alpine région.

In figiu'cs 2, 3, the contact beween rhe two indi-

car-ed cycles orgroups deals vvirh cecconic, paleo-

géographie and probably palcoclimatic

variations. Structural highs and lows during the

older cycle were formed in the context of a pré¬

valent tectonic cranscurrent régime (sec Arthaud

Marte 1975; Vai et ai 1984; Ziegler 1984;

Ma.ssari 1988; Rau 1990; Cassinis üc Perorii

1994; and others) which, during the younger

cycle, chatigcd into a more pronounced exteasio-

nal iramework. Moreover, in the South Alpine

area the second cycle led to a complété extinction

of the (late)'posrHercynian volcanic activity,

Erosion during the h>rTnation ol rhe Verrucano

an<l Val Gardena deposits generally caused pro¬

gressive flartening of rhe landscape, and this ulri-

mately favoured a décisive transgression of the

sea. However, the shallow-marine intercalations

in somc Stephano-Autunian rocks {Lnio, Elba) of

the northern Apcnnincs dcmonstracc the relative

proximity of rhis sca trom Latesc Carbon if crous-

Early Permian times, and indicare a general

provenance from rhe easr. These incursions

reached north to the Garnie Alps, where the

post-Wesfphalian succession of the lower cycle

was persistenrly characterized by marine condi¬

tions.

South of Tuscany, the parricular gcological scéna¬

rio of the “Calabro-Peloritan Arc”, which is rich

in the pre-Triassic plutonics but lacks a mid-

Carboniferous-Permian sedimentary cover, prob-

ably derived from a group of lands in front of the

Corsica-Sardinia block, but differcncly situaccd,

and sccmingly affected by a mosaic of deeper

structural levels that were later exhumed by the

Alpine cycle.

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216

GEODIVERSITAS • 1997 • 19(2)

Upper Carboniferous to Lower Permian

continental deposits in Sardinia (Italy)

Giuseppe CASSINIS & Ausonio RONCHI

Dipartimento di Scienze délia Terra,

Via Abbiategrasso 217, 27100 Pavia (Italy)

Cassinis G. & Ronchi A. 1997. — Upper Carboniferous to Lower Permian continental

deposits in Sardinia (Italy), /n Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: strati¬

graphie corrélations, Geodiversitas 19 (2) : 217-220.

KEY WORDS

continental basins,

sedimentary deposits,

igneous products,

Upper Carboniferous,

Lower Permian,

Sardinia.

ABSTRACT

The paper is a brief outline on the sedimentary and volcanic continental suc¬

cessions ot a number of Sardinian basins, which hâve been attributed to

Permian and, locally, also to Late Carboniferous rimes. In general this (late)-

postHercynian picture is similar, in most aspects, to the situation in nearby

Corsica, and is also reminescent of conditions in South France and Spain,

with which Sardinia and Corsica were linked before beginning their drift

toward the Tyrrhenian.

MOTS CLÉS

bassin.s continentaux,

depots sédimentaires,

produits ignés,

Carbonifère supérieur,

Permien inférieur,

Sardaigne.

RESUME

Cette note est un aperçu des successions sédimentaires et de volcanisme

continental dans les bassins de Sardaigne qui ont été attribués au Permien et,

localement, au Carbonifère supérieur. En général, cette photographie du

(tardi)-posthercynien esc similaire dans la plupart de ses aspects à la situation

de la Corse voisine et évoque aussi ce que l’on connaît en France méridionale

et en Espagne, avec lesquelles la Sardaigne et la Corse étaient liées avant leur

séparation vers la Tyrrhénienne.

GEODIVERSITAS • 1997 • 19(2)

217

Cassinis G. & Ronchi A.

After rhc fïercynian orogeny, during l.ate

Carboniferouü and Early Permian times, a large-

scale calcalkaline magmatisrn took place on the

island (Fig. 1). The intrusive sequence gave rise

to hundred-s of plutons over a period of more

than 25 Ma, from at leasr 310 Ma ro about

280 Ma 'l'his plutotiic compicx forms the South¬

ern part (about 6000 km^) of tbc Sardinian-

Corsican bailiolith, which, tn Sardlnia, largdy

comprises tonalités to tonaJitic granodiorites and

younger monzogranitic granodiorites to leuco-

monzogranites. Post-tectonic plutons, which

0 _ÿKm

UPPER CARBONJFEKOUS-PERMIAN

CONTINENTAL SEDIMENTS AND VOLCANICS

VARiSCAN PLinONlC COMPLEX

Fig.1 . — Location map of the stratigraphie columns drawn up in

Fig. 2. 1, Pta Lu Caparoni; 2, Perdasdefogu; 3, Escalaplano; 4,

San Giorgio.

occurred under a tensional régime after rapid

régional uplift, contain leucogranites (Ghezzo &

Orsini 1982; Carmignani et nL 1989).

The (late)-postHercynian terrigenous and volca-

nic sequence lies unconformably on a heteroge-

neous, generally tectonized metarnorphic

hascmcnc. As in many parcs of Permo-

C'arboniferous continental Europe, it is made up

both of fluvial to laciistrine clastic deposits,

which accumulated within more or less subsiding

fauU-bounded basins, and of wider volcanic pro-

ducts, which are generally acidic to intermédiare

in composition.

At présent, the San Giorgio Basin in [glesiente

(SW Sardinia) appears to be the oldesT Upper

Palacozoic sedimentary outerop on the island

(Fig. 2). Its upper dctrital deposits, on the basis

of tossil macroflora vvith Pecopieris, Calamites^

Nenwpieris, Corduiles^ etc. (Coeozza 1967), and

of palynoflora which yields Calanmpom pallida^

Florirntvs parims^ etc. (Del Rio 1973), bave-been

identified as belonging to the Upper Srcpbanlan.

More reccntly, howeveu in the lowcrmost layers,

rhc discovery of cccrapod fbotprints, which hâve

been referred to ihe genus Salichnium (already

recorded from the Wesiphalian of Central

Europe and Nonh Africa) and ihus attribuicd to

microsaurs, has encouraged the hyporhesis that

the sédimentation may hâve begun in the San

Giorgio Basin in former cimes (Fondi 1980).

On the other hand, during rhc Early Permian, a

certain number of well-developed basins (Mt. Lu

Caparoni in Nurra, Seui-Seulo in Barbagia,

Perdasdefogu in Üglfasrra, Escalaplano in Cierrei,

Lake Mulargia in Sarcldano, Guardia J^isano in

Sulcis) occurred on the island. Phey were charac-

terized by rhe above-mentioned (laie)-

postHcrc)mian succession (Fig. 2), during which

volcanic products (tuffs, ignimbrircs, lavas and

other igneous exirusive aspects) played an impor¬

tant rôle, and were widespread over exrernal areas.

These continental deposits, which range in

thickness from a dozen to some hundreds of

métrés, are normally rich in Aiuunian plants,

sLich as Anmniax Odontopteris^ Pecopterisy

Anniilarîti^ Ernestodendriou^ Iheniopteris^

Sphenopteris, Corduites^ etc. (Novaresc 1917;

Oosterbaan 1936; Maxia 1938; Comaschi Caria

1959; Pccorini 1962, 1974; Gasperi & Gelmini

SASSARI

nuorq,

IRISTANO

CAGLtARI

218

GEODIVERSITAS • 1997 • 19(2)

U. Carboniferous and Permian continental deposits in Sardinia

I— 1325

1 ;, ,,j ^ irZ-j

1.,,! un<iiflerc«n«edc*lcilkllinc •• sandsloncs

j* "lahaf deposils* l'®’-®*! t^bonale nodules ahalcs, mudalones

cherts ( _>s . ! dolostones I*", “al

|T 11 11 crosion and/or

min dqKsilion

—vyç- croai'mvl «utriicc

•i»uu.utfo»miiy

LNVlRONMfcNl

1. cofKinenial

tc.euane-pamed,

f; fïne-graiited. ,

hlacustrinc)

StÜIMHNTARY STRUCTURES

large scaJe ao» stratification

. smalIscalecrrautiTaiiticahnn

(« ritifiln)

paraRel straliHcalion

lominatinn

channei

' paUeosol

biolurbation

^ slunipitig

FOSSILCONlENf 1

plants

^ palynofloras

iCl fish leeth and scales

nsiracods

^ amphibians

^ fooipnnt»

Fig. 2. — Some Upper Palaeozoic sedimentary and volcanic successions of Sardinia. Vertical distances not time or thickness-re(a-

ted. Géologie lime scalefrom Odin & Odin (1990).

1980; Francavilla (•ta/, 1977i Broutin pers.

comm.) and sporomorphs, such as Potoniehpo-

rites novicus. P. hharadwaj, Latensina triletay

Candîdhpom candida, Cordaithidy Florinites,

LimhoîpoYÏtes. etc. in che Guardia Pisano basin

{Barca rt j/. 1992).

The temporal distribution of rhe overlying per-

motriassic, coarsc- ro fine-grained, mainly red,

dctriiic sédiments, as »n rhe Mt. Lu Caparoni

and Lakc Mulargia basins, is not yet clearly de-

fined. The lower boundary of these clastics pro-

bably .scals a gap of different, but still uncertain

magnitude.. Morcover rhe radiometric age-dating

from a large number of Permian volcanic rocks

(Cozzupoli et ai 197L 1984; Del Moro et al.

1974; Lombanli et al. 1974; Ldcl et al. 1981)

produccd unrcliable results.

From rhe above, Ir follows thaï the (late)-

postHcrcynian picture in Sardinia is similar^ in

niost aspects, to die situation in nearby Corsica,

and is also remiiiiscent of conditions in Provence

(France) and Spain, with which Sardinia and

GEODIVERSITAS • 1997 • 19(2)

219

Cassinis G. & Ronchi A.

Corsica werc united bcforc beginning their drift

roward the Tyrrheniaii. The Lare Carboniferoiis

ro Early Permian fault-block landscape may bave

been formed duiing the rranscurrenr régime,

which is chouglu by many to bave characterized

the European Late Paleozoic climax. This régime

was contemporaneous with the extensional

movements linked ro the progressive thinning of

the Hercynian crust.

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Submitted for publication on Î5 April 1996\

accepted on ] October 1996.

220

GEODIVERSITAS • 1997 • 19(2)

Late Carboniferous to Early Permian

palaeogeography of the Italian and

central Mediterranean area

Gian Battista VAI

Dipartimento Scienze Geologiche,

Via Zamboni 67, 1-40127 Bologna (Italy)

Vai G. B. 1997. — Late Carboniferous to Eariy Permian palaeogeography of the Italian and

central Mediterranean area. /nCrasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: strati¬

graphie corrélations, Geodiversitas 19 (2) : 221-228.

ABSTRACT

An attempt is made ai deriving palaeogeographic constraints for lare

Carboniferous to carly Permian restorations from the new stratigraphie data

mainly collectcd in previously poorly known marine deposits of the circum-

Mediterranean area. The assumption of an early Permian emplacement of

oceanic crust in ihc eastern Mediterranean Levantine and lonian Seas is inde-

pendenilv supported by the new évidences of deep water faciès and faunas

from Oman ta western Sicily. 1 he bearing on the palaeogeographic recon¬

struction for the Moscovian and Artinskian time intervals are tentatively sug-

gested by mcans of two new sketch maps.

RÉSUMÉ

Un essai de reconstitution est fondé sur les contraintes paléogéographiques

du Carbonifère supérieur au Permien inférieur, à partir de nouvelles données

stratigraphiques acquises sur des dépôts, jusque là assez mal connus, du pour¬

tour Méditerranéen. L’hypothèse d'une croûte océanique du Permien infé¬

rieur dans la Méditerranée orientale levantine et ionienne est corroborée

indépendamment par de nouvelles preuves des faciCvS profond.s et des faunes

d’Oman et de Sicile occidentale. Les reconstructions paléogéographiques

pour le Moscovien et rArcinvskien sont effectuées à partir de deux nouvelles

cartes.

MOTS CLÉS

lithofâciè.s,

paléobiogéographie,

ouverture oblique,

croûte océanique,

dépôts profonds,

Téthys.

GEODIVERSITAS • 1997 • 19(2)

221

Vai G. B.

A critical rcview of surface and subsurface strati¬

graphie data published from the Italian area

(Fig. 1) in the last two décades or so (référencés

in Cassinis, Cassinis & Ronchi, Di Stefano &C

Gullo, Pasini &C Vai, Vai Ôi Venturini, this volu¬

me) has changed quite considerably the usual

interprétative palaeogeographic scénario of the

central and western Medicerranean areas in the

late Carboniferous to carly Permian time intcrval

dominated by diftercnc stages of Pangaca deve¬

lopment (Bosellini ik Hsü 1973; Smith &

Briden 1977; Rau & Tongiorgi 1981; Irving

Fig. 1. — Location map of th© Palaeozoic rocks in Italy. showing distribution and faciès of the Moscovian and Artinskian stages. M,

Moscovian. A. Artinskian. Numbers in boxes relate to legend ot figure 3. Numbers in bold refer îo stratigraphie sections described by

Vai (1978); 1-2, SW and SE Sardinia; 3-4, Slilo area and Peloritani Mts., Calabro-Peloritan block; 5, Punta Bianca. La Spezia; 6,

Apuane Alps; 7. Pisani Mts.; 8. lano: 9, Elba Island: 10. Farma area. Montidano-Roccaslrada; 13. Romani Mts.: 14-15, Lercara-

Roccapalumba and Palazzo Adriano (Sosio), W Sicily. The Verrucano Lombardo, Val Gardena and Bellerophon Formations are not

shown.

222

GEODIVERSITAS • 1997 • 19(2)

Carboniferous-Permian palaeogeography, Mediterranean area

1982; Sengôr 1988; Ziegler 1988, 1989),

According to Vai (1994), ncvv dara from penin-

sular Italy and espccially from western Sicily sug-

gest an alternative scénario. Ir is bascd on two

critical points: (1) the deep lonian to Levantine

Sea crusE is best inrerpreted as a fossil, thermally

contracted, undeformed oceanic crust eniplaced

following rhe early Permian (to poÿsibly mid-

Triassic) rrans-Mediterranean (ro Caribbean)

oblique rift: (2) the distribution of the benthic

marine Tethyan fauna (fusuhnids, brachiopods,

etc.) requires a sea-wây connecting western

Tethys CO Texas, bolivia and Colombia diiring

part of the Permian. Récent rcvicws of chc régio¬

nal Permo-Triassic data from Sicily (Catalane et

al 1995; H. Kozur, conim. at the XIII ICC-P,

Krakow. 1995) arc consisienr with the pi*evious

scénario.

'Lhis short contribution is aimed at providing a

tentative palaeogeographic interprétation of the

data collecred from rhe Inilian area and described

in the five previous contributions (rhis volume),

A synopsis of data is presented in figure I. d hc

mcaning of rhe data in rhe framc of the

Mediterranean is discussed separately following a

stratigraphie order.

LATE CARBONIFEROUS: MOSCOVIAN

(Fig. 2)

The Moscovian palinspustic picrure around the

présent Mediterranean arexs is dominated by an

emergenl area to the norih (main Hcrcynian

Europe) and a marine area to the south. Lhis

marine area is separated into an castern partly

oceanic portion and a western shallow cpiconti-

nental sea by the north-south trending large

peninsula shown as the Africa Promontory mer-

ging northward to the Hcrcynian Europe in the

Alps région.

rhe Italian area proper can bc separated palin-

vspastically into four parts;

1 . The intra-Hercynian eastern part includes the

entire Southern Alps to outer Dinarides segment,

From wesc to cast both rhe Hcrcynian chain and

its post-Hercynian cover show a consistent tran-

vsition from inner to outer tectono-metamorphic

zones and from continental through shallow

marine to deeper marine deposirional environ-

menrs. PaJacobiogeographic affinity of benthic

animais (fusulinids, cotais, brachiopods, tnlo-

bires) mainly points oui to rhe Russisn Plarform,

rhe Urals and middie Asia Moral cléments hâve

western Eumpean Eurasian affînity.

2. rhe exira-Hcrcynian Panalrican forcland of

the Alrican Promontory. It is mainly represented

by uplifting basement areas with ongoing érosion

and possible thin marine ingression over Tts

middic vvestern part (in the Gargano 1 well area).

3. The intra-Hercynian Toscan Apennine parc.

This area, poorly known until recenriy, is of spé¬

cial interest because ir shows an almost conti¬

nuons marine déposition from early-middle

Carboniferous to early Permian in a foredeep-

forelaiici setring (as for the serting of Cantabria

and the south Portuguese zone). Again from

nortii to -South a transition from inner to outer

lectonomecamorphic zones appears. Deposirional

environments, however, range from continental

to shallow marine and deeper m.irinc clastics, co

shallow marine carbonates and to émergent fore-

land- Fossil groups such as corals and conodonts

show major biogeographic relation wirh Spain

and centra! American faunas (Ferrari tt al 1977),

wlierca.s floral clcmcnts are typically western

Eu ropeun.

4. The intra-Hercynian Sardinia-Calabrides-

Kabylidcs-Betides partis characterized by scatte-

red, thin and poorly d'evelopcd late

Carboniferous to Permian continental deposics

with West European floral affiniry.

At a more general levcl, active fronts arc found

only in the oceanic domain. The continental

crust domain is rdatively quiet: no first order

transcurrenr or transform faults appear. The

exrent of shallow marine deposits outsidc llie

Hcrcynian Ironr and even inside Ls quitc large

(and larger chan in the Permian). l his suggests a

low isosiatic uplift rate of the orogcnic area,

consistent with small volumes of deep seated gra-

nicoid intrusions. Boili land and shallow seas are

characTeri'zed by a riglu neework of small-scale

pull-apart ba-sins- This rime inrerval is domina¬

ted by extension to small-scale transtensional

conditions.

GEODIVERSITAS • 1997 • 19(2)

223

Vai G. B.

Fig. 2. — Tentative Moscovian palaeogeographic-palaeotectonic map of the circum-Mediterranean area. AP. African Promontory

during the late Carboniferous. NHF-SHF, north and south Hercynian fronts. See figure 3 for legend. and Vai (1994) for further expla-

nations of symbols.

LATE EARLY PERMIAN: ARTINSKIAN

(Fig- 3)

Two quite contntsring processes are shown on the

map. A prominent régressive trend is documen-

ted in northern Alrica, front Arabia to large parts

of Lybia and Algeria, and in the Cantabrian

région (compare figure 3 witb figure 2). Relevant

trangressive conditions are sliown in the rifting

Black Sea (Dobriigca) and luli;in-Carnic areas,

and even more ail through the south

Mediterranean région as far as Tunlsia.

l'hc former African Promontory becomcs kinc-

matically detachcd from its mother Africa by the

westward opening of the Permo-Triassic Tethys,

and gives rise to a structurally independent Adria

block surroiinded by tlie Southern front of

Hercynian Eurttpe. The larger Southern part of

the Adria block becomes submerged by the

Artinskian shell' sca. Again, the Italian area can

bc divided in tu four parts;

l. The Southern Alps and exteriial Dînarides

with depositional environments ranging front

continental to shallow murine carbonates to dee-

pcr marine clastics passing eastward to the

contracting Palaeo-’lethys branch. Borh benthic

organisms and conodonts snggest Russian to

Chinese palaeobiogeographic affiniry.

224

GEODIVERSITAS • 1997 • 19(2)

Carboniferous-Permian palaeogeography, Mediterranean area

2. The Adria bl(»ck wuh mainly erosional conti¬

nental conditions to rhe north and shallow mari¬

ne déposition lo ihe south wich important

carbonate plaiforms.

3. The Tuscam ^Southern and Sicily Apcnnine

belt (extending westward to the Tunisian

Maghrebian chain). Il shows transition from

continental deposits in northcrn Tuscany (San

Lorenzo Basin, Ml. Pisano) to shallow clastics

and carbonates in Southern Tuscany (Elba Island,

Farma area) to a complété séquence *)f deposirio-

nal environments from shallow-water carbonate

platform to deep pelagic and turbiditc, whose

rocks arc often reworked as in rhe rectonîcally

shorchened Mt. Sicani (Sosio valley, and sur-

roundingaieas, western Sicily).

4. The Sardinia-Calabrides-Kabylides-Betides

belt characterized by érosion or ihin continental

déposition.

At a more general level, che following facts arc

relevant.

There is a general major coast line recréât

concurrent wiih the trangressive character of

marine deposits in the Meditcrianean beir. Tliis

is mirrored by the fact that rhe Petraian starts

with a transgression followed by régression at a

global lève! and especially in Gondwanaland,

whcreas an initial régression is followed by trans¬

gression in the Hcrcynian Southern Europe and

Northern Africa.

Large volumes of volcamcs and epiplutonic gra-

nitoids are emplaced concentrating along prefer-

red narrow bêles {e>g. the Venetian and the

Lomhardy Lakes-Corsica belts) close to major

shear lines.

Tlic already actived large-scale dexcral megasbear

in the Levantine and lonian Seas is propagacing

we.srward, accompanied by addirional fragmenta¬

tion of W Europe and iis fbrcland by tneans of a

conjugale megashear System.

The expanding f'ermo-Ttiassic Tethys shifes

Cimmeria in such a way as to close the Palaeo-

Tethys océan. Deep marine calcareous to radiola-

LATE EARLY

PERMIAN

ARTINSKIAN

Fauiis

A - Subduction

6 • Subduction

Oceanic Lithosphère

Manrte Areas

nol sutodivided

Oeecer Varm TurtMOiles

Deepe' Marine Clssiics

Deeper Marine Carbonates

Shallow Marine Carbonates :

Shell Mat Caibonales '

& ClâEhCS

Shallow Marine Shaies

Coast Line

Mainty land Areas with

1 Coniinentai Oeposrls

^3 6

□ 5

(lii 4

oooo

SHF

Fig. 3. — Tentative Artinskian palaeogeographic-palaeotectonic map of the circum-Mediterranean area. Notice the intra-Permian

crustal séparation of Adria from its Precambrian to late Palaeozoic motherland Africa (see figure 2 for symbol explanation).

GEODIVERSiTAS • 1997 • 19(2)

225

Vai G. B.

ritic faciès havc a clitnax within thc eastem and

centra] Mcditerraneati area which wlll be more or

less contiiuiing up to the latc Iriassic espccially

in the two Permo-Iriassic Tethyan edges. In Tact,

the regionally anotnalous marine to deep marine

Permo-lriassic or ‘Inassic séquences (or materiai)

of Punta Bianc.i (N Tuscany), Monte Quoio

(S Tuscany) and Lagonegro (I.ucania) can be

connected onJy with a sourh-eastern sea-way.

The niid Triassic aikaiinc volcanics of W Siciiy,

Punta Bianca, Lagonegto, Biidva, Pindos (ail

associated with deep pclagic rocks) and those

similar of thc Iblci Mts. in £ Sicily (associated

with shallow-watcr carbonate platlorm) arc

consistent with rliis pîcturc. ThLs is jurther truc

aiso for thc dccp-pclagic calcarcotis ro radiolaritic

Triassic fàcics in Halstatt (Austria), Lagonegro

(S Italy) and Sicani Mts. (W Sicily), which are

located just at the apex of the closing northern

Tethyan arm and of the opening Southern

Tethyan arm.

DISCUSSION

Some points need to be stressed.

1. The Early Permian marine bclt ranging from

Tuscany to Sicily niay bave extended westward lo

the Tunisian and Algcrian Maglirehiau chain.

Howcvetj the internai Apennine unirs containing

these important Permo-Carboniferotis marine

deposits in the Apennine.s and Sicily are less

exposed in rlie Maghrebian chain where they

may be tectonically buried under the more inter¬

nai Kabylid nappes or submerged in the western

Mediterranean offshore.

2. The famous chick mid to Late Permian marine

deposits oF Tunisia outeropping in thc Djebel

Tebaga near Medenine and cored from the well

at Bit Soirane (Douville et al. 1933; Skînner àc

Wilde 1967; Vachard 6c Razgallah 1993) are

structurally quirc disrinct from rhe Permian of

Sicily. In Tact they represenr un epi-Baikalian

cover, faulied and tilted heforc Iriassic déposi¬

tion and gcnrly loldcd during nco-Alpine defor¬

mation. Tt is located at the sourh-western edge of

the Pelagian Block, close to the limir with the

Southern Atlas chain and the almost stable

Sahara Platlorm. Moreover, thc mixed shaly-

sandy and carbonate faciès of shelf environment

shows a clear shallowing upwaais (Bellerophon

dolomitic faciès and red ‘Iriassic continental

sandstones), whcrcas thc deep water Permian

srrata ol western Sicily is foUowcd by deep water

Triassic ]imesTone.s and radiolarites. However, the

approximafely ]7l)() ni of marine mid to late

Permian exposed in Southern Tunisia clearly sug-

gests an important subsiding basin possibly

patallcJllng thc two opposite Southern (Sahara

Platform) and northern (Sardic-Calabrid-

Kabvlid-Bctic) beks charactcnzcd by continental

Permian. The E-W trending marine Permian of

Tunisia is unconformably sealcd westwarti main-

]y by onlapping Crcraceous deposits, before

being tectonically buried under thc Maghrebian

thrust belt. The Maghrebian thrust shects are

usually detached from Triassic evaporitic layers.

So, there is qui te a chance to bave a buried £-W

trending marine Permian basin filling incorpora-

ted within thc “basement” ail along the

Maghrebian chain as far as the northern

Moroccan Atlantic coast.

3. According lo Kahler (1974) rhe Fusulinid

fauna fioni 3'unisia is immediately younger

(Murghabian) vtian and bas no .specics in com-

mon with thc onc from Sicily^ alihough a .short

lime overlap cxlsts between the two faunas. This

is mirrored by a quite different original position

of the two areas and may .suggest a physical bar-

rier {e.g. a deep although narrovv sea-way) separa-

ring the Tunisian shelf to the south from the

Sicilian basin and shelf to the north.

4. There is a pruminent marine character of both

latc Carbonifcrous and early Permian deposicio-

nal environments of thc Tiiscan to Sicilian

Apenninic ro Maghrebian beh as compared with

the remaining three other palinspasric units now

assembled into rhe Italian area and characterized

by the nsual European continental faciès (with

exception of the eastern Southern Alps and

Dinarides). This is well consistent with and riee-

ded to explain Iriassic marine deposits pracrical-

ly surrounded by continental deposits (as for the

Punta Bianca near l a Spezia marine Early to

Middle Triassic sequence with pillow-lavas) or

226

GEODIVERSITAS • 1997 • 19(2)

Carboniferous-Permian palaeogeography, Mediterranean area

deep watcr faciès apparenrly isolared within shal-

low-warer platforms (as for the Triassic

Lagonegro basinal deposits and volcanics) (Vai

1994).

5. The reporied vSouih American afTinity of ihe

iVIoscovian d'uscan conodom fauna requircs a

connection which can bc found across N\V

Africa, in fact, aftcr the peak late \lscan trans¬

gression ovcr most of N\V Africa, marine sédi¬

mentation was reduced ro an E-W ucnding widc

belt including the Fourhal, Jérada. Colornb-

Béchar, Reggan, lllizi Basins in the Sahara

Platform, where il lasted until most of the

Moscovian (Conrad eX rf/. 19S0; Fabre Î983;

Legrand-Blain 1983). Marine Moscovian is also

known froin the SW Moroccan Meseta (W of

Fkih ben Salah; Choubert & Faure-Muret 1956).

This marine bclt can bc traccd we.srw'ard to

South America in the Amazon Basin and the

Northern Andes (Ferrari er ai 1977 for lef). In

the remaining part ol ihc Meseta as well as in the

Kabylid-Rîff and Betic nappes, Fermo-

Carboniferous and Peimo-Triassic continental

deposits are only known. In the incermediatc Riff

and Atlas rhrust helt no Permo-Carboniferous

information is avaÜable bccause fhe individual

rhrusts are detached ar the Triassic Icvcl. The

NW Africa Moscovian sea was pnihably connec-

ted with the soiiih Ponugucsc zoncs where thick

foredeep marine deposits as late as Moscovian are

known, whereas continental Westfalian and

Stephanian rocks were accunitilating in the nor-

ihern Ponugal.

6. The reporeed Spanish affinity of the

Moscovian corals trom Tuscany suggests che way

to conncct the almost isolated lare Carboniferons

Cantabrian Basin wirh the world océan System

through a Corsica-southern France and eastern

Spain corridor. In ihis respect, the rich Viséan

marine fauna of rhe Montagne Noire (Mamet

1968), Moiithoiimet, Pyrénées and Catalonia,

followed by miel Carho ni ferons (Narnurian-

Westfalian p.p-) rurbidices (Ebner 1991), is

consistent wirh ihe suggesied connection. The

same applies to the Tournaisian (Krylatov &

Mamet 1966) of the N Corsica Capitello lime-

stone and overlying shales eut by rhyolitic dykes

and followed by late Westfalian megafloral

deposits.

7. As a conclusion one can say chat a sériés of

new ficld data (Catalano et ai 1991; Vai 1994;

papers in ihis volume), togeiher widi reasonable

assumptions hased on indirect ev'idences, woiild

suggest an carly ro mid Permian sea-way cucting

across Norrh Africa and lheria {t.v. separating

Gondwanaland fvom Laurussia) as claimed by

Vai (1994), Further support lo rhis hypothesis

may dérivé from the conrrasting distribution par-

tern of provincial floral (Chaloncr Meyen

1973) and continenral verrebtarç (Romer 1973;

Millsieed R-, Schneider J. W., pers comm. 1995)

éléments passing from Permo-Carboniferous to

late Pcrmian-early Triassic. However, effective

démonstration of this idca can only dérivé from

cither subsurfacc data bencach the Atlas thust

bclt or submarinc drilling along the Moroccan

Atlantic coniinemal margin.

REFERENCES

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western Tethys (SicÜy, Iraly) - new évidences (or

the position of rhe Permian l eihys. P(dacogt'Oj^r^4-

plfy Pdliivvi'linwlo^ Ptiltieovioltmf 87: 75-108.

Catalano R, Di Stcfaiio P. te Vutale F P. 1995. —

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tral and wesrern Sicily belt: new insights. Terra

Niwnl-, 189-199.

Choubcri Cj, & Faure-Muret A. 1956. — Maroc.

Lexique Stmtiç^aphique InlematiorutL Fascicule la,

165 p.

ChaionCr W. Cî. & Mcycn S. V. 1973. —

Carhonifemus and Permian Floras of the Northern

C’onrinents: 169-186, in Flallam A. (ed.), Atlas of

Pulaeobiogenp'aphy, Elsc^'icr..

Conrad J.. Lvs M. te Wey.int M. 1980. — Mise en

évidence du Carbonifère moyen (Moscovicn) au

Sahar.i Lcntral. bassin de Reggan, et conséquences

palcogéographiques. BuihtiH de la Société

Géologique de Frïiuce (7) 22 : 115-124.

Douvillc H.. Solignac M. te Berkuloff E. 1933. —

Découvert du Pcrniicn marin au Djebel Tcbaga

(Extrénu'-Sud Tunisien). Comfnes Rendus de

lALadérulc dci Scitrices^ Paris 196 : 21-25.

Ebner F. 1991. — Circummediterranean Carbonife-

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TOUS preflysch sédimentation. Giormle di Geologia

53/1: 197-208.

Fabre J. 1983. — Afrique de l’Ouest., in Fabre J.

(ed.), Lcxiqî4€ Stratigraphi^ne International, n. s., 1,

lUGS-Pergamon, 396 p.

Ferrari A., Perri C. &C Vai G. B. 1977. — Middle

Carboniferou.s corals and conodonts from the

Hercynian Farma “Mas.sir’ (Tuscany, Italy).

Giornale di Geologia 421 \: 133-164.

Irving E. 1982. — Fragmentation and assembly of the

continents, Mid Carboniferous to présent.

GeophysicalSurvey 5: 299-333.

Kahler F. 1974. — Fusuliniden ans T’ien-schan und

Tibet. Report Scientific Expédition Sven Hedin,

Stokholni, 52, volume 4, 148 p.

Krylatov S. & Mamct B, 1966. — Données nouvelles

sur les terrains palcozoiques de PArgcntella-Tour

Margine (Corse). Bulletin de la Société géologique de

France (7) 8: 73-79.

Legrand-Blain M. 1983. — Le Carbonifère marin du

Sahara algérien, in Fabre J, (ed.), Afrique de

rOuest, Lexique Stratigrapbique InternationaU

lUGS-Pergamon, n. 1: 109-117.

Mamet B. 1968. — Sur les microfaciès calcaires du

Viséen de la Montagne-Noire (France). Revue de

Micropaléontologk 11: 121-136.

Rau A. & Tongiorgi M. 1981. — Some problems

regarding the Paleozoic Paleogeography in

Mediterranean Western Emo'pç:. Journal of Geology

89: 663-673.

Romer A.-S. 1973. — Permian Reptiles, in Haliam A.

(ed.), Atlas of Palaeobiogeography, Elsevier:

159-167.

Sengor A. M. C., Altiner D., Gin A., Ustaômer T. &

Hsü K. J. 1988. — Origin and assembly of the

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Skinner J.-W. & Wilde G. L. 1967. — Permian fora-

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Cenozoic Palaeocontinental Maps. Cambridge

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Vai G. B. 1978. —Tentative corrélation of Paleozoic

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Erdwissenschaftlichen Kommissionen 3: 313-329.

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Ziegler P.-A. 1988. — Evolution of the Arctic-North

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Submittedfor publication on 5 April 1996',

accepted on 11 October 1996.

228

GEODIVERSITAS • 1997 • 19(2)

Palaeogeographic maps of Moscovian and

Artinskian; contributions from the Netherlands

Mark GELUK

Rijks Geologische Dienst, P. O. Box 157

2000AD Haarlem (The Netherlands)

Geluk M. 1997. — Palaeogeographic maps of Moscovian and Artinskian: contributions from

the Netherlands, in Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigraphie cor¬

rélations. Geodiversitas A9 (2) : 229-234.

KEYWORDS

Westphalian,

Stephanian,

Lower Rotliegende,

Variscan front,

basins,

tectofacies.

ABSTRACT

Frequent marine bands in the early Westphalian of the Netherlands are

replaccd hy peat marshes followed upwards by a braidcd-river/fluvial-plain

System in rhe lare Westphalian-Stephanian. Sédiments are ümited to the

dcpocenters Stephanian. Asselian to Artinskian deposits are represented by

Lower Rotliegende volcanoclastics, basaltic volcanics and sédiments of conti¬

nental environment.

MOTS CLÉS

Westphalien,

Stephanien,

Rotliegende inférieur,

front varisque,

bassins,

tectofaciès.

RÉSUMÉ

De nombreux niveaux marins du Westphalien inferieur des Pays-Bas sont

remplacés vers le haut par des tourbes marécageuses suivies par des systèmes

fluviaiiles de plaine deltaïque au Westphalien supéricur-Stephanicn. Les sédi¬

ments stephaniens sont limites aux dépôts-centres. Les niveaux de l’Asselien à

l’Arcinskien sont représentes par des volcanoclastircs du Rotliegende

Inférieur, des basaltes et des sédiments d’environnement continental.

GEODtVERSITAS • 1997 • 19(2)

229

Geluk M.

MOSCOVIAN TO GZHELIAN

The Moscüvian deposirs are represented, accor-

ding to the current idcas, by approximately the

interval of the Westphalian C to Stephanian.

The constraint is provided by the âge dating ot^

Lippolt et al. (1984), which revealed an âge oi

311 Ma for the base of the Westphalian C. The

exact chronostraiigrapliic position of the youn-

gest sédiments (? Stephanian) in the castcrn

Netherlands and adjacent part of Germany is scill

debated, since the palynological assemblages

clearly indicate a yoiinger âge (Autunian) than

the palcobütanical assemblages (We.stpbalian D;

Van der Zwan et al. 1993). T here ïs a tondcncy

in Germany to place these sédiments in chc

youngest part of the Carboniferous, the Gzhelian

(Plein 1995). During ihc Moscovian, an impor¬

tant change in climate occurred front humid tro¬

pical conditions to a (scmi-) arid cHmate, as

dociimcnted by a change in soil type (Sclrer

1989; Van dcr Zwan et al, 1993).

In broad terms, the development of the

Westphalian C to Stephanian deposits is quite

similar rhroughout the onshore and offshore

areas; the main différence consists of the amount

of later érosion of the Carhoniferoas. For ihe

Netherlands, one reference section has been

compiled for rhe eastern Netherlands (Fig. 1).

The presenr-day ourline of the Moscovian depo-

sirs (Fig. 2) in the Netherlands is mainly control-

led by érosion and uplift owing to the Varîscan

deformation phase during the youngest

Carboniferous. In large part of the Netherlands

onshore and western offshore areas B.ishkirian

(Westfalian A/B) deposits underlie the Permian

rocks. Compared to the Westphalian A and B,

the younger We.stpbalian and Stephanian hâve

been deposited under increasing tcctonic instabi-

lity as the Variscan front prograded northward.

This resulted in the intermittent tcctonic activlty

of main faulr zones, and at the end of chc

Carboniferous led to the deformation of the fbre-

land-basin infill. The Variscan phase is conside-

red to have accentuated the différences in

subsidence during the Moscovian. In the basins,

up to 1200 m of Westphalian C to Stephanian

sédiments have been preserved; in rhe uplifted

areas, sédiment thicknesses of this interval were

probably not over 750 m and presumably consist

of fine-grained sédiments.

At the onset of the Westphalian C, extensive peat

maf.shes existed over the entirc Netherlands off¬

shore imd onshore areas. Marine bands, which

frequcntly occurred in rhe Westphalian A and B,

occured only sporadically in rhe Early

Westphalian C Dunng the late "Westphalian C,

owing CO an abrupt influx of coarser graincd

sédiments, these marsbes were replaced by an

extensive braidcd-river/fluvial-plain sy^-tem.

Sédiments came basically from three different

.source areas, the Rlienish Massif in Germany in

the southeast. the Mid North Sea Fligh in rhe

north, and the Brabant Massif to the south

(Fig. 2). 1 here are minor différences in rhe onset

and duration of these sandy influxes beoveen the

different parts of rhe hasim These sandy .sédiments

were replaced ii> the early Westphalian D again by

fine-graincd sédimentation. The only exception is

forrned by the Campîne Basin in north-easrern

Belgium and chc south-easrern Netherlands,

wlicrc the sandy fluvial deposits are Ümired to rhe

early Westphalian D interval (Paprorh et al.

1983). In orher areas, during rhe Westphalian D

déposition took place on a semi-arid flood-plain

with shecr Iloods and braided rivers. Soil types

indicate that thèse flood^plains becaine better

drained during this dmespan.

Fhc occurrence of the ? Stephanian deposirs is

limitcd to the depocentres of the Mosctivian

basins in the eastern Netherlands and probably

the northern Netherlands offshore area. An

unconformabic contact of rhe Stephanian with the

underlying Westphalian D sédiments is assumed

(TaJUow 1993; Van Adrichem, Boogaert &

Kduwc 1993-1996). Stephanian deposirs are for-

med by well-diained distal floodplaiii deposits,

with minor braided channels (Van der Zwan

1993).

ASSELIAN TO ARTINSKIAN

The Asselian to Artinskian deposits in the

230

GEODIVERSITAS • 1997 • 19(2)

Palaeogeographic maps of Moscovian and Artinskian

52-40 N

7-E

Ages according to Odin (1994),

Lippolt étal. (1984)

260 -

Marine stages

Continental stages

Lithology

Thickness

Kungurian

Artinskian

Sakmarian

Asselian

Ghelian

Kasimovian

Moscovian

Bashkirian

Stephanian

Westph. D

Westph. C

Westph. A/B

•O O OOP

. I ■ —

. .J

1200

Rijks Geologische Dienst rgd

Fig. 1 . — Reference columnar section for eastern Netherlands. See Vai & Venturini (this volume) for legend.

GEODIVERSITAS • 1997 • 19(2)

231

Geluk M.

Netherlands are represcntcd only in small areas

of the Netherlands by sédiments. The deposits of

this interval are mosr likcly represented by the

Lower Rodiegend volcanoclastics. These volca-

noclastics occur in two separate areas, namely in

the Ems Low in the eastcrn Netherlands onshore

area and the Central North Sea Graben in the

offshore area (Fig. 3). Volcanic accivity in the

Netherlands and Germany occurred în response

to wrench movements along Variscan fault zones

(Ziegler 1990).

The volcanoclastics in the Fins Low represent

the western oudiers of a more extensive area of

volcanic activiry in Germany (Plein 1995). The

volcanoclastics consist of red-brown to green spi-

litic, basalric volcanics and mudstones. Severai

stacked lava flows occur in the succession. The

thickness of the volcanics reaches a maximum of

80 m. The âge remains spéculative, but, based on

indirect evidence, is assumed to be AsseÜan

(Plein 1995).

In the Central North Sea Graben the sequencc

reaches a thickness of almost 150 m. The volca¬

nics consist here of massive rufFs and lavas up to

severai tens of meters rhick, interbedded with

claystones and subordinate sandscones. No

reliable datings are available for these volcanics

(Plein 1995). I hey are assumed to hâve an

Assellan âge.

Following the Assellan, a long period of non-

deposition followed; sedimenrion was only resu-

med during the youngest stage of the Permian,

the Tatarian.

REFERENCES

Lippolt H. J., Hess J. C. & Burger K. 1984. —

Isotopische Alter von pyroklastischen Sanidien aus

Kaolin-Kohlentonsteine aus Korrelationmarken fur

das mittclcur^^aische Oberkarbon. Fortscbrine in der

Cieologie von lÛte/nLnid und Westjnkn 32: 119-150.

Paproth E., Dusar M., Bless M. J, M., Boukaert J.,

Delmer A., Fairon-Demarcr M-, Houlcberghs E.,

LaJoux M., Pierart P., Soiners Y., Srrud M., Tliorez J.

& Fricot J. 1983. — Bio- and ÜcKosrrarigi'aphic sub¬

division of the .Silesian in Belgium - a review. Annales

rie la Société géologique de Belgique ! 06; 241 -283.

Plein K. 1995. —Norddeurschcs Rotliegend-beckcn;

Rotliegend-Monographic J cÜ II, in Plein E. (ed.),

brratigraphie von Dcut-schland I. Courier

Forschungs-ïnstiiut Senckenherg 183, 193 p.

Selter V. 1990. — SedirnenMlogie und KUmacntwick-

Inng im West/nl C/D und Stephnn des nordwestdeut-

schcn Oberkarbon-Eeckens. DGMK-Bcrichr 384-4,

Hamburg, 311 p.

Tanrow M. S. 1993. — Stratigraphie und seismisches

Er.scheinungsbild dc.s Obcrkarhons (Westfal,

Stefan), Fmsiand. Berliner Geoivissenschaften

Abhandlunget! 148: 66 p.

Van Adrichem Boogaert H. A. Kouwe W. F. P.

1993-1996. — Stratigraphie nomenclature of rhe

Netherlands, révision and update by RGD and

NOGEPA. Mededelingen Rijks Geologisvhc Dienst 50.

Van der Zwan C. J., van de Laar J. G. M., Pagiiier

H. J. M. ik van Amerom H. W. J. 1993. —

ralynological, ccological and climarological s)nrhe'

sis of the Upper Carboniferous of the wcll De

Lutte-6 (eascern Netherlands). Comptes Rendus XII

ICC-P, Buenos Aires, volume 1 : 167-186

Ziegler P, A. 1990. — Geological atlas of western and

central hurope: second and completely revised édition.

Shell Internationale Petroleum Maatscliappij, The

Hague, 239 p.

Submittedforpublication on 5 April 1996;

accepîed on 21 October 1996.

234

GEODIVERSITAS • 1997 ♦ 19(2)

On the biostratigraphy and cyclostratigraphy

of the Moscovian Stage in the type area

Marya Kh. MAKHLINA

Geocentre Moscow,

Varshavskoye shosse, 39a, 113105 Moscow (Russia)

Marya N. SOLOVIEVA t & Nataiia V. GOREVA

Geological Institute of the Russian Academy of Sciences,

Pyzhevsky per., 7, 109017 Moscow (Russia)

Makhlina M- Kh., Solovieva M. N & Goreva N.V. 1997. — On the biostratigraphy and

cyclostratigraphy of the Moscovian Stage in the type area, in Crasquin-Soleau S. & De

Wever P. (eds), Pen-Tethys: stratigraphie corrélations, Geodiversitas 19 (2) : 235-245.

KEYWORDS

Moscovian,

Carboniferous,

biostratigrapliy,

cyclostratigraphy,

Moscow Synciine.

ABSTRACT

Moscovian Stage deposits are widespread in Russia. The stage wus cscablished

in 1890 by Nikicin. It is subdivised in four horizons: Vereya, Kashira,

Podol’sk and Myachkovo. The subdivisions of the stage are based on studies

of brachipods, foraminifera, conodonts, ammonites, bivalves, rugo.sans and

plants. In thi.s paper, new data are due to the correction of the standard sec¬

tion of chc Moscovian Stage and its nc\v interprétation. Cyclostratigraphy

analysis based on the geological histoiy' of the région and its eustatics is a new

aspect of the rcscarch presented in this paper.

MOTS CLÉS

Moscovicn,

Carbonifère,

bio.stratigraphic,

cyclüstratigraphie,

synclinal de Moscou.

RÉSUMÉ

Les dépôts du Moscovien sont largement répandus en Russie. Cet étage a été

défini en 1890 par Nikitin. II est subdivisé en quatre horizons : Vereya,

Kashira, Podofsk et Myachkovo. Les .subdivisions de l'étage sont fondées sur

Tétude des brachiopodes, foraminifères, conodontes, ammonites, bivalves,

rugueux et plantes. Dans cet article, les nouvelles données proviennent de la

révision de la coupc stand.ird de l'éragc et de .scs nouvelles interprétations.

L’analyse cyclosiratigrapliiquc fondée sur l'histoire géologique de la région et

de son eustatisme est un nouvel aspect de k recherche présente ici.

GEODIVERSITAS • 1997 • 19(2)

235

Malchlina M. Kh., Solovieva M. N. t & Goreva N. V.

The Moscovinn Stag;e deposits as well as the

Middle Carbonîfcrous oncs as a vvhole are wides-

pread in Russia and minerai deposits, including

oil and gas, arc rather common in these sédi¬

ments. Subdivision and corrélation of the

Moscovian polylacial deposits connected with

different climatic zones (subtropical and boréal)

represent tJic esscncia! elernetu of geological

mapping and exploitation. Icndency lo adéquate

reliability, précision of stratigraphie scale.s and

high degrce of corrélations achicvcmcnc causcd

the necessiiv to reinve.stigate of the stage and

substage stratotypes.

The Moscovian Stage was establislied by Nikiiin

in 1890 in tbe vicinity ol: Moscow. l'he upper

limit of flic stage was dcfined at rhe base of

Gzhelian limcstoncs.

The Moscovian, according co the ideas of Ivanov

(1926) who had estahlished the fundamental

principles of the modem views on ihe volume of

this stage and its subdivisions based on the stu-

dies of the deposiiional sequence in the Southern

parc ot the Moscow Syneclise, was suhdivided

into four horizons: Vcrcya. Kashira, Podolsk and

Myachkovo. The Tegulifera Horizon (the

Kasimovian Stage) was considered to be a part of

die Upper Carboniterous. Faunal assemblages of

che Moscovian as a whole, as well as rhose of its

subdivisions based on studies of bradiiopods,

foraminifers, conodonrs, ammonites,, bivalves,

rugosans, plants, are rekuivcly well known, zonal

scalcs being estahlished on the hasis of some of

these studied groups. Numerous publications are

devored to che Moscovian Stage in the type area,

which mosr important are rhose by Ivanov

(1926), Ivanova &c Khvorova (1955), Raiiser-

Chernousova et ai (1951). Some papers are

published during the last 20 vears by Shik

(1971), Makhlina (1972, 1976), Makhlina &

Shik (1983), Makhlina et al. (1984), Goreva

(1984), Solovieva (1984, 1986).

New data included tn rhe présent paper w'crc

obtaincd by the correction of the standard sec¬

tion of the Moscovian Stage and its new inter¬

prétation.

The lower houndary of ihe Moscovian Stage,

according to the iraditional views, coïncides wirh

rhe lower boundaty of the Vereya Horizon.

Changes in the standard section interprétation

were caused by die discovery ofa gap in the stra¬

totype section of the Kashira Horizon, where

deposits of the Tsna unit, estahlished by

-Solovieva (1984, 1986) in the fsna River basin

(Ryazan-Saratov dépression) in the easiern part

of the Moscow Synoclisc, arc absent. Cyclostrati-

graphical anal^'sis of the Moscovian Stage based

on the geological history of the région and its

eii.stadc tectonics is rhe new aspect of the rcscar-

ch presented in rhis paper

l'hc Moscovian Stage in rlie type area îs represen-

led by marine deposits. Le hy continuons sériés

of transgressive deposits (130-150 m rhick), in

which sands and clays are graduallv rcplaced by

clayey and pure limesroncs, Subhorizontal hed-

ding and cycticic)^ of deposits give opporrunjt) to

idenrify and follow up horizons, formations and

relatively smaJl subdivisions (suhfbrmations and

memhers) in this région, and to identify cycles of

different order.

If che CnrbonifcroLis S)^tcm is considered to be a

cycle of the third order, Middle and Upper

Carboniferous (Pennsylvanian) are c)'clcs of the

fourth order. The Middle Carboniterous corres¬

ponds CO a tcccono-cLisratic cycle of the flfth

order, tlie Moscovian and Kasimovian stages to

cycles' of che sixih order (Table 1). According to

Tilebomirov (1988), the lattcr includes the chree

units correspondiiig to three phases of che trans¬

gression: initial (a), maximum (jî) and terminal,

or regreS-sive phase (y). Cycles of the sixth order

may be complété or .shortened, rhe former

consi.sting of chree cycles of the seventh order,

che lattcr of two cycles oi the samc order, the ini¬

tial phase being absent- These cycles could be

followed up in different faciès throughout a

rcgioiit and cheir forinacion corresponds lo the

maximum lectono-eustatic changes of basin

levcl. 'Hie A/a, Vereya and T.sna subdivisions

apparenily cotre.spond to rhe cycle of the seventh

order, or to the initial phase of the transgression

(tï) (Table 1). l'he combiacd Ka.shija, Podolsk

and Myachkovo horizons correspond to the cycle

of che seventh order, or to the maximum phase

of rhe transgi-ession (P), whercas chree horizons

of rhe Kasimovian Stage of rhe Upper

Carboniferous correspond to a régressive phase

(y). Within the cycles of the seventh order there

236

GEODIVERSITAS • 1997 • 19(2)

Bio-cyclostratigraphy of the Moscovian Stage

Table 1 . — Subdivision of the Moscovician of the Russian Platform.

Régional

scale

Local scale

Moscow Synclise

Cyclostraligraphy scale

order of cycles

VIII

III

Horizon

Formation

Subformation

Member

Horizon

(Formation)

Substage

stage

Voskresensk

Krevyakino

Suvorovo

Krevyakino

Krevyakinian

Kazimovian

upper

Myachkova

Peski

Myachkovian

Noviinskoe

Shehurovo

Podorsk

Podol'sk

Ulitino

Podolskian

Vas'kino

(32

Smedva

Rostislavr

Lopasnya

Kashirian

Kashira

Khatum

Nara

Polustova

Gora

Nara

Tsna

Tsnian?

Upper

■

Vereya

Vereyan

■

Lower

Shat

■

Melekess

Aza

■

are smaller cycles - those of the eighth order, cor-

responding to separate horizons (substages in the

proposed cyclostracigraphic scale, Table 1) and

those of the first order, corresponding to subfor¬

mations (hori/.t)ns in the proposed cyclostrati-

graphic scale, Table I).

Every stratigraphie unit of any rank can be sub-

divided iiuo two parts: lower^ corresponding to

ihe transgressive pha.se of sedimentarion, and

upper, corresponding lo ihe régressive phase.

Contemporaneous stratigraphie units of different

faciès, which wcrc formed in the paleobasin as a

latéral sequence of rocks rcflect, ncat-shore, per-

iferal, shallow-water and relatively deep-water

environmenrs. Periodicity in the distribution of

faunal assemblages, which always show maxi¬

mum diversiry in a transgressive part of a cycle

and low diversit)'^ in its régressive part (Makhlina

Sbik 1983), is a charnctcristic fcaturc of ail

simultancoiisly formed polyfacial stratigraphie

units corresponding to the cycles (Figs 1-3).

Boundaries between tbese units correspond lo

historico'geological changes of sédimentation

patterns, i.e. to changes in abioric environment

taking place simultaneousiy in the wholc région

(Makhlina 1996).

The Jnain criteria for distinguishing and cracing

ot transgressive-regressive cycles in which combi¬

nation form stratigraphie units (formations, sub-

GEODIVERSITAS • 1997 • 19(2)

237

Makhlina M. Kh., Solovieva M. N. t & Goreva N. V.

formations) are ihe follovA'ing: sedimcntological

and faunistic content, features of texture, perio-

dicity in rhe distribution of ail groups oi iauna in

the section, as well as blostratigraphic;d characte-

ristics for the définition of the gcological age of

the units. ’l'hc sufficient methodical signifîcance

of the lirhological-palaeoecological criteria, ela-

borated by Osipova & Belskaya (1967). should

be emphasized in this respect.

Leaving aside the problcm of rhe lower boundary

of the Moscovian Stage, chat is stÜl discussed

(Solovieva 1986; Aleksecv et ai 1994), let us give

brief characterisrics of the stratotype sections of

the horizons (formations, subformations), Le. of

units of the régional and Joca) s'cales ol the

Moscovian Stage, accepted in Russia

(Anonymous 1988, Table l).

The Vercya Horizon (Formation), in order to

reinvesrigate the stratutype, was studied ncar the

village Alyutovo on the righc bank of the Pronja

river, where it is lying ciansgressively on Lower

Carboniferous deposits (Solovieva 1986)

(Fig. 2-1). Red sand and clays, glauconite Sând-

stones can be found in the base ol the section,

crinoid-bryozoan sandy limestones with forâmi-

nifers, as well as intoibedding of crinoid lime¬

stones, variegated c!ays> maris with brachiopods

and bryozoans overlying them (Ivanova &

KTvorova 195S). l'he chickness of che formation

in this section is 10 m, and in the région ir

changes from 10 to 3? ni. The Vereya Formation

is subdivided into rwo subforniarîons, lower and

Lippcr (Anonymous 1988). Solovieva (1986) pro-

posed the foraminileral Proftisiinella cavis,

Aljutovella aljutovica. AL artificirxHs Zone. The

typical assemblage of the Vereya Horizon

(Formation) ts fcprcsented by tho following spe-

cies of foraminifers; Eostaffelln mutabilis,

Schubertella püuçhepuuay Psvudosmffclla suhqua-

dratUt Profiisulinella cavis, P parvn^ Aljutovella

aljutoviça, A. artificialis, A. scclvevatictu

A. euhnea, ehn^ntft.

Deposits of the Vereya Horizon (Formation) cor¬

respond TO the conodont IdiognatiHndes tubercu-

lattis^ !d. mitrginodosus Zone. Characccristic

species of the zone arc Idiogriathoides dnnhassiens.

Id. shnuxtus^ Id. fossatuf. ïd, ein'rngatus^

Idiognathodus incurvusy Neognathodus atokaensis-,

N. bttsslcri, Dfplognctthodus adoradoensis-,

D. orphnnits, Streptognathodtis parviis.

According to Solovieva (1984) and Alekseev

(1994), the Vereya Formation sensu Ivanov

(1926) is only charaeVerized by the yVlyutovo

fïisulinid and conodont assemblages. The over¬

lying and underlying Shat and Ordynha mem-

bers ( Fable 1) do not contain any orber tàunisric

complex except Alyutovo age.

In the standard of the Moscovian Stage, the posi¬

tion ahove the Vereya Formation in the case of

normal scquence is occupied hy rhe Tsna unit

distinguished hy Solovieva {1984, J986). Tn rhe

stratotype section (Yambirnoye Quarry, Ryazan

région, Fig. l'H) it is represented by inierbcd-

ding ol dcrrital and doloniitr/.ed finc-grained

limestones with greenish clays and marks, rarely

with micro-grained dolomites (Fig. 2-11). The

tliickness of rhe subformaiioii in the stratotype is

16.5 m (Table ty Local Scalc, 1988).

Deposits of the Tsna Subformarion correspond

to the Zone Aljutonelln pritcoideas HctnifitsuUna

volgeyisis. l'his typical forantiniferal asscmbhige,

characteri/ed by a high dcgrec of similarity m ail

régions where the.se deposits arc represented (rhe

Russian Plaiform, rhe Douces Basin,, the

Cisuralian Dépression, Urals, Tien-Shan, etc.),

iücludes the follov^nng species: Schtibemila gTiici-

lis znensis^ Sch. galinae, Ozawainella digitnUsy

ProfnsulificdJa prisen tîntanica^ P nnrûtovensis,

P jmta^ Taitzehoella prolibrovichi, T. pseudolibro-

Vîckd, Aljutovella parasaratovica^ zl. ùuralovtca,

A. priscoidca^ A. znensisy Hemîfusidina dutkevîchi,

H. volgemis.

FfG. 1. — Location map of the stratotype sections (l-X) of the

Moscovian Stage (for the list of the sections, see figures 2. 3).

238

GEODIVERSITAS • 1997 • 19(2)

Bio-q^clostratigraphy of the Moscovian Stage

According to thc prdimlnary investigations, ihe

l'sna Subformatîon corresponds ro the tonodonr

Neogtmthodus bathrops^ Streptognathodus tramiîi-

vus Zone. J'iie lowcr boundary is defined by rbe

entry of Neagvathodus boihrops, the upper one by

the incoming ot Streptoguathodus disi^ectus.

Deposits arc characterized by an inipoverished

conodont complcx. Typical spedes are as follows:

Neognathodîis bothraps^ Streptügndthudus pürinis^

Idiognathodiis delicatus-, Id. cd^llqitus, Diplo-

gnathodus colonidoemis.

Deposits of che Tsna Subformaiion hâve a spotcy

distribution due to the transgressive bedding on

it of thc Kashira Horizon that corresponds to the

beginning of maximum transgression ((îj,

Table 1).

The Nara Subformation is represented by an

interbedding of poorly coloured micrograincd

limestones and dolomites wiih biodetrital lime-

srones and clay seams. The thickness of thc

deposits eau reach 28 ni {Fig. 2-II1). Materials

available give ati opportuniiy lo substantiate ihe

récognition of thc local Hemifiisulhm kushiricUy

H, moellert^ Becekina pscudoelegans Zone. In the

eastern sections of the Southern part of rhe

Russian Platform chcrc arc numerous Neo-

stajjellu, Profusnlinelta pseudolibrovichi, Pr. eoli-

brovichi. Pi. syzranicas Pr. mtHahiUs^

Heniifusulim kashirka. H. pseudobochi. H. mocl-

leri, Beedchm hontu B. Qznwau B. pseu-doelcgatis^

B. d(. proQZiiWiü^ B. kayi. The Nara Subtormation

corresponds to thc conodont Ncognathodiis

bothropSy Streptognathodus disseetns Zone. It is

characicrizcd by ihc following species:

Ncognathodus bothrops^ N. kashtrieiists, Sti: dissec-

tus^ Str. parvus. Diplognathodus voloriidoensis is

very common.

The overlying Lopasnya Subformarion is repre¬

sented by interbedding of pinkish and greenish

limestones, dctrital, micrograincd, with cherts,

variegated maris, more rarely dolomites. Its

thickness is 15-30 ni (Fig. 2-1V)- The subforma¬

tion corresponds to thc local Moellerites lopUs-

viensis, Beedeina ozawai, Fusulinella sahpulchni

Zone (Solovieva 1986). The Ibllowing complex

is characteristic: Ozawamelht stellae., Pmîellilprae-

cuTsor paraventricoui., F. praetypica, Neostajfella

larionovae, Fusidinella subptdchray Hemifusulina

rnoelleri, H. kashirka communis, H. splcndida,

Beedeina ozaivai-, B. paraozaivah B. pseudoelegam.

The Rostislavf member consists of two parts.

The lowcr onc is represented by interbedding of

clays and limestones, or by unfossiliferons days,

or by dolomicic maris (bed 23, Fig. 2-IV), the

upper one by sands, aleurolites, sandstones and

conglomerace (bed 21, Fig. 1-V), The lower part

corresponds to a régressive phase and terminâtes

the kopasoy.a Snhformation, the upper part,

being the transgressive one, corresponds to the

base of rhe Smedva Subformarion.

The Smedva Subformarion, or according to

Ivanov (1926) “dolomites of Smedva”, contains

micnjgraincd dolomites and dctrital limestones

(Fig. 2-V). U was referred to the Podol.sk

Horizon by Ivanov and Solovieva, many of the

subséquent auihors assigned tbi.s subformatinn to

the Kashira Horizon. “Dolomites of Smedva'

represent lagoonal rocks characteristic of a régres¬

sive phase. I hls environment was imfavorablc for

fusLilinids. dliaC is why deposits of the Smedva

Subformation are very poorly characrerized by

this group of tauaa. The Lopasnya and Smedva

subformations correspond to the conodont

Neognathodus medadultirnus^ Streptognathodus

dissectus Zone. The lowcr limit of the zone Is

defined by lhe incoming ot Neognathodus meda-

diiltirniis^ the upper one by the entry ot

N. medexultimm. Characteristic spccies are as fol¬

lows; N. hothrops^ N. medadultiinus, N. colom-

biensis^ Idiognathodus obliquus^ L delicutus^

I. robustiLu Streptognathodus dissectus, Diplogna-

thodus coloradoerisis. This zone can be subdlvided

into two local subzones, each with a characterls-

tic assemblage: Suh/.one Neognathodus bothrops»

N medadultimus, corresponding to thc Lopasnya

Sublormation, and Subzone N. medexultirnus

corresponding ro the Smedva SubRirmation. Ttic

volume of tlic former sub-zone is designated by

the coexistence of A^. bothrups and N. medadultk

mus, the characteristic complex lieing represented

by N. hotbrops, N. medadultufius, Strepîognd'-

thodus dissectus, Idiognathodiis oblitjuus, l he

volume of lhe latier subzune is designated by the

présence of Neognathodus medexultirnus, Stiepto-

gnathodus dissectus, Idiognathodus obliquus,

L robustus.

GEODIVERSITAS • 1997 • 19 (2)

239

^3 ^4 ^5 ^6 ^7

9 10 11 12 hr^ 13 14 l^-:-:;J ib 1'®^ 16

I & I 17 I O I IB l^ I 19 I ^'i ZO I cÿ ) 21 \A I 22 I ü I 23 |g<l 24

r~0n 26 1 f i 26 I 1 27 f-*~^ 20 l'^l L-l 29 l*^»l 30 I ] 31 | lil| | 32

33 IV^I 34 liTÜIll 3B

Fig. 2. — Sections of the Moscovian Stage (Veroya. Tsna and Kashira beds); I. outcrops near ihe Alyutovo village, right bank of the

Pronja River {Solovieva 1986), lectostratotype ol the Vereya Formation; II, Yambirnoye Quarry near the Yambirnoye village, left bank

of the Tsna R'ver (Solovieva 1986'/; the Tsna Suoformaîion holostralolype; III. outcrops along the Oka. Nara. Protva. Besputa rivers:

section oî the Nara Subtomiation of the Kashira Formation (ivanova » Khvorova 1955, fig. 13), !V, ourcfop near ihe Lapmo village at

ihe left bank ot the Lopasnya River (near the Knatun village) (Solovieva 1986): siratotype ol the Lopasnya Subiormatton. layer 1.

Khatun member: layer 23, Rostislavrmember. the lower part; V. outcrops along the OKa. Nara, Protva. Besputa rivers; sections of

the Smedva Suütofrnation ot the Kashira Formalion: layer 21. RostislavI rnember, lhe upper pan (Ivanova & Khvorova 1955,

fig 13).

Legend for figorys 2*3 Depos«ts 1-16:1. Kmestone; 2. d&tr*ta! ai biomorphlc-detriial limêslone- 3, siuôge limestone; 4. microg^ained

limestone; 5, coprolilc-dclnlal limestone. 6. lime sanostone, 7. dolomite; 8, miçrograined dolomite; 9. clayey limestone: 10. mari: 11,

ciayey dolomite; 12 . dolomite mari; 13. dolomitized limestone; 14, Time and aoiomlte ctay; 15. sand sill, sandstone; 1B. fragments oi

chert and limestone. Fossils 17-29; 17, foraminifers; 18, brachiopods. 19, solllary corals: 20, colonial corals; 21, bivalves; 22. gastro-

pods: 23. Dryozoans: 24. fishes. 25. chnoids; 26. echinoids; 27. algae: 28. aigae Ivanovia tenuissima; 29, traces of mud-eaters;

Secondai^ alterations, structure and other signs 30-35; 30. cherts: 31. caverns: 32. stylioliies: 33. cross-beddlng 34. limestone brec-

cia. 35. gap

l'he Podolsk Horizon (Formation), a maximum rcpre-scntcd m;iinly by biomorphic limestones

phase of the Moscovian transgression (p 2 )» is with seams of miçrograined dolomites, greenish

iAr\

GEODIVERSITAS « 1997 • 19(2)

Bio-cyclostratigraphy of the Moscovian Stage

mari and clays; the total thickness is 25-40 m.

Three subtormations can be identified within

this formation.

The lower one (Vas’kino Subformation) is repre-

sentcd by miciograined Jimcstoncs and dolo¬

mites with biomorphic'dctrital limestone seams;

the thickness is 7-12 m (Fig. 3-Vl). At the base,

there are conglomérâtes and maris that could be

traced regionally. The Vas'kino Subformation

corresponds to the tusulinid FusuUneUa colaniacy

Beedeina elegans Zone. The characteristic

compicx is as fbilows: OzMwatnella kumkhoverisis,

NeostaffelLi rosm^zein^ N. sphueroklea^ Taitzebeella

librovitchi aieliidy FusuHnella colaniae,, Hemi-

fusulina splcndida, Bt-rdeina elegans, B. omwai,

B. elshanica vaskinensh, Putrella triangnU-.

1 he overlying Ulilino Subformation is similar to

the Vas'kino in the sedimeniological aspect but

differs m rhe présence of limestone seams with

the algae Ivanovia termissinut. The thickness of

the deposits is 12-13 m (Fig. 3-VIT). The sub-

formation corresponds to the local FusuHnella

Fig. 3. — Sor.tlonç of the ^/1o8COV^* Stage (Podoi'sk. Myachkovo norirona): VI soriionK m mo nasm ot ihe Oka ffive» east of ihe

Kashira towo, near Bolstioyo Huno village, pogoM Rosttftiavi’. and noar Vas'kino village, section ol ihu Vas’Kino Subformatloo of (he

Podol'sk Formation (Ivanovan & Khvorova tP-W. np ?0i VII, Quany near ihü town Podoi'sk: ntraiotype ol the Podoi'&k Formariun

(Ulltino Süblormaiion) [Ivanova & Klivurova 1ÔS5. fig. VHI, Üuarry ooarthe lowo Potioi'i^k. atraiolypao* ÜiaPodolBk Formation

(Shehurovo Sublormation) <lvanova & Khvorova 10W, (ig 23) «X, Ooairy |(ié Ujwn Podolsk hvpostratotype ot Iho Novlinekoe

Subformalion of (hr? Myachkovo Formation (Ivanov;? fi Klivorova 1955. fig. 23); X. Atanusiovo Üuarry noar the Atanaslevo villagH on

the nght bank ni the Moekva River, tteclion of Hie Mvachkovo-KrovyaKino boundary tayors (Middlft/Upper Oarhoni/erüus boundaryl;

layer 6, “lower conHlomarate'*: lay^r 7, dolomite oi Turaovo"; loyer 8..'0trmH8l)a". lay^r fi. aharstia . layer TO, upper conglome-

rate". Hypostratotype of the Peski Subformation of the Myachkovo Formation: it is near Peski raiiway station, on the left bank of the

Moskva River (Makhlina étal- 1972, 1984).

GEODIVERSITAS * 1997 • 19(2)

24 I

Makhlina M. Kh., Solovieva M. N. t & Goreva N. V.

vozghalemk^ Fusidina Utinensis Zone, the follo-

wing complcx being considered as a cbaractcris-

tic one: Fusiella putchella, Neostaffella ozaumi,

Ozawainella mosquensis, FusulinelLi vozhgalensis,

Hemifusulina stabilis, H. polasnemîs, Fusulina

ulitinemh, F. panconeîish, Purtrlla bmzhnikovae.

'l’hc uppermost part of the Podolsk Formation is

identified as the Shehurovo Subformation repre-

sented by dolomites* biomorphic limestones wich

greenish mari and clayey limestone seams.

Limestones are ofren dolomiti/ed and siliceous.

The thickness of the deposirs is 8-12 m

(Fig. 3-Vni). riie Shehurovo Subrormaiion cor¬

responds to Becdcina kameyisis^ Pmrrlla brazhn 't-

kovae, Ozawainellu ynosquensis Zone with

accompanying characteristic complex of

FusuUnella hockiy F. îwzghulensis, B. elegans^

B, shellunem, B. elshanka,

Deposits of the Podolsk Horizon correspond co

the conodont Neognathodus nicdexultimiis,

Idiognathodm podobki^nsis Zone. The lower limit

of the zone is deflned by the encry of rhese two

species, the upper onc by the îneoming ol

Neognathodus roitndyi. The conodont complex as

a whole is not characteristic cnough, the lollo-

wing speciCvS being typical*. îdiopiathodiis podoF

skensis, L nuigtiifictis^ l. delicatus^ Neognathodus

medadulîitynis^ N~ medexultimus,

rhe Myachkovo Horizon (Formation) accom-

plishes the maximum phase of the Moscovian

transgression ((3^,). Tt is represented by biomor¬

phic limestones with micrograined dolomite

scams and Ughtcolourcd mari Icnses. The total

thickness ol rhe deposirs is 17-37 m. The forma¬

tion is divided into rvvo subfotmariuns.

The lower one, Novlinskoc Subformation, is

represented by varions limestones (derrital, bio-

morphic-detriial) with micrograined limestone

and dolomite seams, coral-fusulinid limesStones

being typical of its lower part (Fig. 3-IX). The

thickness ol die deposits is 10-23 m. Deposirs of

the subformation correspond to Fusnlinella hockty

E mra, Beedema samarica Zone. The characteris¬

tic complex indudos SchubertelLx myachkovernis^

Fusielta typka, NeostaffelLt pnradoxa, N. sphaeroi-

dea, Fusulinella bocki, F. bocki paucheptata,

F fluxa, E mosquensis, E rara^ Beedeina samarica^

Pidchrella pulclmu Hemifimdina bocki, FI. stdbilis,

Fusidina cylindrica,

The upper one, Peski Subformation, is represen¬

ted by biomorphic-detrital limestone with lenses

of lightcoloured maris and clays. ‘‘Turaevo”

micrograined dolomite at the top accomplishes

the maximum phase of the Moscovian transgres¬

sion. The thickness of the depo.sits is 7-15 m

(Fig. 3-X). L^eposits of chc Peski Subformation

correspond to the local FusuUnella podolskensis,

F. cylindrica domodedovi Zone. The data avai-

lable, especiaJly those concerning fusulinid distri¬

bution (Makhlina et al, 1972) givc ân op-

porcuniçy to indicatc complcx typical of the

deposirs of chc I*eski Subformation: Schubertella

mjachkovensh. Ozaivairiella mosquensis,,

FusuUnella bockh F yata, F podolskensd^ F. hele-

nae^ F. mosquensis, F. kumpaniy Hemifusulina

bocki, Fusidina cylindrica domodedovi. F mos-

querysis, F. mjachkovcyîsis^ F pachreiysis^ F fortissi-

ma.

The Myachkovo Horizon (Formation) corres¬

ponds to the conodont Neognathodus roundyij

Streptogyiathodus cancetlosus Zone. The lower

limit of the zone is deflned by the entry of

Neogyiarhodus ifum{q!ialh^ N, rouyidyi^ chc upper

one by the incoming of S. subcxcelsusy

Idiognathodm fssheri and by the disappcarance of

Neogtiathodiis spccics. Index species are domina-

cing in this complex, N» ynedcxultinuiSy N inae-

quLtleSy (dfognathndm dehcant<, f. rrigonolobatm

being characteristic ones. 'l'he zone is suhdivided

into rvvo parts considered noivadays ro be local

subztmes. The Noviinskoe Subformation corres¬

ponds tn the Neognathodus ifîaequales Subzone,

charactcrizcd hy tlie acme o( the index spccies.

The Peski Subformation corresporid.s to the

N, roundyi Subzone, i.e. to the period of

N. vQundyi mass development and incoming of

N. dihitatiis •SiVi.à Idiognathodus trigyniolohatus.

The jifïsiiTon of the upper houndary of the

Moscovian Stage, i.e. the Middle/Upper

Carboniferous, is .srül discassed at présent time.

rhis houndary was establi.shcd by Ivanov (1926)

in outerops and quarrics along the Moskv^a river

and its triburaries (in Myarhkovo, Suvorova

Gora, Krevyakino and other localities). Ail these

242

GEODIVERSITAS • 1997 • 19(2)

Bio-cycloscratigraphy of the Moscovian Stage

localities artr connected to a scparate synsedinienc-

ary élévation in the Moscow zone of élévations

and are characterized by varying fades of rhe

boundary beds, as well as by numerous erosional

surfaces with an intraforinaiional conglomerate

incerbed. Some marker beds traced by Ivânov

(1926) in the boundary beds in this région got

their own naines: bed 7 - *‘svinyâ'\ or *^dolomite

of Turaevo” (Makhlina et ai 1972) (Fig. 3-X) -

lightgreen argillaceous mictograined dolomite;

bed 8 - ''gamasba" - interbedding ol green, red

clays and maris, limestones, sonietiines with

conglomerate interheds. In some sections, chis

member is replâced by dolomitic maris and argil-

laceous limestones (Fig. 3-X); bed 9 - “sharsha" -

white mictograined nonhomogeneous “^conglo-

merate-likc'’ limestonc with caverns.

The position of the upper boundary of the

Moscovian Stage, according to the conclusions

based on brachiopods and foraminifera srudies, is

changing within the interval from "the lower

conglomerate lu the base of rhe upper conglome¬

rate”, i.e. within lhe inccrval from bed 6 to

bed 10 on Fig. 2-X (Ivanov 1926; Ivanova ôe

Khvorova 1933; Bolkhovkinova 1937; Rauser-

Chernousovâ & Rcitlinger 1954; Maklilina et ai

1972). Further srudies of the lower conglomerate

interbed (bed 6 on Fig 3-X) undcrlying "dolo¬

mite of Turaevo ” showed that tliis conglomerate

wa.s from intrafonnatiorial origin and nor of inter-

stagial one, becaosc ail thèse interbeds contained

fusulinids of Fusulvja tylindnea Zone, indicating

rhe Myachkovo (Feski Subformation) âge of the

"lower conglomcj’ate” (Makhlina et ai 1972).

d'he complex of foraminifcrs above the "dolomite

of Turaevo” (in beds 8-9, le. in ‘^garnasha” and

"sharsha”) is represented by numerous small fora-

minifers and fusulinids with a widc vertical dis¬

tribution, Ozditvûînella atigulata, Globivalvulina

ex gr. gmnulozd, Schuhertella rnjachkoveinh,

Endothym sp. among them. Recently, fcw oppres-

sed Obsolètes obsolètes wcrc fouud in ibese beds.

Mass Obsolètes enter above the bed 9 ('sharsha”).

Therefore, we draw the boundary between rhe

Myachkovo and the Krev^^akino horizons (i.e. the

Middle/Upper Carboniferous boundary) at the

top of the "dolomite of Turaevo''' (bed 7 on

Fig. 3-X) between the two conglomérâtes, the

lower one and the upper one.

Conodom distribution in rhe boundary beds

demonstrate.s thaï the "garnasha”-"sharsha** beds

should be a.ssigned to the Kasimovian stage, i.e.

to rhe local Subzonc Idiognathodus arendti of che

Streptogtmthodus oppletus Zone (che Krcv}^akino

Horizon). The lower limit of the .subzone is dofi-

ned by the incoming of Idiognathodus arendti,

1. flshert. Sp'eptngfvzthodtts sttbexcelsiu, S. oppletus,

che upper one by rhe entry of S. sugittaüs and the

disappearance of Idiognathodus trigonolohutus.

Characteristic species are as follows:

Streptogitathodus suhexcelsus, S. oppletus, S. excel-

sus, S. eaneellosus, Idiognathodus trigonolobatus,

î. Jishert, J. arendti.

The Lippet boundary of the Myachkovo Horizon

(Formation), established on the basis of cyclo-

stratigraphic analysis at the top ofthe "dolomite

of Turaevo”, is proved not only by faunal distri¬

bution data but by also .sedimentological and

geochemical data. Bed-hy-bcd compatison of

detrital limesrone microstructures pn the

Myachkovo-Krev'yakino boundar)' demonsrrares

rhat in the former cloddy pcllecal cernent struc¬

tures dominate, whercas in the latter (rhe

.Suvorovo and Voskresensk subformations)

mictograined oncs dominate. Compatison of the

geochemical coefficients in the boundary beds

also demonstrates rhe différence in che quaiuitd-

rivc contenr of microelements: in carbonate

rocks and in clays and maris in the Noviinskoe

and Peski .subformaiions, ir is respccrively 10 and

2000 time.s more, than in similar rocks of the

Suvorovo and Voskresensk .subforniations. This

level, therefore, désignâtes the end of rhe

Moscovian transgression maximum phase (p^)

and the beginning of a régressive phase (y). It

corresponds to the Kasimovian time, characteri-

zed by the tcrrigenou.s supply with the micro-

elemental content, dilferent from ilie Moscovian,

by faciès variability in the zone of synsediment-

ary élévations, followed by the érosion and pre-

vailing of unfavorable environments for many

groups of fauna, particularly foraminifcrs

(Makhlina 1976; Makhlina eZ///. 1972).

Based on the data obiained from cyclostrati-

graphical analysis of the Middle/Upper

Carboniferous deposics in che type area, one may

conclude that the Kasimovian/Gzhelian bounda-

GEODIVERSITAS * 1997 • 19(2)

243

Makhlina M. Kh., Solovieva M. N. t & Goreva N. V.

ry was more significant than rh^ Moscovian/

Kasimovian oue, bccause the Kasimovian Stage

represented che terminal phase of the Moscovian

transgression, whereas the Gzhclian Stage corres-

ponded to ihe maximum phase of the following.

the Gzhelian/Asseiian transgression (both the

Moscovian and the Gzhelian/Asselian transgres¬

sions represent cycles of the sixth order). This

cyclostratigraphical boundaiy supports rhe views

of Nikirin (1890), who proposed to dravv the

boundary between the "Moscow Sériés*' and the

Gzhclian Stage below rhe limestone.s of Gzhel.

Taking into account everything mentioned

above, ono may corne to the conclusion thar

almost each of the subdivisions of Kashira,

Podofsk and Myachkovo horizons (formations)

are characterized by zonal conodont and fusuli-

nid assemblages, and can be traced in different

faciès ail ûver rhe major part of the Moscow

Syneclise and other régions of the Russian

Plarform, and aiso outside of it It gives the

opportunity to raise the rank of these subdivi¬

sions and to regard them as rhe horizons (cycles

of the eighth order) of the Russian Platform

Régional Scalc (Table 1). We believe also thar the

horizons estahlished by Tvannv in 1926 (the

Vereya, Kashira, Podol'sk and Myachkovo -

cycles of the eighth ordci) correspond to stages,

as it has heen demonstraced by Ivanova in 1955

and proved by numerous data, obtained during

the following ycars. Howevet. in May 1995, the

Interdepart-mental Stratigraphie Commirtee ol

Russia dccidcd to consider horizons of rhe

Moscovian Stage of the Global Scale as subsrages

with their own n.imes. As ro rhe Tsna

Subformation, the problein oi ils rank still

remains debatable (should il be a horizon or a

substage?). Solovieva considered the Tsna beds to

be of a stage rank. Tt can be traced in the Russian

Platform, as well as in Ticn-Shan, Donets Basin,

lirais and other régions.

REFERENCES

Anonymous 1990. — Decision of the Inter-

departmental Régional Swatigrapbic Conférence on

the Mieidlc and Jpper Paleozoic nf the Russian

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Léningrad, 95 p. [in Russian].

Alekseev A. S., Rarskov 1. S. & Kotionova I., 1.

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Moscow, tome 53: 1-281 [in Russian].

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Submitted for publication on 15 January 1996;

accepted on 1 October 1996.

GEODIVERSITAS • 1997 • 19(2)

245

stratigraphie corrélation of the Upper Permian

deposits from the south of the Cis-Ural

marginal Trough and the adjacent areas

of the Russian Plate

Ijia I. MOLOSTOVSKAYA

Institute of Geology, Saratov State University,

Moskovskaja Street, 161,410750 Saratov, (Russia)

KEY WORDS

Upper Permian,

stratigraphy,

corrélation,

South Cis'Urals,

Cis-Ural Trough,

Russian Plate.

MOTS CLÉS

Permien supérieur,

■Stratigraphie,

corrdations,

Sud Oural,

Cis-Oural,

plate-forme russe.

Molostovskaya I. 1. 1997. — Stratigraphie corrélation of the Upper Permian deposits from

the south of the Cis-Ural marginal Trough and the adjacent areas of the Russian Plate, in

Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigraphie corrélations,

Geodiversitas 19 (2) : 247-259.

ABSTRACT

Studied in detail werc about 100 sections of the Upper Permian marine and

continental deposits from the South Cis-Urals: from the south-eastern edge

of the Russian Plate and the Cis-Ural Trough. Characteristic complexes of

marine and non-marine ostracodes were distinguLshed. Ail the régional strati¬

graphie units of the Upper Permian were characterized in detail from micro-

paleontologic point of view. Associated organic remains were specificd:

tetrapods, bivalves, miospores. Rrief lithologo-facics descriptions of the sec¬

tions from varions structural zones arc presented. Detailed corrélations ofthe

Upper Permian sections from the South Cis-Urals wcrc carried out.

RÉSUMÉ

Une centaine de coupes dans les depots marins et continentaux du Permien

supérieur du Cis-Oural sont étudiées en détail : de Pextrémicé sud orientale

de la place-forme jusqu’à la dépression du Cis-Oural. Des assemblages

d'ostracodes marins et continentaux sont distingués. Toutes les unités strati-

graphiques régionales sont caractérisées en détail du point de vue micropa-

léontologique. Les bio-resres associé.s sont spécifiés : tétrapodes, bivalves,

miospores. De brèves descriptions des faciès et de la lithologie sont présentées

pour les différentes zones structurales. Des corrélations détaillées pour les

coupes du Permien supérieur sont conduites.

• 1997 • 19 (2)

247

Molostovslcaya I. I.

INTRODUCTION

The Permian systcm is distitiguished for the

wide-scale distribution of continental deposits in

Gondwana and Laurasia. It is extremely difFicult

to divide or correlate these deposits due to rheir

facial variations and scarcity ot organic remains.

The Upper Permian contineiiiul formations from

the east of Europcan Russia arc exceptional in

the respect, because diverse lossils hâve been

foiind and stiidied chcre: ostracodes, bivalves,

conchostracans, retrapods, fishe.s, flora and mio-

sporcs. Tetrapods and ostracodes are among

those most studied. Due to tlieir conimon occur¬

rence and fisr evolurionary variability, ostracodes

hâve become the leading launa in régional corré¬

lations. They may prove to be important for dis¬

tant stratigraphie corrélations as well.

rhe présent paper dcals vvith stratigraphie corré¬

lations and complcx biostratigraphic description

o( ihc Upper Permian deposits from the soulhern

Cis-Urals, onc of the most compiicated géologie

régions embracing the junction zone of the

south-east of the Russian Plate, Cis-Ural

Marginal Trough and Peti-Caspian Dépression.

Spécial atrention was paid to ostracodes, whlch

formed the basis for section divisions and corré¬

lations. The rescarch was fouiidcd on wcll and

natural section descriptions made by rbc author

in the process of géologie survey and thcjnatic

Works, and on the materials piesentcd in the

papers by Kuleva (19/5) and Koclictkova

(1970). Ostracode studics werc performed by the

author. Besides the original marerial, définitions

by Kochetkova & Spirina {in Kuleva 1975) were

used, in some cases provided with new strati-

Fig. 1. — The Upper Permian sections from the South-East of

the Russian Piste anp Cis-Urai marginat deflection P^u.

Ufimian; P;kZ, Lowor Kazaman: P^kZ^. Upper Kazanian: Pjt,.

Lower TaUrian Uppwr ïatari^n (North Dvina hoiizon),

Pjtj'^. Uppt-f TatariâM <VyaIkw hori/oii). T,. Luwtît Triassic

1 . Novo-KandaurovKa. tbo CheRuahu ihu Sukhalya River tribu-

tary (P^u, P Kz^, R,k7y) 2, KorneyevKa. lhe SuKnaiya River

(Ppkza)- 3, Yutoaly, Mit* SuRhâivs River (P;.Rz,. P-^kZ;ï* 3*,

Taimasovo iho Ûol. Kuyutqarü River (P^kz-, P>Kz^>. 4,

Yalchikayevo. the Shaitanka Rivet (P^u. P=Kz,^- 5 Well 104

Byelozyorka îhe Satmysn River fP^u. P^k^i P-kz^). 6.

Karmalka. Ihe Saimysh River tP^kz,. P>kzJ. 7 Well 124.

Petrovka (P^u. P^kz., P,,kZy, P_T,). 8. Well 1*22, Verknnî Gumbet

(P;;U, P> 2 ,. PAz^, P*i,)- Ô. Weli 123. Vûskresanskûye (Pa-

PAZi. PjkZs. PA)' ^0. Well 13*^. the Sheshmir River (PA^i*

Pgt,). 11. Well IS"-'', the Shestirn'rr River <P,u. Pikz.. 12.

Nlzhni Babatar (PAz,)- 13. Wall 388. Yangiz (PT, PAz,. PA^c-

P^l,). 14, Ihe Shesiimif River (PA^g. 15, Well l52k

Maryevka. the Saimysh River (P^u. PaE. 1^-

Well 157‘'. MaryevKa <P,u. PAz-,. Pjkz,) 17. Brody Spring

(PAZ;:. Pd-)- 18« Well 1 Brody (P è. PAz,). 19. Well 43>-.

Tiryak-Lizyak iPA' PA^v PA^^) 2<), Wall 48* (State farm)

OktyabrsIOi (PAZ;- Well 55. Budyonnovskij (Pjt-,.

22. Well 52''.*Anatolyevka. the Salmy.sh River (P u,

PAz,. PAz ) 23, Well Sakmara F.kz, PAz^. PA^

Well 1*'. Sakmait* (PAzi. 25. Well 3n-. Grebeni (PAz..

PAz^, PA). 26, Krasny GuHy. üioboni (P^u, P.lc,. PAZi,. PJ,)-

27. Well Ofstwni (P..w, P.^.. P..kz..). 28, Well 7^ Grebeni

(PAz,. PAzd- 29. Well 39'. Grebeni JPAz.- P kz^. PAÏ- 30.

Well 6‘. ChDb^fvkl (P Ar,. H^t ). 31. WcH 30. Neznenka (P,u.

PAz,. PgkîPyt,). 32*. drenhiirg iP^z,) 33, Weii 70^ Boislioi

Sulak (PA^i. RAz^) 34, W^il 94^. Bojsho] Sul^ik lP-u, PAZt,

PgkZg. PA. Kl.-*)- 35. Well 80. Dzhoan-Tyubinskaya (PAz-.

PAzg. Pot.). Ûé. Well 79\ Ozhuan-TvuOinskaya (P,u. PAz .

PAz,. Pat,. PA‘"- 37. Well 98*. Karavanny (P le. T,) 33.

Well 59*. Boyevaya Ml. (PAZ;)- 39, Wek 60'. Boyevaya Mt.

(PAz,. PA^d* *19. Wall 53', Boyevaya Mt. (PA^j. paA ^1-

Wells 61*‘-67''. Krasnoyarka (PAz.. Pokz^. PdW 42. Well 73\

Kamennaya (P^u, PAz,- PAz^- PAi* ^3.

Yelshanka (P^iA, T,). 44. Korneyevka, ihe Yarykly River (PAz)-

45, Yeldashevo, the Yurgashka River (Pgt,)- 46, Skvorchikha,

the Yergabusha River (PA)- ^7. Osipovka, the Budenya

(PAz>) 48, Karatalka. rhe Te>ryuk Rive*' (PAz,} 49.

Rodniküvsk, lire Tviryuk River (PAz?)- 50. Verkholor. Ihe Tor

River fPAzJ. 51, VoskrQsenskoye.'lhe Tor River (P_.t,)- 52.

Vesyoly rhe Nugush River (PJ, PA*'’) 53. Krasnogorka.

tho Nugush River 54. Lipovka (P,t./. 55. Aie.xandrovka,

the WugiJSh nvor (PAZ,- P.Az,. P^!,). 56. Yurnaguzmo, the

Mdleni (PA''^ P. 1;'') 57. Kadyrovo, lhe Menyg River (P.I,} 58,

f^alakqriüvp (PAz,}- 59. Sergeyevsktj. lhe Chukur - Bulyak

River The Bolshoj Yushatur Inbutary iP^i.) 60 Cherrigovskij

(PA*^) 61 Bekechevo ihe Nâk‘j 2 River (PAz,- P Aï,. p 2 i,).

62. Savelyevski) (Pjtp’'*). 63, Sankinskrj iP,!;.•') 64,

Raznomoïka. the Tugdstemir River 65 St’avyanka

(PAZ;, P^U)- 66 AJiaberdino (PAz^) 67. Davletkulovo, lhe

Yaman-Yushatyr River (PAz?- PA) 68. Well 28 and uve'i 43.

Davletkiilovo (PAz,. PAz 2 . Pa*,)- 69. the Tashla River (PAZg.

Pj!,). 70. Alejtandrovkâ. the Kupiya River (PA'*')- 71. Urman-

Tashia iPîiA**! 72, Kasierînskij. the Boishoi Yushalur River

basin (P.J- '). 73 MaslovsKij, me Boishoi Yushatur River basin

(PA'’)' 74. Smirnovka tPA“’) 75. Alebasirovaya (PA') 76,

Cherepanovka, lhe Burunchar River tPA'*')' 77. Well 41.

Staroseika. tho Bolshol Ik River (PAzi- PAZ;>)- 78, Staroseika

(PAZj) 79, Dmithyevskij (P,t,. Pji,-®). 80 WgM 4- ana 5',

Dmilnyevskij (P,.k 2 .. P^,l, PA"*)- 81 Stary Kaziatr. the Chena

River (PAAT 82, Novosyoiki, the Chena River (P^.l,) 83.

Khoimogory. the Bolsho* Ik River {P;4,). 84. NovoKulchumOvo,

lhe Sakmara River (P;;t^^‘^. PT^'^)- 85, Well 121,

Novokufchurnovo (PAZi- P^t). 86. Vyazovka. iho Ural River

P?!/'). 87, Well 102. Vyazovka, (P;Ar?. Pji,! 88.

Well Ostrovnoye. the Urai River (PAz.. Paz,., PeM- 89.

Blumontai Gully, Ihe-Burtya river (PA'''^TÏ 80 Zhoiloyo. the

Sakmarâ Rtver (PA^J- 91 . Giryâi, ihe lirai River (PA"’- Pîln**)-

92. Well 73. Acbvny (PAZ:- Pdd 83 Well 44.

Verkhneozernoye, lhe Ural River (P;kz,i. 94. Verkhneozernoye

(PAZ-, P-.i\ 95- Wells profile 5-22 lhe Burly River (P.i,. PA^’.

P.iA)'

a. outerop exposure. b, well. c. boundary ot the Cis-Ural margi-

r>al deflecliop- d, boundary of Per-Caspian Dépréssion A-B,

lhe line ot the sections studied in Fig. 2. C D. lhe line of the

sections sudied in Frg. 3. E^F. the (me of tlie sections studied in

Fig. 4.

248

GEODIVERSITAS • 1997 • 19(2)

Stratigraphie corrélation of the Upper Permian, South Ural

57 ®

56 ® 57 ^

GEODIVERSITAS * 1997 • 19(2)

249

Molostovskaya I. I.

graphie mtcrpretarioiis.

Bivalve complexes were Sîudicd by Kuleva

(1975), fish by Minikli & Minikh {tn Ochev et

ai 1979), conchostracans by Lopato {in Kuleva

1975), miosporcs by Shatkin^kaya (Hfremov &:

Shatkinskaya 1972). letrapod définitions belong

to Tverdokhlcbova, Chudinov & Ochev {in

Ochev et al. 1979). The data on marine macro-

fauna was taken Injin the works by Kochetkova

(1979) and Rom.inov (1972).

The Wells were drilled by the Orenburg

Territorial Géologie Service from 1960 to 1985.

UPPER PERMIAN DEPOSEPS

The upper section ot the Permian system in the

South ol the Cis-Ural marginal bend and the

adjacent région ol the Russian plate is represen-

ted by the Ufimian, Kazanian and Tatarian

stages. The Kazanian and Tuarian .stages are each

represented by iwo substages; ihe lower and the

upper oncs. I he lowci substage of the Tatarian

consists of the Urzhum horizon, the upper one

of the North Dvina and Vyarka horizons.

According to the feamres of the Lare Permian

sedimentogenesis, this territory is divided

(Fig. 1) into chree structurahfacial zones: the

western (Novo, Kandaurovka, Grebeni and

Yelshanka sertlemenis), the axial (Raznomoika,

Vyazovka, Blumental) and the eastern (Tor,

Khohnogory, Biirly). The principal stratigraphie

units from each zone possess lithologie composi¬

tions, thicknesses and minerai complexes that

differ to varions exrents (Figs 1 -4).

The Ufimian s iage

l’he Ufimian stage Iront chc western zone is stu-

died in exposures and cores from numerous

mapping and pioncer wclls (Fig. 1, Kandau¬

rovka, Shestimir, Yangiz, Urnyak, Brody,

Sakmara, Grebeni, etc.).

The stage i.s composed predominantly of red ter-

rigenoLis rocks that arc replaced by halogenic

Kungurian structures downwards along chc .sec¬

tion. The boundary between the Ufimian and

Kungurian beds is convcntionally drawn over the

roof of the last more or Icss chick interlayci of

chemogenic rocks. Clays, aleurolites, sandstones

dominatc in the section, mari, limestone and

dolomite interlayers are rare. Rock gypsification

is charactcristically observed, significant in the

lower portion (Fig. 2). The thickness varies from

75 to 190 m. Diverse qcganic rcmains occur:

ostracodes, bivalves, conchostracans, miospores.

Ostracodes. Pnleodarwin itln ahunda

(Mandclstam), /? nugiistn (Mandclsfam), P. par-

phawvae (Bclousovu), P proara (Mandclstam),

P. litncetiformis (Kashevarova), P. trita (Palant),

P. burjevoensis (Palant), P. luhimovae

(Kashevarova). Garjainùinda Uja (Spirina et

Molostovskaya), Ç. kulevae (Spirina et

Molostovskaya), G. gracilh (Spirina et

Molostovskaya), Prasnchonella stehruirta

(Kashevarova), Pr, kargalrnsis (Kotshetkova),

Pk ka^nyschemaensis (Palant), Darwiniiloides

djurtjulivnsis Palant, Sinusnella pergraphica

Mandclstam.

Bivalves. Pahi-emnutela attenuata Gusev, P. ova-

tiièformis Gusev» P sinlasensis Gusev.

Conchostracans. Hernicyeloleaia baentschiana

(Bcyrich), Limnadia {Paleolimnadia) rossica

Molin.

Miospores. They are represented by rwo com-

plexe.s; rite early (Miospore.s Hl) and the late

oncs (Miosporcs H2) (Efremov & Shatkiriskaja

1972). Within the Hl miospore contpiex domi-

nate Zonotriletesy significanrl)^ Dri/rivwr, associa-

ted Vitratinai characferisric Lycospora variahilis

(Jansonius), Clrratriradites prncumbem (l.uber),

Stria topodoenrpttes tajfne>tsis' Sedova,

Strititnidiplapiyiites elangam (Ltibcr), Vittatina

s tVH} ta 1 -U b e r, Gra n isp o ri tes os m u n da e

(Samoilovich), (hannlatisporites resiste^h (Luber),

Cnratriradites provumhem (Luber), Platysacctis

alntrjs (Luber), Striatohapïopiniles perfectus

(Naumova).

The Ufimian beds are poorly studied in the cen¬

tral zone due to little outeropping and the lack of

cote materials. A 180 m thick scqucnce of red

gypsiflcd clays, maris, sandstones with gypsum

interlayer.s, situated a bit to chc north of the area

concerned, near chc village of Yar-Bishkadak

(Kotschcllvova 1970), bas been assigned to the

Ufimian. The confirmed Ufimian beds to the

South, were pcnccratcd by wcll 79 in the left-

bank région of the Ural River. They are represen-

ted by red clays, aleurolites and sandstones.

250

GEODIVERSITAS • 1997 • 19(2)

Stratigraphie corrélation of the Upper Permian, South Ural

Molostovskaya I. I.

Wells show the Ufimian beds to be up to 360 ni

thick. In chc castern zone> the Uhnùan deposiis

occiir along the Nugiishu River (Vishnevskaya

and Alcxandinvka villages). They are represented

by a thick (about 700 m) sequence of red conglo¬

mérâtes with rtinr pebbics, sandstoncs» aleuroliies

and maris with rare thin limestone interlayers.

Coarse clasrics are characreristic of the middie

portion. Along the Nakyz river near the

Ryazansky l'arm and the basins of the Bolshoj Ik

and Bolshoj Syuren Rivers, the Ufimian deposits

are represented by thick pebblc conglomérâtes

often changed by boulder ones. "Uiesc conglomé¬

râtes consist of coarse pebblcs of diverse nicca-

morphosed and igneous rocks» limestones with

Carboniferous l’annal remainst quartz and Oint.

Sandstone lenses occur among conglomérâtes»

and very seldom interlayers of maris and sulfur

silicified limestone (Kotchetkova 1970).

In the vicinity of Zalair-llyinskoye and .Staroscjka

villages, the LIlîmian deposits are represented by

68 m thiciv reddish-brown argillices with iiuer-

laycrs of browni.sh-grey sandstones and grey

limestones. The âge of the set|uence is cstabli-

shed according (o osrracode complex: the zonal

guide fo s s i I Pale fi lia rw 1 n ti la a h ii n eln

(Mandelscain) and R angasïa Mandelsiam,

P. lancetifornns Kashevarova, etc.

The Kazanian srAc.t

The Kazanian stage according to its lithologic-

lacial featiires is divided into two subsrages: the

lower and the upper ones.

The lower Kazanian stage

The lower Kazanian stage has a complicated

structure wichin the area considered. In the west,

it is represented by marine faciès subscituted by

lagoonal-contincntal ones farther castward,

mainly in the axial zone; rhis reflecrs rhe trans-

gressive-regressive cycle of the Kazanian sea

(Fig. 1, Urnyak, Brotly, Sakmara, Grebeni,

Nezhenka, etc.).

Within the western zone, the lower Kazanian

substage is conipo.sed of grey santLsiones, aleuro-

lites, clays and limestones. Clays and alcurolites

dominatc in the lowermost of the section; chc

middie part is represented mainly by limestones,

maris and clays.

rhe upper third of the sequence is built of clays,

aleurolite.s and sandstones, the larter ones often

con.siiiuting up to 50-70% of its volume. The

substage thickness varies froin 60 to 200 m.

Diverse organic remains occur wîtliin the lower

Kazanian deposits: ostracodes, corals, bryozoans,

crinoids.

Ostracodes. Ostracodes are represented by the

in,irine species* the guide fossil Amphhshes tscher-

dynzevi Posner and Psendoparaparchites fornnda'

biUs Schneider» AccumineUa bella Khivïntscva,

Corntgclla valosa Khiviniscva, Kirkbya tara

Khivintseva, Moorea facilis Schneider, Cavellina

grandis Schneider» Cavellitui unior Kotschetkova,

Hcaldia posreomnra Schneider, H. oblonga

Kotschetkova» llealdia shnpUx Rouody. H. pseu-

disfmplex Kotschetkova» H. snhfriangula Kots¬

chetkova, H. reniformis Schneider» Healdianella

vulgata Kotschetkova, Cribroconcha tmehakensis

Kotschetkova, Bnirdia heedei Ulrich et Bassler,

B. garrisonemis Up.son, B. pomptlioides Harlion,

Acratia bascbkirica Kotschetkova, Tabalicyprh cre~

pidalis Kotschcikova, Actunna diffusa Schneider,

A. seennda Kotschetkov.i, Monoceratina fiistigiata

Kotschetkova, M. faveolaia Kotschetkova,

M. parvnla Kotschetkova, M. exiUs Schneider,

Fascianelbi mnabilis .Schneider.

Foraminifers. Glmnospira sp., Ammodisens cf.

b ra dy nus J* a n d c I . Venieuitrno i d es basa n i ca

Ucharskaya, Cornuspira mcgasphaerica Gcrke,

C miiTOsphiierica K. M. Maday. Caldvertella

knsixnka K. M. Maday, Nodosaria cushmani

Paal/.üv, N. Joteimeniformis K. M. Maday,

N. hexagona ( fscherdynzev), N. aff. noinskyi

l’scherdynzcv, N. krotovi 'fscherdynzev, Pseudo-

nodosaria lata K. M. Maday, Frtmdicularia Ion-

gissirna (K. M. M.idav), Fr, geinitzinaeformis

(K. M. MaeJay), Geinitzina spandeli Tscher-

dynzcv, Teirattixis sp., Tristis permiana Gcxkc, etc.

Brachîopods. Cleiotbyridiiui pectinifera Soweiby,

Cl. semiconcava Waagen, CV. nyssiana KeyserÜng,

Stepanoviella be m i sp ha e r i uni K ii t u r g a,

Pr. (Gantrinelta) cajicrifii Vtnieuil, Pn konincki-

anus Keyserling, Licharewia riigulatia Kutorga,

/.. cuTvirostris Verneuil, Üielasnia elongata

vSchloihcim» D. elliptka Nctschajev» D. angnsta

Nctschajcv, Linguta orientalis Golowkinsky,

Atdosicges honescens Verneuil.

Bivalves. Leibea haiismanni Goldfuss, Allorisma

252

GEODIVERSITAS • 1997 • 19 (2)

Stratigraphie corrélation ofthe Upper Permian, South Ural

elegnns King, PseuiJobakewellia sulcata (Geinirz),

Ps. ceratnphragiuformis Noinski, 5. tutchburia

îschernyschevi LichareA'.

In rhe central and eastern zones, the lower

Kazanian comprises a sequence of grey-colored

sandstones, aleurolites, clays, maris, limestones

and dolomites of lagoonal-deltaic and littoral'

marine gcncsis (Figs 1, 2, 3, Davietkulovo,

Bekeshevo, Srarosejka, Ostrovnoye, Verkhneo-

zernoye). The sequence contains the Kazanian

complex of non-marine ostracodes: guide zonal

fossil Pakodarwiimlii fainae (Bclousova) and

P aineata (Kotschctkova), P. imme (Bclousova),

Prasueboveibi hclchetcfî (Belousova), Darwinu-

bides cf sentjakotsis (Sharapova).

Non-marine bivalves. Paleomuieta sintaserisis

Gusev, P ovataeformh Gusev, characteriscic ofthe

Uflrnian and Lower Kazanian deposits,

Flo ra. Pecopteris iUithrisctfolia Meyen,

Sphenophyllum, Asterodheus.

Pollen ol üord.iitcs: C.ordahina uralensis (laiher)

Samoilovich, C mbrouita (Luber) Samoilovich.

Ginkgos: Ginkgocycadopbytus crosi4s (Luber)

Samoilovich.

Co n i fe rs: Protodiploxypinus çlongaim

Samoilovich, Protopodoempm akttus Samoilovich.

Some pollen of obscure systematic affiliation:

Azonalites [Rugosina) tenuü Luber, A. (Ihiuella)

levi-s l.uber.

Fern-like .spores: Aztmofriletes cf. résistons Luber,

A. Samoilovich (Kuleva 1^75).

The upper Kazanian suhstage

The upper Kazanian substage in the western

zone is represenred by lagoonal-continental for¬

mations: red, less frcquently grey clays, aleuro-

lires, sandstones, and, r.o a smaller extenr, by

limestones, maris, dolomites (Valchekayevo, the

Shestemir River, Shesccmir, the Karmalka Spring,

Tashla-Lhiiyak. Sakmara, Grcbcni, Nczlienka,

etc.). The lower boundary ot the laie Kazanian

deposits is clear. drawn over the roof of marine

sandstones, overlain by clays wirh the zona] guide

fossil Paleodanvinula fainae (Belousova). Its

thickness varies froin 110 lo 14() m.

Within the axial zone (Davlctkulovo,, Slavyanka,

Islayevka, O.sirovnoyc), the upper Kazanian sub¬

stage is composed of non-marine irucrlaid clays,

aleurolites and sandstones with rare interlayers of

limestones and maris. Within che section near

Davietkulovo village, scattered smâll flint and

mari pcbbles occur as wcll as small lenses of fiue-

pcbblc conglomerate.s. The substage is up to

600 m thick thcrc. Uie section near Ostrovnoye

village is distinguished for chiner rocks; it is

250 m thick.

The upper Kazanian substage bas a somewhat

unet^en structure in che eastern zone. At rhe Tor

River (Kotchetkova 1970), this is represented by

a thick (556 m) carbonate-terrigenous sequence

composed of Inlerlaid brown, lilac and grey

clays, aleurolites, maris, limestones, sandstones.

The Kazanian is nul divided into substages

within the section along the Nugush River.

Assigned co ii is a thick (over 700 m) sequence of

brown, lilac, grey maris and aleurolites with

sandstone inierlayer.s; this sequence overiies a

sand-conglomerate one, chat is conventionally

considered to belong co thé Ufimian stage.

Coarse clastics are rathet significant near

Zhyoltoyc village*, sandstones, gravelstones and

conglomérâtes. The section near Novokul-

chimovo is represented by a rather monotonous

interlayers of concretionary and bedded brown

limestones. Diverse organic remains occur within

the upper Kazanian deposits over the whole of

the territory: ostracodes, bivalves, conchostra-

cans, tetrapod-s, flora and miospores.

Ostracodes. Ostracodes are represented by the

foliowing spccics: Paleodarwinuln fainae

(Bclousova), P akxandrimie (Bclousova), P ire-

nac (Bclousova), P euneata (Kotscheikuva),

P. tichonovichi (Bclousova), P. tuirnazensls

(Kotschctkova), P. tHinanufttvae (Belousova),

P. inornarinaeformis (Bclousova). R chemnovella

(Beioitsnva), P amnavae (Bclousova), P persim-

plex Kotschctkova, P procurifa (Kotschetkova),

Garjainowula lija (Spirina er Molostovskaja),

G. ex gr graalis (Spirina et Molostovskaja),

Prasuehnnella tkbwinskaja (Belousova), /? beb-

heica (Beloust)va), Darwinuloides semjakensis

(Scharapova), Plaeidea ex gr. lutkevichi

(Spizharskyi). Schneideria kazanka Kotscherkot-a

occurs only in che lower par: ol the section.

Bivalvc-s. Bivalves are represented by the Bclebcj

complex ; Palaeanodorua rhomboidea {Ner-

schaev), Palaemuiehi cebbrata Gusev, P. cfuadraia

Kuleva, P, novalis Netschaev, P. umbonata

GEODIVERSITAS • 1997 * 19(2)

253

Molostovskaya I. I

TRIAS

ixl

2 û- >

5 Û. ic

< 3 y)

2 n

> O)

=7 O’"

cc ^

h* •J

_Wjfj

30oJ ....

Fig. 3. — Corrélations of the sections of the Upper Permian deposits in central part ot Cis-Ural marginal deflection. 1. conglomé¬

râtes. 2. Lirai rocks pebbles. 3. local rocks pebbles. 4. sandsîones. 5. aleurolites (siltsiones). 6, clays. 7, maris. 8. limestones. 9,

organogenic-clastic limestones. 10. nodular limestones. 11, dolomites. 12, gypsum. 13. anhydrites. 14, salts. 15. ostracodes. 16,

bivalves. 17, conchostraceans. 18, brachiopods. 19, foraminifers. 20, gasteropods. 21, tetrapods. 22, fishes. 23, flora. 24. mio-

spores.

GEODIVERSITAS

Stratigraphie corrélation of the Upper Permian, South lirai

(Fischer), P. krotovi Nctschaev, R olgae Gusev,

P. doratifonnis Güsev.

Conchostracans. PaldeolimnadiopsU eichwaldi

(Netschaev), Ctyptoasmussia exiqua (Eichwald),

Cyclotimgusîîes kazanen$is Molin. ULiigkemia

Novojilov, U. orengurgiana Molin, U. pétri

Novojilov, Sphiîcret^theria ikevsis Molin,

Pieudestheria ktuhwica Mol in.

Tetrapods. l*I(U\*tps sp., Denterosauriis sp.,

Tapinocepbalidüc> similar in dimensions to

Deuierosaurus gigm Efremov.

Miospores. Charactcristic Cordaitina, Limiti-

sporiies leschikii KJaus> Cigafitosporites hallsta-

thensls Klaus, Striatites marginalis Klaus,

Striatohaplopinitci latissimus (Liiher), Striata-

pkeites suebineash Sedovâ, Vfttattna striata Luber,

associa t.ed Cyclogranisporites^ Açanthotriletes,

Azonali'tes.

Flora. Carpolithes sp., Phyllodaderma sp-,

Noeggerathîopsh sp., lepeophyllum Samaropsis

sp., sp., OdoHtapteris 5^.^ Eqitisetinu

sp., Rtiflaria sp., Taeniopteris sp., Recapteris sp.,

Voltzia mamadysihemh Zalessky, Samawpsis irre¬

gu taris Ncuburj», Piygmaphyluni expansum

Brongnian. Odoutopteris cf. vossica Zale.ssky,

IJllmanuia Inarmiya Eichwald.

The Tatarun s tage

The Urzhum horizon

d'he lowcr Tacarian siibstage (Urzhumsky in

figures 2'4) in the western zone discontinuousiy

overlies rhe Kazanian beds and i.s characterized

by binary structure (Shesteniir, Sakrnara.

Grebeni, Nezhenka, Boyevaya Mr.). Its lowcr

part is composcd of obliqucly la)-'ercd red sand-

stones, aleurolites, clays and finc-pcbblc conglo¬

mérâtes of local-rock pebblcs. The upper half is

built of red jleurolites, clays, fine and more sel-

dom coarse-grained sand.stones. The horizon is

up to 200 m thick.

This division in two parts bccomes progressively

le.ss vivid ea.stwards (Kamennaya, Dzhuan-

Tyubinskaya).

rhe axial zone of rhe Urzhum horizon i.s distîn-

guished for high fhicknesses, alcurolite-clayey

composition, cunglomeratc-lens occurrence and

widely spread nodular limestones. The number

of conglomerate interlayers reduces southwards

(Fig. 3), the number of nodular limestones

increascs. ’Fhc section ncar Davled\ulovo village

is composed of red intcriaid clays and aleurolites,

sandstonc, ümestone and mari Interlayers, rhin

lenricular interlayers of finc-pcbblc conglomérâtes

and gravelstoncs with their clastics consisting

mainly of flints. Uneta’nly scattered flint pebbles

and gravels occur in somc aleurolire interlayers. A

thick f6 m) intcrlaycr of coaxse-pebble conglomc-

rate lies in the base of rhe section. The boundary

between the Kazanian and Tatarian deposits i.s

drawn over its rugged lowcr surface. The appa¬

rent thickness - 430 m. Fhe EJrzhum horizon sec¬

tion near the villages of Ostiovnoye and Vyazovka

looks more inonoconous and consists of finet

rocks. It is over 550 m thick. The Urzhum hori¬

zon is unevcnly structurée! within the eastern

zone (Fig. 4). le is characterized by binary structu¬

re in the nonh of the zone, in die sections aiong

the Tor, Yergabusha and Yurgashi ri vers. Its lowcr

Irak consists of a conglomeratc-sandstone séquen¬

cé with rare interlayers oi icd-brown clayvS and

maris. The upper onc is represented by a

marl-clay-sanclstone sequence with interlayers of

grey claycy limestones and aleurolites. The hori¬

zon is 780 m thicic.

Southwards, ncar the villages of Bekechevo,

Dmitriyevo, Kholmogory, rhe Urzhum horizon

is dominared by interlaid clays, aleurolite.s, inter-

laycrs ol tinc-gralned sandsrones and hrown

concretionary limestones. Fine and coarse-pehble

and e\^en boulder conglomérâtes are ai.so impor¬

tant. Their clastic matcrial is poorly sorted. T he

pebble sizes var)* Irom ! to 10 cm, the boulders

are up to 20-25 aemss. Large pebbles and boul¬

ders are represented by the Lower Permian and

Middle Carhoniferous limestones and sand-

stones; fine pebbles by fiinu. Conglomérâtes are

usually füund withiii rhe bases of sédimentation

rhythms which are clo.sed by clays with nodular

limestones. Conglomcrace members in rhe lower

part of the section arc up to 8-10 m thick.

Upwards along ihe seaion, conglomerate mem-

bens beeome diinncr and the sizes of clastic mate-

riais dccreasc (Kuleva 1975).

Farther souch, cowards the Peri-Caspian

Deptession (Buriy), and to ihc west of the Lirais

forefold.s (Novokulchumovo), the sizes of clastic

material and the share of coarse-clastic rocks in

the section decrease. The principal position in its

GEODIVERSITAS * 1997 • 19(2)

255

Molostovskaya I. I.

Structure is occupicd by clays> aleurolires and

fine-grained sandstoncs. The following Fcatures

are characreristic of these sections: nuher mono-

tonous brown color of rhe rocks, scattered lime-

stone nodules, aleiirolite prédominance wiihin the

lower part of rhe section and that of clays in its

upper part. The apparent rhickness of the Ur-

zhum horizon section at Burly constitures 960 m.

Ostracodes. The paléontologie description of

the Urzhuin horizon is complété and involves

large variety of forms. Ostracodes are repre^senred

by a rich complex consisring of the following

spccies: zonal guide fossil Pahodarwiniih

formis (Kashe^^arova) and P. elongata (l iinjak),

P fragilis var. mjgmta (Schneider), P hmrnatinae

(Lunjak), /? chramovi (Glcbovskayaj, P. formais

(Kotschetkova), P. faba (Mischina), P. impostor

(Miscbin.i), P defluxn (Mischina). P, tirida

(Molostovskaya), P abvhï (Moloslovskaya),

P. gartainovi (Molostovskaya), Prasuchonella

nasalis (Sharapova)'. DtirwinulQtdes hiigurnda-

nicus Kashe\'arova, Sinustiella ig?iota Spizliarskyi,

Placidca Unkevwhi (.Spizharskyi),

Ail the species listed above are rather widcly dis-

tributed wiîhin the Urzduim horizon rocks over

the whole üf the Russian Platform (Molostovslcy

& Molostovskaya 1967; Molostovskaya 1974,

1993). Besides, the upper part of the Urzhum

horizon in the territory^ considered is characte-

rized by isolated localitîes of endetnic cytherides:

Tscherdynzi'vianu squamoset KotScheikova,

Wetluginellû (?) tatiîrifa Molostovskaya in press,

Kasebevaroviana delkatu Molostovskaya in press,

K. pectunatu Molostovskaya in press.

Bivalves. Abiella subovata (Jones), MîcrodanttUa

microdonta (Klialfin), M. plotnikovskiensis

(Fedotüv), Paliiemuteln doratiformis GuSev,

P. pciraUelogramma Kuleva, P. gmevi Kileva,

Anthracoudia verneitili (Amalizky)j 7l. aktubams

Gusev, Anîhrdcorututii {Prokopievskiiî) pseudophil-

lîpsi Fedütov.

Conchoscracans. Pscudoilherin angulata

(Lutkevich), Sphacresiheria belorussicu NovojiloV,

Triedrolophui tverdochlebovi Mol in, Pseudostberla

otchein Moliu, Aiegdsitum jaroslavknse Novojilov.

Tetrapods. MncTneiosaurus juhilaeui Novikov,

Metosaurus sp., Dmtrrosaiirus sp., Platyops sp.,

Notosyodùvi sp.

Miospores. Characteristic Lebachiacites pulcher-

riynus (Sauer), Striatoleachites^ JiigasporiteSj

F/ninipollenitrs^ Jaeniiisporites albertal Jansonis,

Vittatiua striata Luber; associated PLttysacctis sp.,

Alisporites strhitübaplopinhes.

rhe North Dvina horizon

The North Dvina horizon (Severodvinsky in

F'igs 2-4) in chc western zone is repeesented by

interlald red clays, alcurolites, sandstoncs, rare

lenses of fnie-pebblc conglomérâtes of mostly

local rocks and isolaied interlayers of brown

clayey limcsioncs (Budyonovsky, Ostrovnoye,

Kamenny).

As in the western zone, tlic North Dvina horizon

section in the south of the central zone is charac-

lerizcd by rather fine tertigenous composition

and red roclt-color (well 7:3^ Dzhuan-

Tyubinskaya, Vyazovka).

The North Dvina horizon is ununiform in its

structure in the north of the central zone and in

rhe castern zone. Ir is variegated and characteri-

zed by carbonate-clayey composition, being for-

med of redrown, lilac, grey clays, aleuroFues,

sandstoncs, limestones and maris, l’hc interlayers

ol grey rocks generally contatn large amounts of

charred plant détritus (Gumaguzino, Vesyoly,

RaznomoikUi Chernigovsky. Alcxandrovka on

rhe Kupiya River, Uman-Jashla, Dmitrovsky,

Novukulchumovo, Girydlv Burly). In some sec¬

tions (Chernigovsky, Raznomoika, Dmitri-

yevsky), coarse clasrics (sandstoncs and conglo-

mciatc.s) are rather significanr in the horizon

structure, riiev are generally associated with the

lower hali of the section, sometimes forming a

sequence up lo 300 m thick there (Cherni-

gov.sky). l’he amount of coarse terrigenous matc-

ria! within ihê North Dvina horizon decreases

westwards and southwards froin the Urals ro the

Peri-Caspian Dépréssion. The numher of grey-

rock interlayers decreases in rhe same direction,

l’hc thickness of the North I^ina horizon varies

from 100 m ((Tstrovnoye) to670 m (Burly).

The rock âges within rhe North Dvina horizon

are determined hy numerous and multiform

organic romains.

Ostracodes. Ostracodes are represented by rich

and diverse associations. The following spccies

are ubiquicous; zonal guide fossÜ Snchonellma

futschiki (Kaslievarova) and 5. inornata Spizhar-

256

GEODIVERSITAS • 1997 * 19(2)

Molostovskaya I. I.

skyi, 5. pixrallela Spizharskyi, S. iindidaia

(Mishina), 5. daedala (Mishina), .S*, cultetla

(Mishina), S. degitaiis (Mishina), 5, spizharskyi

(Pozner), PmuchnncHa stelmachovi (Spizharskyi),

P. sulacenùs (Starozhi)ova), Oarwhndnides hugu-

Tîislamcus Kashevarova. Permlana elongata

Posner, P oblonga Pmner, Tschndynzcviana pyl~

chra Belousova, 7. buzidukensh Kashevarova.

Besides rhe ostracode-listed above, some peculiar

sciilptured endetnîc cyrherides occur in rhe eas-

tern zone ; Tsvberdyuzt‘viana htinihicensis

Kashevaro\^, T. penuatit KoLschctkova, T tibscau-

dita Kocschctkova, Netsvhnjewianû costata

Kotschcrkova, Nugtachia sintzyni Korschetkova.

Kaschevaroviana dclkata Molostovskaya in press.

K. pectmiiXîii Molo.stovskaya in press, Ititigumidm

minis Molostovskaya in press, Permtanclla inila-

terata Molostovskaya in press, Pamilio primaviî

Molosrovskaya in press. They are clearly difFerenr

from thosc common for thc Russian Platform in

their morphologie ^eaturcs, being close to marine

and scmimarinc cytherides of the Triassic from

the Peri^Caspian Dépréssion.

Bivalves. Bivalves are represented by

Palaeomutela hiostranzevi Amalizky. P. keyserlingi

Amalizky, Palaenodonta fïscheri Amalizky,

Opokiellii ignutjevi Gusev.

Conchostracans. Siberioleain oblonga

( M i tse h e 11 ), lïnn icycloleaia intermediata

(Mitschell). Pseudastheria cican'icûsa (Novojilov).

Tetrapods. Chroniosiiurua dongusensis

Tverdnehlebova^ Rophnnodun rva-dochlehovae

Ivachnenko, Mkrophon ex'tqtius Ivacbnenko.

Fishes. Isadia aristoidensis A. Minich, I. sucho'

nensis h. Minich, Toyemia werdochklmn Minich.

Flora. Pursongia awfdirzkîi Zalessky, Cordaites

clercii Zalessky.

Miospores, Limitisporites sp., Jugasporites sp.,

Lticckisporites virkkîae Potonie et Kremp,

Taeniaesporites alhcrtae Jansoniiis.

The Vyatka horizon

The Vyacka lionzon (Vyaesky in Figs 2-4) in the

western and central zones, lîkc ihc North Dvina

one, is compo.sed of ceriigcnous and mostly red

rocks: clays, aleurolites and. ro a smaller exrcnr,

sandstoncs. Rare ihin conglomcrare inter!a}'ers or

lenses occiir, wich their clastic nuterial represented

by local-rock pebbles, more seldom by flints and

quartz (Savclycvka, Sankinsky, Kasterinskv, Mas-

lovsky, Oscrovnoyc, Dzhuan-Tvubinskaya. Ka-

mennaya, Yelshanka, Vyazovka, Blumcntal). Grey

and greenish-grcy conglorner.3tc.s and sandstones

in Blumenta! Gtilly are Associated with copperore

manifestarions. Ail the rock therc are chanicrcrized

by large amoiint.s ot charred plant rcmains: cquise-

tite stem fragments, pieœs of .srlicilied wood.

’Fhe Vyatka horizon sections in the eastern zones

are dominared by bmwn and, more seldom, grey

clays, aleurolites, sandstones. Grey, Hlac, brown

limcsroncs and mnrls are aiso important. Some

conglomérâtes occur, forming rather large lenses

and inrerlayets. Their clastic material is represen¬

ted by flints, quartz, limcstones, effusive rocks

and more seldom, local red rock (Vesyoly,

Krasnogorka, Yumaguzino, Smirnovka, Alcba-

strovaya, C'herepanovka, Novokulchu-movo,

Ciiryal, Burly). The thickness of the Vyatka hori¬

zon comprise 245 ni ncar Novokiilchumovo,

465 ni ncar Vyazovka.

The rocks from the Vyatka horizon contain

diverse organic remains.

Ostracode&. Ostracodes are represented by the

following species: guide fossil SueboneUina irape-

zoideti (Sharapova) and 5. parallèle Spizharskyi,

S, xinduLiui (Mishina), Wjiitkellina fragilina

(Belousova), W. fingitii (Schneider), W vindimk

rittn (Belousova), DvinelLx ex gr. lyno (Zekina),

Sui'honclla typtea Spizharskyi, Tatariella iVigtdata

Mishina, Plucidea luikeviihi (Spizharskyi),

Tscherdynzeviiitiû ptdchra iBclousova),

Besides theni. the sections from thc eascern zone

bear endemie sculprured cytherides, conveyed

from thc North Dvina horizon Tscherdynzcviana

penuntd Kotschcrkova, Nelschajewuxjui costata

Kotschcrkova, fùshcvarotnana delkata Mnlnstov-

skaya in press, Pamilio primaris Molostov.skaya in

press.

Bivalves, Palaeomutela iruntranzevi Amalizky,

P. orthodonta Amalizky, P. ovalis Amalizky,

P. plana Amalizky, Palaeanodonta fîsheri

Amalizky. P akemh Am.dizky, Opokiella tscherny-

schevi Plütnikov.

Conchostracans. Limnudia angulidorsa

Novojilov, /. maitschatica Novojilov, L {TaLùsca)

fn raten Novo j i I ov, Megan/tu ;// kaljugcnse

Novojilov» A/, vanum Novojilov.

Tetrapods. Chroniosuchus uralensis Tverdoch-

258

GEODIVERSITAS • 1997 • 19(2)

Stratigraphie corrélation of the Upper Permian, South Ural

lebova, Kotlasyia sp.. Raphanodon sp., Scutasaurus

sp., Inostrancevia untlrnsis ’l’atarinoVj Stylaco-

stichus orenhufgeusis Tatarinov, Dicynodon cf.

amalitzkii Suschkin.

Fishes. Jsadia uristovlensis A. Minich, Wodnika

invicta A. Minich.

SUMMARY

AU the Upper Permian scratigraphic uniis from

the Southern Cts-Urals are at présent provided

with rcasonably conipleie paléontologie descrip¬

tion. Their decailcd division was carried out

according co ostracode fauna. The red beds of

rhe Ufimian stage are characterized by a non-

marine ostracode complex doininatcd by repré¬

sentatives Paleodarwïnula genus. Within the

sections with the Kazanian nurine and continen¬

tal deposits, the marine-rock sequences are cha-

racterized by rîch marine-ostracode complexes of

Healdia^ Bairdui. Ajnpbissitts-, etc.» généra. The

non-marine Iwzanian deposits conrain a single

complex of non-marine oscracodes, mainly of

Pideod^irwhmLi and Darwinuloidcs généra.

The most detailed stage division by ostracodes

was carried out for the Tatariaitv with the

Urzhum, Norrh Dvina and Vyatka horizons

clearly distinguished by the ratios of cerrain spe-

cies and généra. The Urzhum horizon ts defined

by rhe combination of PaleodarwinitLi species

and abundant Prasuchonellax the North Dvina

one by domination of SuchoneUina and

PrasuchanclUiy the V'^yatkian horizon by origina-

non of new genera; WjatkellifKK Dvinella and

Suchonella.

The peculiarities of ostracode complex distribu¬

tions revealed in the Cis-Ural Deflecrion, are sus-

tained ail over the Russian Plate (Molosrovskaya

1993) for detailed corrélations within vast terri-

tories from rhe boréal régions to the northern

fringes of the Tethys.

The présence of peculiar endemic cytherid com-

plcx in the south-east of Cis-Ural Marginal

Deflection may point to a possible link between

this territory and the Tethys marine plain in the

Tatarian âge.

Thorough search for ostracodes in other régions

should be considered a primary task aimed to

distant corrélations.

REFERENCES

Efremov V. A. & Shatkinskaya E. F. 1972. — Spore-

pollen complexes within the Ufimian rocks from

the Sulmydi dblucaiion zone in the Orenburg Cis-

Uiais. (ieahigy pwhleTm (d d?e South Urab and Volga

Saiaiov Universily Publication, Sth issue:

l-ir> [in Ku-ssianJ.

Kocherkova N. M. 1970. — Smuigraphy /wd Oitra-

codt^ vf thr (Ippn Permian beds fivm îhc souihern

)'egwns bashkoia and the adjacent areas of Qren-

burg région. Nedra, Moscow, 118 p. |in RussianJ.

Kuleva C. V. 1975. — Ihc Upper Kazanzan and

Tatarian continenial deposits fi’om the Southern part

of Cis'-Ural Marginal Deflection (ivithin the

Orenburg and south Baskirhtn Cis-Unds). Saraiov

Ihiivosity Publication, Saratov, 1^4 p. [in Russianj.

Molostovsky E. A. & Molostovskaya 1. 1. 1967. —

Stratigraphy the Upper Kùz:^nian and Lower

l’atarian dcposiK from tnc Sillmysh zortc. Geohgy

problems of the South Urals and Vfdga Région^

Saratov Universitv Publication, 4th issue part 1:

35-42 [in Russi.tnf.

Molo.s[ovskaya I. I. 1974. —The Lower l'atarlan

ostracodes from the upstream .Samara River basin

und iheir stratigraphie importance. Geology pro-

blenot of the South Ufuls and Volga Reghnu Saratov

LJniversity Piifaliciuion: 53-58 |in Russian].

— 1993- — Non-marine osiracodcïi and paleobiogeo-

gr.iphical distribution of the Late Permian basins in

the Easi of Russian Plare. Coniribuiion to Eurasia

Cieology. Assosional PubUcniioiis F.SRJ New Sériés,

Universit)' South Caroline No.9B: 95-100.

— in prtss. — New Late l^etmian ostracods from the

Cis-Ural. Report of Russian Academy ofScience.

Ochev V. G., Tverdokhicbova G. I., Minikli M. G. &

Minlkh A. V. 1979. — Stratigraphie and p-alcogeo-

graphie iniporiance of the LJpper Permian and

Triassic verrebrarcs Irom the East-European

PJatform nnd Cis-Urals. Saratov L'niver.sity

Publication. Saratov, 81 p. [in Russianl.

Romanov V- V. 1972. — To the stratigraphie subdi¬

vision of the Early Kazanian marine beds from the

bordering platform part of the Orenburg Cis-Urals.

(.Tt'ology problems of the South Urals and Volga

Rvg^on^ Saratov Llniversity Publication, 8rh i.ssuc:

17-30 [in Russian].

^ubmittedfor publication on 15 Janiiary ]996\

accepted on î Octoher 1996.

GEODIVERSITAS • 1997 • 19(2)

259

Depositional conditions in the Southern

Cis-Urals basin during Late Permian

(biostratigraphic, lithofacies and

petromagnetic data)

Edward A. MOLOSTOVSKY & Ijia I. MOLOSTOVSKAYA

Instftute of Geology, Saratov State University.

Moskovskaya Street, 161,410750 Saratov (Russie)

Sylvie CRASQUIN-SOLEAU

CNRS, UPMC, Département de Géologie sédimentaire, case 104,

4 place Jussieu, F-75252 Paris cedex 05 (France)

Molostovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S. 1997. — Depositional condi¬

tions in the Southern Cis-Urals basin during Late Permian {biostratigraphic, lithofacies and

petromagnetic data), in Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigraphie

corrélations, Geodiversitas 19 (2) : 261 -278,

KEYWORDS

Upper Permian,

Cis-Ürals,

Riisskn Platfbi m,

Peri-Caspian Dépréssion,

biosiraiigrapby,

petromagnetLsm,

paleogeography.

ABSTRACT

This paper conrains ihc rcsult.s of the analysis of the Late Permian depositio¬

nal environments in the Southern Cis-Urals, The work is based on the data

of several terms of référencé sections, Thicknesses, faciès and organic remains

contens of the sédiments were studied showing ihc régional stratigraphie

boundaries caused by events of géologie and géographie histor}' of the région.

The main evenis of the géologie histor)^ were conncctcd wiih ihc develop-

mental pecularity of three contacted tcctonic structures, i.e. the Ural

Mountains, the ntarginal pan of the Russian platform and the Peri-Caspian

Dépréssion.

MOTS CLÉS

Permien supérieur,

Cis-Oural,

Plate-forme Russe,

Dépre.ssion Peri-Caspienne,

hioscratigraphic,

pétromagnéiiîuine,

pùléogéogldpliie.

RÉSUMÉ

Les résultats de l’analyse des paléoenvironnements de dépôts dans le sud du

Cis-Oural au Permien supérieur sont présentés ici. Ce travail est fondé sur les

données de plusieurs dizaines de coupes de références. Les épaisseurs, faciès er

contenu paléontologique mettent en évidence des limites correspondant à des

événements de l’histoire géologique et géographique de la région. Les princi¬

paux cvcneinents sont en connexion avec le développement des trois grandes

unilé.s tectoniques encadram la région : l'Oural, la bordure de la Plate-forme

Russe et la Dépression Pen-Caspienne.

GEODIVERSITAS • 1997 • 19(2)

261

Molostovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S.

INTRODUCTION

The South Cis-Ural Région, embracing several

northern districts ot Orenburg région and a part

of souch-western Bashkiria, occupies an area of

about forry thousand square kilometers within

5I°53’30”N and 55-57'^E, rhis rectangular terri¬

torial deiachmeni is limired by ihe Ural

Mountains to the east and che Salmysh River val¬

ley CO the West, its northern boundary is conven-

tionally drawn along the Salavar Kitirude, and the

Southern one along the Sol-Ilecsk latitude.

The région is of spécial gcological interest, since

it represents a complicated tectonic )uncnon, a

meeting point of several major structures: the

south-easrem ffinge of the Russian Plarform, the

CLs-Ural Marginal DcfIcction. the Uralfolds area

and the Peri-Caspian Dépression (Fig. 1),

The morpho-cectonic .structure of the région

developed and rook shape in the l.ate Permian,

in the prpeess oF the Ural geosyricUoe closure at

the final stages of the Hercynian tectonic cycle.

Active orogeny in the Ural Mountains zone,

inception ol the Cis-Ural Marginal Deflection,

epi-orogenic o.scillation.s at the edge of the

Russian Plate and an extensive transgression of

the boréal Kazanian sea, bave determined the

succession of the Laie Permian paleogeograpbic

events not only for the South Cis-Urals but for

the adjacent areas of the Icthys northern tringes

as well.

l'hc major parc of the territory dcscribed is occu-

pied by the Cis-Ural Marginal Deflection filled

with the Upper Permian and L.ower Triassic

red-bed deposics With the underlying Kungurian

sequence. The Southern part of the DcfIcction,

between the Bashkir Arch and the Peri-Caspian

Depressionj is known under the name of the

Belskaya Dépréssion; its eastern border is marked

by the front tidge of the Ural Mountains and the

western one is escablished by the steep sinking of

the Kungurian salt-complex roof. The last phe-

nomenon is clearly recorded by the siib-southern

zone of tsohypse closeness in thé référence elec-

tric horizon (Mavrin 1970* 1979).

The Cis-Ural Maiprul Ücflcciion within the ter-

riiory considered may he divided into the

western, central and eastern zones according to the

structural-facies features of the Upper Permian

red-hed molasse, l'hc boundarics of the structural-

facial zones are indicaicd by two sub-southern

belts of linear ri.ses of che Kungurian halogcnic

sequence marked by sali-dome chains (Fig. 1).

RESEARCH SUBJECT

The paper deals with analyses of Late Permian

Fig. 1. — Main structural éléments of the Southern Cis-Ural.

262

GEODIVERSITAS • 1997 • 19(2)

Depositional conditions during the Late Permian, Southern Urals

depositional settiags in tJie South Cis-Ural

région. The research is based on thc marerials

collected by the authors in thc proccss of gcolo-

gical survcying and thematic palcomagnctic and

biostratigrapliic .studie.s (Molo.srovsky &

Molostovskaya 1967; Molosrovskayn 1974,

1985, 1993). It .SLimmariscs the original data on

several tens of référencé sections and wells, and

the materials of Kotschctkova (1970), Kuleva

(1975, 1979), Tverdokhlebov (ICuIeva &

Tverdoldilebov 1974), Forsh (1955).

Beside lithafàdes and palcontoJogical data, thc

palcogcographic reconstructions itivoJvcd the use

of measurcments of scalar magnctic rock charac-

teristics: natural rcinnaiit magnetism (Jn) and

magneric suscepcihility (æ). The liandamcncals of

magnetometric data interprétation are presented

in detail eisewhere (Molostovsky 1969, 1986); in

essence, the levels of rock magnétisation are

controlled mainly by ferromagneric minera!

concentrations. Sedimentary sequence saturation

wirh tcrrigenou.s magnctic niaterial i.s dircctiy

related to the paleogcographic conditions of sedi-

mencogenesis and with thc gcodynarnic settings

in the source land provinces. In che peculiar set-

lings of thc South Cis-Urals, magnctic paramc-

ters proved ro be a sensitive indicator of the

principal l.atc Permian tectonic speeding up of

the lülded Urals, since the Paleozoic volcanogc-

nie scqucnces of thc Trans-Ucals providcd the

main magnctic-matcrial input to che Cis-Ural

Deflecrion (Molostovsky 1969).

SEDIMENTATION CYCLES

IN THE LATE PERMIAN

Five sedintentation cycles are quiie distinct in the

Lace Permian hiscory of thc South Cis-Urals: die

Ufimian, Early Kazanian, l.ate Kazanian, Early

and Late Tararian oncs. Each of ihcm was caused

by major tectonic and landscapc-climacic

changes, recorded in tlic lithofacies, paleontolo-

gical and petromagnctic characteristics of the

Upper Permian formation compicx.

The UriMIAN SEDIMUN IAI ION CYlXI:

The First stages of che Lace Permian sedimentoge-

nesis coincided with the Kungurian saliferous

basin extinction, related to tectonic movemenc

speeding up within the folded Urals zone and

with che input of significant amounts of fresh

water and terrigenous materials.

Strong magnétisation of the Ufimian deposits in

the eastern zone of the marginal deflection indi-

cates that dénudation bas affected the Paleozoic

volcanites tn the eastern zone of the folded Urals,

and that the Bciskaya Dépression existed as a

négative morphostructure as early a? in thc

beginning nf the Late Permian.

In the platlorm part of the South Cis-Urals, thc

Eacly LJfimian sédimentation rock place under

the conditions of a shallow rcsidual basin with an

unstablc sait régime. In ihc Orenburg district,

within thc zone of thc Salmysh riscs, accumula¬

tion of red-hed sdtites and sandstones started,

alternaring with evaporites-gypsums, dolomites,

dolomitised maris and limestones,

A.s the post-Kungurian réservoir was gradunlly

freshening, and the lacustrine-alluvial plain was

being formed, che Orenburg Cis-Urals hâve

becomc lhe area for lerrigenoiis continental sédi¬

mentation which hroughc about a red-bed silf-

sandstonc sequence about 100-150 m thick. The

principal structure pccuHaritics of thc Southern

type Ufimian section arc recorded in numerous

ourcrops :9nd wclls.

To thc norch of thc région considered, within thc

Ba.shkir Cis-Ural.s, saliferous basin relicrs were

preserved in the firsl stages of thc Ufimian sedi-

inentation cycle. Dolomites, dolomitised liines-

tones, gy()sums and anhydrites were srill

accumulating inccnsivcly enough; their grey-

colourcd sequence is rccognised as ihc Solikanrsk

horizon (Kochetkova 1970). In the second half

of thc Ufimian âge, thc palcogcographic serting

wa.s gtadually adjusting and thc led-bed Sheshma

horizon from Southern Bashkiriu is idcntical to

che corresponding deposits from the Orenburg

Cis-Lkals in its liihofacics features.

Aquatic biota is teptesented by non-marine

ostracodes, bivalves and rare conchostracans. The

most rich biocoenoses are associaied with the

upper hait ut the section. Among ostracodes,

chose of the généra Paleodarwinula and

Prasnchonellii arc thc most conimon, Darivinu-

loides and Sinusuella are less abundanc. Oscracode

biocoenoses are characterized by rather large den-

GEODIVERSITAS • 1997 • 19 (2)

263

Molostovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S.

51 ®

55 ® 57 ®

264

GEODIVERSITAS • 1997 • 19(2)

Depositional conditions during the Late Permian, Southern Urals

sicies and extents. Clayey or carbonate silts served

as biotopes for rhcm. Bivalves arc represented by

rhe species of Palaemuieta and Palaeunodonta

genus. Their rare localities arc associalcd with

clay incerlayers.

The firsr plastic deformations of the hydroche-

mical sequencc and origination ot the salt-dome

rises in the marginal deflcction bcgan with the

Ufimian tectonic activation. An opinion exi.sts,

chat rhe principal diapirism processcs in the

South Cis-LJrals are associated with the

Early/Middle Triassic boundary (Gar)'ainov et al.

1973). Nevertheless. analyses of the Upper

Permian marine tacies spatial distributions show

that as early as the beginning of the Kazanian

âge, many s,ilt dômes, as well as anticÜne struc¬

tures of rhe Salmysii zone, were clearly expressed

as positive lorms of the ancient landscape.

The e-\rlv Ka/anian cycle

Since the beginning of the Kazanian boréal sca

tran.sgre.ssion, a predominantly terrigenous sédi¬

mentation régime was established in the Cis-Urals,

under the shelf-zone conditions tji an extensive

basin with its central part in the Volga région and

in the north of'European Russia (l'orsh 1955).

Fig. 2. — Location of ihe Upper Permian sections In south-east

of the Russian plate and Cis-Ural Deflection. a. natural section;

b. well: c, structural limits of Cis-Ural Deflection; d, limit of Peri-

Caspian Dépréssion- Others symbols of legend in figure 6.

Sections numbers 1, Nnvo-Kandi^iimvkn (the Ohrtku$hu - The

Sukhalya River tnbulary), 2, Korneyevka. the Sukhalya River; 3.

Yumaty, the Sukhaiyâ River: 4. Yalchikayovo. tho Shaitanka

River 5, well 10<t. Byelo^yO'ka, lhe Salmyah River; 6

Karmalka. lhe Salmyeh river, 7, well Peitovka: 8. well ï22,

Verkhni GurDbet: 9, weti 123. Voskresenskoye, 10, well

the Sheslirnir Rivor; 11, well 12®'- lhe Shesfimir River; 12,

Niehni Babalnr; 13. weK Yangiz, 14, lhe SheetimiV River;

15, well 152^*, Maiyevka, lhe Saimysh River. 10, well

Maryevka; 17, Brody Spnng: IB. well 3, Brody; 19. well 43'',

Tiryak Lizyak 20. well 48^ Slrtl» farm Qklyabifikii; 21, well 65.

Budyonnovskii: 22, well S2^, Arvatolyevka. the Saimysh River;

23, well 2''. Sakmara. 24, weu 1**, SakmarA. 2B, well 3i\

Grebani: 26. Kraeny Guliy. Gr«rj*^ni. 27, 5''. Grebeni: 28. wel) 'A.

Grebeni. 29, wtfll 39N Grebont; 30. well 6\ Chebenki; 31,

well 30. NezhonKA: 32. urenburQ 33, well 70L Holfrhoj Sulak;

34 well 94*', BolRhoj Sulak 35. well 00. Ozhuan-TyubinsKaya:

36, well 79''. Ôzhuari-TvubmsKayb: 37. wall 9fcP. Karavanny: 38,

well 59*. Boyevaya Ml,; 39. well SO, Boyevaya M» ; 40. well 53'.

BoyGvâya Mt. 41, wells 81^-67''. Kta^inoyarks, 42. well TSE

Kamennaya; 43. Yelshanka. 44, KorneywvKa, Iho Yarykly River;

45. Yeldaahevo. the Yurgar.hka Kivor; 46. SkvorchiKha, the

Yergabusha River, 47 O^lpovk^ ttie BMÇlenya, 4$, Karaiglka,

the Teiryuk River; 49. Rodnikovsk. the Teiryuk River; 50.

Verkhotor, the Tor River: 51. Voskresenskoye, the Tor River;

The transgression procceded in a rclacively calrn

hydi'odynamic setting with graduai change of

continental and marine sériés. With graduai

basin deepening, formation of a grey-bed

sequence began, con-sisting of pyrirized clays and

■siliites with .subordinare sandstone interlayers

and solitary thin layers of limestones,

Grcai abundance of thinly dispetsed plant orga-

nics and a .stagnant hydrodynamic régime within

subaquatic cfepre.ssion.s favoured rhe formation of

a rcducing environment with pronounced hydro-

gen sulphide contamination.

Bottoni water gcochcmiscry caused lhe impoverî-

shed biocoeno.se.s in the lower horizons of the

Kazanian srage; rhose are mainly represented by

small-si/ed thin-W'^alled brachiopods of the genus

Lingula.

The Kazanian transgression maximum was

accompanied by a general normalisation of rhe

hydrochcmical régime, firsi of ail, in rhe elevared

areas of the sea-bouom. It was rhere, in the w'ell-

aerated, clcan shoal sites, ihat organogenic-clascic

limcstones started to accumulate, with diverse

and rich communities of brachiopods, hryo-

zoanS, algae, corals, crinoids, forarninifers and

ostracodes.

52, Vesyoiy. the Nugush River; 53, Krasoogorka. the Nugush

River: 54. Lipovka: 55. Alexandrovka. the Nugush River; 56,

Yumaguzino, the Meleuz; 57, Kadyrovo, the Menyu River; 58,

Malakanovo: 59, Sergeyevski], the Chukur, Bulyak River, the

Bpishuj Yuâliaïuf Ifibütary. 60, CherntgovsKij; 61, Sekechevo.

lhe NaKuz River: 62. SavelyevsKij. 63, SankinskiJ: 64.

Raznomaikti. lhe Tugosiemir River- 65, Slavyanka, 66,

AHaberdino, 67. Davioikuiovo. the Yaman-Vushatyr River; 68.

well 28 and well 43. Davletkulovo; 69, îhe Tashia River; 70.

Alexandrovka, lhe- Kupiya River; 71. Urman^Tashla, 72,

Kasteiin&kij. ihe Bùiijhoi Yushator River basin. 73. Masiovskij.

lhe Bolghoi Yuyhalur River basin: 74. Smfrnovka: 75.

Alebastrovaya. 76, Che'-epanovka. tho Bcrunchar Hiver; 77

well 41. Sîaroseika, the Bolfthoi Ik Rivet, 78. ‘Sia/Odeika: 79.

Dmitriyevskij; 80. well 4- and 6'. Dmithyevskii; Bt. Stary Kaztair.

the Chena River; 82. NovofiyolUt. the Chena Rlv^r. 83,

Kholmogory. the Rolehbi IK Hiver; 84, NovoKufchumovo, tho

Sakmara River; 85, wol! 121. Novokulchumovo; 86, Vyazovka.

the Ural River; 87 well 102. Vyaznvka 88. well

Ostrûvnoye, lhe Ufdi River: 89, Blumeriiai OuHy. tho Burtyu

river, T, ; 90. Zlioltoyo, ihc Sakmara River 91. Giryal, tho Ural

River; 92. well 73, Activny: 93. wel' 44, Verhhnpûzernoye. the

Ural Rivoi’, 94. VefkhtieOîenioye, 95. wellô' profile -'5-22. the

Burly-i River; 96. 97. 98, Tyatt-r River. 99, 100,1he Net River;

101. Zildyarovo (Forsh 1955): ï02. Artyyokhovko (Forsh 1955),

103 109, the noriheiM-pfofila wells of tho '’RuyuruwIariheflT trust

(Forsh 1955). 1l0. Fyodorovka (Forsh 1255); Hî. Kardaly

(Forsh 1955): 112, Shaktyr (Forsh 1955).

GEODIVERSITAS • 1997 • 19(2)

265

Molostovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S.

Brachiopods arc rcprcscnted by thc généra

Cleiothyridiha, StepaNoviella^ Caricrinella,

Ucharewia, Dieldsnuu Becchcria, Aulosteges.

Foraminifers, by Hypcr(vnmi}ui^ Glomospira,

Ammodiscus, Coruuapim, CakitomeUa^ Nodouwa,

Pseudonodosariii, frondkularitu Geinitzhm, etc.

Ostracodcs, by Healdhi^ CavcUhia, Bairdiûy

Acttiar'my Acratith Amphhntes, Moorea, Pseudo-

pamparchitcSy Momceratinay FiUcianetLi, etc.

Calcarcous silis and lüncstoncs were deposited in

local dépréssions during chat period.

The claycy-siltites and limestone rnembers corn-

bined constitvite thc transgressive parc of thc

marine séries chat maintains irs structure within

the wholc ot thc South Cis-Urals région. The

peculiaritics of thc spatial distribution of thc

transgressive rhythm fiicies are presented in the

schemc (Fig. 3).

In the north-western part of the région, in the

Lipper reaches of thc Salmysh River and in ihc

basins ol the lyater and Ashkadar Rivers, the

Lower Kazanian sequence is represented by a

complicared inter layering of clays, siltites, sand-

stoncs and ümestnnes.

Siltites and clays dominate in the section to the

South, d'he lirncsionc mcnibcr is présent every-

where, but its ihickness changes rapidly from 1-2

to 7-12 m.

The transgressive scrics sédiments arc up to

90-100 m thick in the north-western paît of rhe

région; the rhickness decreases to 50-60 m regu-

larly to the souih and to the east.

The Kazanian sea regeession wa.s accompanied by

rapid shallowing of the easiern shelf, where a

member of grey-coloured cross-bedded sand-

stoncs and sandy siltite.s was formed> completing

the section of the Kazanian marine deposits.

In the western part of the deflection, marine

sédimentation procccdcd under the same condi¬

tions as in the adjatenr régions of thc plarform;

this is shown by the unitorm faciès sequencc

within sri'atigraphic sections.

The exrreme [loitit where marine formations are

established wiiliin thc deflection is located on the

eastern flank of thc Dzhuvan-Tyubinskoye rise

(E-SE of Orenhurg), close to the western

salt-dome range (Fig. 3, No. 36). This rise-

system was probably controling the position of

ilic Kazanian sca shore-line during its maximum

transgression.

A terrigenous sédimentation régime under the

conditions of a brackish-water basin was cstabli-

shed in thc central part of thc deflection at the

bcginning of thc Kazanian âge. Marine faciès

analogues are represented by a sequencc of

dark'grey stitices, clays and flne-grained sand-

stones, saturated with disperscd plant détritus

(Fig. 3» No. 87, 88).

Non-manne ostracodes, PaleodarwtfHih and

Darwifiuhid^rs, occur within diem, as well as thc

Bclebej complex bivalves {Palacomutela and

Palaeanodorna) and a spore-pollen complex* ana-

logous to the Early Kazanian marine-bed palyno-

complex in its composition.

The cascern part of the deflection at the begin-

ning of the Kazanian âge has become an active

homogenic sédimentation zone; the produers of

this sédimentation are traced within a narrow

(10-12 km) piedmont baiid over moie than

100 km, from rhe Tashia river in rhe south to the

Tor and Nugush rivers close to thc northern

extremes ol the Bciskaya Dépréssion (Fig. 3,

No. 51, M). Dolomites, dolomitiscd Ümestones

and maris, and, to a lesser extent, grcv-coloured

clays and siltircs wcrc accurnularing there.

Siltiric-claycy scdiincm bccanie dominant in the

section whilc thc basin was giadually freslienlng

and thc terrigenous drift became more intensive.

Ostracüde and mollusc biocoenose.s arc concen-

rrated within rhe upper, Icss niiiicialised luirizons

of lhe lagoonal sequencc. rhey are represented

by brackish-water spccics of Danvitudouich and

Pnlcodarwinulns common for the whole of the

Kazanian stage: thaï is why corrélation ol' these

faciès to marine deposits from the western

régions is established from palynologie data

(Kuleva 1975). The whole of thc 150 m thick

lagoonal sequencc, irrespecüve ol iis rock-com¬

positions, i.s distinguislicd for exiremcly low

magnétisation (Jn = 0.5-1.5 X 10^ A/m,

æ = 214 X 10 SI uniis). The lack of imgnetic

maicrial in the sédiments shows that thc lagoon

was completely isolatcd by thc surrounding salt-

domc vises. The terrigenous drift was tarer on

accomplishcd at ihc expense of baring of rhe

Lower Permian and Carboniferous weakly

magnetised terrigenous and carbonate scquences

266

GEODIVERSITAS • 1997 • 19(2)

Molostovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S.

from thc western slopes of the Urals.

No lagoonal facics hâve been reliably revealed in

the Southern part of the eastern /one, and the

Lower Kazatiian substage was ihought to com¬

prise the grey-coloured sequence of alluvial-del-

taic sandstones and siltites with rare clay and

mari interlayers, coniaining the remains of fresh-

water bivalves and land vertebrates (Kuleva 6c

Tverdokhlebov 1974).

The late Ka/anian sedimfn i ai jun cycle

The middie of the Kazanian âge represented a

turning point in the South Cis-Urals géologie

history. A continental sedimentanon régime has

finally estabhshed iiself in the région as the resuit

of the Urals tcctonic acrit^aiion and the Boréal

Sea régression towards the centre of the Russian

Plate.

rhe Cis-Ural Dcflcction and the adjacent

régions of the Platform hâve changed inro an

extensive .iccumulative plain with a complicated

combination of basin, lagoonal, lacustrîne and

alluvial-proluvial lacies; both Southern and lati-

tudinal zonings were évident in theii spatial dis¬

tributions (Fig- 4). In the souih, within the Ural

and Salmysh Ri vers Basins, b.isinal rerrigenous

sédimentation has eAtahlishcd itseK, and a mono-

tonous inrerlaid sequence was accumularing of

siltites, clays and llne-grained sands with single

interlayers ol maris and obliquely-laminaied

polymictic sandstones ot deltaic type. In the

western part of the deflection and in the plat¬

form, mostly red-bed sédiments were dcveloping.

In the South of rhe central zone of rhe deflection,

a sequence was k>rmed of interlayering red-beds

and grey rocks.

The principal portion of rhe deflection central

zone was occupied by a lacustrinc-alluvial plain,

accumulating a complcx of rcd-coloured alcuro-

pclitic deposirs with subordinate interlayers of

fine-graincd sands and clayey limcsfones. A limi-

ted amount of sandy-conglomerate faciès of

channel alluvium is represenred in the section.

The northern régions, embrating the Nugush,

Belaya and Dyorna basins, were occupied by a

major interior réservoir with increa.sed minérali¬

sation; it was limited with a number of sait

dômes from the south. An interlayering sequence

of siltites, clays, limestones and maris has accu-

tnulated within it. Sulphaies were precipiiaiing

at some sites (Kochetkova 1970).

A narrow piedmont band along the eastern bor¬

der of the deflection comprised an alluvial-prolu-

vial plain, where the principal part of che

sandy-pebhie material carried Irom the mountain

Urals was deposited (Kuleva 6i Tverdokhlebov

1974).

The beginning of the Late Kazanian sédimenta¬

tion cycle is clearly recorded in the section from

rhe central and eastern zones of the deflection by

sharp incrcases of rock scalar magnetic characte-

ristics. At this houndary, the Jn and æ values

increase up to 0.1-0.2 A/m and 300-^00 x

10"^ SI unies, respeaivcly. The very character of

the section pctromagnctic in homogcncity icsti-

fies 10 a volley éjection of grcai amounts of lerri-

genous material from the Urals eastern slopes

(Fig. 7).

Diverse sédimentation seiriiigs in che Cis-Urals

bave affecred the structure of rhe Lite Kazanian

aquatic biota, which is di.stinguisheJ for Its spe-

cies diversiiy, being relatively lirniicd in tlie num-

her of généra. Osiracodcs of Pmsut /wr^eUd genus

dominaied in the aleuro-pelitic grounds in the

zones of mobile hydro-dynamics and sulphate

minéralisation of waters. Calcareous and calca-

reo-dolnmiric grounds served as an ccological

niche for stenofacial Darwinulmdes. The dayey-

calcareoiis lithofacie.s were occupied by

Paleodarwimda and Prasuchonclla. Ptileodiinvi-

nulîi proved to be the only oncs to adapi chem-

selvcs to the non-carbonate silty grounds.

Widely occurring bivalves .ire represented by the

brackish-water species of Palneomuttla and

PnLieonodofttn, whicli possessed thin-wiilled shells

and preferred the silty sédiments of hydtodyna-

mically calm zones (Kuleva 1975, 1979).

Bcside oscracodes and bivalves, few conchostra-

cans and Rsh were présent in the aquatic bio¬

topes. Swamp Coastal plains seived as habitats for

terresrrial plants and tetrapods.

Tim KARIY TAIAKIAN Si niMENTAHON O'Cl.F

The early Tararian paleogeographic setting was

determincd by tectonic aciivity in the wholc of

the South Cis-Urals.

In the western part of the région, the deposits,

assigned to the lowermost of che Tatarian, were

268

GEODIVERSITAS • 1997 • 19 (2)

GEODIVERSITAS • 1997 • 19(2)

Molostovsky E. A., Molostovskaya I. I. èc Crasquin-Soleau S.

being formed in ihe inherited Ute Kazanian

réservoirs with increased minéralisation. Cyp-

sinaces and srones were depositing ihcre (Fig. 4).

High sulphatisation of the réservoirs was adverse-

ly affeccing the organic life development. The

clayey-aleuricic grounds rhcrc were inhabited

only by ostraœdes of Pmsuchomllu genus* some-

tlmes associared wirh rare depressed Palcadmun-

nula. Carbonate sÜts arc associated wirh rhe

1 o c a 1 i t i e s o f Da r w lu ulotdes ische rdl nzcvi

Kashe\'arova^ a n'pical dweller ofhighly minerah-

sed carbonate reserv^oirs with increased magnesia-

liry (Molostovskaya 1974).

The principal cycle of the early Tatarian sédi¬

mentation began with vast alluvial plain develop¬

ment; the plain is traced by a characteristic faciès

set in the form of a Southern band to the south

from the Bashkir Cis-Urals, righr lo rhe town of

Sol-Iletsk. The alluvial sequence is composcd

mostly of cross'iaminared channel sandstones

and pebbles of local rocks, kess common are

red-coloured aleurtî-pelires of the flood plain and

dead-channel facie.s.

In the second half of tbe early latarian cycle, lhe

alluvial sédimentation was changed in the basinal

one; ics products appe.u iii the upper horizons of

rhe section over the sequence of alluvial sands, in

the form of a member of siltite-clayey beds

(Fig. 5, No. 31,36, 42).

Easrwards. rhe lowcr Tatarian alluvial plain rur-

ned into tbe lacustrine-alluvial onc, occupying

the greater part of the central and easrern zones

of the marginal deHcction. A monotonous

sequence ot ced aleuro-pelitic silts was deposited

wirhin it, with interlayers of alluvial sands and

conglomérâtes.

Along the northern fringes of rhe lacustrine

plain, in the basins of the Nugusb, Tor and

Bclaya Rivets, an alluvial-deltaic régime was esta-

blished during the initial stages of the Early

Tatarian sédimentation; this resulted in a thick

(300-400 m) sequence of cros.s laminatcd .sands,

gravelstones and conglomérâtes, l.ater on, a

réservoir with increased water-miueralisation was

lormed irt this territory; pelitic and carbonate

silts were precipitating chere (Kochetkova 1970).

In the eastern llank of the marginal deflection,

the régime of ailuvial-deltaie and proluvial .sédi¬

mentation dominated (Fig. 5, No. 45, 46, 50,

51, 52). Wirhin a narrow piedmont band there,

a major portion of coarse clastic material was

deposited; judging hom its composition, this was

carried from the central and western parts of ihe

mountain Lirais. According to Kuleva &;

TVcrdodolchlcbo (1974), quarrz, Hinis, quart-

zites, Carboniferous and lower Perniian limes-

tones dominated in the lower Tatarian pcbble

stoncs. A slgnificanr parc of the piedmont molasse

consists of the proluvial material with its typical

“rubbish’' horizons, conipri&ing unsorted sands,

pebble stones and aleuro-pelitic sédiments.

Among rhe organism.s, inhabiring rhe early

Tuarian réservoirs, bivalve.s and ostr.tcodes are

the most abundant ones. .Aleuro-pelitic sédi¬

ments of the flood pliiin n pe are associated with

the localiiics of bivalves of rhe Kama and

Chepersk complexes, consisting of ihe

PalnconmieliU Avthraconaht and Pahminodonta

généra représentatives. Osrracode Pakodimoinula

.ind Paleodarwinnlti'Prasnclnmella com muniries

are also associated to tlie sanie faciès.

Fbe .sédimentation secring of an alluvial plain is

chiefly characceriscd by numerous accumulations

o( chick-wallcd shclls of the Doskinsk)' complex.

The t)'pical species of this complex, Antmeonuia

ifci'neuïlt Amalizky, is a r)'pical inhabitant of rhe

channel faciès (Kuleva 1975).

Paleodarwinula arc the most common of ostra-

codes chere.

Highiy minerai iscd carbonate réservoirs provided

rather favourablc conditions for biota develop¬

ment. In the clayey-carbonate rocks there, alga

fragments, fush scales, bivalve and ostracode

shells occur. Ostracodes are most abiindant.

They are represented by diverse communiries;

Diirwin îiloide:^^ Danoiri uloides- Palcodilnvin u la,

Palcodnru'iuulu, Palcodarwinuhi-Pntiuchoitella

and Pmucfmwlla.

The spécifie featurcs of the cbanging palcogeo-

graphic setting are clearly recorded by sealar

perromagnetic cbaracteristics. In the référencé

sections from the central and eastern zones of the

Cis-Urals Deflecrion, the beginning of the Early

Tatarian sédimentation is marked by a sharp

4-5 fold decrcjse in rock magnétisation of

red-bed mc)las.se: to modal a; values 25-30 x

10*^ hl unies with rate ‘"burscs” up to 70-90 x

10'^ SI units (Molostovsky 1969).

270

GEODIVERSITAS • 1997 • 19(2)

Moloscovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S.

In the wstern part of the deflection and in the

adjacent régions of rhe Russian Plate, the diangcs

in the facial scrrings almost dtdn’t affect magnéti¬

sation of the sedimenrs. The basin dcposits of the

Kazanian age and ihe cross-laminaved sandstones

of the lower lacarian alluvial plain are distingui-

shed for cxtrcmely uniform decrcased magnétisa¬

tion with the modal Jn values of 6-9 X 10 -^ A/m

and chose of x - 12-20 x 10^ SI unies (Fig. 7).

The pcculiaricics ol pctrornagnetic section .struc¬

tures show chat in chc period of the early

Tacarian sédimentation, the whole of the South

Cis-Ural terrirory was to a significant extent iso-

iated front the Trans-Ural source provinces. 'Fhc

central and easfern zones of che deflection were

being fîlled with the terrigenous mareri.tl from

the sedimenrary and metamorphic séquences of

the western slopes of die Urals. fhc source lânds

to the western alluvial plain were probably situa-

ted in the norrh, in the regioms of the Tatar and

Bashkir Archbends, where the weakly magnetised

horizons of the sedimenrary cover were exposed

to wash-ouc. Local source centres might originace

within the arch portions of the local rises.

The late Iatarîan sedimen i ai ii')N o'Cle

The late Tatarian scdimciitation was prcccdcd by

the lirais ascending motions. I his rising has pro¬

bably involved the Salmvsh Bar zone, characteri-

zed by the absence of the upper l*atarian

deposits. Stable accumulation was pre.served only

within the deflection enclosing the marginal

zone of a large cpicontincntal basin territorially

connected wûrh che Pcri-Caspian Dépréssion.

The non uiiiform hydrochcmical sctlings in lhe

réservoir have predetermined the .Southern

zoning in îts tacics spatial distribution.

Its western part, the most spread onc, lias bccoine

a site for terrigenous sédimentation which resul-

ted in a homogennu.s sequence of inrerlayering

red clays, sihire.s and fine-grained .sandstones. The

band of terrigenous accumulations was traced

along more rhan 150 km from the noith to the

.South (from Bashkiria to the town of Sol-Ilcrsk),

but its real extent hasnt been estabjished. This

facial zone i.s limired by a Southern band of the

Kungurian rises and the Cis-Ural Deflection bor¬

der lo the east and to the wesr (Fig. 6: I).

The red-bed sequence acquires a somewhat more

Variegated, poly-componenr composition to che

casi, within the central zone of the deflection.

Siliitcs and clay.^ con.stituLe the sectUms principle

cotnponents there. The arnount of arenaccous

sédiments insignificantly reduccd, thin gravclite

and pebble stone Icnses .ippear, limesronc and

mari interlayers and calcareous eJay members are

encountered with accumulations of carbonate

nodules and concrétions.

Sedimenus carbonate contents increase regularly

from the north ro the south, and maris and

limestones hecome important components of the

sections from che basins of tlie Tor, Nugush and

BcJayâ Rivers (Fig. 6: II).

The conditions of the upper Fatarian sequence

formation within chc central part of die deflec¬

tion arc* analysed in detail hy Botvinkina and

"FverdoKfilebov. Botvinkina (1962) reconstructs

the hydrodynainic settings of the large marine-

type basin. In Kuleva & Tverdoldilebov schenies

(1974), this terriior}' is assigned to a lacusirine-

swanip plain with the accumulation level cluse to

zéro,

Significant dcposic thicknesses (> 500 m), fo.ssil-

remains compositions, numerous intra-formatio-

nal gaps testify to dynamic hydrogcologic régime

o( sedinieruaiiori aguinst the hackground of

intensive basin-flour deflection. Tins data more

likcly conibrms to the hypothesis of a large réser¬

voir penetrating inro the low land as narrow

intrusive tongues> and reaching distant northern

areas, riglit rn the pencünal closiire of the Belaya

dépréssion

In rhe eastern piedmont flank of che marginal

deflection, similar to the early ‘latarian rime, a

narrow alUiviaLproltivial plain w'as situated, eut

hy permanent and remporary warer flows.

Numerous fans are formed within ir, çonsisting

of sandy, houlder-pehble and gravel marerials.

l.imesroncs, flints, quartzîtcs and variously com-

posed eff'usives occur among dasts (Fig. 6: J II).

The upper Tacarian dcposits arc distingutshed for

diverse pecromugnetic chatacterLsiics with some

certain ordcring in their .spatial distributions.

Fhe pcliiiic arenaccous sédiments from the west¬

ern facial zone arc marked with w'eak uniform

magnétisation and arc practically idenrical ro rhe

lower and upper Fatarlan Ibrniarion.s in Jn and

æ values.

272

GEODIVERSITAS • 1997 • 19(2)

Molostovsky E. A., Molostovskaya 1.1. & Crasquin-Soleau S.

In the ea,srern and central ^nes of rhe dcflection,

the sequences are distinguished for excremely

high non uniform magnétisations with Jn and

æ vaiuCsS of tens and hundreds of SI unies. A

sharp change of vveakiy- and strongly-magnecisa-

tion sequences is recorded wirhin the wells of the

profile 9S (the Burlya River basin); the level of

this change is practically coïncident with the

lower/uppcr Tatarian boundan' (Fig. 7).

The petromagnetic data comparison makes it

évident thaï the laie Tatarian sédimentation was

accompanied by the change of the source lands

and that the central part of the deflection was

still a kind ot an accumulative bath, receiving

practically ail the nugnetic marçrials carried in

from the greenstone heli of the easrern Lirais

rhe ecological setting was favourable for the

development of a rich and diverse aquatic biora.

On the claycy-alcuritic grounds within the zones

of relatively calm hydrodynamic settings,

thin-shelled bivalves of the Vyazovsky and Olcsky

complexes resided, represented by Palaeoinutela,

Palaeanodonta and Anthraconaia généra. The

Coastal zones with moderately active hydrodyna-

miçs wcrc occupied by the Severodvinsky com-

p|cx bivalves^ including Palaeomutela^

Piil-aeanodonla, Oligodontelht and OpakielLi géné¬

ra (Küleva 197>).

Multiple and variously composed ostracode com-

munirîes were distribiited over clâyey-alcurltic

and carbonate grounds. The eury-facies

Stidwndlina dominared in the late Tatarian bio¬

topes, formjng independenc commünities there

or associated with Sucho}ielIa, Dvinella,

\X'jatkinelb and CcrdixUa (Molostovskayâ 1993).

The steno-facics Sifmsuella^ Perrniana and

Pladdea were usually localiscd within the bot-

fom-water zones of incrcascd carbonate mincrali-

satïon. Their rare localirics arc associated with

marl-carbonare layers,

In the eastern zone of the deflection, an ostraco¬

de association was formed, consisting of rhe

représentatives of SucbonelUnn, Suchnnella and

numeroiis small endemie Cythcracopina, posses-

sing little, elongaced, sculptured shells. In their

morphologie features, the latter ones are close to

WESTERN ZONE

CENTRAL ZONE EASTERN ZONE

B4l

Fig. 7. — Petromagnetic curves of the Upper Permian deposits in CIs-Ural Deflection. 1, Krasny Ravine: 2, weil 31^ Grebeni; 3,

Shestimir River; 4, Sakmara; 5, Brody; 6, Yelshanka; 7, Blumental: 8, Davieikulova, Yaman-Yushatyr River; 9. Sergeevsky; 10,

Vyazoka; 11, Novokutchumova; 12, Bekecheva, Nakyz River; 13, Nugush River; 14, well profite 22, Burty River.

274

GEODIVERSITAS • 1997 • 19(2)

Depositional conditions during the Late Permian, Southern Urals

rhe Triassic Cyrhcrocopina from ihe Peri-Caspian

Dcpressioa, but difFer subscatitially from the

upper Permiaa C}^herocopiaa from the Rus-sian

Plate. This spccilic complex \s territorially limi-

ted within a narrow piedmont band of die mar¬

ginal deflection, traced from the south to rhe

north for over 200 kin (from rfie Burlya River to

rhe basins of the Tor and Nugudi Rivers).

Conchostracans, gastropods, Spirorhis worms

and algae were comnion, but not numerous

in habitants of the Taiarian réservoirs; thcir fossi-

lised remains are also conccntratcd in clayey-car-

bonate rocks.

The marsh-ridden Coastal areas of the low land

served as an ecological niche flir small tetrapods.

Considering various aspects ol rhe l.ate Permian

paleogeography ol (lie South Cis-Urals, il is a

matter of principle to réalisé the cxtent this

rarher peculiar local région was related with tfie

Tcrhys northeru fringcs during its évolution.

Spatially and siructurally, rhe Southern part of

ihe Cis-Ural Marginal Dcflectjon is continuous

with the castern part of rhe Peri-Caspian

Dépréssion. It is natural that corrélations of stra¬

tigraphie sections and lithofacies features of the

Upper Permian deposiis from chese régions pré¬

sent a spécial interest.

The detailed information on die structure of the

Upper Permian formation from the Peri-Caspian

Depre.ssion is given in the papers of Movshovich

(1977), VainbluL (1969) and Zamareiiov et al.

(1969). A comparative analysi.s of the data on the

South Cis-UraU and the Eastern Cis-Caspian

reveais significant section similarines lithology,

chronological succession of faciès, stratigraphie

boLindaries characrer and bionomie characteris-

tics. These similarities are especially évident for

the Kazaniaii and Tatarian stages.

Within the Cis-Ural Deflccnon, as well as in the

eastern Cis-Caspian région, the Kazanian stage is

represented by non-mari ne brackish-water faciès

with terrigenous compositions. In rhe lower por¬

tion of the section, grey-coloured argilüres and

siltites dominare, sarurated with thinly dispersed

plant détritus and authigenîc iron .sulphides.

rhe upper Kazanian substage Ls cverywhetc

represented by the séquences of interlaid grey-

and red-coloured rocks with the laiier ones clearly

dominating. Vainblat (1969) and Zamarenov et al.

(1969) suppose that the Kazanian sédimentation

took place within extensive shallow-watei* réser¬

voirs, experiencitig hydrostatic liead from the

boréal basin at various stages. Lagoonal and deltaic

sédimentation proceeded in individual sites.

The Tatarian stage from ihe eastern Cis-Caspian,

as well as from the Cis-Urals, is represented by a

red-coloured complicated structured terrigenous

sequence, comprising variously rationcd alterna¬

tions of argiilite and aleuro-psammite beds with

rare limcstone interlayers.

'l'he total numbers of the Upper Permian sedi-

mentanon c\xlcs in both régions arc idendcal; it

is significant, that ail the stage and substage

boundarics arc nvarked with stratigraphie, and in

the Cis-Caspian by angalar disconianecs.

d he peculiarity of the Upper Permian deposits

fr<jm the eastern part of the Peri-Ca.spian

Depre.ssion consisis in thcir saturation with

pcbblc-stone maccrial, including tliiits, quartz,

mçtamorphic shalcs and eftusives, t.e. practically

the whole of the typomorphic sec of rocks from

the centra) and eastern Urals.

The Ural niaterial is présent practically ail over rhe

eastern fringe of ihc Peri-Caspian Dépression

(from the Cis-Ural Dcflccdon to the Emba River).

The lithofacies information obtained from

drilling, plays a certain rôle m the long discus¬

sion toctonists hold on the structure of rhe

Cis-Ural Marginal Dcfiection within the

Peri-Caspian Dépréssion. Gorctsky (1972),

Shlezinger (1974) and some other authors advo-

cate the idea of the Cis-Ural Détection passing

into the System of periclinal déficelions f'ringing

the folded Urals from the south and sonth-west-

Movshovich (1977), Mi/inov (1974), Lapkin &

Tomashunas (1966) and orhers provide diverse

arguments in faveur of the idca of an abrupt turn

of the Ural folded System and the Cis-Ural

Dcfiection to the west and thcir jointing the

Karpmsky Ridge and the Cis-Donets marginal

deflection in rhe norrhern Cis-Caspian, between

Gurjevand Astrakhan.

Grcat ahundance ol pebble rnaterial in the south

ol the Peri-Caspian Dépression represent rather

subsfantial arguments in favour of the second

conception.

rhe ring of the lïercynian structures during the

whole of the Late Permian was acting as an effec-

GEODIVERSiTAS • 1997 * 19(2)

275

Molostovsky E. A., Molostovskaya I. 1. & Crasquin-Soleau S.

tive barrier isolating rhc epicontinental

CiS'Caspian basin from rhe Tethys. The

Cis-Caspian géographie isolation from rhe région

of marine sedimeniatioii has affected the structure

of the Upper Perniian biota, which in its ostraco*

de and bivalve composition was very similar to

chose from the Russian Plate and die Cis-Ural

Marginal Defleenon. In the sections from the

Cis-Caspian région, ostracodes are represented

by DanvinuLi^ Dunvinuloides^ Sucho7tella, Sncho-

nellina généra. Among bivalves^ the brackish-

water généra PalacümutAa and Palaeonodonta are

indicated.

Lithologic-facies and paléontologie records tesri-

fy to the auionomoLis development of the epi-

continental Cis-Caspian réservoir in the Lace

Permian and dont provide any more or less sub-

stantial arguments in favour of ks récurrent

connections with the Terhys.

CONCLUSION

The mean features of rhc Lare Permian paleogco-

graphy in the South Cis-Urals wcrc determincd

by the tectonic actlvity of the Ural orogen, and

in the beginning of the Kazanian (by an extensi¬

ve boréal transgression). Eath sédimentation

cycle was preceded by the UraU upÜfting, haring

processes animaiion within the source lands and

régional wash-oucs in accumulation basins,

Consequcntly, the boundaries between the

Upper Permian stratigraphie units arc of cpisodic

character and correspond to ihc initial stages of

sédimentation cycles,

*rhe central and the eastern zones of the marginal

deflection, during the whole of the Late Permian

epoch, existed as a major dépréssion morphostruc¬

ture, accLiniLilating the main portion of the allo-

thigenic material arriving from the région ol the

folded Urals. l’hc wesrern part of the dcflcction,

in its présent configurarion, has a iot in commoii

with rhe adjacent areas of rhc Russian Place in

lithology and rhicknesses, and constitutes a single

structural-facies zone with rhe Plate.

One may suppose rhat rhe western border of the

dcflection in the end of rhe Permian was situared

to the cast of its présent position and ran over

the zone of the Southern Kungurian élévations.

Thus, some migration of the dcflection axis

towards rhe Platform is outlined, which is gene¬

ral ly characterisric of such structures type.

Southern zoning is outlined in the Jithofacies

spatial distribution within tlie marginal deflec-

tion; a sufllcieiu rôle in ihis deflection origina-

tion was played by rhc western and eastern zones

of lincar élévations of the Kungurian halogcnic

sequence. Besides» rhc sub-latitudinal zonalky is

outlined in distrihurion of the evaporiîe and rer-

rigenous faciès; this zonaliry persists at ail the

stages of the Late Permian sedimentogenesis:

from the Ufimian ihrough the laie Tatarian.

The main portion of the sulphate-carhonate

accumulations is concentrated in rhe northern

pan of the région, where a System ui inherited

lagoon-type réservoir is knowii to hâve existed

for a long rime, ’i'hc lerrigcnous sédimentation

in the souchern régions is most logically explai-

ned by an active river discharge and, consequenr-

ly> by accumulation - basins freshening. The

analyses of thickness’es, faciès and organic

remains compositions, demonstrate thaï gener-

ally basin sédimentation régime prevailed in the

South of Cis-Urals, with wide development of

low accumulacivc plains chaructensed by alluvial-

proliivial and lacustrine-swamp sédimentation.

Not wirhsranding peculiar paleogeographic set-

tings, caused by rhe proxirnity of the mountain

lirais, the South Cis-Urals région in its géologie

development was closcly rclatcd both ro the mar¬

ginal part of the Russian Platform and co rhe

Peri-Caspian Dépression,

rhe Cis-Ural Deflecrion reveals a lot of similari-

ties with the eastern part of the Peri-Caspian

Dépréssion in lirholog)', fades set and hiota com¬

position, It used to nepresent jusi a narrow gulf

of an extensive epicontinenial réservoir.

An active material discharge from the Mountain

Urals région constitute.s a peculiar fealure of the

Late Permian sedimentogenesis in the eastern

Cis-Caspian and South Cis-Urals. The Influence

of rhe Urals is revealed ail over the eastern fringes

of the Peri-Caspian Dépréssion: from che Ural

River valley in the north to the Fmba River basin

in the south.

rhc analyses of the data on the upper Permian

deposics from this région show chat the intracon-

tinental basin of the Cis-Caspian in the Late

276

GEODIVERSITAS • 1997 • 19 (2)

Depositional conditions during the Late Permian, Southern Urals

Permian was dcvcloping in an autonomous régime

and didnï hâve any long-term connections with

the Tethys area. T he narural barrier between

them consisred of rhe System of rhe Hercymian

mountain structures of the Urals and Karpinslc}'

Embankment, joining each odier in the zone of

die present-day Caspian aquatorium, in the area

bcnveen die Ural and the Volga mouths This

isolation was brokcn up in the Olenekian âge

and in rhe Middlc Triassic, vvhcn major invasions

of rhe Tethys into the Cis-Caspian région occur-

red. No events of similar scale hâve bccn revealed

in rhe Lare Permian, bue this probletn needs spé¬

cial studying.

Iri this connection, the communities of intricatc-

ly-.sculptured Cytheracea seem rather inreresting;

rhey appeared in the souch of rhe Cis-Ural

Marginal Deflection in rhe second hâlf of the

Tatarian âge. In their morphologie fearures they

arc similar to certain Cytheracea from the

Middlc 'J'riassic Cîs-Caspian complet, which,

according to Lipatova & Srarozhilova (1968), is

analogous to the ostracode complex from the

Middie Triassic of Germany. Very small ostra-

codes with smooth'Valve shells also occur there;

they are morphoJogically similar to Purucypris^

die représentatives of which are common mainly

in seas. Originarivjn centres and movement cracks

of rhese ostracodes are still unknown. They may

prove to be endemic, but one canT rule out ihc

possibility of cheir betng some Southern

migrants, to certain extent associaced with the

marginal part of the Tethys.

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tecionic stages in me .South Ci.s-lJrals devclopmein>

in Morozov L S. (ed.^j Geology problems of the

South iJrak and the Volga région. Saratov University

Publication: 111-124 [in Russian].

Mizinov N. V. 1974. — Prospects of oil and gas

explorations in the subsalt dcposiis of the south-

wesicrn Peri-Caspian Dépréssion. Geologïya nefti i

gaza lOilandgasgeology] 4: 48-50 [in Rus.sianj.

Molosiovsky E. A. 1969. — To ihe use of magnéto-

merrit daui in paiettgeography: the case of the

research of (hc tippec Pertnian and ITiasslc beds

from the Orenburg Cis-Urals, in Vostiyakov A. V.

(ed./l, Geology problems of the South Urals and the

Volgî région. Saratov Universiry Publication, issue

6: 39-49 (in Russiin].

— 1986. — Scalar magnecic charactcristics as indîca-

fors of scdiincnnirton settings: 58-73 [in Russian],

in Sholpo V. (ed.j. Rock magnetisyn usage for géologie

survey. Nedra, Leningrad.

Mülostovsky E. A, ôc Molostovskaya 1. I. 1967. —

Stratigraphy of (lie Upper Kazanian and Lower

Eatarian depo.sits from the Salmysh zone, in

Geology problems of ihe South Urals and Volga

Région. Saratov University Publication, issue 4, part

1: 35-42 [in Russian].

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Molostovskaya 1. 1. 1974. — The Lower Tatarian

ostracodes from the upstream Samara River basin

and their stratigraphie importance, in Geology pro-

blems of the South Urab and Volga Région^ Saratov

University Publication: 53-58 [in Russian].

— 1985. — To the division of the Upper Tatarian

substage from the south-east of the Russian

Platform by ostracodes, in Stratigraphy problems of

the Paleozoic^ Mesozoic and Cenozoicy Saratov

University Publication: A7-57 [in Russian].

— 1993. — Non-marine ostracodes and paleobiogeo-

graphical distribution of the Late Permian basins in

the East of Russian Place. Contribution to Eurasia

Geology. Assosional Publications ESRJ New Sériés,

University South Caroline, No. 9B: 95-100.

Movshovich E. V. 1977- — Paleogeography and paleo

tectonics in the Lower Volga région in the Permian

and Triassic periods. Saratov University Publi¬

cations, 239 p. [in Russian].

Shlezinger A. E. 1974. — Late géosynclinal and early

platjorrn structures in Eurasian Hercynides. Nauka,

Moscow, 223 p. [in Russian].

Vainblac A. B. 1969. — Stratigraphy and lithology of

the Upper Permian deposits from the eastern part

of the Peri-Caspian Dépréssion: 79-87 [in

Russian], in Vinogradov D. (ed.), The

Permo-Triassic of the fiussian Platform and its oil

andgas content. Nedra, Moscow.

Zamarenov A. K., Kukhtinov D. A., Zamarenova

E. N., Alexeyeva V. I. & l’aran L. V. 1969. —

Stratigraphy, lithology and formation settings of

the Upper Permian and Triassic deposits from the

eastern-border margin of the Peri-Caspian Déprés¬

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The Permo-Triassic of the Russian Platform and its

oil andgas content. Nedra, Moscow.

Submittedfor publication on 15 January 1996‘,

accepted on 1 October 1996.

278

GEODIVERSITAS • 1997 • 19(2)

Ichthyofaunal corrélation of the Triassic

deposits from the northern Cis-Caspian

and Southern Cis-Urals régions

Maxim G. MINIKH & Alla V. MINIKH

Saratov State University, Moskovskaya Street, 161,

410750 Saratov (Russia)

Minikh M. G. & Minikh A. V. 1997. — Ichthyofaunal corrélation of the Triassic deposits from

the northern Cis-Ca^ian and Southern Cis-Urals régions, in Crasquin-Soleau S. & De

Wever P. (eds), Peri-Tethys: stratigraphie correiations, Geodtversitas (2) : 279-292.

KEYWORDS

Ichth^fauna,

Triassic.

norrhern Cis-Caspian,

Southern Cis-Urals,

ABSTRACT

AH the known data on rhe Triassic ichthyofauna from south-casr European

Russia are summarized. The matcrial studted cornes From thirry-nine locali-

ties From the Lower and Middle Triassic référencé and stratocype sections oF

the South Cis-Urals and northern Ci.s-Caspian régions. Data on terrestrial

vertebrates, ostracodes, and charae are u.sed as well as paleomagnetic .sam-

pling résilies. A certain stratigraphie importance of the Triassic gnaihorhiza

and ceratods is demonstrated relative to lungfislt, the une of hybodonrid.s

relative to squaliforms and the one of saurichthiid.s among actinopierygians.

Two super-ichthyocomplexcs wero revcaled wirhin the Triassic .sections

according to dipnoan distribuiions: ihose of gnathorhiza and ceratods. Thcir

change in the région occairs in the middle of the Olenekian âge and is asso-

ciated with the rather short Akhtuba rime in the Cis-Caspian and with the

synchronous Eyodorovka tîme in the South Cis-Urals. Considering the data

on other fish groups, threc independent ichthyocomplexes are recognized in

the Trias.sic ichthyofauna: the Vetlugian and Yarenian ones in rhe Early

Triassic and anochcr one in the Middle Triassic. The Yarenian ichthyocom-

plex comprises two clearly manifesced groups of different âges (the Akhtuba

and Bogdo ones in rhe Cis-Caspian and the Eyodorovka and Gamskaya ones

in the South Cis-Urals). The Middle Triassic ichrhyocomplex comprises ihc

Donguz and Bukobuj fish groups. The rcgularities revealed in ffsh-taxa

changes with rime, arc traced wirhin the sections across the adjacent terrico-

ries from the Cis-Urals to the Cis-Caspian. The Lower Triassic Akhtuba

suite from the Cis-Caspian Bogdo section was corrclaced by fish with the

lowermost part of rhe Petropavlovka suite» and the overlying Bogdo .suite

with the re.st of the Pctropavlovka section from the Orenburg région. The

Middle Triassic Donguz and Rukobaj suites from rhe Cis-Urals are srratigra-

phically analogous to the Eicon and Indcr suites from che Middle Eriassic

GEODIVERSITAS • 1997 • 19(2)

279

Minikh M. G. &C Minikh A. V.

section in thc northcm Cis-Ca5pian. The succession reve.iled in rhe Triassic

ichthyofauna development is maintained ail over the icrritory of Ruropean

Russia. U is traced in the adjacent régions and may serve as the basis for stra¬

tigraphie divisions and interregional corrélations of different-tacies marine

and non-marine sections of rhe Tri;tssic-

MOTS CLÉS

Ichthyofaune,

Trias.

nord Cis Caspienne,

sud Cis Oural.

RÉSUMÉ

Toutes les données connues sur Tichthyofaune triasique du SE de la Russie

européenne sont compilées. Le matériel étudié provient de trente-neuf locali¬

tés des coupes de références et stratotypiques du Trias inférieur et moyen du

sud du Cis-Oural et du nord de la Cis-Caspicnnc. Les données sur les verté¬

brés terrestres, les ostracodes. les characées sont urilLsées aussi bien que les

résultats palcojnagnéiiques. Deux supet-ichthyocomplexes sont mis en évi¬

dence dans les coupas du TruivS. Leur changement dans la régii>n se produit

au milieu de rOIcnekien. il est rattaché à l’intervalle court de Akhtuba dans

la région de la Cis-Caspicntïc cr à l'intei'valle synchrone de 1 yodorov^ka dans

la région du Sud du Cîs-OuraL Considérant les données des autres groupes

de poissons, trois itlilhyocomplcxes indépendants sont reconnus dans le

Trias. Le Vcllugiaii er le Yarcnien dans le Trias inférieur et un autre dans le

Trias moyen. I.’ichthyocomplexe Yarenlen comprend deux groupes d’âge dif¬

férents (l’Althruba et le Bogdo dans la Cis-Caspicnnc ci le Fyodorovka et le

Gamskaya dans le sud du Cis-Oural). L/ichihyocomplexc du Trias moyen

comprend les groupes de poissons de Donguz cr de Bukobaj. Les change¬

ments dans le temps de la faune de poisson.s sont reportés sur les coupes à

travers les territoires depuis le Cis-Oural jusqu'à la Cts-Caspienne. La suite

d’Akhtuha, du Trias inférieur, de ki coupe de Bogdo (Cis-Caspicnne) ast cor¬

rélée par lc.s poisson.s avec la partie basale de la suite de Pctrovpavlovka, et la

suite de Bogdo sus-jacente avec le reste de la suite de Pcirovpavlovka dans la

région d'Orenbourg. Les suites du Tcias moyen de Donguz et Bukobaj

(Cis-Oural) sont stratigraphiquement analogues aux suites de Elton et Inder

de la coupe du Trias moyen du nord de la Cis-Caspicnne. La succession dans

le développement des tchthyofaunes du Trias est une constante .sur tout le

territoire de la Russie européenne, elle est tracée pour les territoires adjacents

et peut servir de base pour des divisions stratigraphiques et des corrélations

interrégionales des différents faciès marins et continentaux du Trias.

INTRODUCTION

In the territory of European Russia, the Triassic

deposits are developed in two disconnected

extensive fields: che Southern and northern ones.

The présent paper considers the ichthyofauna

only from rhe Southern Triassic field, embracing

the rerritories of the nortlïern Cis-Caspian (the

Peri-Caspian Dépression), the south of thc Cis-

üral Marginal Deflection, rhe Southern slope of

the Volga-Ural Anficli.se (Obshchy Syrr) and,

partially, the zone of the Don-Medveditsa dislo¬

cations. The Triassic accumulation, as well as the

aquatic paleobiota development in thèse régions,

were direcily or indirectly controlled by the

Tethys paleo-ocean régime. The fir.st paleonrolo-

gically characterized Triassic deposil.s in Russia

were establistieJ wifhin thc Southern Triassic

field, in the Bolshoye Bogdo Mountain, near che

laite ol Baskunchak în che northern Cis-Caspian.

In thc middle of rhe eighieeiuh cemury, Pallas

(1788) discovered ammonite.s in the Bogdo

limestones; latet on, ihose were dcscribed by

Bukh (1885) as Ammonites bogdoanus Buch.

280

GEODIVERSITAS • 1997 • 19(2)

Triassic Ichthyofauna of Southern Urals

While making a layer-by-layer descriprion of rhe

same section, Auerbakh (1871) found some

remains of labyrinihodont^ Mastodonsaurm (?)

sp., and fish, Hybodm plicatilis Agassiv., Acrodus

dunkeri Auerbach, Sphaerodus yninimm Agassiz,

Saurichthys sp. Those fauna-bearing layers are

comparable with the Middie Triassic

Muschelkalk from Germany. It was only wlien

Mojsisüvich (1882) foiind cerantes in the ammo¬

nite fiiuna of Bolshoye Bogdo, lace in the nine-

teenth ceniury, iliat rhe section could be

compared co rhe Campilian layers of the Alpine

Lovver Triassic. Larer on, Khabakov (1932) des-

cribed two lungfish toorh plates from the Bogdo

limestones: Ceratodus ex^ gr. kaupi Agassiz, and

C. facetidens Chabakov. Ir is worth mentioning

Fig. 1. — Principal Ichthyofauna (ocallties In the northern Cis-Caspian and Southern Cis-Ural régions, main sections; 1- The Don

Bend; 2. Gmelinka. well 5041-c (1521-1526 m int): 3. Yuzhno-Yershovskaya. well T (931*934 m int.); 4, Bolshoj Bogdo Mountain: 5.

Novokazanka. well k-6 (424.5-427 m int.), 6, Zhundykuduk. weli 46 (depth 440 m); 7. Zhundykuduk, well 22 (487-491 m Int.); 8.

Barkhanny, well k-4 (35B-365.5 m Int); 9, Azf-MoIIq-1 ,-2; 10, Kok-Tau; 11. Kara-Bala-Kantemir; 12, Mechet, 13, Markovka; 14,

Mirolyubovka; 15. Rossypnoya., 16, Nizhneûzyornoye; 17, Chyomaya-t ; 18, Donguz-1, -2, -12; 19, Berdyanka-2, -3: 20, Bukobaj-5;

21. Karagachka; 22, Kzyl-Saj-2; 23, Krasnogory-2: 24, Bekhteyev Gully; 25, Petropavlovka-I, -2; 26. Kaltayevo-2, -3; 27, Yaslav, 28.

Muraptalovo; 29, Yamangulovo: 30. Sankubaj, well G-1 (890.1-893.6 m int.); 31, Rozhykha; 32. Yelshanka-I; 33, Dolgy Yar.

GEODIVERSITAS • 1997 • 19(2)

281

Minikh M. G. & Minikh A. V.

that thc first of the rwo forms was first described

from the Germàn MuschelkalL Subsequenriy,

lungfish remains were found wirhin the Triassic

beds from the Middle Don (the Don Bcnd loca-

lity), the South Cis-Urals (DongiR-l and

Kaltayevo-2 localities), and over vasr areas of rhe

northern Trjassic field (Ffremov ik. V'yushkov

1955).

The authors began to study fo-ssil fi.sh from the

Triassic of Russia in the mid-sixtics. An ample

material from over 150 localities was collcctcd,

representing Early and Middle Triassic squali-

forms, lungfish and actinopterygii from F.astern

Europe. The Late Triassic fishes from the région

are still unknown. There are over forty localities

of the Triassic ichthyofauna in the south of the

East European Plarform and in the South Cis-

lirais (Fig. 1). It was largely chis material that

provided the basis for revealing rhe stratigraphie

importance of lungfisli (Vorobyova Minikh

1968; Minikh M. G. 1969, 1977), squaliforms

and acrjnoptcr)^ii rcmains (Minikla A. V. 1975,

1985, 1992). Frequent joint finds of fish and

retrapod remains proved to be ol much use. The

study of both (Ochev et al. 1979). combined

with informations on oclxcr fossils and the data

from lithologie (Tverdokhlebov 1966, 1970;

Lipatova et al. 1965; Lipatova 1967, etc.) and

paleomagnctic research (Molostovsky 1983),

made it possible to develop unified stratigraphie-

division schemes lor the Tri.assic ol European

Russia (Anonymous 1982).

STRATIGRAPHIC ICHTHYOCOMPLEXES

Notwirhstanding considérable taxonomie diversi-

ty of certain Triassic fish groups, a number of

regularities are observed in their cvulurion, which

may be used for stratigraphie purpo.ses.

Dipnoans served a.s the basis for récognition of

rwo major stages^ or superichihyocomplcxesj

changes in the Triassic from ihe Easi European

Platform and the Ci.s-Ural deflection: the gna-

thorhizian and ceratodian ones. The first one has

a worlwide distribution from thc Late

Carboniferous to the Eaiiy Triassic. The second

one appears in the Early Triassic and exists up to

now. It is in the Lower Triassic that their change

occLir, which is clearly demon.strated hy our

materials. Ar the boundary of the Vetiugian and

Yarenian, in the Olenekian age, everywhere over

rhe Russian Plate, ccratods appcar in thc dipnoan

fanna, with gnathorhiza .still existing. They

co-exist during the rachcr short Fyodorovka time,

after which the gnathorhiza vanish. l'his pheno-

menon is clcatly evident in thc Cis-Caspian,

within thc Bolshoye Bogdo section, as well as in

a juunbcr ol localities from rhe Moscow and

Mezen syncclises. The revealed changes in fossil-

fish compositions with time in this région were

used for distinguishing the ichthyocomplcxes

there: iwo in the Lower (thc Vetiugian and

Yarenian) and onc in thc Middle Triassic.

1. The Vetiugian ichthyocomplcx is represented

by gnathorhiza - Gnathorhiza. triasnca triassica

Minich, Gn. lozovskü Minich, and hyboduscs -

Hybodiis spasskiensis A. Minich. The dominant

torm here Ls Gn. triazsica triassica Minich, which

dues nor occur in any younger deposits. This

ichthyocomplcx is more complété in thc nor-

rhern Triassic field; a number of stratigraphie

groups are recognized within il.

2. The Yarenian icluhyoconiplex Ls subdivtded

into twe» groups: ihe early, the Akhtuba one

(witli dipnoans: Gnathorhiza bogdemis Minich,

Gn. utscbcvî Minich, Gn. triassica basku7ichûkfnsis

Minich, Ceratodus ninlticristatus Vorobyova,

C. jethiirtiensis Minich, C. gracHis Vorobyova;

and squalilorms: Hybodns spnsskiemis K. Minich,

tiybodus maxinn A- Minich) and the laier, the

Bogdo one (with ceratods: Ceraitnlus rerticristutus

Vorobyva, C. donensis V'orobyva et Minich,

C. muliicrisîatus Vorobyva, C. inidticrisîatns lipo-

x>emis Minich, C jecharriensis Minich, C. katipi

Agassiz, C faceridens Chabakov; .squaliforms:

Hybodus maxinu A. Minich,. II. plicatilts Agassiz,

Acrodus dunkeri Auerbach, làssodns anguhitus

Stensio; and actinopterj'-gii: Sphaerodns mhmnus

/\gassiz, Colobodus varhis Giebel).

3. The Middle Triassic ichthyocomplex is also

subdivitled into two groups of various âges. In

the earlicr group, the Donguz one, fishes are

represented by Ceratodus gracilis Vorobyva,

C. bucohaensis Minich, C. orenburgensis Minich,

282

GEODIVERSITAS ‘ 1997 • 19(2}

Triassic Ichthyofauna of Southern Urals

C. rectîcristiUlis Vorob)^^a, C clonensis Vorüb)^a

et Minich, C jechartiensis Minich, Saurichthys

dongusensis A. Minich, Hybodus otschevi

A. Minicil, Hybadns kuragatshkiiensis A. Minich.

Cemtodus recticrisUitus Voroby\a, Hybodus othche-

vi A. Minich and Saurichthys dongusensis

A. Minich arc cbaracteristic of the considered

group. In rhe youngcr, tire Bukobâj group, fishes

arc rcpresciircd b}^ Ceratodus bucobuetish Minich,

C. grucilis Vorob)^'a, C orenburgerpis Minich,

Saurichthys uliimus A, Minich, llybodiiskara

gatshkaensis A. Minich, Ceratodus hucobaensis

Minich and Saurichthys ultimus A. Minich.

General information on ail rhe known ichihyo-

launa localities. Mnthin the Southern Triassic

field, is presented below and its corrélative possi-

bilities arc revealed.

REVIEW AND CORRELATION

OF ICHl’HYOFAUNAL LOCALITIES

The Vett.ucian ichi HyocoMPi.KX

Within the Vetlugian sériés of the Ixnver Triassic

froni the South Cis-Urals and the adjacent from

the west régions ol Obshchy Syrt, fish rcmains

were encountered in several bone-hearing sites.

The mo.st ancient ol ihose is YeI.shanka-L à locâ-

lity 9 km to t(ie South of ihe town of Buzuluk in

Orenburg région. Iboih plate rcmains bclongiiig

to Gnathorhim lozooskii Minich» t}'pical of the

Vetlugian ichthyocomplex, were found there m

an interlayer of red brown aleurolices within a

sand séquence of the Kopanskaya suite. The

soundness of chis gnathorhiza being assigned to

the Kopaii lc\cl is confirmed by rhe discoveries

of Tupilükvsaurus sp. vertebra, typically représen¬

tative of the tupilakosâur group of the vetluga-

saur ccrrescrjal verrebrate fauna (Ochev 1992),

Another localit}', Nizhneozyornoye, is -siruated in

the left Wall of a gully, falling inrn rhe Ural River

near Nizhneozyornove village, Krasnokholmsk

district, Orenburg région. The Early Triassic

hybodont shark remains, Hybodus spasskiensis

A. Minich, were found there in an abandoned-

channel suite, rcprcscnced by a sequence of

brown cross-bedded sands wirh clay and sandsro-

ne interlayers with apparent thîckness up to 5 m.

Chyornaya-Î locality is associated with the upper

pan of the Vetlugian séries, ihc Kzylsaj suite; It is

situated along the right bank of the Chyornaya

River. 5 km to the south of Krasny Kliolm villa¬

ge. Orenburg région. A typical Early Triassic

gnathorhiza form. Gnathorhiza otschevi Minich,

was found there in red-brown sands (lO m).

There is another known locality^ the one of

Muraptalovo-I, on the right bank of rhe Bolshoy

Ynshacyr River ncar Muraptalovo village,

Kyurga/.y district in die south of Bashkiria. I he

section is represented by a séquence of red brown

cross-bedded satïdstones (over 25 m), In one of

the lenticular interlayers wxs found a fin spinc of

a .squaliform, Hybodus spasskiensis A. Minjch,

typical of die Early Triassic deposiis. Hybodus

spasskiensis A. Minich fin spine.s were also

encountered higher in the section, near Yakutovo

village, in similar sandstones containing remains

of the Vetlugian tcctapod fauna {Wedugasaurus

sp., Bemhosuchui bashkhietp Otebev). Two other

bone-bean'ng sites from the Kzyisaj suite of the

Vetlugian séries, containing a r}'pical Vetlugian

ichthyocomplex, arc known from Büzuluk dis¬

trict, Orenburg région. One of them is Dolgiy

Yar locality in the same-named gully falling into

the Fogromnava River (the Samara left tributa-

ry), from the left 2.3 km north-west of

Logadiyovka village. vSeveral welLpreservcd lung-

fish tooth plates were found in an interlayer of

brown claye)^ aleurolices within a sequence of

cross-bedded sandstones. They belonged ro

Gnathorhiza triassfca bereznikiensis Minich, typi¬

cal of the uppermost laycrs of the Vetlugian séries

of rhe more northerly régions of the East

European Platform. The second site, Rozhikha

locality, is siruared in the mourh of Ro/hikh.a

Gully, falling inio the Grachyovka River (the

Buzuluk left tributary) 1.4 km north of

Grachyovka village, Buzuluk district. In the simi¬

lar rocks of the K/.ylsaj suite there, a large toodi

plate of Gnathorhiza otschevi Minich was found,

typically représentative of the Vetlugian ichthyo-

complcx. The Vetlugian Icvcl of rhe Triassic sec¬

tion from the Peri-Caspian Dépréssion is

penerrated by a substantial number of wells, but

wirh incomplète cote .selecrion, lung fish remains

{Gnathorhiza triassiea îriassica Minich) were

found only in well No. G-1 (Sankubaj), within

the 890.1-893.6 m depeh interval. These dip-

GEODIVERSITAS • 1997 • 19(2)

283

Minikh M. G. & Minikh A. V.

noan forms arc extremely common in Vetlugian

deposits, included the area of rhe northern

Triassic field, and may serve as good corrélatives

of the host beds.

The Yarknian icirniYOCOMi’LLX

Formations of the Yarenian âge are widely disrri-

buted over the considered régions of the South

Cis-Urals and northern Cis-Caspian. Bone

remains of terrestrial vertebrates and fishes occur

there rather freqiienriy. Taken cogether, rhey

constitute the basis for détermination of the rela¬

tive géologie âges of the deposits. Wlrhin the

Peri-Caspian Dépréssion, the Yarenian ichthyo-

complex waü scudied in the Triassic section frorn

the Bolshoye Bogdo Mountain, on the souih-

western bank of Baskunchak brinc lake (Minikh

1972, 1977). Diverse Bsh rcmaitis from both

groiips of the Yarenian icbrhyocomplex were

found there at varions levels, in the Akhtuha and

Bogdo suires (Fig. 2). Niimcrous gnarhorhlza

and cer.irod remains were found in the red-bcd

clayey aleurolircs of the Akhtuha suite (bone-bca-

ring site A): Cnathorhïzn truuika haskurichakensis

Minich, Cn. hogdensis Minich. Gn. otschevi

Minich, Gn. sp., Ceratoflns mnlticristatns multi-

cristatus Vorobyova. Combinations of gnathorhi-

za and ceratod remains within ilie Lower Triassic

sections are characteristic ol tlic Ahhtuba group

from the Yaretiian ichihyocomplex of ihe

Cis-Caspian. Saurichthian remains {Saurichîhys

sp.) occuj within the Akhtuha suite from

Bolshoyc Bogdo alongsidc with dipnoans. A

typical form of the Alclituba group, Gnathorhïza

triassica biiskunchakensh Minich, was also

encountered at the depth of 553 m in a core

from K-6 wcll (Barkhannaya), drilled berween

the üral and the Volga. This part of the Triassic

section was assigned to the upper hall of the

Olenekian stage, according to rhe ostracode

{Gerdalifi triassiana (Belousova), G. wetlugensis

Belousüva) and charofite {Vorochara triassica

(Saidakovsky), Auerhachichara achtubensis

Kisilevsky) complexes. The lungfish from this

section indicates an Akhluhian âge of déposition.

In the South Cis-Utals, the early Yarenian

(Fyodorovka) group of tite Low'er Triassic ich-

thyofauna is only represented in Kyzyl-Say-2

locality (Garyainov & Ochev 1962). In the

Burty'a River basin (a left rributary ol the Ural)

near Andreycvka village (Burtinskij district,

Orenburg région), in the sand-cojtglomerate

séquence of the Perropavlov-skaya suite, repré¬

sentatives Gmuhorhiza and Ceratodns oeewu cha¬

racteristic of the carly Yarenian group

(Gnnthorbisa triassica haskurichakensis Minich

and Ceratodus multicristatus muliicristatus

Vorobyova). In the suite section they arc associa-

red wirh hybodont sharks remains, Hybodus

spasskiensis A. Minich. l’hus, the prcsence of

Gnathorizds and Ccratodids in chc Lower

Trias.sic sections malccs it possible to corrclate the

Akhtuba suite of chc Peti-Caspian Dépréssion

with the lowennost part of rhe Petropavlovka

suite of the South Cis-Urals in tlie réference sec¬

tion along rhe Kyzyl-Say Gully. Fwo explanations

may bc offered for the lacis of represenrativeness

of this fish-group in the suite 5trator)'pc section

Jtcar Petropavlovka village. 1 he Pirsr one scems to

bc opr.imistic: the discoveries are waiting ahead.

The second one runs as follows: either this part

of the section is absent from the stratc»C)'pe or che

conditions for fish burial were unfavourable near

Petropavlovka at that rime.

The late Yarenian (Gamskaya) group of the Early

Ttiassic ichehyofauna is reasonably completely

represented in the South Cis-Ural-s and in ihe

adjacent western région of the E.ist Furopean

Platforni. First of ail, let us mention che availabi-

licy of a purcly ceratod dipnoan association in

ihe Petropavlovka suite siratocype {Tverdo-

khlebov 1967a) This is siruaced on che bank of

the Sakniara (Fig. 1),. in che vicinity of

Petropavlovka village, Sakmara district,

Orenburg région, h is mainly huile (Fig. 2) of

greyish brown sandstoncs with aleuroÜte and

clay interlayers of a total thickness up to 250 m.

Dipnoan remains {Ceratodus multicristatus lipo-

vensts Minich and C jechartiensis Minich) were

found there at varions levels (Petropavlovka-1

and -2 locilities). l'hesc fish widely occur in the

late Yarenian deposits of the Fast Furopean

Platform. Ceratodus multicristatus Upavensis

Minich tooth plates were also encountered

(Fig. 3) in the Petropavlovka suire-developed

along rhe Dongu? River (Donguz-9 locality) near

Meschetyakovka village, Sul-lletsk district,

Orenburg région, in Bekhteyev Gully within the

284

GEODIVERSITAS • T997 • 19(2)

Triassic Ichthyofauna of Southern Urals

H H n CORRELATION OF PRINCIPAL SECTIONS BY ICHTHYOFAUNA

€/) O

>. UJ C/)

(/) W

Barkhanny well K5

Bukobaj V

Kara-Bala-Kantemir

^-Azy-Molla »l —

□ æ 1 ——— 1

üj O ^

Kattayevo It. I

I I Donguz !, Xll

_ Don Bend _Bolshoj Bogdo —

fc jyi ); y it 5 O

D NI

g i

't =±= 1 '^

O ^Petropavlovka 1. Il Donguz I, Xll

O ———

I 3——

Kzy|.Sai II

tr Wü»?:

Chyomaya I

/ Yelshanka I

T^AIeurolite Argillite it FIsh

Conglomerate

Fig. 2. — Corrélation of the Triassic sections from the northern Cis-Caspian and Southern Cis-Urals régions according to ichthyofauna.

GEODIVERSITAS • 1997 • 19(2)

285

Minikh M. G. & Minikh A. V.

Ural'Sakmara watcrshtrcl, and in rhe vncinity of

Yaziav Farm, Kyurga/.y district, Bashkiria. There

is a major Triassit vcrtcbrare.s localiry,

Rossypnoyc, tu lhe wcst of the Cis-Ural deflec-

tion, in lhe territoty of Ohshchiy Syrt (Efremov

& V’yushkov 1955). It is located in the righr

slope of Mayachnaya Gully, opencd from thc

right inco tlie Ural valley 1.0 km lo thc north-

east of Rossypnoyc village. Ilekskij district,

Orenburg région. Ccratod toorh plates Ceratodus

recticristatus Minich (Fig. 3) occur herc alongside

with parotosuchian fauna tetrapod remains, in

red clays.

An even richcr locality of Karly drlassic verte-

brates, the Don Bend (Rykov & Ochev 1966), is

known Irom the sourh-eascern slope of the

Voronezh untcclinc dislocations. It is situated

(Fig. 1) in a large bend of thc Don, north of

Sirorininskaya village, in Lipovski) Gully (a Don

righr tribucary). Diverse fish renvains occur rherc

in the npper, .sand-conglomerate portion of rhe

Lipovskaya suite, together with the parotosu¬

chian tetrapod fauna remains. Among flsh, dip-

noans are found there: Ceratodus mulicrhtatus

lipovensis Minich, C. jcchartieusis Minich and

C donensis Vorobyova et Minich; sharks Hybodus

maximi A. Minich, î.issodm angulatHs Stensio,

actinopterygii Saurivbthys sp., ,ancl other, forms of

squaliform and actinopterygian fîsh th.it are nor

decribed yei. On thc whole. according to the

composition ol iossiis cncounccrcd there, thc

Don Bend locality bclongs to rhe Lace Yarcnian

(Lipovskaya) group ol the Early Triassic ichtbyo-

fauna, and may bc corrclatcd by fish with most

of the Pciropavlovkii suite (rom Ohshchiy Syrt

and from thc Gis-lirai Dcflection; through the.se,

it may also bc correlatcd wilh the Gamskaya

suite from Safonovsky Dcflection ol Me/en syne-

clise. It is interesting co compare Ceratodus

donensis Vorobyova et Minich, very common in

the Lipovskaya suite and described by the Don

Bend matcrial, with the dria.ssic ceratodes known

from ail over the world. Among thc European

forms, C. priscus Fraas from the I.ower Triassic of

Schwar/wald (medium moriled sandstones)

seems to be the most similar one. This allows us

to correlate, in a first approximation, rhe Lower

Triassic dipnoan bearing beds from the Easr

European and West European Platforms.

Wirhin the Peri-Caspian Dépréssion, thc Late

Yarenian (Bogdo) group of the Early Triassic ich-

thyofaun.i is most clcarly seen in thc Bogdo suite

section (Fig. 2), from the BoI.shoye Bogdo

Mountain (bone-bcaring site B). Fish remains arc

represenred there by dipnoans (Ceratodus midti-

cristatm lipovensis Minich, Ceratodus facetidens

Chabakov and Ceratodus ex. gr. kaitpi Agassiz)

and squaliforms (llybodus plieatilis Agassiz and

Acrodus dunkeri Aucrbach). Actinopterygii arc

represented by pcrleidids {Colobodiis varius Giebel

and Sphaerodus w/Vi/w/cr Agassiz) .ind saurichriids

(Sauriehthysapiutlis .^\gassiz and Sauriehthyshp,).

Evolurioiiaiy levels idenrities, and .similariries in

a number of luugflsh, squaÜform.s and acrinopte-

lygians from the single late Yarenian group of the

Early IViassit icluhyofauna wdchin che

Gis-Caspian Bogdo section and ihosc (rom the

Triassic section of ihc Don Bend (Ceratodus

multicristatiis lipovensis Minich, Lissodus sp. and

Sauriehthys sp.), make ir passible co correlate

with cerrainty thc Bogdo suite wah che

Lipovskaya suite of thc Middie Don, che

Petropavlovka suite of thc souch-castern slope of

the Volga-Ural antecline and thc south of the

Cis-Ural dcflection. The présence in thc Bogdo

group of ceratods, Ceratodus kaupi Agassiz, very

commun in the Middie Triassic Muschellulk of

the German basin impÜes, in irs rurn, probable

paleogengrapliic and ichthyofnan.il connections

between the Bogdo and Gernian marine sédi¬

mentation basins lowards thc end of thc Early

Triassic. Such a connection between the

Peri-Caspian and North German (Répressions

miglu be accornplished through the Gis-

Caucasian marginal dcflection, the System of the

Dnieper-lRonet.s depres.sions, Pripyat ÎReflecnon

atid Poli.sh-Lithuanian syncline. At the end of the

Early Tria.ssic, u lot ol interconnected freshened

.semi-marine hasins exLsted ail over that région,

which might providc the cxcbange of brackish

taunas.

Thi. Middi.I'. Triassic ichthyocompM‘.x

In rhe terri tory of European Russia, the Middie

Triassic ichrhyofauna was firsr di.scovered and

described from che South Cis-Urals (Vorobyova

bc Minikh 1968). It cornes from thc Donguz and

Bukobaj suites (Tverdokhlebov 1967b) and is

286

GEODIVERSITAS • 1997 • 19(2)

GEODIVERSITAS • 1997 • 19(2) 287

Principal fish

localities from

the Northern

Cis-Caspian

Bukobaj V

Kaltayevo III

Oonguz XII

DonguzI

Karagachka

Berdyanka II, III

Kaltayevo II

Rossypnoye

Yazlav

Donguz IX

Bekhteyev Gully

Petropavlovka II

Kzyt-Saj II

Dolgij Yar

Chyomaya I

Nizhneozyornoye

Rozgykha

Mechet I, II, III

Yelshanka

PiG. 3. — Ichthyofauna distribution within the sections of the Triassic from the Southern Cis-Urals régions.

Triassic Ichthyofauna of Southern Urals

Minikh M. G. & Minikh A. V.

known from the faunas ot a luimber oi locaJities,

where it is often encountercd rogethcr wirh the

remains of eriosuchian and masrodonsaurian ter-

restrial A'^ertebrate faunas (Ochev 1992). The

principal localities of the Middie 'IViassic ich-

thyofauna are associated with type and référencé

sections ot both suites. The Donguz suire straro-

t}'pe is located along the Donguz River (left tri-

butary ol ilic Ural) near Perovka village,

Sol-lletsk district, Orenburg région, The section

is geneially coniposed of variegated aleuro-clayev

and arenaccous rocks up ta 150 m thick. In ibe

middie parc ot the suite, in the conglomcrace-likc

interlayers among variegated aleurolites and clays

of the Dortgu/'I localiry (Figs ]'3), luug fish

tooth plates were discovered (Cmnorius gracilis

Vorobyov.T, C. recticriualu^ Vorobyova, C. aren-

burgemis Minich and C jechnniensis Minich).

The latcer forms, aliliough quilc cotnmon in ihe

upper layers oï the Lower Friassic, ;irc rather rare

in the Middie Triassic. About 75 m higher in tbc

section of the Donguz suite, in the Donguz-12

locality in a lens ot unsorted sandy-.ileuritc rocks

rogethcr with bones ol' tetrapod eriosuchian

fauna and tooth plates ol teratods (Ccratorlus

gracilis Vorobyova, C recticristatus Vorobyova,

C. oreriburgensis Minich and C baca-baensii

Minich), sonie other fossils wcrc found: hybo-

dontid fin and head spines (Hybûdus oischevi

A. Minich), tcech ot Lissodns angulatns Stensio,

teeth of new squaliform généra and .species (iheir

descriptions arc being prepared for publication)

and actiuopierygian jaws {Saurichthys dangusensis

A. Minich). Almosi the sanie set ot taxa occurs

among the lungfish and squalitonn rcmains,

from a number ot- other veriebrate localities, ar

varions levels of Uie Donguz suite of the South

Cis-Urals. Fhese arc Bcrdyanka-2, Bcrdyaiika'3,

Karagachka, KaltaycAno-2 localities (Figs 1-3). Fin

pines of yer anoiher Hybodus speciCvS were found

in the larter two ones: llybodus karagatshkiiemh

A. Minich, typical of the wholc of the Middie

Triassic ichthyoconiplex.

Thus, the Donguz gtuup of the Middie d’riassic

ichthyofauna clearly stands apan from the above

considered Early Triassic ones, becuuse ot tlic

new dipnoaii spccics appearing within the sec¬

tions {Ceraiodus gracilis VovohyoY^, C. bucobaen-

sis Minich), new squaliforms {Hybodus

haragatshknensis A. Minich, //, otchevi

A. Minich) and actinopferygians {Saurichthys

dongusensis A. Minich). Ail these torms may be

regarded as typical f)f the Middie Triassic ich-

rhyocomplex on the whole. The combination of

rhese forms wirh those known from rhe Early

Triassic deposirs {Ceratodus recticristatus

Vorobyova and C. jeelmrtiensis Minich) makes it

possible ro separate the Donguz group btirh from

rhe earlier and Irom the younger groiips of the

Triassic ichrhyt>rauna.

Along with fish remains in the Donguz suite of

the South Cis-Urals, ihe remains ot eriosuchian

tauna ccrrcstrial vertebrates occur, which correla-

tc wirh the Ladinian tetrapod association from

the uppcrniost Muschclkaik and lowcr Keuper of

Germany. according ro common plagiosaur

gênera {Plagiostcmun/ .md Plagioscutum).

l’he Donguz suite correlates wuh ihe Flron suite

establishcd in the northern Cis-Caspian, accor¬

ding to rhe ichthyofauna. ‘l'hc section ot the

Middie Triassic and its ichthyofauna were stu-

died clierc (Fig. 4) from the cores of sevcral réfé¬

rencé and paramctric wells and troni rhe natural

outerops on the north-castern shore ol Inder

Lake. The lake is situated in the left-bank région

of ihc Ural. soutli-east oflnderborsky .seitlcnient,

Gurjev rcgion> Kazakhstan. A rather complété

.section of the Ifiassic, typical of the central parts

of rhe Peri-Caspian Dépréssion, i.s known there

on rhe slopes of rhe Kok-Tau Range and along

the lake shore.s. The F.arly Triassic Cis-Caspian

sériés are represented in the Inder section by the

basal red'becl claycy sequence (over 200 m). The

Middie Triassic is represented by the Eicon (a

red-bed arenaccous-tonglumerate sequence, up

to 110 m and an arenateous-clayey one up to

60 m) and Inder suites (grey-coloured limcstone-

dayey séquences about 250 ni). ’Fhc Une Triassic

variegated sandstonc sequence lies above rliem

(up CO 100 m), the Masceksaj horizon

(Anonymous 1982).

'Fhe Lower/Middie Triassic boundary was

previously drawn (Ochev & Smagin 1974)

within the Elton suite, betvveen the basal saridy-

conglomcraïc and the red-bed sandy-clayey

scqueiice-s. Oui* point of view regarding this pro-

blem was determined aher the discovery of cypi-

cal Middie Triassic ichthyofauna remains in the

288

GEODIVEflSITAS • 1997 • 19(2)

GEODIVERSITAS • 1997 • 19(2) 289

Fig. 4. — Ichthyofauna distribution within the sections of the Triassic from the northern Cis-Caspian région.

Triassic Ichthyofauna of Southern Urals

Minikh M. G. & Minikh A. V.

sand-conglomerate sequence of the Elton suite.

Lungfish tooth plates {Ceratodus gracilis

Vorobyova) and undefînable rctrapod bone frag¬

ments were found there in rhe Kok-Tau and

Azi-M(»lla-1 locations. Tliis ccratad species îs

known as a component of thc Middie Trîas.sic

(Dongiiz) ichthyocomplcx from the South

Cis-Urals. In the nonhern Cis-Caspian, this .spe¬

cies is aiso found in some cores from the wells

penetrating the Middie Triassic sections (the âge

was determined from ostracodes and charo-

phytes). These are rhe sections of the Yii/.hno-

Yershovskaya-l well (931.0-934.0 m interval),

Barkhanny K-5 well (379.0-383^9 m and

385-9-392.9 m intervals) and Zhundykuduk'46

well (490 m depth). Be-side.s çeratods, some sec¬

tions contain the rcniains ol hybodont sharks

typical of thc Donguz fish-group (Hybodus

otschevi A. Minich; Gmclinka 304 1-C well,

1521-1526 m intcrval) and new species of thc

shark geiuis Lissodus (Barkhanny K-4 well;

361,5-365.3 m intcrval).

The prcscntcd data on ichthyofauna distribu¬

tions wdthin thc Middie Triassic deposits,

confirin that Ceratodus gracilii Vorobyova

belongs to the Middie Triassic ichthyofauna of

the Donguz group; it.v taxonomie composition is

rather stable within rhe whole of rhe Southern

field of the Trias.sic devclopnieiu in Europeun

Russia. On the basis of thèse lungfish discoverics,

rhe age of the basal sandy-conglomerace sequcnce

of the Elton suite, from the Inder Triassic sec¬

tion, may be dcfincd as the Middie Triassic.

The younger, Bukobaj group of rhe Middie

Triassic ichthyofauna, from the South Cis-UraLs,

is known from thc itraiotype section of the

Bukobaj suite in Bukobaj-5 locaÜt)'. It is situated

in Bukobaj Gully falling in the Berdyanka river

(left tributary of the Ural) from the right, up-

stream Bclyaycvka village, Sol-lletsk district,

Orenburg région. Within the lighr-grcy sands

and sandsiones of this area, lungfish tooth plates

were discovered (CertUodus gracfUs Vorobyo\'a

and C hHvohaensii Minîch), as well as the

remains of sauriçhthiid Saurichthys ultimus

A. Minich. typical of thc Bukoba) fish group.

Some mastodonsaur tecrapod fauna rcmains were

aIso found thexe. The Bukobaj suite comprised

also the deposits, outeropping along the right

bank of thc Bolshoj Yushatyr river ncar

Siarokalcayevo village (Efremov & V’yushkov

1953). In rhe Kaltayevo-3 location thcrc, within

rhe grey sandsiones, hesides tetrapods

Maiîodonuiums torvus Konzhukova and orhers,

squaliforms were found, Hybodus karagatshkaen-

sis A. Minich, which occurs ns early as at the

Donguz level, and rhe latesi of thc saurichihiids

known from rhe région, Saurichthys ultimus

A. Minich, similar in rheir morphologie features

to saurichthys from the Ladlnian stage of Turkey

(Minikh A. V. 1992).

In rhe norrhern Cis-Caspian> the Inder suite is

correlated ro rhe Bukobaj suite from rhe South

Cis-Urals by terrapod and fish faunas. A verte-

brate localit)', Kara-Bala-K.intenijr, was discove¬

red in lhe suite stratotype in the vicinity of Inder

Lalcc (L)chcv Smagin 1974). This is situated

on the north-eastern shorc of Inder Lake on ihe

hill top, 200 m co thc south of Kara-B.ila-

Kancemir graves (masars). l'hcre, in the greyish-

green clays of thc Inder suite, along with the

bone.s of mastodonsaur fauna tetrapods, ostra-

codes and charac (Lipatova et al. 1969). the

rcmains wcrc found that are typically représenta¬

tives of thc Middie Triassic Bukobaj ichthyotau-

nul group: ceratodontid tooth plates {CeiUtodus

orenburgensis Minich) and a cartilaginous ganoid

{Saurichthys ultimus A. Minich).

CONCLUSION

The wide distribution of ichthyofaunas, similar

in composition, in the south-east of the Russian

Plate and in the northern Cis-Caspian, as well as

elle general succession in its change wiih tiine,

indicate the uuity of depo.sitional basias in the

l'fiassic, ail over thc considered territory. -Such

fishes as hybodusc.s, ccratods and saurichthii

prove to bc very cosmopoliran. They^ are wides-

pread and common in the Triassic deposits from

practically ail the continents of the globe

(Minikh 1977; Minikh A. V. 1982). This may be

used for solving the important problems of dis¬

tant inter-regional and intercontinental corréla¬

tions of marine, semi-marine and continental

Triassic deposits.

290

GEODIVERSITAS • 1997 • 19(2)

Triassic Ichthyofauna of Southern Urals

Acknowledgments

Wc would like fo express our graiirudc to Prof.

V, G. Ochev, Prof. D. A. Kukhtinov and Dr.

V. P. Tvcrdokhlebov for granting ihe sione mate-

rials on rhe Triassic iciithyofaima and for their

helpful consultations on some sections from the

South Cis-Urals and northern Cis-Caspian.

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and Bashkifia Cis-UraU, in Geology problems ofthe

South Urahand Volga région, The Mcsoztàçy Saratov

Lbiiversit) Pliblicatinn, issue 3, part 2: 3-24 [in

Russian].

GEODIVERSITAS • 1997 • 19(2}

291

Minikh M. G. & Minikh A. V.

— 1967a. — New data on the stratigraphy of the

Lower Triassic deposits from the Orenburg and

Bashkiria Cis-Urals, in Geology problems of the

South lirais and Volga région^ Saratov University

Publication, issue 4, part 1: 45-77 ([in Russian].

— 1967b. — Stratigraphy of the Middle and Upper

Triassic from the South Cis-Urals, in Geology pro¬

blems of the South Urals and Volga région^ Saratov

University Publication, issue 4, part 1: 78-91 [in

Russian].

— 1970. — The Baskunchak deposits from the left-

bank région of the Samara River and Obshchy Syrt

(Orenburg and Bashkiria Cis-Urals), in Geology

problems of the South Urals and Volga région, The

Paleozoic and Mesozoic, Saratov University

Publication, issue 7, part 1: 96-101 [in Russian].

Vorobyova E. 1. & Minikh M. G. 1968. — An expé¬

rience of biometry application to ceratodontid

tooth-plates study. Paleontological journal. No. 2:

77-87 [in Russian].

Submittedfor publication on 15 January 1996\

accepted on î October 1996.

292

GEODIVERSITAS • 1997 • 19(2)

An essay on régional geology and stratigraphy

of the Upper Cretaceous deposits

of Southern Lirais territories

Edward O. AMON

Instituts of Geology and Geochemistry, Urals-branch of Russian Academy of Sciences,

620219 Ekaterinburg, Pochtovyi per. 7 (Russia)

Joyce R. BLUEFORD

Math/Science Nucléus, 4009 Pestana Place. Fremont, California 94538 (USA)

Patrick DE WEVER

Laboratoire de Géologie. Muséum national d’Histoire naturelle,

43 rue de Buffon, F-75231 Paris cedex 05 (France)

Victor I, ZHELEZKO

Instituts of Geology and Geochemistry, Urals-branch of Russian Academy of Sciences,

620219 Ekaterinburg, Pochtovyi per. 7 (Russia)

Amon E. O., Blueford J. R.. De Wever P. & Zhelezko V. I. 1997. — An essay on régional

qeology and stratigraphy of the Upper Cretaceous deposits of Southern Urals territories, in

Crasquin-Soleau S. & De Wever P. (eds). Peri-Tethys: stratigraphie corrélations,

Geodiversitas (2) : 293-317.

KEYWORDS

stratigraphy,

correlarion.

Cretaceous,

South Ural.

paleontolog)'.

ABSTRACT

The Turgay région is con.sidercd as the north-ea.stern border of the

Peri-Tethyan basins duiing the Cretaceous. This area contained éléments of

each area's faunas; the rclatively vvarm Pcri-Tcthys faunas with chc coolcr West

Siberia faunas. Cretaceous deposits are found throughout the Southern Urals,

especially in the western and Southern Primugodzharie, Aktyubinskian

Priuralie, and Pri-Irgizsk)^ areas. Cretaceous deposits are covered by Cenozoic

rocks, shown from well cores of rhe south-eastern betrder of Mugodzhar

mountains, l’urgay and northern PriAralie. 7’he Lower Cretaceous in the Sou¬

thern UralvS was prcdominatcly contiueiual. In rite western Primugodzharie

and Aktyubinskian Priuralie région, marine sédiments of Neocomian, Aptian

and Albian âge were deposiced. Red continental sedimentary rodes were depo-

sired during the Neocomian. Coal and bauxite were deposited during Aptian

and Albian. l’he Lower Cretaceous boundary was marked by a marine régres¬

sion, while the Aptian and late Albian-early Cenomanian are characterized by

extensive continental rodes on rhe entire territory, with the exception of the

l urgay région. A widespread marine transgression is évident during the

Cenomanian.

GEODIVERSITAS • 1997 • 19(2)

293

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

This transgression influenccd the sedinienrarion in thc Southern Urals, Easc

European. Sqnhian, '[ uran and West Siberian pktforms. Upper Cretaccous

was dominatcd by shallow marine fades. Coastal and shore deposlcs. Marine

transgression continued iintil late Maasirichtian. The end of the Late

Maastrichtian was characterized by the appearance of very shallow water and

lagoonal régressive fades, d'hc Cretateous/Paleogene boundary w’as marked by

a pause of sédimentation with erosional unconformitles in the boundary bet-

ween the Maastrichtian and Danian. boraniinifera, radiolaria, bclemnites, sela-

chians, molJusca, pollen, and spore revcal the timing of events and suggest the

paleoenvironment of this région during tlie Upper Cretaceous.

MOTS CLÉS

stratigraphie,

corrélation.

Crétacé,

Oural méridional,

paléontologie.

RÉSUMÉ

La région de Turgay représente la bordure nord-orientale de rensemble

Péri-Téthysien au Crétacé. Cette région comprend des éléments des diverses

provinces fauniques; des faunes Péri-Téthysiennes relativement chaudes et

des faunes froides Sibériennes. Des dépôts Crétacés existent partout dans

rOural méridional, et particulièrement dans les zones occidentales et méri¬

dionales de Prémugodzharie, du PériOural Alctyubinskien, et les zones de

Péri-Irgizsky. Des forages de la bordure sud-orientaJe des monts Mugodzhar,

Turgay et de PériAralie septentrionale onr révélé que les sédiments Crétacés

sont recouverts de roches Céno/oiques. Le Crétacé inférieur de TOural sep¬

tentrional c.sf c.s.sctuicllcmcnr continental. Dans le Primugod/.haric occidental

et la région du PériOural d*Aktyubiiisk. des sédiments marins du

Néocomien, de TAptlen et de l’Albicn existent. Dc.s roches scdimcntaires

continentales rouges se sont déposées au cours du Néocomien, puis du char¬

bon et de la bauxite à l’Apticn ci l’Albicn. La limite inférieure du Crétacé

est marquée par une régression marine alors que TAptien et PAIbicn supé-

rieur-Cénomanien inférieur est caractérise par une grande extension des

dépôts continentaux, sur rcn.scmblc du territoire, sauf d.ins la région de

Turgay. Une large iraiisgrcssion marine se manifeste au Cénomanien. Cette

transgression a influencé la sédinieniaiion dans l’Oural méridional, l'Europe

orientale, et les plates-formes Scyihicnnc, de Turan et de Sibérie occidentale.

Le Crétacé supérieur hir dominé par des faciès de mer peu profonde, et des

dépôts côtiers et de rivage. La transgression marine a continue jusqu'au

Maastrichticn supérieur qui s*c.st terminé par dc.s faciès rrès peu profonds et

régressifs lagunaires. La limite Crétacé/Paléogène fut marquée par une pause

de sédimentation et des discontinuités érosives à la limite Maastrichticn-

Danien. Les foraminifères, radiolaires, bélemnites, sélacbjans, mollusques,

pollens, et spores indiquent la chronologie des événements et révèlent les

types de paléoenvironment de cette région au cours du Crétacé.

INTRODUCTION

Tectonic activicy in the Uralian mobile belt cea-

sed at thc beginning of the Mesozoic, completing

the suturing of the Russian platform and West

Siberian plate. A new tectonic régime began to

evolve. During thc Late Jurassic-Lower Paleogene,

the Uralian epihercymian platform was generally

uplifted. Mountain building coupled with éro¬

sion were the predominate mechanisms during

this tinte. Thin beds of continental sédiments

were accumulating in the surrounding basins.

294

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern Lirais territories

During ihe carly part of the Cretaceous» the

northern portion of che Urals downwarped at a

faster race. A transgressive cycle flooded this

région wirh northern boréal watcrs. Thb epicon-

tinental sea was a mixture of waters from the

Polar» North Atlantic and North Pacific paleoba-

sins. The Southern portion of the basin was not

invaded, as ihere is only évidence of continental

sédimentation in local dépréssions.

During che latcr parc of the Crevaceous» the Sou¬

thern porrion of West Siberia was tectonically

downwarped allowing the transgressions ro fully

invade che Russian Plarform,. West Siberian Basin

and Peri-Tcchyan basins of che Turanian Plate.

The Turgay trough allowed the north-western

portion of central Asia and north-western

Kazakhstan to expérience marine conditions

(Papulov 1974).

This connection influenced the microbiota of

West Siberian during rhe l.ate Cretaceous.

Eléments of che Terhyan fauna are found in

semi'isolared marine basins. Components of

foraminifera, radiolarian and mollusca of the

West Siberian région can be correlated to the

fauna of che Peri-Tethyan région. The Turgay

Trough records rhis mixed fauna.

The Turgay Trough Is situated between the east-

ern slope of sourhern part of rhe Ural Mountains

and che Kazakh Shickh The northern Turgay

area has well preserved Upper Cretaceous assem¬

blages and is a reference section tor foraminilëra

and radiolaria for Cenomanian, Conacian»

Santonian, Campanian, and Maasirichtian.

Upwarping in the north near Kustauay City,

Kazakhstan, was the Southern limir between rhe

West Siberian basin. South of this area marked

the area of the Peri-Terhyan basins, wbere arctic-

boreal waters of West Siberia raixed with the

warm waters of the Peri-lëthys. This basin bas

faunal représentatives of the warm waters ot Peri-

Tethyan ba.sins with the arctic-boreal faunas of

West Siberian basins. I hese assemblages are key

to understand rhe interaction of the West

Siberian, European. and Peri-Tethyan basins\

Understanding the biostr-atigraphy iri the

Cretaceous of the Southern Urals will help to

correlate viming of events of the Peri-Tethys and

West Siberia.

Fig. 1. — Location map. la. Or’-llek Hills area; 1b, Mugodzhar

Mountains: le. eastern Mugodzhar Mountains; 2a,

AKtyubinskian Priuralie; 2b. western Prtmugodzhane; 2c. South¬

ern Primugodzharie; 3a, north-eastern Uslurt; 3b. northern

PfiAralie; 4a. western side ot Turgay Trough, 4b, soulh-western

Turgay; 4c. Turgay Trough: 4d. eastern side of Turgay Trough.

STUDYAREA

This area encornpasses a vast région (Fig. 1), with

few ovuerops. The termination of the Urals in

rhe South is hordered by tlie Of-Ilek Hills and

Mugodzhar Mountain.s. The Of-llek Hills (alti¬

tude 30-509 m) repre^sents the dividc between

the Of and Ilck Rivets basins. The Or-llek Hills

arc approxîmately 100 km wide, ranging from

Orsk City on the east ta Aktyubinsk City ou lhe

west; and 200 km long, extending from ihc Ural

River Valley on the north, to Kandagach in the

GEODIVERSITAS • 1997 • 19(2)

295

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

South. The Mugodzhar Motinrains are low moun-

tains South oF the Or’ River* The Mugodzhar

Mountains consist in sev^eral ranges and groups oF

low mountains and hills. The highest peaks an?

approximarely 650 meters. The Shoshkakolian

Range (altitude 274-408 ni) is the most Southern

extension ol the Mugodzharian Range.

The Podutalian area (Hmbian ITateau) is South¬

west of the Or’-llek Hills, Mugodzhar

Mountains and Shoshkakolian Range. The

Embian Plateau is an erosional surface draining

toward the PriCaspian lowland. The East

Mugodzharian plateau is norrh-east of the

Mugodzhar mountains and south of the Or’

River. The Hast Mugodzharian plateau drains

toward the Turgay plateau.

The south-wesiern portion i.s formed by the

north-eascern Irame ot the Ustyurt Plateau

(100-200 m) and the Shagray Plateau

(100-150 m) and the Shoshkakolian Range in

the south. The PriAralian Plain (150 m) is the

territory north of Aral Lake. le contains the

sandy Bolshic. Malye Bnrsiiki, Barshakum and

PriAralian Karaltum Déserts. The eastern portion

of Turgay l'rough is rhe Turgay Plateau. It is

spread between the massifs ot the sourhern Lirai

mountains, east of the Mugodzhar Mountains

and west of the low lying îxazakh Melkosopoch-

nik Hills, Central Ka/akh. The length is around

800 km (north-south), and width (east-west) is

300-450 km.

The south-western païf of Turgay Plateau, adjoin-

ing to the Easç Mugodzhar Plateau, is called the

Pri'lrgiz Plâin (150 in). The western part of the

Turgay plain is the eastern border of Zauralian

Plateau (altitude 250-350 m). The Turgay Plain

in the north is called the Kustanay Plain (altitude

170-220 m): the central part is called the

Aday-Urka)'ak plateau (altitude 220-300 m); the

east is called the E;tst Turgay Plateau (200-400 m)

and the south is called che South Turgay Plain

(altitude 150-180 ni) (Miletsky, 1981; Ozhiganov

1964; Zakltarov Si Udri 1971; Verescliagin et ai

1975; Gerasimov et ai 1968; Yanshin 1953).

STRUCrURAL OVERVIEW OF AREA

The Lirais are divided into areas that reflect dif-

FiG- 2. — Scherne çt subdivision of Lirais

dunng lhe Cretaceous. t. Preduralie: la. Polar. Pripolar and

nofihern Preduratie; Ib miclclle and Southern- 2. Zauraüe 2a.

Pripolar and north westorn Zauralie; 2b. Pripolar and north; 2c,

middie and south-wost 2ù. mtddie and south. 3.

Predmugodzhàriu; 3a, Orakyâiea; 3b, Khobdinsky, IleksKy, and

Zhurunsky area; 3c, north-west Turgay; 3d, north-east Turgay.

296

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern Lirais territories

ferences in structure iind depositional environ-

mènes. The Russians refer to thèse as struciural-

facies divisions. Figure 2 shows the general

schemc of chc struccural-facies divisions of rhe

Urals during the Crcraceous. This paper empha-

.sizes the Upper Cretaceous events that occurred

in the Southern rerminarion of the lirais and

adjacent territories (Fig, 2: 3a'd))

The Southern lirais is subdivided into four main

structural-facial zones (Fig. 1): (1) Southern ter-

mination of the Ural Zone; (2) western adjoining

plains or Primugodzharie and north-easrern

Pricaspian Zones; (3) Southern adjoining plains

or PriAralie and nnrth-eastern Ustyurt Zones;

and (4) eastern adjiùning plains orTurgay Zone.

The Or'-lick Hills area corresponds lo che

Central Uralian anticlinorium and includes the

area west of che Kosisteksky région (the Southern

continuation of the Sakniarian Zone of Southern

Urals), and the area casr of the Kempirsaysky

région (conriniiation of South Uralian Zone).

The Mtigodzhar Mountain area (Fig. 1: la-c)

includes the sr>uthern terminations ot three

widespread Uralian régional structural unies:

Tagil-Magnitogorskian synclinorium, East

Uralian anticlinorium, and portions of rhe

Zauralian anticlinorium.

The Primtigdozharie Zone (Fig. 1: 2a) includes

the area west o( the Mugodzhar Mountains and is

referred to as the Aktyubinskian Priuralie area.

This corresponds to Aktyubinskian pericline

rrough of ihe Ural fold sysccm, which is partly

covered hy Mcsozoic-Cenozoic hlanlvct deposits.

The western Primugodzharie (Fig. l: 2b) is a

broad belt west of the Mugodzhar Mountains.

This area corresponds to rhe Kempirsayskian

Zone of Ccntral-Uralian antitlinoriuiri und to che

eastern border ol Pri-Caspian dépression of Easc

Europeaji platfornt. The western portion of chc

western Primugod/harie and .Southern Primugod¬

zharie areas are similar to the east-norih-eastern

parts of chc PriCaspian lowland area. In the South¬

west area of the Mugodz.har Mountains, ihe

région referred to the Southern Primugodzharie îs

located (Fig. 1: 2c). The ShoshkakoHan Range is

located in this région and is considered as a conti¬

nuation of the Mugodzhar Mountains, which is

équivalent lo the eastern part of soudi Emba area

(Zakharov & Udris 1971; Sobetski 1982).

The PriAralie Zone is located in the souihern

adjoining plains (Fig. 1: 3a. b) The western por¬

tion is referred to the north-eastetn Ustyurt

région. It is formed by horizontally bedded

Neogcnc, Oligocène, F.occnc, and Cretaceou.s

deposits. This area is équivalent to the eastern

part ol the PriUstyurt area. The northern

PriAralie adjoins the North Aral Lake and is cha-

racterized by a Palcozoic geosyncline basement

and thiclc McsozoiC'Ccnozoic sedlmenrary cover.

The Turgay zone (Fig. l: 4a-c) includes the

Turgay Plateau from the West Siberian plain in

the north to rhe PriAralian Karakuin Deserr in

the South. Therc are scveral fold Systems idenii-

fied in this' area, includîng the Kustanayan syn¬

clinorium, Ubaganian anticlinorium, Aksuar-

skian synclinorium, and Esilskian synclinorium.

In the eastern slope of the Urals, rhe Zauralian

anticlinorium is che western border of rhe Turgay

trough. The south-western Turgay région is

situared between rhe Mugodzhar mountains und

the northern PriAralie. This area has a cleepiy fol-

ded basement wich a well developed sédiment

cover. (n rhe Southern portion is the boundary

between the Central Kazakhstan fold sysrem,

PreCambrian and Early Paleo’zoic rocks ourcrop

in the Ulyiauskian anticlinorium and form the

eastern frame of furgay rrough. 'Fhi.s région is

referred to as rhe eastern border ol Furgay trough

or eastern Turgay. These boundaries are welt

documented in rhe litcrature (Mileisky 1981;

Ozhiganov 1964; Zakharov & Udris 1971;

Yanshin 1971 ; Vereschagin et a/. 1975; Moskvin

1986, 1987; Naidin et/y/. 1986; Papulov 1974).

S'FRATIGRAPHY OF CRETACEOUS

DEPOSITS

CENüiVL4NlAN (Figs 3-5)

During chc Cenomanian, the Southern Urals

range from continental to marine. Continental

and semi-marine (lagoonal lacusirine) rocks of

upper .*\lbian ro lower Cenomanian (AJcykuduk-

skaya Formation). Coastal marine rocks are cha-

racceriscic of the Nogaytinskaya Formation

(Primugodzharie and PriAralie) in the

Primugodzharie and PriAralie régions. Semi-

marine and continental rocks of Cenomanian-

GEODIVERSITAS • 1997 • 19 (2)

297

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

Turonian âge (Slictiregizskaya and Novoko-

zyrevskaya Formation) are located in Turgay..

Lower-middle Cenotnanian Coastal marine depo-

sits are found in thc western Primugod-

zharie and Akiyubinskian Priuralic. Upper

Cenomanian deposits in tlic western areas are

absent.

The latc Albian - carly Cenomanian Altykuduk-

skaya Formation occurs on marine deposits of

the Aptian-AJbian Bogdanovskaya Formation in

the Aktvmbinskian Priuralic région. The

Altykudukskaya Formation in western

Primugodzhnric andOr-Ilck Hills is unconform-

ably laid on Paleozoic rocks. In thc Southern

Primugodzharic, north-easterti Uscyurt and

northern PriAraÜe, thc Altykuduskaya Formation

lies on the continental deposits of the Aptian-

Albian Karashataukskaya and Kysylshenskaya

Formation. Ifi the western area the

Altykudukskaya Formation has surface oiitcrops.

l’hroughout thc rest of thc région, the deprh has

been determined by boteholes (Zhelezko &

Segedin 1972; LMilcrsky I9S1).

The AJcykudulcskaya Formation mainly consists

of whitc to yellow, siltstones ro conglomérâtes,

unconsolidated clays to gravel, with sandy

concrétions and plant débris. Two sections can

be recognized. The lower unir contains lighr grey

to ycllow-grcy, poorly soited, qiiaitz rich sands in

horizontal or slanting beds. Gravel and pebbles are

found in die sand layers with kaolinitc. The total

diiclciiess of the lower unir ranges from 20-120 m.

Spores and pollen (SPA IV. 1) from early

Cenomanian âge are found in thc lower units.

Fig. 3. — Corrélation of Upper Cretaceous deposits of eastern PriCaspian, Aktyubinskian Priuralie, and western Primugodzharie.

298

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern lirais territories

The iipper portion of rhe Altykudukskaya

Formation is fount] in the western areas and has

wcll preserved selachia (shark teeth) wtiich arc

from the Palaeoanaconu volgensîs Zone of Albian-

early Cenomanian âge (Zhelçzko & Segedin

1972). Flora from the Koldenen-Temirskian

palcoflora (LFA 1) of laie Albian-Cenomanian

age is found in sandy horbons (Shilin 1986).

In the eastern PriCaspian région, transgressive

Cenomanian Coastal and deeper marine deposits

are found on continental Albian rocks. J'he

Cenomanmn roclts in this area consist of yellow-

grey, grcen-grey, yellow, quart/ rich glauconitc

sands, grey sandy clays, and sandstones.

Ammonites of the Kamaroites grossouvrei Zone

(early-middic Cenomanian); selachians of the

Palaeoanacorax ohliquus Zone (early-rniddle

Cenomanian); mollusca of Oxytoma pectinata

Zone (earJy Cenomanian); and foraminifers of

the Gavtdinella cenorruinica Zone (early-rniddle

Cenomanian) are found. The total thickness

ranges Irom 20-40 m (Nevesskaya 1985; Azbel

& Grigyalis 1991).

Idie western Pj’imugodzharie. transgressive depo-

sits of marine quartz sands, sÜtstones and clayey

siltstones of the Nogaytinskaya Formation over-

lics continental deposits of rhe Altykudukskaya

Formation. The total thickness of rhe

Nogaytinskaya Formation is 5-10 m. Typically

clayey siltstones are in the upper portion, wicli

beds of mollusca and .selachians ot the

PaLuvanUCorax obliqum Zone toward the middle

Or'-llek Hills

Southern Primugodzharte

North-eastern Ustyurt

Northern PriAralie

T urgay

marly, chalky, clayey, sandy

marine Coastal rocks

20-170 m

clayey. marly, sandy marine

Coastal rocks, marine rocks

110m

clayey, marly

marine Coastal,

marine rocks

87 m

Zhuravlevsakya Formation

sandy, clayey. marly, siliceous

marine Coastal, marine rocks

_ 5-65 m

clayey, sandy,

marine Coastal,

marine rocks

20 m

® sandy, silty,

5 clayey

4: siliceous marine

Q Coastal,

marine rocks

J sandy,

I clayey

^continental

Coastal'

clayey, sandy marine Coastal,

marine rocks

15 m

I sandy, clayey continental,

Coastal marine rocks

9 m

clayey. sandy. sandy. clayey. .marine rocksi

silty continental silty I 30 m

rocks marine rocks |-;- -j

Iconlinental

_L® m_ 80 m __ I r ocks 30 m

Altykudukskaya Formation

sandy, clayey continental, coastal-marine,

lagoonal rocks

20-160 m

sandy, silty

continental,

semi-rnarine

rocks

25 m

sandy,

clayey

' contin¬

ental

rocks

0-100 m

Fig. 4. — Corrélation of the Or’-llek Hills, Southern Primugodzharie, and Turgay.

GEODIVERSITAS • 1997 • 19(2)

299

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

to lower portion of rhc section. Conglomérâtes

and sandstones are in the botrom of the section

(Zhelezko & Segedin 1972).

Cenomanian-Turonian (Figs 3-5)

The Cenomanian-Tutonian rocks arc widespread

in the Tiirgay trough and represenced by the

Shetirgizskaya Formation (continental to semi-

marine) and Novokozyrcvskaya Formation

(continental). Surface outerops arc only found in

erosional and karst dépressions.

Composition of the Shctirgirzkaya Formation

varies with the area. In the northern part of the

Turgay trough-, the Shctirgirzkaya Formation is

about 10 m rhick, composcd ol grceu-greeu

monmorillonite-beidellite sandy silt)' clay to kao-

linite clay.s with lignite, coal and pyrite. This sec¬

tion lies unconformably on Carbonifereous

limestones, wiili Santonian marine deposits lying

on top of the section (Papulov et ai 1990).

In the soutliern part on vhc Kazalvh Republic, the

deposits arc thicker (up to 60 m) and range Irom

coarse grained sandstones to silty claysiones, with

some plant débris. The lower portion of the

Shetirgizkaya Formation contains sporcs/pollcn

of early Cenomanian âge, whilc the upper por¬

tion corresponds to lace Cenomanian-carly

Turonian. Flora of Cenomaniân' luronian age is

also found ofrhe Ayat.skian régional flora (Shilin

1986). Marine deposits of thé Santonian age lie

on top, while Albian grey clay.s arc at clie base of

the section,

The Novokozyrcvskaya Formation lies on wea-

thered Paleozoic rocks chroughouc the région

Overlying disconformably varies from Santonian,

Campanian, Maasnichtian or Paleogene, depen-

ding on the location. A 43 m section is found in

the Novokozyrevsky' quarry, near the Tobol River

near the town of Okcyabrsk}*. The bottom of the

section coniain.s kaolinito-hydromica clays with

clasts of Paleozoic rocks. A 15 m layer of bauxite,

which is commercially mincd, is présent up in

the section. Fhc top of the section is approxima-

tely 15 m of kaolinitc-gibbsite dark clay with

lignite and coaly plant deposit, with che upper-

raost concaining bauxite with plant remains.

The Novokozyrcvskaya Formarion rhroughout

this région ranges in fhickness from 0-100 m. It

can be characterized by three parts including a

lower coarse grained sandstone, a middie bauxite

bcaring layers, and an upper kaolinire clay with

plant remains. The lower part usually contains

sporcs/pollcn association of early Cenotnanian

age, with the middic and upper layers coiitaining

latc Cenomanian-early Turonian age (Papulov et

al. 1990).

Thcrc arc other Cenomanian- Furonian deposits

in the western side of rhe Turgay trough, deposi-

ced in a lacustrine/coniinental environment. It

outerops in karst depre.ssion and other erosional

régions. Ncâr the Ayat River, an outerop of

approximately 16 m is found. The base of the

section has sandstoncs with Paleozoic weathering

débris. Kaolinite clays with lignite overly grade

into quartz rich sands loward the top of the sec¬

tion. Santonian ooliiic bearing sânds are found

lying conformably ort lire top of chc section. This

deposit contain.s spores/pollen of latc Cenoma¬

nian-early 'Furonian age, with a flora assemblage

of Turonian age called the y\yatskian'

Kazakhstânian flora (Shilin 1986).

In the notth-easrern corner of the Turgay région,

the Upper Creraceous sedimentary scqucnce of

Turgay, is replaced by West .Siberian scquences.

The semi-marine deposits of Shctirgizskaya

Formation (s gradually rcplaccd by tbc semi-

marine West ÿiberian Uvatskaya Foimation,

which contains the Trochammina ivetferi-

Trochatmnfna mbhotinae Zone of late Cenoma-

nian. The radiolarian zonation also cotrclates a

latc Cenomanian age [Cevodiscus ccnomanicus-

Stichocapsnferosia uvatica Zone).

Tuuoman (Figs 3-6)

Continental, marine, and coastal-marine deposits

of Furonian age arc widespread in Southern

Frimugodzliarie, northern PriAralie, and Turgay

i rough in .siihsccrion. The thickness of Turonian

deposits ranges from scvctal merers in the north

to 80 m in the sourh in the Southern Priimigod-

zharie, and increases to 300 m in the PriAralie

région.

in rhe Akcyubinskian Priucalie, deposits of

Turonian age arc found on Cenomanian sand-

siones- along the Ilck Rivet. ATuine clay rich

quartz sandstoncs and clays (up to 12 m) are

found with fuoceramiis and ammonites of che latc

Turonian Inoceramus labiatus Zone and foramini-

300

GEODIVERSITAS • 1997 • 19(2)

GEODIVERSITAS

Foraminifera

Radiolaria

Belemnites

Selachians

Mollusca

Hanzawaia ekblomi

Brotzenella praeacuta

Spiroplectamrnina

kasanzevi

Neobelemnella

kazimirvviensis

Squalicorax

Oxyotoma danica

Gaudryina rugosa spinulosa

Orbiculiforma

renillaeformis

3B/crmnoHs ium. .^Uirtfinais

Qaiifftin'Stfla tancentâîB

Osfemnella hctiâtetf

pristodontus

Oxyotoma uralica

Bolivina kalinini - Brotzenella taylorensis

Amphipyndax

stock!

ejcgr lattgei.

Squalicorax ex gr.

phstodontus

Inoceramus balticus

Sptroplectammina optata

.TlWVOrMW

Spiroplectamrnina senonana pocurica

Prunobrachium

crassum

Balerrtÿf'iCâmdX nitimmitatus

mitcwnnia êHifw

Squalicorax plicatus

AûUnocàmM laevtgat{}*i

Beiemnnella ümecurscr

muaonalitormifi.

Squalicorax lindstromi

Ammobaculites dignus

Pseudoclavulina hastata admota

BeienmHBfla praocumar

praecursoi

Squalicorax kaupi

Oxyotoma

tenuicostata

Goniocamax fundgreni

uUiojs

Squalicorax papulovi

Squalicorax santonicus

Inoceramus

cardissoides

Haplophragmium chapmani

Ammoscalaria antis

Reussella kelleri

Goniocamax tundgrenr

Ivndgreni

Squalicorax falcaîus

Inoceramus

schloenbachi

■A

Goniocamax inîermedius

Squalicorax sagiscus

Inoceramus

labiatus

Palaeonacorax

Intermediumus

O®

Ligulogavelinella globosa

Trochammina tmfîàn

''roctïammtna subOotinae

Rotalipora

cushmani

Stichocaspa

ferosia ufawca

Gavelinella

baltica

Thalmanninnella

deeckei

Thalmanninnella

appenninica

Palaeonacorax

obliquas

Kamaroites

grossouvrei

Oxytoma pectinata

cenomanica

Hoeglundina

goaldorsoplana

Palaeonacorax

volgensis

Fig. 5. — Corrélation of foraminiferans, radiolarians. belemnites. selachians. and mollusca in the Southern Urals région (adapted from Naidin et al. 1984a. b; Naidin & Kopaevich

1977: Azbel&Grigyalis 1991).

Legional geology and stratigraphy, U. Cretaceous of Southern Urals territories

Amon E. O., BluefordJ. R., DeWever P. &Zhele 2 ko V. I.

fers of the late Turonian Gavelinella momltjorrnh

Zone. Santonian rock.? arc found conformably

on top of this section.

In tlie Kazalcli Republie, near Novofedorovsky, a

13 m section lies on Cenomanian sandstones.

The section concains a phosphoritic horizon of

concrétions in quartz-glauconite sandstone. Dark

grey to green grty clayty maris arc found in the

rest of the section. The section is ovcrlain by

Santonian phosphoritic layer.

In the Or’-Ilck Hills area, in the Kirgeldinslcy

graben on the Ural River, the luronian is repre-

sented by micaccous quartz rich sandstones and

siltstones. Inoceramtis lamarcki park can be found

in this région.

The Turonian deposits of the Southern

Priniugodzharic outerop near the flanks of the

Shoshkakolian anticlinorium. In the northern

portion of this area the deposits arc continental,

but become more influenced by marine sédimen¬

tation in the South of the Shoshkakolian Range

area. On the Ustyurt plateau and in the

north-western part ol the PriAralic (Kulandy

Pcninsula ol the Aral Lakc), the Turonian depo¬

sits arc tnarinc. Jn the south-cascern Turgay area,

the Turonian rocks range from continental (carl-

iest sédimentation) co Coastal-mari ne (latcst).

Continental deposits of kaolinicc clays, sand¬

stones, and siltstones are called the Zliirkindek-

skaya Formation in the Southern Primugod-

Russian Piatform

Western Kazakhstan

Crimea, Caucasus,

Carpathians

Hanzawaia ekblomi

Pseudotextularia vahans

Brotzenella praeculate

Abathomphalus mayaroensis

</'

Brotzenella complanata

Bolfvinoides dtaco draœ

Brotzenella complanata

Globotruncana stuarti

Angulogavelinella gracHis

sÿ

Globorotalites embdyensis

BfvUenBlfa mylorsnsts

eol'vma Hatlnini

Ohifri(foicàf?e' voifstanue

Globotruncanita morozovae

Brotzenella monterelensis

Cibicidoides îermirensis

Cibicidoides Clbiadoides

termirensis aktuiagsyensis

Bolivnoides decoratus decoratus

Gavelinella demenUana demetMiana

Gavelinella stelligera

Bolivinoides stngillaîus

Globotruncana fornicata

Osangularia whitei whitei

Gavelinella infrasantonica

Stensioeina granulata perfecta

Globotruncana concavata

Stensioeina exculpta granulata

Gavelinella costufata

Globotruncana primitiva

Stensioeina granulata granulata

Gavelinella kelleri

Globotruncana angusticarinaîa

Gavelinella moniliformis

Gavelinella praeinfrasantonica

Globotruncana lapparenti

Gavelinella ammonoides

Gavelinella moniliformis

Gavelinella nana

Globorotalites hangensis

Helvetoglobotruncata helvetica

Hedbergella tioltzi

Fig. 6. — Corrélation of foraminifera zones from the Russian Piatform, western Kazakhstan and Crimea, Caucasus. and Carpaîhians

{western part of the west European Paleobiogeographic provinces).

302

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern Urals territories

zharie. rtorthern PriAralie, and south-wesccrn

Turgay.

Marine deposirs of Turonian-Coniacian âge com-

posed of greenish monmorillonite with admixtu-

re of kaolinite, with intcrlayers of glauconite

quartz rich siltstones, clayey sÜtsiories, and fine

grained sandstones are found in Northern

PriAralie. The total thickness of thèse deposiis

are approximately 100 ni. Phesc deposics contain

macrofos.sils of the lato 'Juronian Inoceramm

labiatus Zone and Coniacian Imceramus schlocrt’

hacbi7.o\\c (Yanshin 1953).

In the eastern PriCaspian région, late Turonian

deposirs are lighr grey - gtey saiidy limestones,

carbonate sands, with a phosphoritic horizon in

the base. The total thickne.ss ranges from

2-25 m. Thèse marine deposiis contain macro-

tossils of the late Turonian InutTramm labialus

Zone, Squdlicanix sagiikus Zone and the forami-

niferal Gnvt'liuelld monilifonnis Zones. Conti¬

nental depoS'its contain spore/pollên in the

SPA IV.3 Zone.

The Ayaiskaya Formation in lurgay» was former-

ly considered luronian deposks, but is not consi-

dered Turonian in this study. In the

north-eastern région of the Turgay région near

the büundary of the West .Siberian plaiform, the

Turgay faunas are rcplaced by West Siberian fau-

nas. The foraminifera and radiolaria indicate

Turonian âge in the West Siberian Uvatskaya and

Kuznetsovskaya Formations (Amon I9S8, 1990).

Coniacian (Fig.s 3-6)

Coniacian deposirs are absent from the majority

of the région, but arc found in the extreme west,

souch, and easi. Thèse deposirs may hâve been

eroded diiring a very dynamic transgression

during the Santonian-Campanian.

In the Western Primugodzharie région, marine

rocks of Coniacian age are présent. They are

chalky maris, maris and clays with a thickness of

approximately 5 m. In rhe south-wesrern to

Southern Primugodzharie, 1 5 to 20 m of marine

blue-grey sandy limestones with phosphoritic

concrcrions and sandy carbonate claystones are

Coniacian. This depo.sit contains the molluscan

Inoccramm schloenbachi Zone and the foraminife-

ral Gavelifiella kelleri Zone (early Coniacian) and

late Coniacian Gavelinella costulata and

Stcnsioeina gnnuildtd gymntkfd Zone,

In western IVimugodzharic and Akcyubmskian

Priuralic, the upper Coniacian deposits are repre-

sented by the lowcr portion of che Kubleyslde

bedsv which is found in the basal section of the

Koldcnen-Tcmirskaya formation. It is üght

green, fine grained sandstones and siltsiones with

a phosphoritic unit (Zhelezko & Segedin 1972;

Zhelczko 1987, 1988). Upper Coniacian belcm-

nites of the Gonheamax lundgredi lundgreni

Zone and sclachians of the Sqmlicorax fiilçatus

Zone arc found in this horizon. These are trans¬

gressive deposits found on Cenomanian sand-

siones of the Aliykudukskaya Formation: on

maris of Turonian age; and/or on deposits of the

Zhirkindekskaya Formation. In the Turgay

Trough, Coniacian intcrvals arc not found.

Sedimentülogical évidence shows that they were

prôbably eroded. U has been suggested that por¬

tions of the Eginsayskaya Formation, in the

northern part of Turgay, Ls Coniacian. This cor¬

rélation is only possible because the Eginsayslêaya

Formation in Siberia contains Coniacian

fbraminifers of the Haplophrag^mum rhapmani-

Ammosvdlarui antis-Reusella kcllen Zone and

Coniacian radiolarians of the Ommarodiscus

nwbilh'Lon^ (Amon 1988. 1990).

vSantünian-Campanian (Figs 3-6)

Marine deposiis of Santonian-Campanian age

arc found in the western Primugodzharie and

Aktyubinskian Priuralic. Upper Coniacian-lower

Campanian déposas of the Kj^ldencn-Tcmirskaya

Formation includes two lithologie umts. The

lowcr unit is sandy-phosphoriiic Kublcskic Beds

and is 9 m thick. The upper unir is .t phosphnn-

tic siltstone, 17 m thick, cailcd the Zhiiriinskie

Beds. Lower-upper Campanian Zharykskaya

Formation and upper Campanian Kursayskaya

Formation are aiso found in these régions.

Outemps of rhe Koldenen-Temirskaya and

Zharylcsluya Formation on the Ternir, Koldenen-

Tctnir, and Kuhley Rivers hâve providcd a conti-

ruioiis section. ITiis sequence contains late

Coniacian, .Sanronian and early Campanian

deposits.

Light grcen, fine grained sandstones and silt-

stones with a phosphoritic horizon make up the

Coniacian interval. Lower Santonian intervals,

GEODIVERSITAS * 1997 • 19 (2)

303

Amon E. O.. Blueford J. R., De Wever P. & Zhelezko V. I.

ranging from silistones to fine grained sand-

stones, contain cwo pliosphoriüc horizons. Early

Santonian belemnites of chc Qmun'amux limd-

greni uiliciis Zone and selachians of Scp4alicûrax

santonkus Zone and SqUtiUctmix pauhnn Zone are

helpfui ta define tins laycr. Foraminikis of chc

Stensioehm exculpta exculpta Zone and Stensioeina

gmmdnta perfecta Zone indîcace an early Santo-

nian âge. The. late Santonian interval contains

bclemnites of rhe Belemnitclla pmecursorpratxur-

sor Zoncv hivalve.s of the Oxyloma îenuicostata

Zone, selachians of the Squalicomx kaupi Zone,

and foraminifers of the Gavelinella steUigera

Zone. Early Canipanian contains belcmnites of

Actinocanuiiix Itmngana-Beletyinîtdla praecursor

mucronatifomh Zone,^ selachians of Sqiuilicomx

lindstromi Zone, foraminiters of Gavelinella de-

mentiana dementiana Zone and Bolivinoides

decoratm decomtus Zone.

Zharykskaya Formation în western Primugod-

zharie and yVktyubin.skaian I^rjuralie, wa.s deposi-

ted transgressively over the Koldenen-lcmirskayn

Formation. Rhythmically alternaiing layers

(5-7 m thick) of silty, maily, dark grey ro greeiv

grey clay.s, and glauconite liglit grey, yellow grey

siltstones wîlh pho.sphoritic concrétions, reach a

thickness of 40 m in the Zharyskaya Formation

(Zhelezko &c Segedin 1972; Zhekezko I98S:

Naidin et al. 1991). Rocks in ihc lower portion

contain early Campjnian bclemnites of the

Bele 7n n e l lo ca max m a m wHatus-Bele m ni tella

mucronata alpha Zone? selachians of the

Squalicataxplicittus Zone and iorarninifers of rhe

Cihiddoides U'niifT)i>ii Zxjiie. I lie upper portion

of the (-oriTiatlon contains late Campanian

bclemnites ot the Belemuitdln mucronata mucro-

naui Zone, foraminilcrs of Brotzenelln monterez

lensis Zone and Cihicidtndes vollzliinas Zone.

The late Campanian Kiirsayskaya Formation in

the western Primugod/.harie and Aktyuhinskian

Priuralie transgressively lies on tlic Zharykskaya

Formation. The Kursay.skaya Formation is com-

posed ol Galcareous light-yellow-grey .silisiones,

silty maris with isolated phosphuritic concré¬

tions, as well -as phosphoriric horizon toward the

base of the formation, wiih a thickness of 15 m.

Late Campanian bclemnites of the Belemnitdla

ex gr. langei Zone, mollusca of the Inoceramus

balticus Zone, selachians of the Squalicorax ex gr.

pristodonUis Zone, foraminifers of rhe Balivina

kalinini Zone and Brotzenella taylmrnsis Zone are

found in rhis aj'ea (Zhelezko & Segedin 1972;

Zhelezko 1988; Naidin r/(?/. 1991).

In the eastern margin of the PriCaspian Zone,

Santonian marine deposits, nii.ved with

Campanian deposits, arc widespread. The

Santonian deposits can be divided inro lower and

upper units. The hiwer Santonian sédiments are

10-50 m of light grey, green-grey, bluc grey

sandy limesiones, with rare phosphoriric concré¬

tions. liuerlaycrs of calcarcous sands and chalk-

likc, claycy limestoaes arc aiso prcsciu. Fhetc are

belcmnites of tlic Goniocamax lundgreni uilicus

Zone (early Santonian), selachians oi Squali-

rorax santonreas Zone (early vSantonian), scla-

chtans of Squalicorax papulovi Zone

(early-middlc Santonian); foraminifers of

Stensioeina exculpta exculpta Zone (early

Santonian or l.tre Comacian-F.arly Santonian).

Thç upper Santonian sédiments range In ibick-

ness from 5-35 m and are light grey, grcen-grey,

blue-grey sandy clays and limesrones, with rare

pliosphatic and pyritic concrétions. Tbcre are

bclemnites- «T Belemnitdla praecursor praecursor

Zone (late Santonian); mollasca of the Oxytoma

temùcosiata Zone (late Santonian): .selacfiians of

the Late Santonian Squnllcorux kaupi Zone: fora-

minilers of Gavelinella stelligera Zone (late

Santonian or laïc SantonUn-carly Campanian),

The Campanian deposits ot the Eastern

PriCaspian Zone are divided înto lower and

upper sedimentary uniis. Lower (vau^panian

sedimeius (5-.50 m) arc light grey, chalk-like

limestones, maris, calcarcous clays with belcm¬

nites oî Actinocarnox laevigtiis-Bdeninitella prae-

cuxsor mucronatiformh Zone (early Campanian),

Belemnelloctimax mammilaius*Btlemnitella

mucronata alpha Zone (early Campanian); sela¬

chians ot Squalicorax lindstromi Zone (early

Campanian). Squalicorax plivatus Z.one (early

Campanian); and foraminifers of Gavdinella cle-

inentiana derrienîtana Zone (early Campanian),

Bolivinoides decornrus dceoratus Zone (early

Campanian), Cibixidoides temirensis Zone (early

Campanian). Upper Campanian sédiments are

light green to grey, sandy maris, clayey chalk and

range in thickness 5-30 ni. d herc are bclemnites

of Belemnitdla mucronata mucronata Zone (late

304

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern Urals territories

Campanian)» Belcmnitella ex gr kngà Zone (laie

Campanian), foraniinifcrs oi BrotzaiMi montere-

lensis Zone flate (^ainpanian). Cibici’tMfles volt-

zianus Zone (late Campâiiian)» Bolivim kalinini

Zone (late Campanian). and Brotzevelhf tayloren-

Zone (late CaiTipanian) (Naidin 1991)

Santonian-Campanian marine rocki in the nor-

thern portion of PrlAtalie ând souihcrn lurgay

are transgreüsively laid ofi continental furonian-

Coniacian deposits (Papulov & Naidin 1979).

The lower units hâve a thin layer (U2 m) of

conglomcrate which coniains sands', phosphoritic

concrétions, pebbles of argillires, moilu^,ca, shark

teeth, siliciUcd wood, cemented with calcareoiis

clay. Santonian deposits include marine sands

with gra/el and phosphoricic concrétions.

Mullusca of the late Santonian age» Oxytonw

tenuicostata Zone; selachians tif Squtilicohvç kaufi

Zone. Campanian deposits are represented by the

calcareoiis clays and maris with belemnites of

Biiemnitella rnucronntii Schloth., sA.\ foraminifers

ol Early C-ainpanian CJbiddrndes teinireynis Zone

which reseniblcs the Early Campanian Zones of

the Mang}*shUk and PriCaspian depressioas.

In the Turgay Tix>ugh. the Santonian-Campanian

sédiments are represented by the Eginsayskaya

and Ayatkaya Formations. Thiçkness and posi-

tion of these deposits are dépendant on the relief

on which they were lain and the dynamics of

coa.sial marine déposition. The Eginsayskaya

Formation ranges* in thiçkness from 3-]59 ni, is

widespread rcflecting Coastal, shorelinc and

lagoonal deposits. The Ayatskaya Formation is

found oniy in isolated areas (Ayar river near

Taranovskoe, Sokokwsky and Sarbaysky quarrics

near Rudnyi city in Kustanay area) and rcllects

lagoonal sédiments thac are gradually replaced by

the marine rocks of rhe Eginsaysicaya Formation.

The Eginsayskaya Formation is best exposed in

the Kachar quarry (Fig. 6). The Novokozyrcv-

skaya Formation overlics continental Jurassic

deposits. rhe formation is Ceno-manian in âge,

determined by spores and pollen. The sedimen'

tary rocks include intcrlayering of grey-pink

clays, multicolorcd sîlty clays, silty bauxite, hiack

and brown Ugnite, and vi.scous grey clays. The

total thiçkness is 11.3 m.

An unnamed 15.8 m gtoup of rocks overlics the

Novokozyrevskaya Formation. It is analogous to

the Kuznccsovskaya Formation of West Siberia.

Spores and pollen give this group an âge of

Turonian. The sedimentary rodes indude lamb

nated, yellow-grey, quartz rich medium graincd

sandstones and yellow-grey silty clays. This

group is cerminared by a stratigraphie uncoiifor-

mity.

The Eginsayskaya Formation is conipo.sed of

boih Santonian and Campanian rocks, l’hc

Santonian Eginsayskaya Formation is confirmed

by several fossîl groups. A 5.3 m thick horizon of

dark-grcy platy clays with intcrlayering of glau

conite quartzeous siltstones and concrétions of

siderite uses pollen and spores. A 3-3 m horizon

of green-grev siltstones and sandstoncs has évi¬

dence from cephalopods {Baculites)^ bivalves

[Trigoniti), selachian, spores and pollen. Spores

and pollen are nsed in a 3 1 m rhick horizon of

dark-grey, black .solid silfy clays- A 4.1 m thick

horizon uf green-grcy clayey quartz-glauconicc

sandstones and siltstones, with intcrlayers of

sandy dark-grcy days, are in the Ammobaculites

dignits-Pseudodavulina hftsuuta admota foramini*

fer Zone and arc found along with .selachian,

spores and pollen.

In the Maastrichtian Zhuravlevslcaya Formation

cephalopods (hclemnitcs) and foraminifera

(Gandrytna rugo^a spiuulosa assemblage) arc pré¬

sent. interlayering of silicificd calcareous silt-

srtines and opokas (siliceous mudsconcs) arc

found throLighoLic its thiçkness of 6.0 m. A sandy

mari with a thiçkness of 5.0 m contain ccpbalo-

pods (belemnites) and foraminifera of

SipiropUxtammina kasanzevi assemblage. Marine

Falcogcnc deposits lie conformably above the

Zhuravlevskaya Formation.

The Ayatskaya Formation lie.s on 0.6-3 m of

conglomérâtes and sand.stone.s. Deposits up to

7 m are dark-gtey, green-grey glaucoiiiic quartz

rich siltstones with spores and pollen, indicaiing

an early Santonian âge. Mollusca from the

Inoccramus {■ardis:i(jideh Zone (early Santonian)

are found in coarse glauconite sandstones with

bcidellire-mommuriilonite-halioysite clays w4th

sideritic and iron-ore concretion.s (î.5-5 m). This

is followed hy 2 m of green grey to yellow

siltstones and fine grained poorly cemented

sandstones and 1.5 m of dark beidellite-

montmorillonite-halloysite clays with gypsum,

GEODIVËRSITAS • 1997 • 19(2)

305

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

siderite and iron ore concrétions. A red to yellow

brown, yellow grecn oolidc iron ores in sands

and clays is approximately 1-2 m just before a

stratigraphie unconformity. Campanian sédi¬

ments of fine to medium grained diagonally bed-

ded sandstones wiih mollusca make up 2 m. It

coniains laïc Campanian fossils of Pyconodonta

sp., P. cf hippopodmn^^ ActUosP'ea cf. aaitirositrh,

Inoceramus sp., /. cf halticus and foraminifers of

Spiroplec-tammina optaîa Zone.

Sanconian interval concains che spores and pollen

of SPA IV; foraniinifers of Ammobaculites dignus-

PseudoclapHlim bastata adniota Zone, as well as

the bivalves of Turgayan hiocemmns cardissoides

Zone (early Sanconian) and selachians of

Squalicorax santonicm Zone and Squalicorax

papiilovi Zone (early Sanconian), selachians ol

Squalicorax kaupi Zone. Campanian interval

concains the spores and pollen association

SPA IV.5; selachians of Squalicorax lindstromi

Zone (early Campanian); Squalicorax pUcatus

Zone (early Campanian); Squalicorax ex gr. pris-

todontus Zone (late Campanian); mdiolarians of

Prunobrachium crossim Zone (early Campanian),

Amphipyndax stocki Zone (late Campanian); fora-

minifers of Spiropltctammina senonana pacurica

Zone (early Campanian); Spiroplectammina opta-

ta Zone (late Campanian), Bolivina kalinini-

Brotzenella iaylorensis Zone (late Campanian)

(Amon 1987).^

Maastrr:htian (Figs 3-6)

The western portion of the Primugodzharie and

Aktyubinskian Priuralie marine deposits of

Maastrichtian âge are lepresentcd by a calcareous

clay mari of the Zharska)^ Formation. A total

thickness of 15 m of light grey siltstones and

maris contain phosphoritic concrétions throu-

ghout the dcposjt. Maris in the lowcr parr of the

section contain bclemnltes of Belemnella lanceù-

lata Zone, Belemnella sttmensis sumensis Zone,

Belemnella summshprisiodontus Zone; it contains

aiso foraminifers of Angutogavdinella gracilis

Zone, Brotzenella complunuia Zone and

Bolivinoides draco draco Zone. Maris of the upper

part of the formation contain bcicrnnites of

Neobelenmella kazimirovknsis Zone; mollusca of

Oxytoma danica Zone and PseudoUxtularla ele-

gans Zone.

In the castern margin of the eastern PriCaspian

Zone» Maastrichiuan deposits are widespread.

’i’bc early Maastrichtian sédiments are transgres-

sivcly occurring on Campanian rocks and com-

po.sed of chalk, chalk}^ limcscone with belemnttes

of Belemnella lanceolata Zone, Belemnella siimen-

sis sumensis Zone; foraminifers of Angulo-

Fig. 7. — Columnar section of the Kachar quarry reterence sec¬

tion.

306

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Crecaceous of Southern Urals territories

gavelinella giTtcUh ZonCi Brotzenella compldnata

Zone and Bolivivoides dmco draco Zone; thick-

ness is 30-60 m. Upper MaastricJitian sédiments,

ranging froni 12-80 m thick, arc represenced by

the same rocks wirh belemnites ot Neohelemnella

kaztrnirfmensis Z<.ine; mollusca ol Oxytorna dani-

ca Zone; foraminifers of Brotzenella praeacuîa

Zone, Pseudotextularid elegans Zone (Naidin et al.

1991).

In northern PriAraJic and south-western Turgay,

Maastricht ian deposits are transgressivcly deposi-

ted on Santonian-Campanian rocks or Paleozoic

rocks. They arc represented by maris, cbalks,

clayey siltstoncs, calcarcous siltstoncs, sands and

sandstones, cemented by calcarêous clay.

Mollusca, belemnites and brachiopods can bê

found wirhin the 30-50 m thick iormation. Early

Maasirichcian deposits contain belemnites of

Belemnelln lanccolata and foraminifers of

Gaiidryina mgosa spinulosa Zone. The foramini-

fera zone can be correlated to deposits in the

Magyshlak and PriCaspian dépréssion. The Late

Maastrichtian deposits contain belemnites of the

Neobelernnella kazimiroiriemis Zone and forami¬

nifers of Spiroplectammiua kitsitnzei>i Zone,

which can akso be correlated to the Magyshlak

and PriCaspian dépréssion.

In the dutgay area, the Maastrichtian deposits

include calcarêous sandstones and silcy clays, cal¬

carcous siltstoncs, mari, quartz-glauconitc sands

and sandstones of the Zhuravlevskayâ

Formation, This formation ranges in thickness

from 5-85 m and i$ rarely found in outerops

except in the river valleys of the western portion

of the Turgay trough. The Rachat quarry (Fig. 7)

and Ayat River sections are the hesi reference sec¬

tions. Thick Paleogenc deposits cover most of

the Zhuravlevskaya Formation.

7’he Zhuravlcvskskaya Formation contai ns early

Maastrichrian spores and pollen of the SPA 1V.6

and rare belemnites of the early Maastrichtian

Belemnella snmensû Zone. Mollusca of the

Oxywma nraliea Zone ïs fovmd in the nortb-eas-

cern portion of the Turgay trough. Radiolarians

of the OrbicuUforma renillaeformis Zone and

foraminifers of the Gtmdryina rugma Zone reflect

early Maastrichtian.

Lare Maastrichtian intervals contain belemnites

of Neobelernnella kazimiroviensis Zone, foramini-

feis of Brotzenella praeacuta Zone and

Hanzawaia ekblomi Zone (late Maastrichtian)

(Amon 1987).

SUMMARY

During the Cretaceous, microfossils are impor¬

tant to correlate on a global and interregional

scale, especially in the Peri-Tethys area (Amon &

De Wever 1994). The corrélation proposcd by

Koch (1977) is mainly valid for western and

north-wesiern Europe. The zonal scale based on

ammonite and belemnitc zonation ts only valid

for Kuropean Russia, Ukraine, Byelorussia,

Moldavia, and soiithem adjacenr counrries

(Zhamoida 1989, 1994). The zonation shown in

figute.s 5 and 6 can bc used in the Southern Lirais

to help correlate to the East Euiopcan platforni

during the Cretaceous. 'rhe régional stratigraphy

and corrélation arc summarized in figures 3 and 4.

Acknowledgments

Lhis Work has been supported by the Peri-Tethys

programme (projects No. 95-10, 95-18 and

95*19), We arc grarefull to Dr, Jean-Pierre

Bellier, Université Paris VII, France and Sylvie

Crasquin-Soleau, CNRS, UPMC Paris VI,

France, who helped us to improve the manus-

cript.

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on stratigraphy of Cretaceous dcposics of the

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Submitted for publication on 15 Decetnber 1995;

accepted on 15 September / 996.

APPENDIX

CONTENT OF BIOSTRATIGRAPHIC

ZONES

BELEMNITES

• Neobelemnella kazimiroviensis Zone:

Neobelemnella kazimiroviensis (Skolozdr.),

Belemnella sp., B, siimensh snmensh Jel., B.

siirnenshpraearkhangelskii Naid.

• Belernnellci surneusis sumensis Zone*. Belemnella

sp., B, ex gt*. sumensis B, sumensis sumensis

Jel., B. ex gr. lanceolata (Schloth.).

• Belemnella lanceolata Zone: Belemnella sp,

B. ex.gr. lanceolata (Schloth.), B. lanceolata

(Schloth.), B, ex gr. sumensis ]e\.

• Belemnella licharevi Zone: Belemnella sp.,

B. licharevi ]é.

• Belemnitella ex gr. Ljngei Zone: Belemnitella

ap., B. lange{ tangei Schatsk., B. langei minor

Jel„ B. Lmga najdini Kon.

• Belemnitella mucronata mucronata Zone:

Belemnitella sp., B ex gr, mucronata (Schloth.),

Br mucronata mucronata (Schloth.) Arldi.

• BelemncUocamax mammilatus-Belemnitella

mucronata alpha Zone: Actinocamax sp.,

Belemnellocamax mammilatus (Nilss.), Paracti-

nocamax ex gr. p'ossouvrei (Janet.), Belemnitella

sp., B. mucronata mucronata (Schloth.),

B. mucronata alpha Schatsk.

• Actinocainax laevigatus^Belemnitella praecursor

mucronatiformii Zone: Actinocamax sp.,

A. laellignuis Arkh., Paracti nocamax ex gr. gros-

souvrei (Janet.), Belemnitella sp., B. praecursor

media ]c\., B. praecursor mucronatiformis ]ç\.

• Belemnitella praecursor praepraecursor Zone:

Actinocamax sp., A. ex gr. verus Mill., A. verus

fragilis Arkh., Belemnitella sp, B. ex gr. praecur¬

sor Stoll., B. praecursor praepraecursor Naid.,

B. praecursor media Jel.

• Goniocamax lundgreni uilicus Zone:

Actinocamax .sp., A. ex gr. verus Mill., A. verus

frtgilis Arkh., Goniocamax ap., G. lundgreni

uilicus (Kolt.).

• Goniocamax lundgreni lundgreni Zone:

Goniocamax sp., G. intey'tnedius (Arkh.), G. ex

gr. lundgreni (Stoll.). G. lundgreni lundgreni

(Stoll.).

• Goniocamax interrnedius Zone: Goniocamax

sp-, G. intetmedius (Arkh.).

MOLLUSCA

• Oxytoma danica Zone; Teniupteria argentea

(Conrad), Oxytomadanica (Ravn).

• Oxytoma uralica Zone: Chlamys pulchellus

(Nils.s.), PycnodontevesicuLire (Lam.), Oxytoma

uralica Glaziiti.

• Inoccramus haïtiens Zone; ïnoceramus haïtiens

Bochm.. Pyenodontehippopodium (Niiss.),

Acutostrea aff. acutirostris (Nîlss.), Chlamys

spp., Dianchora Libiata (Wahl.)

^ • ïnoceramus azerhaidjanensis Zone: Inoccramus

sp., ht. azerbaidjanemis k\\e\.

• Oxytoma tenuicostata Zone; Sphenoceratnus

angustus (Beyenburg), S. papubvi AtabeUjan,

S. cf. lingua (Goldf.), Inoccramus cycloidcs

Wegner, Oxytoma tenuicostata (Roem.),

Pycnodonîc vesictilare (Lam.), Gryphaeostrea

lateralis (Niiss.), Lopha scmiplana (Sow.),

Acutostrea curvirotris (Niiss.).

GEODIVERSITAS • 1997 • 19(2}

309

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

• Inoceramtis cardùsoîdes Zone: Inoceramus car-

dîssoides Gold-E, 1. pachti Arkh., Korobkovi-

trigonia amudarieusis (Arkh.), K. toholica

Pojark., Chlarnys faujasi (Deft.).

• Inocemrnus scbloenhachi. Zone: Inoceramus sp.»

1. ex gr. L Moenhacht Bochm.

• Inoceramus lahiatus Zone: Inoceramus ctivieri

Sow., L labial us Schloth., L lamarcki Park.,

/. wehsteri Mant., Placenti ceraspLicenta Dckay,

7? arkhangelskii ll)iu, Collsgnonkeras woolgari

Mant.

• Kamaroites grassouurei Zone: Kamaroites sp.,

K. afh subtîLh (lijin), K. grossouvrei (Sem.),

K. mediasiaticum (Luppov)^ Schloenbachia

varians (S(iw.), 5. variam cl. febramata (Sow.7»

5. subvariaiis Sparh., 5. lumtricosa Stieler,

Sciponoceras haculoides (Mant.), Mantelliceras

mantellî (Sow.).

• Oxytoma pectinata Zone: Inoceramus crippsi

Mant., L orhsctdaris Mueiist., L pictus Sow.,

/. orbicularis Miienst., Oxytoma pectinata

(Sow.), Entoliuri orbiculare (Sow.), E. noetlingi

(Sob.), Acutostrea delettrei (Coq.), Amphiodonte

conicum (Sow.).

SELACHIANS

• Squalkorax prhtodontus Zone: Squalicorax pris-

todontiis (Ag.), Pseudocorax affinis (Ag.),

Cretolatnmi borealîs Prim.

• Squalicorax ex gr. prhtodontus Zone:

Squalicorax ex gr. prhtodontus (Ag.)»

Pseudoisurus laevis Lcriche.

• Squalicoiux plkatus Zone: Squalicorax plicaïus

(Priem.), Paraanacorax ex gr. ohruchein

Glueck.. Scapanorbynchus ex gr. raphiodon

(Ag.), Rhaphiûdiscus texanus (Roem.).

• Squalicorax Ibidstromi Zone: Acrolamna acu-

rninata dilatuta Zhel., Protolanina arcuata

(Woodw.)^ Squalicorax lindstromi (David),

Paraanacorax ohruchevi Glueck.^ Eostriato-

lamia ierkhet Glueck, et Zhel

• Squalicorax kaiipi Zone: Acrolamna acurninata

(Ag.), Protolanina aduncata suberecta Zhell.>

Squalicorax kaupi (Ag.), Eostiiatolemia segedini

Glueck, et Zhel.» f. venusta (Leriche),

Scapanorhynchus raphiodon (Ag.).

• Squalicorax papulovi Zone: Squalicorax papulo-

vi Zhel., Eastriarolamia aktohensh Zhel.,

Scapanorhynchus temirensh Zhel., Ptichocorax

dolloi (Leriche), Pt)>chodus deccuirens Ag.

• Squalicorax sautonicm Zone: Squalicorax santo-

nicus Glueck, et ZhcL, Piychocorax dolloi

(Lcriche), Microanacorax praeyangaensis

Glueck., Eostriatolarniâ ex gr. venusta

(Leriche), Cretoxyrhina mantelli (Ag.),

Pseudocorax laevis Lcriche.

• Squalicorax fcilcatm Zone: Squalicorax falcutus

(Ag.), Alicroanacorax ex gr. praeyangaensis

Glueck., Eostriatolamia ex gr. venusta

(Leriche), Ptychodus ex gr. venusta Dixon.

• Squalkorax sagisicus Zone: Cretilantna appen-

dicidata (Ag.), Squalkorax sagisicus Glueck.,

Arwlamna ex gr. crassievrnis Zhel.

• Palaeottnacorax intermedius Zone: Paleoana-

corax intermedius Glueck., Eostriatolamia ex gr.

angustidens (Ag.), Scapanorhynchus ex gr.

raphiodon (Ag.).

• Palaeoanacorâx oblicpuiis Zone: Paleoanacorax

oblicfUHs (Reuss.), Pseudoisurus semiplicatus

(Ag.), Eostriatolamia ex gr. subulata (Ag.),

Cretoxyrhina hasalis (Chebel.).

• Palaeoanacorax votgensh Zone: Parahurus

tnacruthizus (Pict. et Camp.), Cretodus subatus

(Gcin.), Cretoxyrhina denticulata Glueck.,

Palaeoanaeorax volgensis Glueck., Hispidaspis

gigas (Woodw.).

FOR.^VMINIFERA

Maastrichtian, Latc 2

• Pscudotcxtularia elegans Zone: Cibkidoides clh

peatus (Vass.), Gavelinclla danica (Brotz.),

Hanzawaia ekblomi (Brotz.), Pseudotexndaria

degans Rz.eh., PseudotextuUria vanans Rzeh.

Maastrichtian, Late I

• Brotzenella praeacuta Zone: Anornaltnoidespin-

guîs (Jenn.), Brotzenella praeacuta (Vass.),

Cibicides kurgatiicns Neck., GuvelineUa mid-

uuiyensis (Plumm.), Gavelinclla pertusa

(Maiss.), Gavelinella welleri (Pliitnm.),

GlobigerincUoides subcarinatus (Bronn.),

Gyroidinoides globosm (Hag.),. Pseudouvtgerina

cristata (Marss.), Tappania seulmeyisis

(Cushm.).

310

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern Urals territories

Maastrichtian, l.ate, PrLAralie

• Spiroplectammimt kitsanzevi Zone; Anomalin-

bides jiistm Podob., Brotzenelld pseudopapilosa

(Cars.), Bidimina rosenkrantzi R rot/.., fJetero-

stomella fovtolata (Marss.), (^uinqueloculina

fusiformis Putrja, Spiroplectammina kasanzevi

Dain.

Maastrichtian, Late 2, Turgay

• Hanzawaia ekhlomi Zone: Spiroplectinella sen-

gibabensis (Rala-khni.), Gaudrytna gigantica

Subb., Angnlogavelinella caucasien (Subb.),

Hanzauutia ekblomi (Broc/.), Kaneria fallax

Rzeh., Bulirnina erninenta Ehrem., Gueblerina

robusta De Kl as/..

Maastrichtian, Late K Turgay

• Brotzenella pmeaeiua Zone: Spiroplectammina

kasanzevi Dain, Arcnohnlhnina oblique (Orb.),

A. presit (Reuss), Gaudryina nigosa rossica

Balakhm., Gaudryinopsis subbotinac (Kypr.),

Neoflabellina reticidata (Reuss), Valvulincria

procera Podobina, V. hniiata Olss., Gavelinclla

midwayemh (Plumm.), Cibicidoides bembix

kazakhstanicu Neck., Brotzenella praeacuta

(Vass.), Anornalinoides pinguü plngais (Jenn.),

Nonionella kalinini Volosh., Remsella cimbrica

(TroeJs.), R. biU'illuma Ehrem,> Bolivina incras-

sata gig/intea WicJier, Bolivinoides peterssonl

(Brorz.), Rugoglobigerina rugosa (Plumm.),

R macrocepbala Broun.. Clohotruncfina bava-

nensis (Voorw), TritinelLi scattt Rronn., Hete-

rohelix navarroensis Locbl., Pseiidoguem-bellina

kempensis Esker, P. palperba Bronn. et Brown.

Maastrichtian, Early 3

• Bolivinoides draco draco Zone: Bolivinoides

draco draco (Marss.),Co/e/to crispus Vass.,

Gavelinella midwayemh (Plumm.), Rugoglobi-

gerina rugosa (Plumm.), Spiroplectammina

suturalis Kal.

Maastrichtian. Early 2

• Brotzenella complanata Zone: Angulogavelinella

ex gr. caucasica (Subb.), Anornalinoides ukrai-

nions (Wolosch.), Biglobigerinella bijoraminata

(Hoflv.), Bolivifia inorassata. crassa Vass.,

Brotzenella complanata (Reuss)^ Gavelinella

welleri (Plumm.).

Maastrichtian, Early 1

• Angulogavelinella gracilis Zone: Angulogave-

linelta gracilis stell-aria (Vass.), Bolivina decur-

rens (Ehr.), Bolivinoides delicutulus Cushm.,

Bolivinoides peteissoni Brotz., Brotzenella taylo-

remis (Cars.), Cibicidoides bembix (Mauss.),

Gyroidinoides globosus (Hag.), Neflabellina

pracreticulala Hile., Nêflahellina reticulatcL

(Reuss), Osanguiaria navarroana (Cu.shm.).

Maastrichtian, Early, PriAralie

• Gandryim rugosa spinulosa Zone: Ataxophrag-

rnium rimosum (Marss.). Bulirnina quadrata

Plumm., Cibicidoides aktulagayensis (Vass.),

C. spiropunctatus (Call. et Morr.), C. bembix

bembix (Marss-.), Dorothia pupaides ovata.

Podobina, Gaudryina rugosa spinulosa Neck.,

Siphogaudyjina stephensoni dhtincta Podobina,

Spiropkctanmiina kelleri Dain, Spiroplectam¬

mina Viiriabtlis Neck., 5. kelleri Dairi,

ValvuUneria imitata Olss.

Maastrichtian, Early, Turgay

• Gaudryina rugosa spinulosa Zone: Spiroplec-

tanirnina brevis niodesta Kiss., Spiroplectinella

variaspera (Kiss.), S. baudouiniana (Orb.),

Gaudryina rugosa spinulosa Neck., Siphogau-

dryina stephensoni Cushrn., Quinqueloculina

srolley Broiz., Lagena spp., Cuttulina spp.,

Disçorbis parVHs Ehrem., Angtdügavelinella gra-

cilisstellaria Vass,^ A. praecaucasica (Vass.)r

Valvulineriti lenticula (Reuss), Ste^isioeina pom-

merana Brotz., Gyroidinoides mrgidus (Hag.),

G. berescwiemh (Balaklim.), Osanguiaria nava-

roarui (Cushm.), Gavelinella welleri (IMumm.),

G. mira Podob., Cibicidoides vùltzianus (Orb.),

C spiropunctatus (Gall. es Morr.)> C bembix

(Marss.), Brotzenella complanata (Reuss.),

B. menneri (Kell.), Heterolepa orçina (Vass.),

Cihicides ghlngermifimnis Neck., C. gankinoeit'

sis Neck., C kurganicus Neck., NonionelUna

spp., Rheinhold^lla brotzeni Olss., Ephtnrnina

fax Nauss, Praebulimma. carseyae (Plumm.),

Bulirnina spp., Bolivina incrassatainertissata

Reuss, B. decinrens (Ehrcnb.), Bolivinoides deco-

ratmdmcofor77îis Vass., B. draco HÜt, et

Koch., B. seno7iicus Dain, Ptille7iia. kazakhsta-

nica Dain^ P amerieaîja Cushm., Quadrr-

morphina allomorphinoides (Reuss).

GEODIVERSITAS • 1997 • 19(2)

311

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

Campanian, Lare 4

• Brotzcnelht tayhrensis Zone: Boliv'ma incrassata

incrassflta Reuss. Bnlivînoides gigayiteus Hilt. et

Koch, BwtzeneLla taylaremh (Cars.), Globo-

truncana. area (Cushm.)» G. morozovae Vass.,

Gyroïdinoides turgidus (Hag ), Hc-terostomella

praefoveolata Mjatl., Orbigyiyna tnflata (Reiiss),

0. achefi (Reuss), Pseudouvigerina cristata

(Marss.)> Rugoglohigerina kelkrï (Subb.).

Stensioeina fyommerana Brorz.

Campantan, Late3

• Bolivhia kalinini Zone: Bnliintia kaUninl Vass.,

Bolivinoides decoratus dracojormis Vass.,

B, milinris Hilt. et Koch, Eponides frankei

Bror/.., GavelrnelLi cdyeuxi mangyschlakensis

(Vass.), Gemelliides ordnus (Vass.), Globotrun-

cana tnajzoni Sig. et Deb., G. ventricosa White,

Rugoglobigerina rugosa (Plumm).

Campanian, Late 2

• Cibicidfiides vtdtziamis Zone: Cibh idoides volt'

zianus (Orb.), GiU^elinella dememuma laeviga'

ta (Marie), Globorotalites cmdycnsLs Vass.,

Globotruncana morozovae Vass., H'eterostomella

praefoveolata Mjatl., Plectina rinhenica (Reuss),

SitelLî iitevh (Beiss.)

Campanian, Late I

• Brotzenella monterelenüs Zone: Ataxophrag-

mium crassmn caspiurriMz^^.^ Brotzenella men-

neri (Kcll.), Brotzenella monterelensis (Marie),

Cibicidtndes aktulagayensis (Vass.), Globotrun¬

cana linneiana (Orb.), Ilaterostomella praefo¬

veolata Mjatl., Orbignyna sacheri (Reuss),

Sitella carseyae (Plumm.), Voloshinovella lafittei

(Marie).

Campanian, l-ute, PriAralie

• Cibicidoides aktulagayensis Zone; Ataxophrag-

rnium crassum easpium VavSS., Orbignyna ovata

Hag., Voloshinovella laffittei (Marie),

Hetenntomella praefoveolata Mjatl., Eponides

biconvexiis Marie, A. fivnkei Brorz., Gavelinclla

clementiana laevigata (Marie), Brotzenella

monterelensis (Marie), B. uiylotensis (Cars.),

Cibicidoides aktulagayensis (Vas.s.), Globotrun¬

cana itna (Cushm.), G, morozovae Vass.,

Pseudeuvigerina cristata (Marss.), Rugoglobige-

rina kelleri (Subb.), Boüvina kalinini Vass.

Campanian, Late 2. Turgay

• Bolivina kalinini-Brotzenella taylorensis Zone;

Spiroplectanirnina variabilis (Ncck.), Plectina

ruthenka (Reuss), Ataxoplmigmitrn compacturn

Brorz,, A. spongiosum Kriv. A. crassum easpium

Vass., Orbignyna in/lata (Reuss), 0. sucheri

(Reuss), Arenngatidryina granosa Podobina,

Nodosaria spp., DentaUna spp., Valvulsnaides

urnouat (Kypr.J, Globoroialfles erndyensh Vass.,

G', michelinianus (C3rb.), Gyroïdinoides oblk

qiiaseptiitus (AljatJ.), Eponides biconvexus

Marie, Eoponidclla linki Wick., Gavelinella cle¬

mentiana (Orb.) s.L-, Brotzenella taylorensis

(Carsey), AnonutUnoides fahiplancronicus

(Balakhm.), Bolivina kalinini Vass.. B, plaita

Carscy, Bolivinoides decoratus decoratus (Jones),

B. laevigatus Marie, Glohigerinelloides asper

(Ehrenb.), Heterohelixglohulosa (Ehrenb.).

Campanian, Late 1, Turgay

• Spiroplectammina optata Zone: Bathysiphon

vitta Nauss. Thurammina papillatu Brady,

Ammodiscus glabratns CJushm. et Jarv.» Haplo-

phragmoides ruidus crispas Podobina, //. cf.

idanemis Podobina, Haplophragrnium pianum

(Belous.), Spiroplectanirnina hrevis Ki.ss.,

S. multivenurata îüss., S. kelleri Dain, 5, vpta-

ta Ki.ss., Bolivinopsis rosula (Ehrenb.)s Donnhia

pupoides (Orb.l, Ataxophragmium nmosum

(Marss,), Valvulineria lac vie B r o t z.,

Gyraidinoules umbilicatulus (Orb.), Osangu-

laria cordieriana (Orb.), Eponides sibirtcus

Neck., Cibicidoides erik^dalcnsis Brotz.,

C iikîulagayemis (Vass.), Broizcnella montere-

Icmis (Marie), Anomalinoidcs pingnis neckayae

Vass., Allornorphina nomoninoides Dain.

Campanian, Early 3

• Cibicidoides temhrnsh Zone: BoUinnitella galea-

îti Vass., Bolivinoides decoratus decoratus Jon.,

Bolivinoides laevigatus laevigatus Marie,

Cibicidoides aktulagayemù (Vass.),, Cibicidoides

montanus (L3ol.), Cibicidoides temimnis (Vass.),

Eponides biconvexus Marie, Gavelinella dainae

(MjarL), Gavelinella stelligera Marie,

Osangularia conliaiana (Orb.), Plectina conver-

gens (KelL), Stmsioeinapommerana Brotz.

312

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern Urals territories

Campaniaii, Early 2

• BoUvinoides dcconitus decoratus Zone:

Biglohîgerinella algertana Si g. et Ten Dam,

Boli vino id es dec o ra t us déco ru tus J o n.,

BoUinnoïdes gninidutus Hofk-, Eponïdes mosk-

vini (Kell.)v Gavclinclla clenientiana pseudoex¬

colata (Kal.), Globigerinalloides iwlutus

(White), Orbiguyna irreperta Wolosch.

Campanian, Early 1

• Gavelinella clemefitiajta clementiana Zone:

BoUvinoides lacvigarus ftniîimtis Vass., Dorothia

pupoides (Orb.), NeofltibeUinu ntgosa (Orb.),

Gaîfeltnella clementuina dementianu (Orb.),

Gavelinella cLiinae (Mjatl.), Glohigerinelloides

àsper (Elir.), Glohigerinelloides davatus Bronn.,

Globotruncana area (Cushm.), Neojlabellina

rugosa (Orb.)» Reussella pseudospinulosa Troels.,

Stensioeim pommcrami Brotz.

Campanian. Early PrL,\raiie

■ Cibicidoides temirensis Zone: Aiaxophragtyiium

orbignynaeforrnh Mjacl.» Stemioeina nuirsataen-

sis Vass-, S. pùjninerana Brotz, Eponides mosk-

vini (Keller), Osangulariu cordivriami (Orb.),

Gavelinella cosnilnia (Marie), G. dainae

(Mjatl.), G. clementiana pseiidoexcolata Kalin.,

Cibicidoides temirensis (Vass.), BoUvinoides

decoratus decoratus Jon., B. laevigatus laevigatus

Marie, Bolivimtella galeata Vass.

Campanian, E'arly Turgay

• Spiroplectammina senonana pocurica Zone;

Rhabdammina cylindrica (Glaessn.), Bathy-

siphon nodosariaformis Subb., Tburammina

splendens Egger, T. porosa Egger,. Glomospira

corona Cushm. er jarv.. G*, gordialiformis

Podob., Reophax proprius Poclob., R. angustus

Belous., Adercotrynui glnmeratoformis (Zasp.),

Haplophragmaides giganteus Belous., Cribro-

stomoides cretaceus exploratus Podob., C. trini-

tatensis sibiricus Podob.. Labrospira fraseri

propensti Podob., Arnmobaculiîes fiugmentarius

Cushm., Ammomurginulina crispa (Kypr.),

Spiroplectammina senonana pocurica Ralakhm.,

Trochammina boehmi Franke, Gaudiyinopsis

vtilgaris (Kypr.), PseudoclavuUnia hastatu

admota Podob.

Sanronian, Lace

• Gavelinella sidligera Zone; Ataxophragmium

orbignynaefurmis Mjacl., BoUvinoides strigillatus

(Chapm.)) Cibicides excavatus Bruez., Cihici-

doides eriksdidensis (Broiz.), Gavelinella costulata.

(Marie), G. ex gc. sîelligera (Marie), G. stelligem

(Mai*ie)> G. umhiUcatuk (Mjacl.), Globoroialites

mklidinuvms (Orb.), Globotruncana bulloides

Vogl., Üsangitlaria whiteî crassa (Vass.), O. lohi-

tei polycamerata (Vass.), O. whirei praeceps

(Brorz.), O. wbitei wbitei (Brotz.), PraehuUrnina

ventricosa Brot/.., Spiroplectam-mina rosula

(Ehr.), Stensioeina exculpta exculpta (Reuss),

Stensioeina exculpta p'acUis Bror/.., S. granulara

petfecta Koch, ValvuUneria inariei Vass.

Santon ian, Turgay

• Ammobaculites dignus-PseudorlavuUna bastata

admota Zone: Rhizammina sp., Bathysiphon

vitta Nauss, Psnmmosphaera laevigaia White,

Saccammina spp., Ammodiscus cretaceus

(Rcuss), Reophax inordinatus Young, R. gutti-

formis IVjdob., Haplophragmaides tumidus

Podob., H. Cushm., Cyctammina flexuo-

sa Podob., Labrospira spp., Ammobaculites

dign us Podob., A m mosea la ria i n eu Itus

(Ehrenb.), Pseudoclavulina sp., P. bastata

admota Podob.

Sanconian, Early 2

• Stensioeina granulata peifecta Zone: Cibicides

excavatus Brotz., Cibicidoides eriksdalensis

(Brotz.), Prkebulimina ventricosa (Brotz.),

Spiroplecutmmina rosula (Ehr.)» Stensioeina gra-

ntdata incondita Koch, Stensioeina granulata

peifecta Koch, ValvuUneria maiiei Va.ss.

Sanconian, Early 1, upper part ot lace Coniacian -

lower part of early Sanconian

• Stensioeina exadpta exculpta Zone. Cibicidoides

erikedalensis (Brotz.)> Gaudryina laevigata

Franke, GaiseUnella infi'osantoriica (Balakhm.),

Gavelinella utnbilicatula (MjatL), Spiroplectam-

mina rosula (Ehr.), Stensioeina exculpta excidp-

ta (Reuss), Stensioeina granulata granulata

(Orb.).

Coniacian, Latc 2

• Stensioeina granulata granulata Zone: Eponides

GEODIVERSiTAS • 1997 • 19(2)

313

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

concinmis planas Vass., Gavelinella costîüattt

(Marie), Cs, infmsantonica (Balaldijn.), G. thaï-

manni (Brotz.)t Globorotalites mkhdiniamis

(Orb.)j Qsangularîâ ivhitei whitei (Brotz.),

Spiroplectammina embaensis MjatL, Stensioeina

granulata granulata (Orb.)» Valxmlineria laevis

Brotz.

Coniacian, Laie 1

• Gavelinella costulata Zone: Gavelinella costula-

ta (Marie), G. infmsanioriica (Balakhm.),

G. thalmanni (^voVL?!^ OsanguLtria whitei whi¬

tei (Brotz.), Bolivinita eleyi (Cushm.),

Spiroplectammina embaensis Mjarl., Statsioeina

granulata granulata (Orb.)

Coniacian, Early

• Gavelinella kelleri Zone: Bolivinita eleyi

(Cushm.), Eponides concinnus Brotz.,

Gavelinella kelleri (Mjatl.), G. praeinfrasanto-

nica (Mjatl.), Globotruncana renzi Gand.,

Gyroidinoidei targidus (Hag.), Reussella kelleri

Vass., Stensioeina granulata kelleri Koch,

Verneuilina muemteri Reuss.

Coniacian, lurgay

• Haplophragmium chapmani-Amrnnscalaria

antis-Reu^sella kelleri Zone: Ammabacttlites

dignits Podob., Ammobaculoides unicus

Tanach-, Anmoscalaria antis Podob., Haplo¬

phragmium chapniani (Tapp.), Spiroplectam¬

mina senonana oriema/is Kiss., Trochamrnîria

boehmi Franke, T arguta Podob., Discorhis

sibiricîts Dain, Reussella kellen Vass., Eponides

concinnus planUs Vass., Gavelinella costulata

(Marie), G, infrasatitonica (Balakhm.),

Heterohelix spp.

Coniacian, Zauralie

• Discorhis sibiricus Zone: Arenobulimina sp.,

Nodosaria sp., N. zippei Reuss, N. hastata

Schar., Dentalina sp., D. basiplanata Cushm.,

D. tineajomiis Schar, Discorhis D. sihirims

Dain, Stensioeina emscherica Baryschn.,

Valvulineria lentioula (Reuss), Eponides sp.,

E. incognitus Kypr., E. karsteni (Reu.s.s),

G a veli ne lia i nfras ait to n ica (Balakhm.),

G. praeinfrasantonica (Mjatl.), G. sibirica

Dain, Cymhalopora martini (Brotz.), Reussella

>tW/m Vîss., Praebulirnina Heterohelix

Coniacian, Early W Siberia

• Haplopb ragm i u m ch a p rn a n i-A m m ose a la ri a

antis Zone: Amrnobaculites dtgnus Podob.,

A. fiagmentarius agglutinans Podob., Ammoha-

cîdaides unicus Tanach., Amrnoscalaria antis

Podob., Haplophragmium chapniani (Tapp.),

Spiroplectammina senonana orientalis Kiss.

Turonian. Lare

• Gavelinella moniliformis Zone: Ataxophrag-

mmm cornpacturn Brotz., Gaudrylna pariabilis

Mjatl., Gavelinella tnoniliformis (Reuss),

Globorotalites multiseptus (Brotz.), Globotmn-

cana lapparenti Brotz., G. marginata (Reuss),

Hedhergella agalarovae (Voss.), Reussella cari¬

nata Vass., Spiroplectammina praclonga

(Reuss.),

Tiuonian, Late,.W Siberia

• PsèudoôliivuUna hastata- hastata Zone:

Ammôscataria antis Podob., Haptophragnoides

çrikmayi Scelk et Wall., H, rota sibiricus Zasp.,

Pseudoclavnlina hastata hastata Cushm.,

Textiilaria anceps Reuss, Trochammina aiguta

Podob.

Turonian, Early, W Siberia

• Gaudryinopsis filiformis angusta Zone:

Amrnobaculites tuaevi Zasp., Ammomarginu-

lina haplophargoidaeformis (Balakhm.),

Gaudryînopsts filiformis angusta Podob.,

Haplophragmium incomprehemis (Ehrem.),

Labrospira collyra (Nauss,), LiUtomba confusa

Zasp., Trochammina subboîinae Zasp.,

IJvigerinammina manitohensis (Wick.).

Cenomanian, Upper, W Siberia

• Trochammina wetteri- Trochammina subbotinae

Zone: Ammobaculites luaevi Zasp., Neobu-

limina subcretucea (Cushm.), Reophax ïnordi-

natiis Young, Saccamrnina scruposum Berth.,

Thurammina papillata Brady, Trochammina

suhhotinae Zasp., T. wetteri Stelk & Wall,

iJvigerinammina manitohensis (Wick.).

Cenomanian, Lower and Middle

• Gavelinella cenomanica Zone: GavelinelLi bal-

314

GEODIVERSITAS • 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern lirais territories

tica (Brotz/)» G. cenomarnca cénomanien

(Brotz.)> G. cénomanien roncava (V;<ss,),

Glohigennellolcki bentonernh (Morn). G. ultra-

micrus (Subb.), Gyroidinoirics nitidus (Reuss),

G. subconicm (Vass.), Hagenowella chapmani

(Cushm.). Hedbergella caspia (Vass.)»

Ho egl undhia pos tdo rso plana ( Va s s. ),

Lingulogavelinella bïlaniellosa (Balakhm.),

Valvubnerta lentkula lenticula (Reuss), V. len-

ticula plummerae Loetr.

RADIOLARIA

Turgay

• Orbiculiforma renillneforniis Zone; Orbictdi-

forma nniillaefonnk (Camp, et Clark), 0. aus-

tralis Pess., O, regis Pess., Crucetla espartoensis

Pess., Tholodkciis fresnoensis (Forem.), Sticho-

capsa asymhatos (Forem.), Dictyomitra spp.

• Amphipyndax stocki Zone; SpxmgQtrocln^ more-

noensis Camp, et Clark, Orbictdifbnna maxima

(Lipm.), Phasvliforma subcarinata Pess.,

Patellula verteroemis (Pess.), Amphibrachium

mucronatum Lipm., Prunobracthium articula-

tum (L.ipm.), Amphimentum tibiricum Lipm.,

Theocarnpe sibirica Lipm., Amphipyndax stocki

(Camp, et Clark), Dictyomitra spp.. Lithos-

trobus rostomevi Lipm.

• Ikunohrnchium crassnrn Zone: Spongppyle inso-

lita insoliui Kozun, Spongatrocims polygonatus

(Camp, et Clark), Prunobruchium crassnm

(Lipm.), A^riphibrachium ornatum Lipm.,

Porodisciis cretacein. Camp, et Clark, Botryo-

metra amazon (Forem), Thvocampe artirnula

(Gorh.), Inirnersotharax marinas (Gorb.),

Dictyomitra spp,, Littwstrobus rostovzevi Lipm.

• Ommaiodhetis mobilis Zone; Phaseliforma

concenirica (Lipm.), OmrnUtodiscus mohilis

Kozl., Spongodiscus spp., Orbiculiforma spp.,

O. multa (KozL), f^tylarta longispttia Squin.,

Dictyomitra striata Lipm.» D, sorquata Forem.

• Stichocapsa pyranUdaui Zone; Cenosphaera sp.,

C. magna Grig.. ElUpsoxiphus asper Ruest,

Trochodiscus spiniger Lipm,, Spongodiscus spp.

Orbiculiforma spp. Stylûtrochus dolichacanlus

Lipm., Stichocapsa sp., St. pyramidata (Grig.),

Dictyomitra spp,

• Cenodisous cenomanicus-Stichocapsa ferosia uva-

tîca Zone: Cenodiscus venornanious Aliev,

Triadiscm lozyniaki Amon, PeyiiinastriLm kiir-

ganicum Amon, Spongotripus aculeatus Lipm.,

Stichocapsa sp., St. ferosia uvalica Amon,

Çryptamplnmella conara (Horejn*)i Holocrypto-

canium barbai Dumitrica.

SPORES-POLLENS ASSOCIATIONS

Maastrichiian, SPA IV.6:

• dominants: Pinaceat\ Taxodiaceae^ NermapoUes

Pk, Trudopollis PL, nonperfectus PL, T. spe-

ciosus PL:

• siibdominants: Gleichenidites sp., Pinus sp.,

P. aralica Boleb., Concavisporites sp., Mato-

nisporites spp., Polypodiisporites Ep., Laevi-

gatosporites sp,, Cyathidites sp., Cedrus sp.,

Casuariniditex sp,, Triorites sp., Triporopol-

lenites sp., Betidaepollenitcs sp., Kuprianipollis

sp., Ocubipollis sp.,, PUcapallis sp.\

• attendants: CbissopoUis sp., Gneuiceapolleintes

sp., Epbedrim sp,, Triporopollenites rnutabllis

(N, Mtch.) Bratz., T. radiatostriaius (N.

Mtcli.), Triatriopollenites exelstts (R. Pot.),

T. rurensis PL. Subtriporopollenhes amiLitus PL,

Vaaiopollis spp., Nudopollh PL, Extratriporo-

poUeniles PL, ALancicorpus N. Mtch., Aqidla-

pollenites Ruuse et N. Mtch., Proteacidites

Cook. r^Coup., Triprojectus^A. Mtch.;

• microphyToplankton abondant.

Campanian, SPA IV.5;

• dominants: Gleicheniidites senonicus Ross.,

G, laettis (Bolch.) Bolcli., Plicifera delicata

(Bolch.) Bolch., Pinus sp., P. aralica Bolch.;

• subdominants; Concavisporites sp., Matonispo-

rites sp., Polypodiisporites sp., Laevigatosporites

sp., Cyathidites sp., Ariadnaesporites verrucatus

(Elsik) Hills., Cedrus .sp., Casuarinidites sp.,

Triorites sp.. Triporopolknites sp.l Betulacpol-

lenites sp.» Kuprianipollis sp.» IhtdopoWs rector

PL, L hemiperfectus PL, T. parvotrudens PL,

T. sp., Oculopollis sp., Plkapollis serra PL,

P conserta PL, P. sp.;

• attendants; Appendicisporites sp., Ckatricosi-

sporites sp., Hernitelia sp., Balmeisporites sp.,

Vacuopollh spp., Nudopollis PL, Extratripo-

ropollenites PL, Postnormapolles PL, Manci-

GEODIVERSITAS • 1997 • 19(2)

315

Amon E. O., Blueford J. R., De Wever P. & Zhelezko V. I.

corpus N. Midi., Acjuilapollenitcs Rouse et

N. Midi.;

• rare: Canuiroztmosporites Kr,, Taurocusporites

reduncus (Bolch.) Srover, Stenozonotiiles radia-

tus Chl., Divisisporites eukirchcnensis Th.,

Foraminisporis harangaejuis (Nagy) Pacl.;

• microphytoplankton abundant.

Santonian, S PA 1V.4:

• dominants: Gleicheriiidites senonicus Ross.,

G. laetus (Bolch.) Bolch., Plicifcra delicata

(Bolch.) Boldi., Pintis sp,, P. aralica Bolch.,

Cedrtîs parvhaccata Saucr, C, pmlUx Saucr;

• subdomiiiants: Concdvisporites spp., Matoni-

sporitcs spp., Polypodiisporiteî flexHs Chl.,

LaevigaiosporsttJ ovatuf Wils. et Websi.,

Cyathidiies nuUraÜs Coup., C minor Coup.,

C puHctatus Delc. et Sjirum., Gedrus pachîder-

ma. Sauer, Taxodiaccae^ Casiuirinidites cainmoi-

cus Cook, et Rikc, Priorités harrisH Coup.,

Triporopollcuites plivoides Zakl., BetulaepoF

lenites micwexelsm P Rot., Scabratricolpites legi-

bilis Samoil., Kuprumipollîs santaloides (Stelm.)

Kom., K. vlegitns (Zakl.) Kom., Complexiopollis

spp., Viicuopullis Vf pyriimisV\.\

• attendant.s. Appendicisporitcs sp., Cicatricosi-

sporites%Ÿ.^ tiamielia mirabilis Bolch., //. sepa-

rata Chl.. H. sp., Balmehporites ntius Kond.,

B. striatus Koiid., B. sp.. Thûrnsonipollis

magfiijiats (Th. et Pf.) Kr., CornavipoUis Pf.,

Multiporopollenites sp., Bombacacidites sp.,

Liliacidites sp., Ahuocolpites sp„ Symplocaeites

sp., Proteacidites sp.. Tripotopollenites sp.,

TrudüpoUis sp.;

• rare: Camarozotiosporites Kr., Taurocusporites

reduncus (Bolch.) Stover, Stenozonotriletes

radiatus Chl.» Dildsisporites ettkircbenemis Th.,

Foraminisporis barangaetisis (Nagy) Pacl.;

• microphytoplankton abundant.

Turoniaii, SPA 1V.3:

• dominants: Gleiheniidites spp., Selaginella

spp., PUcifera delicata (Bolch.) Bolch.,

Pinaceue;

• subdoniinaïus: Fauroaisporites reduncus

(Bolch.) Scover, Cyarhidites australis Coup.,

C. spp., Hemitelia maxonii Ros.> Matonia-

sporitcs spp., Lygodinm. spp., Contignisporites

perplexus Sind., Laevigatosporites ovatus Wils.

et Welist-, Polypodiisporites fïexns Clil.,

Retitricolpites spp., Tricalpites cf retiailatus

Cook., r erugatus Hedl. et Norris, Quercites

sparsus (Marr.) Samoil., Araliaceac^ Rulacraey

NyssapoHemtes sp., Polyporites clarus N. Mrch.,

Monocolpites bisutcus Mart., Liliacidites sp.,

Disulcites reticidatiis Pot , Erteipites sp

• attendants: Camarozonnsporites ratus Kr.,

C spp., Concavisporiies kainopbytkns Voron.,

C jiincturn (K.-M.) Semenova, Kornilovites

crispus K.ilm., K trisegmentatus Kalm.,

Cicatriensisporites perfhratus (Marr.) V'oror.,

C exilioides (Mal.) Voron., C dorogemh Pot.

et Ccll., Appendicisporites sp.. Anémia sp.,

Complexiopollis Ph, Kuprianipollis Kom.,

Furonipollis Ameron, Tricvlporopolleniies Pf,,

Triaritesx

• microphytoplankton rare.

Late Cenornanian-early Turonian, SPA 1V.2:

• dominants: Gleiheniidites sp., G. senonicus

Ross.» G. laetus (Bolch.) Bolch., G. stellatus

(Bolcli.), PUcifera delicata (Bolch.) Bolch.,

Pinaceae\

• subdomiiiants: Cyathidites australis Coup.,

C. spp., Hemitelia maxonii Ros., Matonia-

sporites .spp., Lygodium sp.. Z., japonkforme

E. Iv.. granulatum E. Iv., Contignisporites

perplexus Slng., LaciLgatosporites ovatus Wils.

et Webst., Polypodiisporites flexus Chl.,

Retitricolpites verrnimurns Brenn., R. granosus

lledl. et Morris, /?. mdgaris Pieite. Tricalpites

cf. reticulatus Couk., T. erugatus fledl. et

Morris, Rottsea rnkilipollU .Srivast.. Viburnum

sp., Quercites sparsus (Mart.) Samoil., Aralia-

ceacy Rutüceacy Nyssapolknifcs sp., Polyporites

clarus N. Mich., Monocolpites bisukus Mart.,

Liliacidites sp., Disulciref reticulatus Pot.,

Erkipites sp.;

• attendants: Camarozonospontes ratus Kr.,

C. spp., Concavisporites kainophyticus Voron.,

C junctum (K.-M.) Semenova, Kornilovites

crispus Kalm.. K. trisegmentarus Kalrm.,

Cicatricosisporites perforatus (Mart.) Voion.,

C. exilioides (Mal.) Voron., C dorogensis l*ot.

et Ccll., Appendicisporires sp.> Anémia sp.,

Complexiopollis Pf., Kuprianipollis Kom.,

TurenipoUis Ameron, TncolporopalImites Pf.,

Triarites sp.;

316

GEODIVERSITAS » 1997 • 19(2)

Régional geology and stratigraphy, U. Cretaceous of Southern lirais territories

• rare: Taurocusporites reduncus (Bolch.) Stover,

T. segmentatus Stover, Foraminisporis wontha-

giensk (Cook. Detcm.) Detrm.;

• microphytoplankcon rare.

Early-micldle Cenomanian, SPA IV. 1:

• dominants; Gleiheniîdites sp., G. senonicus

Ross., G. Lietiis (BoJch.) Bolch., PwuSy CedruSy

Podocatpus, Dacridium.j Phyllocladites;

• subdominants: Dicksoiiiaceae^ Cyntheaceae,

Matonïaceâe, Polypodiaceue^ Lygodium sp.,

L. japonicifonne E. Iv.;

• attendants: Lophotriletes, Hymenozonotriletes,

Camarozoïwsporites^ Concavisporites^ Cicatri'

cosisporites sp., Appendicisporites sp.. Anémia

sp., Cascanea luikhraneevi Bolch., Tricolpites

sagax Norris, T, alhiensis Kemp., Cipuliferoi-

daepollenites minnttis (Brenner) Sing., Platanus

orientai!forrnis Samoil., Menhpemium turonP

cum N. Mtch.. Quercites sparsus (Mart.) f. ves-

CHS Samoi 1., Rhamnaceae ;

• rare: Cingiiulatisporites eiikirchensoides Delc. et

Sprum., Taurocusporites reduncus (Bolch.)

Stover, Peromonolites reticulatus Brenner,

Typha sp.

FLORA

Leafy flora assemblage LFA 1:

• Asplénium dicksonianum Fieer, Onychiopsis psi-

lotoides (St. et Webb) Ward, Gleichenia sp.,

CJadophlebîs foergeissenii (Heer) Vachr., C. kîd~

densis Vachr., Sphenopteris sp., Nissonia

kazachstanica Vachr., Otozamites jarmolenkoi

Vachr., Zamiîes ? sp., Podosamites ellipsoïdes

Sap., Séquoia heterophylla Vclen., S. fastigata

Fdeer, Magnolia sp., Menispermites hyschto/ovi-

r/i;7 Vachr., Myrica ? kuldensis Vachr., M. zen-

keri (Etr.) Hccr., Platanus psendoguillelmae

Krass., P. cuneiformis Krass, P golenkinii,

Vachr., P. prirnaeva Lesq., P. newberryana

Hcer., Dalhergites sewardiana (Shap.) Vachr.,

D. simplex (Newb.) Sew., Leguminosites ovalifh'-

lius Hecr, Acer janscbinii (Vachr.) Vachr.,

Ziziphus menneri Vachr., Vitis cretacea Vachr.,

Cissites uralensis Kryshc., Aralia formosa Hecr,

Diospyros prirnaeva Heer, Dicotylophyllum

rhomhoidale Vachr.

Aktyubinskian Priuralie, Western Primugod-

zharie, Upper Albian-Cenomanian.

So callcd Koldcnen-Temirskian flora (according

to Shilin, 1986).

Leafy flora assemblage LFA II:

• Regnellidium sp., Taxites kasachstanica Shilin,

Magîollia alternans Heer, M. amplifolia Heer,

Laurophyllum sp., Platanus sp., P pseudoguilleF

mae Krass., P cuneiformis Krass., Celtidophyl-

lum praeustralc Krass., Dalhergites simplex

(Newb.) Sew., Ilex sp., Ziziphus ajatensis

Vachr., Diospyros prirnaeva Heer, Eucalyptus

uralensis Vachr.

Turgay trough, Cenomanian-Turonian.

GEODIVERSITAS • 1997 • 19(2)

317

Mesozoic radiolarians from

the European Platform: a review

Patrick DE WEVER

Laboratoire de Géologie, Muséum national d'Histoire naturelle, URA 1761,

43 rue de Buffon, F-75231 Paris cedex 05 (France)

Valentina S. VISHNEVSKAYA

Institute of Lithosphère, Academy of Sciences, ILSAN,

22 Staromonetny, 109 180 Moscow (Russia)

De Wever P. & VIshnevskaya V. S. 1997. — Mesozoic radiolarians from the European

Platform: a review, in Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigraphie

corrélations, Geodiversitas 19 (2) : 319-381.

KEYWORDS

radiolarians,

Peritethys,

Mesozoic,

Silica,

plankton.

ABSTRACT

This paper is primarily concerned with providing an overview oF studies on

Mesozoic radiolarians and présents a general background of living radiola¬

rians and the dift'erent stages they go through (the filters) from their State as

plankton to their State as fossils, as geologists find rhem in rocks. Tlïis is fol-

lowed by a review of the main publications documenting radiolarians world¬

wide since their discovery. The main purpose of rhis paper is to présent to

westerners the various work related to the eastern European platform coun-

trie.s (European part of rhe former Soviet Union) as the majority of these

papers are writren in languages unfamiiiar co most geologists. We hâve therc-

forc chosen co présent here their hisrorical background, and their lociuion, as

precisely as possible, in order to allow further comparisons.

MOTS CLÉS

radiolaires,

Péritéthys,

Mésozoïque,

Since,

plancton.

RÉSUMÉ

Nous présentons ici un survol des études ayant porté sur les radiolaires méso¬

zoïques. Nous nous intéressons d’abord au contexte général des radiolaires en

tant qu’organismes vivants et aux étapes qu’ils Iranchisscnt (les filtres) depuis

leur état d'organisme planctonique (usqu’à leur état de fo.ssilcs, tels que le

géologue les rencontre dans les roches. On envisage ensuite les principaux

travaux à travers le monde permettant de mieux les œnnaîïrc, depuis leur

découverte. Le principal but de cet article est de mettre à la disposition de la

communauté occidentale les résultats portant sur la partie orientale de la

plate-forme européenne (partie européenne de l'ex-Union Soviétique), ces

Travaux étant le plus souvent difficile d’accè.s à la plupart des géologues. Nous

avons donc choisi de présenter ici leur contexte historique, et leur localisa¬

tion, aussi précisément que possible, afin de permettre leur utilisation et des

compaiaisorts ultérieures.

GEODIVERSITAS • 1997 • 19(2)

319

De Wever P. & Vishnevskaya V. S.

INTRODUCTION

Stratigraphical corrclation has been hampered by

lack of world-wide cooperative studies, Now thar

scientific exchange is casier berween Eastern and

Western workers tlie solutions to ni.tny stratigra¬

phie problcms may be found through joint pro-

jects and enable researchers vo compile a more

complété fossil record. Improved networking can

now allow interested workers to develop modeJs

that will facilitate more accurace incerpreraiions

of geological basJns. The goal is to make biostra-

tigraphicaJ basin analyses a more u.seful tool boîli

for industry and for academies. Some fossil

groups have been studied for a long time, arc

relatively wcll known and their corrélations bet-

ween sevcral basins are possible, even thongh still

imperfect. On the contrary, other fossil groups

rcmain almost ignored wich potentially impor¬

tant groups often overlooked as stratigraphie

tools. The utility of these groups is excellent

when sy.siematic conformiry is applied by the

specialist communkies. The changing reknion-

ship of some fossils groups wich other groups

often signais changes in basin and océanographie

conditions. Taxonomie and stratigraphie syn¬

thèses are publishcd or in préparation from

Tethyan régions but often no corrélation is pos¬

sible wich gcographjcal areas which werc under

Boréal influence. This gap in otir knowledge

results from; (1) different paUeogeographic

domains (Boréal jfs Tethyan); (2) rhe fier that

much of the Boréal data was acquired m eastern

countries where mechods and technica] mcans

are different U'.e. no common use of the scanning

électron microscope). Contparisons berween chc

relevant fossil assemblages are problematical partiy

because of the inaccessibiliry of much of the

published literaturc, especially in référencé to the

taxonomy, and partly because of rhe iack of good

photographie illustrations in rhe published

monographs.

In order to progress towards rhe corrélation bet-

ween Boréal and Tethyan basins it is firsc ncces-

sary to .standardise the different biological

chronometers of rhe existing studies available.

The objective Ls to consolidate information st)

that other geologists interested in these deposits

can use rhe imerrelationship of microlossils as a

valuablc tool. Other indirect beneflts are to be

able to understand Russian Verminology in iratis-

larion, and eventually. standardise tenns. Our

project will be accomplished by developing a

three-fold process, each part of which can bc car-

ried out simuhaneousiy. Firstly a State of the

knowledge has to be scitled; this is chc objective

of the present paper. Secondly the systematics

must bc dealt with (re-examinarion of the taxo-

nomy of somc sclected fossil groups from west¬

ern basins and from the Russian Platform,

Caspian Sea Regiorit Siherian Lowlands, North

Kazakhstan, ... which have been worked on by

many spécialises), fhirdly. to develop biostrati-

graphical and palaeoenvironmental application

by comparisons of lithology, géologie history,

abondance and diversity wich other fossils, This

enormous lask will then allow problems to be

jointly stated and solutions to be recorded.

To exrrapolare the original biological environ-

menMl -signais from the geological fcalurcs recor¬

ded requires a gotïd knowledge ot (i) successive

filcers which have changed it and of (ii) the origi-

nators of these signais {Le. the radiolarians),

Radiolarians have existed since che Cambrian

(Nazarov 6c Ormiston 1993) and comprise seve-

ral thousand species. They w-crc disregarded for

stratigraphie purposcs for a long time, but since

Riedel {1952, 1957) proved their stratigraphical

worth, they have been studied more thoroughly,

especially since the 19S0s and their high value is

now cstablished. Because of the difflculty extrac-

ting radiolarians from siliceous rocks, the first

zonations were only proposed for the Cenozoic

and the Mesozoic during late 1970 s (beginning

with ihe Cretaceous then rhe Jurassic and lacer

for Triassic times) and for the Palaeozoic since

the 1980 s.

INTERPRETATION OF OBSERVATIONS

The initial stratigraphie problems were due to

the initial taxonomy which u-sed an unnaiural

taxonomie System and which did noi reflect phy-

letic relationships. 3lii.s phase in rhe progress of

Cenozoic radiolarian ta.xonomy and stratigraphy

has depended largely on material collected. As

more natural groupings replace the artificial ones

320

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

of Ehrenberg and Haeckch généra and familles

chat extend from PaJaeozolc to Mesozijur, or from

K4esozoic to Ceaozoic> become the peculiar-

ity rather ihan the iule (Riedel iy67b). The

Hacckelian syscem of radiolarian classification

now persists in use only to the extern that the

arduous t;uk of the tracing of phyleiic rclation-

ships remains incomplète. Disputablc laxonomy

for some radiolarians hampers the regisicring of

assemblages in their entirety, at the levcl of spe-

cies. many taxa are variously dclimited by diffe¬

rent authors, so thaï a work bas Utile utiluy

unless it describes and illustrâtes (or icfers to a

published, illustratcd description of) the mor-

phological variability invoivcd for each namc. A

perplexing decision to be rcquired, at the begin^

ning of an investigation of radiolarian strarigra-

phy, is the cxient to which it is appropriate to

quaiuify abundances of taxa. It is gcncrally unsa-

tisfactor)'^ to record onlv présences and absences,

because the observation of hundreds of spéci¬

mens of a taxon in an assemblage cleaiiy carries

more wcighi in interprétations than does a single

spécimen. And an absence recorded after sear-

ching througb few spccimens bas less mcaning

than one recorded after searcliing throiigh ten

thousand. On the other h.md, it can be a futile

effort to coLint abundances wilh gréai précision,

unless detailed palaeocnvironmental interpréta¬

tions are the main goal. When thousands of spé¬

cimens are présent on each slitle, as it is

commonly the case in Cenoxoic radiolarian stu-

dies, it is possible to conducr a middic policy

berween excessive and insiifficietit c]uanrification

by estimacing hovv many specimens miisr be sear-

ched througb, ta find a certain number of spcci¬

mens of the t,i\on being recorded, and rben

converting ihls number lo a ratio of the total

assemblage. The rcsulting estimâtes of abundan-

ce are iiscful not only for the weighting of bios-

tratigrapbic events but ai.so for broad-scale

palaeoenvi I on mental indications. Préservation of

tbe radiol.arians is anorher important factor in

stratigraphie interprétations, for tbe rccording of

which therc arc not, as yet, any satisf.ictory

conventions. It is not unusual for authors to

record asscml^lagcs as ‘wcll vs poorly presert'ed”,

‘Mightly VS greatly corroded”, etc., and thèse

indications are useful in evaluating the signifi-

cance of absences of délicate species from the

assemblages, or concentrations of particularly

robust species.

From plankion to rock

Radiolarians, présent in all océans and open seas,

arc floaiing predaiors and include in rheir cy'to-

plasm symbiotic algae (zooxanthellae) which also

contribuce to thcir nutrition. Sevcral groups of

radiolarians hâve a high endoplasmic content uf

oil-droplets. A connection with volcanisni, which

has aiway.s been presumed. is crroncous.

Radiolarians live in the upper part ot the waier

column and do not require a deep océan. A laii-

tudinal distriburion does exist for radiolarian

associations. Ii is also possible to differenriate

surface from subsiirface assemblages. In sédi¬

ments below upwclling sites a mixture of fauna

systemaiically occurs; cold and warm-water spe¬

cies as off Peru wherc Ancarciic waters arc mixed

with tropical waters (De Wever et al. 1995,

NAUTIPERC), surface and subsiirface waters as

off Somalia (Caulci et al. 1992). flence, the

chances of disiinguishing Tropical-Tethyan as

against Boréal fauna when working on fossil

radiolarians extracied from radiolarite are almost

non-existent since radiolarite faciès resuit from

upwclling .Systems (De Wever et al. 1994, elf). tt

is thcTcforc necessary' to invcsligatc radiolarians

from other f.tcic-s lo be able to depict biopro¬

vinces and rbe sédiments of the Russian plat¬

form, having borh Tethyan and Boréal

influences, are good candidates. Pnlycysrines (a

Superorder), with their siliceous skeleton, are the

only radiolarians s.t. which ,arc preserved as fos-

sils. At présent, among Polycystines, the order of

Nassellarians are the most diversified, alrliough

chose of the order of Spumellarians seem to be

the most abundani (Lombari &C Bowden 1982).

After deaih, an individual test is at Icast partially

di.ssolved during ils setriing through the water

column, then while ir lies on the sea floor and

finally within the sediment. Mo.st of the radiola¬

rians that scltlc occur in faccal pcllcfs. Sédiments

deposited at the same time as the bioca tend to

average ont the background variations such as

seasonal changes. Robust forms and those of

blooms are over-represented in sédiments when

GEODIVERSITAS • 1997 • 19(2)

321

De Wever P. & Vishnevskaya V. S.

comparée! with rhe common plankton (vSwanberg

& Bjorklund 1992). The numbers of individuals

and specics arc lowcr in sédiment (and a fortiori

in the rock) than in plankton. Ir is esrim.ired rhat

less than 1% of rhe sUica fixed by planktonic

organisms in surface waters is preserved wirhin

rhe geologicaJ record. This différence is greater

when planktonic individuals are not abundanr.

Radiolarians may be abundanr in relarivcly shal-

low basins close to a shoreline where prevailing

Chemical condilious lavour iheir prcservaiion

and where detriial inpui is very low, e.g. lhe

Santa Barbara Basin, ofF California at a depth of

below 500 m (Kling 1979). Other cxamplcs can

be quoted in Norwegian fjords (Swanberg &:

Bjorklund 1992). Abundanr radiolarians and

foraminifers frequently share the same geogra-

phical water domains but in sédiments tliey are

ofren murually exclusive: when siliceous fossils

are preserved, caJeareous ones are noi and tncc

versa, Radiolarians behave as otber planktonic

organisms: the mosr important factor being rhe

abundance of nutriments, not rhe abundance of

silica. A scénario where transgressions arc associa^

ted wirh a significanr input of organic marter

and a radiolarian bloom has been proposed by

Sreinberg (1981) for rhe main epochs of silica

déposition.

The biogenic silica Opal-A is unstable and trans-

formed into Opal-CT then inro quartz.

Transformations from opal ro quartz are sépara-

ted by a liqiiid stage (Carr & Fyfe 1958;

Mizutani 1966). Température and rime srrongly

affect silica diageneric phases (Murata Larson

1975). Hence, chert prevails in older or deeper

sédiments and porcelanites in younger or shallo-

wer ones. Silica phase transformations arc

accompanied by porosity réduction. The original

porosity i.s higher when ihe sediment is richcr in

silica and during diagenesis (Isaacs 1981). L'or

the geologist, the porosity dccrease (volume) cor¬

responds tu a diminishing of oïdy one Jlmcnsiorî

(the thickness) and the important decompacting

factor has ro be taken inco account when accu¬

mulation rate and palacoproductivlty calcula¬

tions are made (De Wever et ni. 1994). In

addition to pressure and température, rime

favours both opal transformations. Cherts thus

aie more prévalent in older sédiments (Palacozoic

and Mesozoic) and porcelanites in more recent

ones (Cenozoic). The transformation of Opal A

ro OpahCT is esrimared to oeem at 25-50^^ and

takes 20 m.y. in areas uf low to inoderate sédi¬

mentation rates and 5-10 m.y. in areas of high

sédimentation rates (Kastner 1981). lhe

Opal'CT to quartz iTansformacion occurs wirhin

40-50 Ma (Keene 19/6). Ail the possible modifi¬

cations which affect a radiolarian test {dissolu¬

tion in the water coluinn, near the

sediment-intcrface and during diagenesis) after

ics dearh are so grear rhat the chances for a skele-

ton to be obseiwahle by a geologist are almost

zéro, especially when onc adds the ciching with

hydrofluoric acid to free the test from ihc rock in

the laboratory.

POTENTUL IMPORTANCE OF RADIOIARIAN

CONTRIBUTION TO MARINE PETROLEUM SOURCE

ROCKS

As shown by Lisitzin (1971), rhose areas in

modem océans thar hâve high organic producti-

viry are invariably rich in diatoms and/or radiola¬

rians, and lhe.se arc dcpositetl in chc bottom

-sediment. Primary production of organic matter

in the present-day marine environments is main-

ly as.sumed by various group of unicellular,

microscopie planktonic organisms. Radiolarians

were probably an important produccr during

Palaeozoic and early Mesozoic rimes when plank-

torfic foraminifers, coccoliths and diatoms had

nor eniergcd (Ormi.sron 1993). Production of

biogenic silica and marine organic matter both

resuk from a Ingli planktonic activity (Takahashi

1986; Diester-Haass et al. 1992; Caulet ei al.

1992: Saruthein et al. 1992) but do not aiways

remain associated in .sédiment (De Wever &

Baudin 1996).

Somc source rocks hâve their kerogen présent as

strucrurcless, amorphous matcrial not aitrihut-

ablc to any spécifie organism. It is not uncom-

mon, however, to read référencés to such

sriucturcless amorphous matcrial as being of

“■algal" origin despite a lack of rigorous proof. It

is suggested by Ormiston (1993) that radiola¬

rians, which are a common bioiic élément in

source rocks, could bave contribured significant-

ly to their organic richness as they are known to

322

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

conrain significant concentrations of lipids, even

though the identity of tliosc lipids tcmatns a

mystery. A steady contribution of radiolarian

lipids CO océan sédiments could hâve bccn

mcdiated by the minute faecal pellets (minipcl-

lets 10 ro 30 pm in si7.e) these organisms hâve

recently been found to producc (Gowiiig &

Silver 19H5). The main biochcmical cornponents

of radiolarians consist of carbohydrates, prorein

and lipids, the lattcr bcing an Lmponant compu-

nenr of organic molecul.cs accrctcd in the sédi¬

ment. Certain colonial radiolarians are

particularly lipid-rich (Anderson 1983)- The

organic carbon content ot such colonial radiola¬

rians is, narurally, high [f this lipid-rich material

aecretes in subsianrial amounts in ooeanic sédi¬

ment, it ought to be a significant contribuior to

organic richness oF rhose sédiments. Some

modem colonial species which arc lipid-rich (sec

illustrations in De Wever 1994) and bave a pre-

servable skclcton arc abundantat certain rimes of

the year lu occanic vvaters. Calculation reveals a

significant potential contribution of lîpid input

to modem océan sédiments by colonial radiola¬

rians. Wc can reasonably infer that ancient radio-

laria aiso conrained substatuial lipid-rich

vacuoles as these are so important, both'as a food

resource and as an aid to flotacion. Radiolarians

are predators and feed from a diverse range of

Food sources (Swanberg 6c Anderson 1985)

which suggests that they would hâve access ro

such a sélection of molécules that cheir bioche-

mical make up might bc highly varied. More-

over, theit symbionts conrribute ro an important

extent ro the lipid dropicts incliidcd in cheir cen¬

tral capsula, eitlier direcily or indircctly

(Anderson 1983). l'he dircetness of the pathway

from these symbiotic algal cells to the lipid dro-

plet of radiolarians suggest.s thaï thosc lipid dro-

plets in radiolviri.ms might hâve molécules wirh

an "algal signature^ Research is still needed to

recognise possible bionuu’kcrs în living radiola¬

rians. The identification of a diagntjsric radiola¬

rian would not only provide a meaiis te» idencify

radiolarian conrriburion to Üpid-richness ol

ancient sédiment. Ac ieast until such chemical

evidence i.s available one .should include palaeon-

tological study of body fossils in aiiy scudy

attempting palaeoenvironmental characterisation

of such sedimentary rocks because of sc'veral Fac¬

tors: (1 ) silica may act as a dilureni of the organic

matter (Bogdanov et uL 1980; Aplin et/il. I992)î

(2) porosirt^ bas an important rôle in the préser¬

vation or otherwLse of the organic matter, per-

miiting exchanges, oxygénation or action of

sulphaies which clestroyed il (Aplin et fd. 1992),

To conclude, there is a relation beeween organic

mauer and silica but rherc is more than one para-

meter thaï influences their abundancc in sedimen-

rar^ rocks and rhese facror's identity and

importance are not well idendfied yet. They boch

resuit from a high productivity but, as their condi¬

tions of préservation are not the same, diey are not

systemarically associated in sedimentary rocks. It

would now be of grear interesv lo compare these

Mesozoic depositional sites with some other rela-

ted faciès such as phranites of Western Europe.

HLSTORICAL BACKGROUND

In order to présent a general scope of the studies,

we have chosen to address rhe general State of

world'wide knowledge, wirh spécial emphasis on

Europe, before providing ail rhe information

from Russian plarform in a more detailcd form.

AUhough Ehrenberg (1854-1856) had sufficieut

marine sédiments and land-based samples U) pro¬

vide a general portrait of Cenozoic radiolarians,

he did not possess good Mesozoic samples.

Consequently it was Zittcl (1876) who dcscribed

the firsi fcw Crcraccous radiolarians from nor-

thetn Germany. Al about ihe cime that Haeckel

(1881, 1887) was publishing hi.s taxonomie Sys¬

tem of radiülariati.s collectcd by the Challenger

Expédition, Rüsr (1885, 1898) was working on a

broadly based investigation ot European

Mesozoic and Palaeozoic assemblages. Ruse

applied Haeckel's gcneric names, iniciaced for

Cenozoic radiolarians, to his pre-Cenozoic

forms. An unlbrtunate conséquence is thar many

of the généra introduced by llaeckel in 1881

hâve, as type species, Mesozoic forms de.scribed

by Riist (1885) from poorly presctA^cd assem¬

blages, because Haeckel’s descriptions of spccics

did not materialize uncil 1887. Accordingly

many of Haeckefs généra are not as firmly based

GEODIVERSITAS • 1997 • 19 (2)

323

De Wever P. &C Vishnevskaya V. S.

as chey would haVc becn with Aveli-prescrvcd

Cenozoic fornis as their n^c species* and a tcn-

dency was initiated for Cenozoic and Mesozoic

forms to be assigned to the same genus, encoura-

ging an impression rhat radiolarian généra bave

long stratigraphie ranges. During the following

décades, Cretaceous râdiolarians were described

from many scattered locdlitics (Table 2), but

there was little stratigraphie progress bccausc of

the unnatural taxonomie System used. In an

effort to ovcrcomc ihis obstacle» Hindc (1897,

1900) began to expand the rcmark by Rüst

(1892) thar Mcsozoïc radiolarian assemblages

include higher ratio of cyrtoid spccies than do

Palaeozoic ones. Alrhough this method of

apprnximare âge détermination was quesrionable,

as was underlined by Tan in 1931, it was still

being used, in a somewhar elaborated way, for

example, by Kobayashi & Kimura in 1944.

Reports of the end of rhe 19th centui^' are essen-

tially descriptive, and rhe studted samples are

often undated because the absence of any other

fauna. The modem phase of Mesozoic radiola¬

rian stratigraphy started with Khabakov (1937),

who understood that the seemingly exrended

stratigraphie ranges of many taxa were the reper¬

cussion parily ol the unnarural taxonomie Sys¬

tem, and pardy of mistaken age-dcccrminarions

of strata. Researchers used Haeckelian systema-

tics for décades {e.g. Campbell &L Clark 1944;

Campbell 1954). Since rhe vvork by Riedel on

Cenozoic matcrial (1952, 1953) rcvcalcd rhe

Haeckelian syseem inapproprintc, it bccamc clear

that the taxonomie System for Mesozoic radiola-

rians would have to bc reconsidered and thaï it i.s

disjunct from thac for tlic Cenozoic (Ricdcl

1967b). Indicarions for a sudden change in fauna

at or ncar the Crctaccous/Paleocenc boundary

arc documented by Lipman (1952) and Forcman

(1968) resuhing in ensuing large numbers of

new généra and scveral new families being descri¬

bed for ihe Mesozoic (PoreTnan 1968; Dumitrica

1970; Pessagno 1969a, b, ...). During the I96ü'sr

some stratigraphie charts were published for

Cretaceou.s radiolarians^ but thcsc were generalty

of local appJicability. Zbamoida (1972) compiled

a summary of Mesozoic radiolarian occurrences

in rhe “Pacific mobile belr”, and Zhamoida Ik

Kazintsova (1981) reviewed Mesozoic radiolarian

literatLire appeai'ing berween 1967 and 1978. In

the 19'^0’s, the Deep Sea Drilüng Project

(DSDP) afforded the chance to correlate the évi¬

dence bervs'een conrinental and marine localiites,

making possible rhe construction of stratigraphie

charts of wide applicability, and also allowing the

calibration of radiolarian occurrences with calca-

reous microfossil groups zonations.

Triassic

Despite the grcat divcrsiiy existing among Upper

Non'an and Rliaetian radiolarians, relatively few

Taxa have been described.

Wor/d (exclndirfg Europe)

Pacific, Atlantic, Indian. Noue.

America. Some earlier studies in North America

were publisited by: Martin et al, 1915, and

Smith 1916, A new set of studies was initiated

on western Norrh America by Pessagno et ai

(1979) in Raja Californui. Pessagno & Blome

(19S0) studied the évolution of pantanelliid

radiolarians and described species of several otber

généra from the upper Norian on Queen

C'harlorte Islantls. RIome (1984a. b) further stu¬

died this fauna, described new spccies and pro-

posed a prcliminaty radiolarian zonation for i:he

Upper IViassic of western Norrh America wirh

rhe ropmost Triassic subzone, the Berracciiim

cfeweveri Sub/.one,, bascd on upper Norian faunas

of Monoris âge from ilie same locality. Further

invGsrigarions in the Queen Charlovrc Islands

wcrc Lindcrtaken by Carter (1990, 1993) who

also studied the diverse Rhactiaii fauna from the

Sandilands Formation and proposed threc preli-

minary radiolarian assemblages. Subséquent stu-

dics bave incliidcd documentation of rhe

Triassic-Jurassic boundary itr northern Queen

Charlotte Islands (Tipper &: Carter 1990), evo-

lutionary trends in latest Triassic and earliest

Jurassic faunas (Carrer 1994^ Tipper et ai in

press) and a phylogenetîc siudy of the genus

Fentsium (Carier 1992). In the northern Cache

Creck 'lerrane of Southern Yukon, Canada,

upper Norian radiolarians have been reporred

from a ehert sample by Cordey et al. (1991 ).

Eisewhere in western Notth America, Blome,

Reed ÔC Tailleur (1989) found upper Norian

radiolarians. Yeh (1989) studied radiolarians in

324

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

rhe upper pair ol' the Fields Creek Formation, be Triassic, and describcd some eighty species,

east-central Oregon. His fauna (sample rC35) is predominancly spherical and elliptical forms,

suggested to be Lower Jurassic, but it compares multi-segmented cyrtoidsi cogether with some

closely with radiolarians from the Sandilands closed cyrtoids and chree-armed spongy forms.

Formation and is more likcly Rhaetian according Brouwer (1921) beheved this assemblage to be

to Carter (199.3) who described and illustrated Late Jurassic. In tlie Phillipines, more recently

miich of the Rhaetian fauna of the Qucen Cheng (1989) illustrated upper Nt)rian radiola-

Charlotte Islands. rians from bedded chert of Uson Island. Furthcr

SE Asia (Japan, Indonesia). In Indonesia studies in this area by Yeh (1990; 1992) and Ych

Hinde (1908) investigated well-prcservcd radio- & Cheng (1996) indicate thaï, in addition to fau-

larians from a number of Moluccan localities nas of late Ladinian and late Carnian âge, two

(notably on Rôti and Savu) which he bclieved to radiolarian assemblages dated as late Norian and

Fig. 1 . — General map of eastern Peri-Tethys domain showmg the investigated régions listed on table 1 . Main areas of investigation

are marked with zones. The numbers refer to those given on table 1. Detail maps are provided on Figs 2, 3.

GEODIVERSITAS • 1997 • 19(2)

325

De Wever P. & Vishnevskaya V. S.

Table 1 . — List ot publications dealing with Mesozoïc strata of the Russian platform. Each publication has a number which corres¬

ponds to that on figures 1-3. For each publication, the âge, région, latitude and longitude, subject of investigation, paleoenvironment

and other involved fossil groups are provided.

n°

Auihor

Age

Région

Longitude

Latitude

Subject of

investigation

Paleoenvironment Other group

ot fossils

Kariski 1889 in

Petrushveskaya 1986 p. 144

K2 St

Simbirsk

(Uljanovsk)

48'15'E,

54''25'N

Presence of rads

was eslablished

Rads ooze from

"santonian clay"

information

Khudyaev 1931

J2cl.

J3 km-KI ne

Povolgje

Sysola Riv. Bas.

52' 20‘E, Sg 'SS'N

49''3Û'-52^30'E,

60^00'-61"00’N

Rads from phosphate F''

49 sp .

(With 20n.sp.)

Marginal sea

Ammonites

Khabakov 1937

J3-K1 ne

Basin Vjatke Riv

Basin Kama Riv

50^00’-53'00‘E

56' oo'-eroo’N

Rads from 2 horizons:

Volgian and Neocomian

94 gen. ^ species

Upwellrng zone

Ammonites

Lipman 1952

K2 st-cp

Kuznezk district

of Penza région

47^O0’-48'OO'E.

53^2a'-53'50'N

Descrlpt. of 48 sp.

with 37 n.gp.

Moderate water

Forams

Gorbachik & Druchziz 1959

K1 al

Crimea

34M5'E. 45-‘20'N

Presence of rads in ctay

Shallow water

Forams

Aliev & Smirnova 1969

K1 al

Vladimir district

40'’10'-41'^30'E.

55'15'-56''30'N

Presence of rads in cfay

Shaliow water

Forams

Koziova 1971

J3 km

Pechora basin

57‘“E. 62 N

First quotation of rads

iist ot 6 n.sp.

Shallow water

Koziova 1976

J3 V

numerous rads. 1 n.sp.

Shallow water

Gorbunov 1971

K1 al

Slavjansk

37'’30’E, 49"00'N

badly presen/. rads

from clay ar>d sand

Shallow water

no data

Sichera &

Semenov 1982

K2 St

Voronezh

38‘'00’-39°00'E,

5r30'-52"00‘N

well preserved rads

in sand

ailern. shallow &

moderate waters

no data

Bragina 1987

K2 St

Uljanovsk

4a=0a'E, 54'OO'N

id.

no data

Vishnevskaya 1987

Kl al-K2 cp

1 -Moscow

2- Vladimir

3- Brjansk

37^00‘-39''00’E.

55^0Q'-55''30'N

39 OO'E, SÔ 'OO’N

35 E. 54^-55 N

Biozonation

Moderate

water depth

1- Inoc^amus

2- Forams

3- Forams in

Kl al

Vishnevskaya &

Kazinsova 1990

Kl-2

Central Russian

platform

30=-50'’E.

40"-60'’N

Comparison of

rad. biozones

no Info.

Vishnevskaya 1993

K1-K2

1- Moscow

2- PrecaucasuB

37’-39"E.

55^00-55 30'N

37'^-40"E.

44“30'-45’30’N

Rads zonation

4 illustration

Moderate

water-depth

Forams

Bragina 1994

K2 t-cp

Khotkovo of

Moscow district

37°30’E. 55^30'N

Rads siratig.

Inoceramus

Koziova 1994

J3 km

Pechora

57°30'E, 62-^30'N

presence of rads

no Info.

Macrofauna

Amon & De Wever 1994

Povolgie

50^-60"E.

50-^^60^N

Comparison of

biozones

shallow water

Forams

Amon 1985

K2 t-cp

Usa river

57=’-67^E,

66°-67^N

Rads biozone

shallow water

Kazinsova &

Olferiev in press

Kl al

Moscow région

37^-39^E. 55''N

Rads from

"Paramonov" clay

shallow water

Forams

326

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

early RJiaetian are présent also.

In New Zealand, radiolarians trom Kapiti Island

(Torlesse Terrane) studied by Blome, Moore,

Simes ôc Watters (1987) are coeval with upper

Norian faunas From rhe MonotLs beds at Kunga

Island. In the Waipapa Terrane, Aita (in Sporli &

Aita 1988) figured a mixed Patina of Upper

’Triassic and Lower Jurassic Terhyan radiolarians

from the red chert of Kawakawa Bay. Fucther

refcrenccs to this tanna and its use in solving

complexities of terrane accreiion in New Zealand

are found in Sporli, Aira &C (nbstjn (1989).

From Japanese cberts Yehara (1927) illustratcd

six rather nondescript circulât torms from

Sbikoku. Other localiiies (Kimura 1944a, b) sus-

pected to be ’lriassic yielded poot ly preserved cir¬

culât radiolarians, spongy torms with three arms,

and closed cyrtoids. Since tKc lare 1970 s a nuni-

ber of radiolaricin zoiial schemes For rhe Upper

Triassic bave been proposed by workers in Japan.

Amongsr tbese Yuo, Matsuda & Iso/.aki (1980)

established tbree successive radiolarian assem¬

blages of Middlc Triassic to Early Jurassic age

from continuons séquences of chert in che

Inuyama area, central Japan. The lowct assem¬

blée is Middlc Triassic; the middlc one is Late

Triassic, and the upper one is Early jurassic. The

Late Triassic assemblage was later separated inro

three sub-assemblages (Yao et al, 1980); the

upper two ot thèse wcrc proposed for laie Norian

and Rhaetian forms, respectively. Numerous

undescribed taxa were also figured at this time.

In 1982, Ki.shida &: Sugano ostabli.shcd five

assemblage zones for Triassic strata from the

Cbichibu Belt in ihe Kodii and Oita Préfectures,

Japan. Kishida & I Usada (1986) renamed and

subdivided some of their as.semblages. Matsuoka

figured upper Norian radiolarians (rom the Sou¬

thern subbclt of the Chichibu Belt, Koebi

Préfecture (1983b) and discuSsed faunas from

the Togano Group (1984b).

Subsequently Sato, Murata Sc Yoshida (1986)

established the Betraccium dcwevcri Zone for

upper Norian strata in the Southern part of the

Chichibu Terrane in Kyushu. Yoshida (1986)

examined a Late Tfia-ssic to Early Jurxssic hedded

chert sequence in Kagamigahara City, Gifu

Préfecture, central japan, and .subdivided it into

seven radiolarian zones.

Aiso noteablc arc the works published by Ishida

(1983). Kishida 8c Sugano (1982), Kojiina

(1982), Matsuda & Isozaki (1982), Nakaseko &

Nishimura (1979a, b), Takashima & Koike

(1982), Yao (1972. 1979, 1981, 1982a, b, 1983.

1986). Yao, Matsuoka & Nakatani (1982). In

northern China, in initial studîes of radiolarians

from the Nadanhada Range, Kojima &r Mîzutani

(1987) figured upper Norian and Rhaetian taxa

from Triassic hedded chert. Subsequently,

Kojima 0989) discus.scd the accrctionar)' history

of terranes along the continental margin ot East

Asia during Mesozoic time iising Mlddle and

Upper Triassic radiolarian assemblages (including

somc upper Norian and Rhaetian t.axa) to point

out simllaricies bcLvvccn the Nadanhada-Westem

Sikhote-Alin l'erranc, and the Tamba-Mino-

Ashio Terrane of Southwest Japan. Implications

are that the Nadanliad.a Range Ts tlic northern

extension of the Japanese terrane. The history of

this Mesozoic superteriane is further discussed by

Mizutani, Shao & Zhang (1990) along with

simUar tectonostratigraphic terranes in rhe

Ryukyu arc, rhe Philippines and probably

Bornéo. A moïc recent paper by Yang &

Mizutani (1991) outJines the geology and bio-

straiigtaphy of the Nadanhada Terrane, pre.scnts

preliminary révision of parasarurnalids, and des-

crihes new paras'atuinalid taxa of latest Triassic

and early Jurassic age.

fn eastern Russia, Tria.ssic faunas in the Sikhote-

Alin Terrane, Sakhalin Island (Verchojan areas),

and the Koryak UpUnd were .siudied by Bragin

(1986, 1991a. b, 1994). Radiolarians and cono-

doiHS of mid Early Triassic to latest 'Triassic age

(including late Norian and Rhaeti;m faunas) are

présent in chert scquences at SikFioie-Alin where

.seven radiolarian zones and seventeen conodont

zones hâve been e.sLahli.shed. J'hese forms arc dis¬

cussed and illustrated and new taxa are descri-

bcd. Goltman (1969) listed radiolarian généra

occurring in the Triassic of Pamir, but until ihcy

are illustrated a comparjson with enher fauna Is

impossible. Among other publications from Asia

one can also mentioned the works by: Bailey

Mc Callien (I9*i3); Hudson et al. (1934);

Ichikawa (1930); Kimura (1944a, b); Kobayu-shi

BfT Kimura (1944b); Scrivenor (1929); Yehara

(1927); Zhamoida (1958).

GEODIVERSITAS • 1997 • 19(2)

327

De Wever P. & Vishnevskaya V. S.

Europe (cxclndin^the Russian ptaîform)

Records of radio)jrians are srill relatively rare in

Triassic sedimentary rocks if rhe variety of levels

involved is considered. In fact, most of the infor¬

mation availablc to date lias bccn obtained from

Alpine faunas.

Triassic radiolanans bave been recognised for a

long time but compréhensive srudies are quire

récent. Indeed, following a prcliminary note in

1887, Rüst recorded in 1892 about twenry spe-

cies from twenty-eight Triassic samples of central

European hornsteins and calcareoiis Umestones.

In the sarne year, Parona figured about a dozen

poorly preserved forms including somc with cir¬

culât and clliptical ouflincs together with appa-

rently spong)' forms with thrcc and four arms.

Cyrtoids, of which some arc niulciscgmemcd and

conical and others with inflated middle and

lower sections and apparentJy closcd, tubular

prolongations arc also documented by Parona

(1892). Wirz (1945) illustrated a fcw circular

and cbambered radîolarians in rhin sections of

dolomite from south of Lake Lugano (Italy).

Most of rhcsc assemblages arc not sufliciently

weli-described ro permit comparison with faunas

described in more recent papers. Following some

other minor .siudies (Winkler-Hctniaden 1934;

Andrusov 1950), a rcnewal will corne from seve-

ral Austrian séquences of clays and limestoncs,

Kozur & Mostler (1972) described some fïfty

weü-preserved radiolarians bclonging ro the

emended Coccodsicids, a&traccurids, hcliodsicids,

saturnalids and veghicyclids. in their .study of

Middle and Upper Triassic radiolarians, Kozur &

Mostler (1981)^ Kozur (1984a, b) described a

great number of uew species and new généra

from the Poischenkalk (Sevat) and Zlambach

maris (Rhaetian) of Austria. Lahm (1984) fïgu-

red Middle and Uppor Triassic taxa from norih-

ern Italy and Austria; some of rhese ranging

upward into the Sevat and Rhaetian. During rhe

1970 s and 1980 s there was a renewal of irnerest

on these levels (from Greect-, Sicily and Turkey;

De Wever et oi 1979; De Wever 1982a, b; from

Austria and Northern Italy; Donofrio & Mostler

1978; Kozur & Mostler 1978,. 1979a> b, 1981,

1983, and subséquent work; from the

Carparhians; Dumitrica 1977, 1978a, b;

Dumitrica et al. (1980); from Yugoslavia:

Gorican & Buser 1990; from northern Italy:

Lahm, 1984

Samples yielding radiolarians are rare and locali-

ries wlde-spread but, in Europe, mainly concen-

trated in the Tethyan realm: from Austria. Italy,

.Slovcnia, Serbia, Monténégro, Albania, Grecce

and Turkey. Most of the Triassic bioevenrs hâve

been inter-correlared and calibrated with

Conodonts or Ammonites or Pelecypods No

well-preserved and comprehensively described

Rureal or sub-Roreal faunas are known in sufFi-

cient number to be able to be considered as

represenr.uive. Only recently some faunas bave

been recorded in Russia from northern Siberia

(Egorov &C Bragin 1995J-

This synopsis illustrâtes tliat radiolarian workers

around the vvorld hâve shown a renewed interest

in upper Norian and Rhaetian faunas since

1980, and that the tempo of rcsearch lias accele-

rated quite rapidly in the past five ycars. Despite

this intensiry, the majority of the Rhaetian fauna

remains undescribed.

) b RASSI C

Worl/l (excluding Europe)

Pacific, Atlantic, Indian. None beside.s the

paper from Colom (1954) in rhe Atlantic Océan.

America. Following somc prcliminary work by

Boner bi Trejo (1956), Riedel & Schlocker

(1956) and Smirh (1916), the First substaatial

papers dealing with Early Jurassic radiolarians

from Northern America werc published by

Pessagno and his collaboracors (Pcvssagno bc

Blome 1980, 1982; Pessagno & Whalcn 1982)

and more recently by \ch (1987). In the

Carihbean apparently only one questionable

paper by Vcrniunt (1937) can be quored.

Mattson bc Pessagno (1979) reported Late

Jurassic and Early Crcraceoiis radiolarians in

Puerto Rican cherts and limestones. Pessagno

(1977b) was able to erect a radiolarian zonation

lor the Late jurassic, on the ba*,is of lorms occur-

rlng in cherts and lime.STone nodules in

California.

SE Asia (Japan, Indonesîa, Far East Russia).

In the circunvPacific région, I linde (1917) listed

poorly preserved Lare Jurassic radiolarians in

cherts from several localities in the Celebes.

328

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

Some général quotationi of Jurassic rudiolarians

in SE Asia may be found in Bailey 3c Mc Callien

(1953), Hudson étal, (1954), Huzimoro (1938),

Kawada (1953), Khabakov (1932, 1937).

Khudyoev (1931), Kimura (1944a), Kobayashi

(1935), Tromp (1947, 1948), Yehara (1927),

Zhamoida (1972), and frora Indonesia in

Brouwer (1921), liinde (1917), Krumbeck

(1922) and Vogler (1941). Coomaraswanny

(1902) recorded the presence of Jurassic radiola-

rians togecher with planr rcmains in India. A

broad summary of l.are Jurassic and Cretaceous

radiolarians, with a définition of seven disrincr

assemblages, was provided by Nakaseko 3c

Nishimura in 1981. Since then recent workers

arc elucidating japanese occurrences such as Aita

(1982), Mizutani (1981), Matsuoka (1982a,

1983a) and numerous other workers,

Europe (excliiding the Rmnaa Platform)

The pioneer work on I.ate Jurassic radiolarians

was based on Italian and Synss localities. Rüst

(1885) provided the original descriptions of

assemblages from jasper.s, flints and siliceous

shales irom a number of localities in rhe Allgau

(southern Germany) and Austria (Urschlau) and

from redeposited pebbles in western Switzcrland.

He aiso obtained rich assemblages from copro-

lites from iron mines at Ilsede, further north in

Germany (ncar Hannover). Tins important

paper presented seventy-two species dated as Late

Lias-Early Doggei by associated ammonites. Rüst

(1885) also recorded radiolarians in the

Tithonian (Aptychus beds) from tlie Alps, in the

flysch of ‘feisendori (in the Ach.ual), in the

flysch from ’Eraustein (Upper Ravaria) and also

from Neocumian levcis of the Carpathians ncar

Podbiel. Wisniowski (1889) described moderate-

ly preserved forrns in siliceous concrétions from

the vicinit\' of IGakow, Poland.

Italian authors described diverse assemblages

from flint nodules in llmcstones at Cittiglio

(Parona 1890), and radiolarite and siliceous

shales at Spezia (Vinassa 1898a, b, 1899),

Monginevro (Squinabol 1913) and the

Bolognesc (Neviani 1900). Cayeux (1896) repor-

red calcitizcd radiolarian skeletons in Tithonian

limescones in the région of the Ardeche in South¬

ern France. Cayeux (1897) mentioned poorly

preserved Jurassic radiolarians (Sch. inflata

ammonite Zone) in the “Gaize"' from Argonne,

from Cher (France).

Muzavor (1977) described well-preserved radio¬

larians from siliceous mari at Oberaudorf

(Bavaria). Steiger (1981) illustrated well-prcscr-

ved forrns from lime.srone turbidides in the vici-

nity of 8alzhurg. l’ioni broadly based studics of

Techyan assemblages rhe First radiolarian bio-

zonations for Europe were made by Baumgartnet

étal (1980) and Kocher (1981).

Radiolarian bioscraiigraphic schemes for Jurassic

and Cretaceous sequences were proposed by

Tikhomirova (1984, 1987) and Kazinsova

(1984) for rhe Carpathians and the Lesser

Caucasus, but, as rhese investigations are based

on thin sections they are out-of-date and prob-

ably inaccurate,

Other early papers dealt with Jurassic levels from

Western Europe (Andrusov 1950; Anonymous

1959; Bergounioux 1950; Cayeux 1891, 1896;

Downic 1956; Cita 1965; Daccjué 1933;

Dcflandrc 1953; de [.apparent 1925;

Dunikowski 1882: Furrer 1951; Geyer 1961;

Heitzer 1930bi Jacob 3c Nicorici 1957; Innocen-

ti 1927i Jaccard 1909; Jodot 1931; Kraus 1914;

Leischner 1961; Pantanelli 1880, 1887-1889;

Parona 1892; Protescu ]933i Rüst 1885, 1898;

Sido Sikaboiiyi 1953; Termier 3c Maury

1928:Trauth 1950; Vadasz 1952; Vinassa 1898a,

b, 1899; Wcynschenk 1950, 1951;

Winkicr-Flermaden 1934). Data for Jurassic

radiolarians arc numerous in folded Tethyan ter-

ranes and radiolarians are the main constituents

of the rocks for numerous Late Jurassic localities

(in ail rhe radiolarite type fades). A large number

of papers hâve been published during ihc lasr

two décades including; Baumgartner 1980; I^e

Wever 1982a, b; De Wever et al. 1986b;

Dumitrica 1970; Ciorican 1994, ...

The First bio.stratigrapbically significant papers

dealing with F.arly Jurassic radiolarians were

publi.shed recently From Tethyan realm (Pessagno

&: Poisson 1981; De Wever 198 la, b, 1982a; De

Wever &c Origlia-Devos 1982; Corican 1994).

An .ivailablc set of stratigraphie markers can be

based on some receni work (Gorican 1987,

1994) and on the synthesis published by the

InterRad group (1995). In spite of the abun-

GEODIVERSITAS • 1997 • 19(2)

329

De Wever P. & Vishnevskaya V. S.

dance nf work published during rhe two lasr

décades, mosi of them deal with the Tethyan

realm and ainiost no significant publications

relate to tlie true Boréal realm. Nu well preservcd

Boréal or sub-Boreal faunas are described in the

lirerature and only some radiolarian species are

mentioned in very sparse localities [Scotland:

Dyer &c Copestake 1 989 and Russia; Khabakov

1937 (illustration of the laiicr is too poor to be

useful). and more rccçntly Bragin (1994) and

Bragin &c Bragina (1995)]. d’hcreforc, at présent,

there is no rcliablc general datum available to use

for the Boréal prt)vince.

No warm i^s cold taunas hâve been ideniified

with confidence to date in western Kurope. This

is mainly duc to rhe laci that much of rhe cur-

rently available information bas been gathered

from radiolarite-iype faciès and that this type of

sedimentary rock was deposited under the most

active parts of upwelling Systems (see above De

Wever (V ^ 7 /, 1994).

Cretac1:ül:s

World (excluding Europe)

Some general reports (by topic or by location)

were published by Krasnyi et al. (1962), Rüst

(1887)> Socco (1905) and, in Africa, by Mvtgné

&Sigal(1953).

Pacific, Atlantic, Indian. Several studies based

on DSDP matcrial hâve contribtited to the taxo¬

nomie and stratigraphie linderstanding of Early

Cretaceous radiolarians (Moore 1973i Riedcl &

Sanfilippo 1974; Foreman 1975). DSDP

sequences from the North and Central Pacific

hâve contribuicd very substaniially to Middlc

and Latc Crcraccous stracigrapluc zonation

(Foreman 1971, 1975; Schaaf 1981) and for a

predominanriy taxonomie snidy by Empson-

Morin (1981). Lare Creraceous radiolarian strati-

graphy in the Eastern Atlantic has been aided by

the Deep Sea Drilling Project (Petrushevskaya &C

Kozlova 1972; Foreman 1978b) DSDP

sequences drilled in the eastern Atlantic provided

information on radiolarian stratigraphy in that

région (Foreman 1978b; Basov et aL 1979, for

the Early Cneiaceotis). Foreman (1977) summa-

rised occurrences in the Atlantic Océan and îrs

borderlands, and refined the Late Cretaeeous

zonation of that région.

DSDP cotes hom the eastern Indian Océan pro¬

vided the basis for rhe description of three strati-

graphically significant assemblages in rhe Middle

and Latc Crctaceous (Renz 1974). Moderately

preserved Late Cretaccous radiolarians are recor-

ded in Indian Late Cretaceous phosphatic

nodules by Garg & Jain (in press).

America, Atnong some of the carliest wttrks

conducted in North America onc can cite: Bolin

1956; Campbell & Qark 1944; Crandell 1952;

Eichcr 1960; Foreman 1966; Coke 1959; Hindc

1894; Nauss 1947; Payne 1962; Ransome 1894;

Riedel & Schlocker 1956; Kuhev 1929; Rüst

1892, 1898; Searighi 1938; Tyrrell 1890;

Woodward &L Thomas 1885, 1895; and for

South America: Galavis 1951; Richter 1925;

Staiïiforch 1948; Thalman 1946; and for

Caribbean: Ayala-Castanares 1959; Bronnimann

iîc Rigassi 1963; Foreman 1966; Palmer 1934;

Pessagno 1960, 1962, 1963; Vermunt 1937. Ehc

circunt-Pacific région is represenred by descrip¬

tions of radiolarian assemblages from rhe

Cenomanian of California (Pessagno 1971a) and

of Costa Rica (Schmidt-Effing 1980),

Radiolarians are recorded in Campanian linies-

tones of Puerto Rico (Pessagno I963)> and as

pyritized skcletons in the Late Cretaceous of

Venezuela (Galavis 1951). Also, in rhe Caribbean

région, the Deep Sea Drilling Project has provi¬

ded data on Late Cretaceous radiolarian srrarigra-

phy (Sanfilippo 6i Riedel 1976). Mid-

CretaceoiKs radiolarians were rep<irred hy

Basarovski (1991) from Central America (Cuba).

Fmr North America, ihc earlicsi record of

Cretaccous radiolarians is from the l^icrrc shaJe of

Manitoba, by Rüst (1892, 1898). Occurrences ot

Albian and Campanian r.idiolari,ins in Alberta

were recorded by Wall (1975). C'.impbcll Clark

(1944) described a diverse C'ampanian as.sernbla-

ge from California, and a sparse Franciscan

,^ssemblage w:is rectirded by Riedel & Schlocker

(1956). Californian assemblages were exploited to

greater stratigraphie advantage by Foreman

(1968) and Pessagno (1970, 1971a, 1972, 1973

and 1976). The paper last cited establi&hcd cîght

Latc Cretaccous radiolarian zones in California,

and described a subsrantial number of new taxa.

Pessagno (1977bj proposed a Berriiisian 10 Albian

zonation and a large number of new taxa on the

330

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

basis of assemblages from calcareous nodules

from a numbcr ot Californian localities.

E Asîa (Japan, Indonesia, Far £ast Russia).

Tbe fîrst investigation of Early Crcraceous radio¬

larians in the circum-Pacific belt was conducced

by Hinde (1900), wbo investigated ihem in

numerous samples of cberts, maris and limes-

tones from Central Bornéo. From die Creraceous

chalks on the Indoncsian island of Rotti,.Tan Sin

Hok (1927) dcscribcd a diverse, well-preserved

assemblage that is now believed to be between

Albian and furonian in âge (RJedel & Sanfilippo

1974).- Nakaseko et al. (1979b) distingtiished a

numbcr of scratigraphically significant assem¬

blages through the Cretaceous and Palaeogene of

Japan, and compared rhem with /onal sebemes

developed for deep-sea séquences. A more recent

compilation of the stracigraphy of Japanese

Middle and Late Cretaceous radiolarians, defi-

ning zones and a numbcr of new taxa, was pro-

duced by Taketani (1982).

Dcscriptiojîs of radiolarian assemblages from the

Cenomanian of Sakhalin include Kazintsova

(1981). vVmong others, the follovving works werc

publishcd: Aliev 1961a, b, 1965; Dundo &

Zhamoida 1963; Hudson étal. 1954; Karitskii

1889; Khabakov 1932. 1937; Khudyaev 1931;

Koziova & Gorbovets 1966; Lipman 1952,

1960; Minermaier 1896; Nakaseko et al. 1965;

Rao 1932; Vassoevich 1938. From Ausrralia and

New Zealand publications include: Crespin

1946, I960; Dun étal. 1901; Etheiidgc ôd Dun

1902; Hinde 1893; Foreman 1966. From

Indonesia: Brouwer 1921; Foreman 1966; Tan

1927; Voglcr 1941. Berria.sian blocks in a

Turonian chert matrix yield well-preserv'cd radio¬

larians from Tibet (Wu & Li 1982), and Dundo

& Zhamoida (1963) investigated Valanginian

radiolarians în siliccous volcanogenic rocks from

the Far-Eastern USSR.

Nakagawa & Nakaseko (1977) listed and Ülus-

rrated radiolarians from a Jurassic and an Early

Cretaceous locality in Japan. A Late Cretaceous

radiolarian occurrence in manganèse carbonate

ore in Japan is described by Yao (1979).

Europe (excluding the Riissiari platform)

As is the case for the Jurassic, mosc of the initial

research on Early Cretaceous radiolarians was

based on European matcrial but today current

investigaiious arc more widely dispersed.

Coproliies and siliceous limestones from Zilli

(Saxony) aitd Gardenazza (norchern Italy) provi-

ded most of the Early Cretaceous forms descri¬

bed by Rüst in his paper of 1888, and ten years

lacer he added forms from the clierc)' limestones

of Cictiglio in northern Icaly (Rüst 1898; see also

Parona 1890). Fischli (1916) illustrated a diverse

faunal assemblage from flints in a Swiss conglo-

meraie. Sollas (1873) menrioned radiolarians in

coprolites from the Cambridge Greensand and,

30 m belüw, in the Gaulr Clay from

Bedfordshire (UK). Quaterly Jourual of the

Geologîcal Soaety (p, 78)) and Grimes (1895:

345) described cwo species from the Power

Greensand of Surrey (UK). In 1883, Wallich

rccorded the présence of four généra of ntdiola-

rians in the cavities of hollow cherts from Surrey

(UK). Fritsch (1893) recorded the presence of

eleven species in marly beds of Prisen (Senonian)

from Bohemia, and Deecke (1894) some radiola¬

rians in chalks flints' at Rügen. HUI &

Jukes-Browne (1895) menrioned the présence of

radiolarians in chalks of the Melbourne Rock

(UK). Cayeux (1897) menrioned rwenty-seven

généra and described numerous species of

Turonian radiolarians from SE, N and NW of

the Paris Basin (France) and from smectitc du

Hevre (Belgium). Holmes (1900) recorded rwen-

ry généra and forty-one specie.s from the chalk in

Surrey (UK). Zirrel (1876) described the firsr

Cretaceous radiolarians from northern Germany,

in spire of a poorly preserved fauna. Tethyan

radiolarian assemblages of Middle Cretaceous âge

bave been described by Squinabol (1914) frotn

the Veneto région of Iraly. Ravn G. (before 1911)

menrioned the presence of Upper Cretaceous

radiolarians in Arnager limestones (Island of

Bornholm, Uenmark).

Over the décades, Cretaceous radiolarians bave

been described from scatlered localities

(Andrusov 1950; Anonymous 1959; Colom

1954; Corti 1896. CusTodis & Schmidt-Tbomé

1939; Deccke 1895; Elberc 1902; Fric 1893;

Furrer 1951: Grimes 1895: Heitzer 1930; Hill

1912; Hill Ôc Jukes-Brown 1895; Flolmcs 1900;

Jodot 1931; Lombard & Schrôder 1939; Neviani

1900, 1901; Pantanelli 1880, 1887, 1889;

GEODIVERSITAS • 1997 • 19(2)

331

De Wever P. & Vishnevskaya V. S.

Parona 1890; Pcrner 1891; Prorescu 1933; Rüst

1887, Squiiiabol 1903, 1904, 1914; Sujkovvski

1931; Vasicck 1947; Vinassa 1901; Vinassa

1900; Wallich 1883; Werzcl 1933, 1961). In the

1960 s évidence accumulated loi* an abrupt evo-

lutionary change at or near the Crctaccous/

Palaeoccnc boundar)' (Lipman 1952; Foremao

1968), and conscqucntly, large numbers of new

Crctaccous gênera and scvcral nevv fatnilies hâve

been described (â.g. hy Cita 1965; Foreman

1966, 1968; Dumitrica 1970; Herm 1962;

Empson-Morin 1981).

Baumgartner cr al. (1980) proposed a prelimina-

ry strarigraphy based on a number ot'widely scat-

tered radiolarian assemblages (rom the leihyan

region. Boyanov &L Lipman (1973) were able to

use a poorly prescn^cd radiolarian assemblage to

détermine chc Early Crctaccous age ol Bulgarian

siliceous shalcs prcviously considered to be

Palaeozoic. and Lozynyak (1969) retorded

assemblages of tbis âge Irom the Ukrainian

Carpathians. In the Kiunet.sk area ol the Russian

Platform, Lipman (1952) recorded nunierous

radiolarian taxa in sampics f’rom drillcd wclls.

Goltman (1971, 1975) recorded occurrences in

limestones and maris of the Tadjiksk Dépréssion,

culminaring in a usefiil stratigraphie compilation

(Goltman 1981). Lipman (1960) described

numerou.s’ assemhlagc.s of Coniacian co Danian

age in wells and surface exposures of the Western

Siberian Lowland, and Kozlova Gorbovets

(1966) described charactcrisric complexes for ihc

Turonian to CJampanian deposits of that region.

Tethyan radiolarian assemblages ol Middlc

Cretaceous age bave been described by Kozlova

in Basov er ai (1979) Irom a DSDP Site ofl

Spain, and by Dumitrica (1970, 1975) from

Romanian maris and radiolarite.

In spire of the abundance ol work published

during the cwo last décades, most of them deal

with the Tethyan realm and alraost no significant

papers consider the crue Boréal realm. No well

preserved Boréal or sub-Boréal faunas arc descri¬

bed in the licerature. Some specics are only recor¬

ded rarely from very isolated localities and

thereldre therc is no available danim to use in

confidence for the Boréal province and we hâve

chosen co omit such darums from the Cretaceous

chart. Biostratigraphic data exists in a sériés of

papens among whicFi the most significant arc Jud

(1994) for the zones in Early Cretaceous.

Erbacher (1994) and O'Dogherty (1994) for the

middie part o^ Cretaceous, Sanfilippo & Riedel

(1985) and Kholdova et ai (1994) for rhe Late

Crctaccous together with LJrquhart (1994) and

Bragin (1995) for rhe Late Cretaceous ol Cyprus.

By the Late Cretaceous, the Tethyan environ¬

ment for rhe accumulation of radiolarian sedi-

ments had pracrically disappeared, and a

Palaeogene pattern was developîng. The tmly

.substantial occurrences in the Mcdiccrranean

région arc in the north Iralian Euganei

(Squinabol 1903, 1904)? and in Greece (De

Wever & Thiebauh 1981). There are significant

records in Senonian and Turonian shalcs of

Czechoslovakia (Berner 1891), in Camf>anian

chalks of northern Germany (Zittel 1876) and in

France and Belgian Campanian silicified lime¬

stones (Cayeux 1897).

Danian-Bai.aeockne

Publications dcalîng with this rime period are

not numeroiis. Literature recording occurrences

from Asia includes the following work: Hollis

1991; Vishnevskaya 1981-1 988c; Basov &:

Vishnevskava 1995; Irom the Atlantic realm;

Sairo et ai 1%6; From the Hast Indie.s: Reinhard

& Wenk 1951; from Europe: Anonymou.s 1959;

Srocsche & Uilrermann 1940; Twerenbold 1955;

Borisenko 1958, 1960, Kozlova 1993 and from

North .\merica: Frizzell ik Middour 1951.

RADIOLARIAN STUDIES FROM

THE RUSSIAN EUROPEAN PLATFORM

KImdjaev 1. E. (1931) in a paper entitled ‘‘On

the Radiolaria in the phosphates in the region of

the Syssola River” described forty-nine species,

belonging to len généra, where rwcnty-cight spe-

cies were determincd as new. They are

Cenosphaera komtemh n..spM C. syssolae n.sp.,

C sp inder. Nl^ C sp. indet. N2, Gnposphaera

ajfinioidfs n.sp., Lithapium luprasphiosum n.sp.,

Lithocyclia ovalh n.sp., Porodiscus sp. indet. NI,

P. sp. indet. N2, Cornutanna ovalis n.sp.,

Dicolocapsa trUpczoidalh ii.sp., D. sp. indet. NI,

D. sp. indet. N2, Tricolocapsa multlpora n.sp.,

332

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

Phonnoctimpe favosa n.sp., Dictyomitm muhipom

n.sp., D. spicularia n.sp.» D. biporosa n.sp.,

Lithocampe syssoluetisis n.sp., /.. sp. indec. NI,

L. sp. indet. N2, Cyrtocapsn rusii n.sp., Sticho-

capsa chabiikovi n.sp., S. regukris n.sp., S. qua-

dripora n.sp., S. kassini n.sp., S. zyrjanica n.sp.

and S. wisingiaua n.sp.

Kliabakov (1937) in his paper “Radiolarians

from Lowcr Cretaccous and Upper Jurassic phos-

phorites of Vjatka and Kama River Basins" des-

cribed nincteen généra and seventy-five species of

radiolarians.

Lipman (1952) in her monograph “Materials on

monographie srudy o( Upper CrecaceoUiî radiola-

rians from the Russian platform” described forty-

eight radiolarian spccics, whcre thirty-cight were

described as new species, They are: Cmosphaem

minor n.sp., C marnwilaîa n.sp.* Cenelilpsi^ elUp-

tica n.sp., Xiphosphaera irregularis n.sp.,

Cromyodruppa comenmea n.sp., Cenodheus Icns

n.sp., Spongopntnum craisum n.sp., S. angiumm

n.sp., S. amcHlatiim n.sp,, Trochodhem spimger

n.sp., Triacticiis triacuminatm n sp., Porodtscus

vulgaris n.sp., Stilodtctya deltcatiiU n.sp., 5. pU-

centalu n.sp., Tripodictya triaciiminata n.sp.,

Euchitonia santonica n.sp., Hagiastrum cmx n.sp.,

Fig. 2. — Location map of sites reported by Khudyaev {1931 ) in published investigations of Oust-Sysolk région (20°-21 “E, 30"'N).

GEODIVERSITAS » 1997 • 19(2)

333

De Wever P. & Vishnevskaya V. S.

Histiastrum crucifcnim n.sp., H. aster a.sp., AJiev & Smirnova (1969) in their paper *‘New

H. membramferum n.sp., H. megulare n.sp., specics of radiolarians from yVlbian of Central

Tesserastrum quadratmn n.sp.. RhopaListrum tri- areas of ihc Russian plaiform" described from

gonale n.sp., R. tumiduni n.sp., R ingens n.sp,, Upper Albian (40 m rhick) clay, wirh Albian

R atteniiatnm n.sp,, Spangodücm impresstts n.sp., foraminiferas of the Vladimir district, six new

Spongodisais dtrus n.sp,. S, maximits iMsp., S, vol- species: Porodiscus kavilkinensis Aliev n.sp.,

gensis n.sp., Spangotripus aciileatus n.sp., P. injlatns Smirnova et Aliev n.sp,, Sethocyrtis

Stylotrochus hexacanthus n.sp., S. dolichacanthus mosquensis Smirnova et Aliev n.sp., Theocanipe

n.sp., S. actacanthus n.sp., Lithostrobus turritella cylindrica Smirnova Aliev n.sp., 'L simplex

n.sp., Dictyomimi scakrts n.sp., D. gigantea n.sp., Smirnova et Aliev n.sp., Stichocampe cuneatus

D. striata n.sp. AU species derived from Smirnova et Aliev n.sp. and one subspecies

Santonian-Campanian clay of Penza région. DscVyomitra ferosia Aliev subsp. angusta Smirnova

Fig. 3. — Location map of sites (drill holes -1* and outerops -2-) reported by Koziova (1994) in published investigations of Pechora

(48°-60®E, 64°-69°N).

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

sub.n.sp. A number of forms firom the Ukrainian

Carpathians are described by Lozynyak (1969,

1975), and oiher forms from Azerbaidzhan are

described in a sériés of papcrs by Aliev (1961a, b,

1965, 1969a, b) on Valanginian, Aptian, Albian

and Cenomanian assemblages in which many of

the radiolarians are calcitized.

Koziova (1971) in her paper "About finding of

radiolarians in the lower Kimmeridgian strata of

the Timan-UraJs région" reported the radiolarian

assemblage from whitc mari strata of U) cm thick

with the ammonites Amoebocems kitchini Salf,

Riisenia cf. irimem Opp. The assemblage inclu-

ded sev'eniecn spccics, where five species were

new; Stylo.sphaera ? aspcralla Koziova n.sp.,

Sïaurodiciya reima Koziova n.sp., Hagiastnm

cmssum Koziova n.sp., //. stpiama Koziova n,.sp.,

Spirema ? >pbiierka Koziova n.sp. Sheempha.size<l

that these ncwly discovered assemblages are simi-

lar to the Lower Creiviceoiis assemblages from

Vjarka anil Kama River Basins, prcvîoiLsly descri¬

bed (Khudjaev 1931; Khabakov 1937).

A paper by Koziova (1973) “New specics from

lower Kirnmeridgian of the Timan-Urals région”

gave the description of ;dl new specics listed in

hcr previous paper (Koziova 1971). Poorly-

preseiv'cd Albian radiolarians from the Dnieper-

Don Basin were reported by Gorbunov (1979).

Koziova (1983) in her paper “Late Volgîan radio¬

larians of USSR North*^ recognized three radiola¬

rian assemblages: lower Kimmeridgian CmcelLt

rwrÆ, Volgian Stichopilidium planocephûla,

Berriasian HemkrypUicapui satymica and descri¬

bed 5. pLxnocepbüLx n.sp.

Koziova (1994) in a paper entided "Assemblages

of Mesozoic radiolarians from the Timan-

Pechora oil-heanng région" describes précisé cha-

racteristics of four radiolarian assemblages: lower

Kimmeridgian Cruadla crassay middie Volgian

Parvicingula papulata, upper Volgian Pseudocro-

lanturn planovephala and upper Beiriasian-lower

Valanginian Hemicryptocapsa salymica-, whicb

werc paicly described in her previous papers

(Koziova 1973. 1976). About rwelve species were

illusrrated as new in rhis paper. Visltnevskaya

(1993) in a paper "Jurassic and Crctaccous radio¬

larian biositaiigraphy in che USSR" illusirated

rwelve species frorn Coniacian-Saiitonian strata

from the Moscow district.

Bragina (1994) in her paper "Upper Creraceous

radiolarians and stratigraphy of Khotkovo

Group, Moscow région" studied radiolarians in

four sections and proposed rwo biostratigraphic

Linit.s: Coniacian (?) - Campaiiian [Archneo-

spongo-prumon bipartitum-Crucella irwmi) and

Campanian {Archacospongoprtinum htieyi-

A, ialurfiï), She counted more than 50% of

Californian species among these Russian plate

a.ssemblages.

Vishnevskaya (1996) in a paper “Peri-Tethyan

radiolarians and their implications” illustrated

eighteen species from Albian-Sanronian of the

Moscow, Kaluga and Brjansk areas.

CONCLUSION

rhe improvement of a taxonomie System for

Mesozoic radiolarians is hampered by a general

lack of well-preserved specimen.s from well orga-

nised .scquences whicb are needed to develop the

basis for a reliable hyporhe-sis of evolutionary

links. Thk bas represenred an important facror

in the approach choscii by some authors {e.g.

Fessagno 1969a, b, 1971a, 1977b: Empson-

Morin 1981, 1982; Kozur & Mostler 1972-

1989) who produced a highly-splir taxonomie

hierarchy indicacing ail observed morphological

characters, A highly-divided taxonomy is useful

for the rccognirion ofslight morphological varia¬

tions which may eventually bc Loinprchended as

expression of paleoenvironmerual conditions.

This does not necessarily, however, advance the

general aim of a taxonomy which considers phy-

letic reJationships, and it often results in species

which are too narrowly delimited to be broadly

stiitablc for stratigraphie purpose.s. Kowever. cor¬

rélations are a primary phase in the move

towards settling the succession of species on

which a narural clas-slficaiion can be based.

Fulfilment of these aim.s would allow a betrer

appréciation of the paleobiodiversity of these

organisais and provide a useful rool for measur-

inggeological time.

Acknowl edgmen ts

This study was carried out during the Peri-Tethys

Programmes (Project No. 94-40 and No. 95-18)

GEODtVERSITAS • 1997 • 19(2)

335

De Wever P. ôd Vishnevskaya V. S.

and in the GDR 88. It was financed hy these

programmes and by ihe URA I76t. We are also

gratefui to Dr. E. Urquharf (UCLondon. UK)

who criticised and painsiakingly helpcd co

improve chc mannscripc as well as for

M. Baconat (MNHN, Paris) who carefully

checked the bibliographie référencés.

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Submitred for publication on 15 July 1996;

accepted on 15 December 1996.

368

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

Table 2. — Publications on Mesozoic radiolarians, with indications of the localities, involved âges and main topic (except publications

dealing with European part of the former Soviet Union, see table 1).

LOCATION

AGE

TOPIC

AUTHOR

Czc Mzc

Evolu.

Kellogg D E. 1982

Pzc Mzc

Gener. Strati Evolu.

KtingS.A. 1978

Mzc Czc

Taxon. DSDP14

Petrushevskaya M. G. & Koziova G. E.

1972

Mzc

Taxon. Skelet.

NaKaseko K. & Yao A. 1973

Czc Mzc?

Levyktna 1, E. 1984

Czc Mzc Pzc

Taxon. Gener.

Moore R. C, 1954

E.Cret.-LJur.

Khabakov A. V, 1937

Cret.

Taxon. N.Sp.

Foreman H. P. 1966

Mzc

Skelet.

DellandreG 1964

Tr.

Taxon. N.Sp. Evolu.

Dumitrica P. 1978a

Mzc Czc

General

DellandreG 1953

Mzc

General Skelet. Morphogen.

DeflandreG. 1960

Czc Mzc

Skelet. Growth Morphogen.

Deflandre G. & Deflandre-Rigaud M. 1958

Mzc

Taxon. N.Sp.

KozurH 1979

PCzc? Mzc?

Plankton

Meyen F, J. 1896

Mzc Czc

Taxon, Evolu. Skelet.

Petrushevskaya M G. 1981

Mzc Czc

Taxon. Skelet.

Petrushevskaya M. G. 1986

Mzc

DSDP26

Pessagno E. A Jr S Michael F. Y. 1974

Pzc-Czc

General Taxon. Biol. Strati

Goll R. M. S Merinteld E. G. 1979

Czc Mzc Pzc

Sedim. Review of papers

HillW 1912

Mzc Czc

Taxon, Skelet,

Petrushevskaya M. G. étal. 1976

Taxon. Skelet.

Petrushevskaya M, G. 1979

Czc

Taxon Skelet.

Petrushevskaya M G. 1975b

Czc Mzc

Skeleton Ontogen. Shape

Nishimura H. 1986

Mzc Pzc

Taxon. Skelet.

Petrushevskaya M. G. 1975a

L.Cret.

DSDP29

Pessagno E, A. Jr 1975

Mzc Czc

Taxon.

Petrushevskaya M G. 1975c

Jur.Czc.

Taxon.

Dumilrtca P, 1988

Late Cret.

Taxon. Evolu.

Empson-Morin K. M. 1982

Cret.

Taxon, Strati

Sanfilippo A & Riedel W. R. 1985

M.Cret. Recent

Skelet

Thurow J. 3 Anderson R. 0.1986

Jur.

Taxon. Skelet

TaKemura A. 1986

Mzc Czc

Taxon.

Riedel W.R. 1967a

Czc

Taxon.

Riedel W. R 1967h

Mzc

Strati Taxon.

Tshedia D. M. 1985

Cret.

DSDP7

Forwman H. P. 1971

Mzc Cret.

Strati Taxon. DSDP20

Foreman R P. 1973b

Cret. Czc

Taxon. Evolu.

Dumftnca P. 1985

Pzc-Czc

Taxon.

Dumitrica P. 1984

Technic. SEM Taxon.

De Wever P. 1980

Mzc

Evolu. Biol.

Doderline L. 1887

Pzc-Czc

Gener. Taxon.

Dumitrica P. 1979

Pzc Mzc

General Taxon.

Forernan H P, 8 Riedel W. R. 1972

Cret.-Czc

Taxon. Strati DSDP10

Foreman H. P. 1973â

Taxon.

Cordey F et ai 1988

Czc Mzc?

DSDP1

Ewing M. et ai 1969

Mzc Czc

Taxon. Gener.

Deflandre-Rigaud M-1969

Africa Algeria

Cret. Alb.'Cenom.

Magné J. & Sigal J. 1953

Amer. N.England, Austral. California

Pzc Mzc

Biake M. C. Jr & Murchey B.L. 1988

GEODIVERSITAS • 1997 • 19(2)

369

De Wever P. & Vishnevskaya V. S.

LOCATION

AGE

TOPIC

AUTHOR

Amer.C.

Mzc

Taxon. DSDP

Pessagno E. A. Jr & Longoria T. J. F. 1973

Amer.C.

Earl.Cret. Mzc

Alcocer V. M. D. 1960

Amer.C. Calif. Mexico (B. California)

LTr.

Strati Taxon.

Pessagno E. A. Jr et al. 1979

Amer.C. Carib. Bahama

Mzc

DSDP1

Pessagno E. A. Jr 1969

Amer.C. Carib. Cuba

Mzc

Vishnevskaya V. S. étal. 1982

Amer.C. Carib Venezuela

Jur.-Cret.

Strati Ophioi.

8eck C. et al 19S4

Amer.C. C. Rica, Teihys. Greece. Italy

L.Jur.-Earl.Cret

DSDP

DevosI 1903

Amer.C. Costa Ricaindian

Jur.-Cret.

DSDP Taxon. Strati

Orlglia-Devos 1 1983

Tethys Greece Italy (Siolly)

Amer.C Costa Rica,

Earl.-Mid.Jur.

Strati Taxon.

De Wever P et al. 1985a

Amer.C. Costa Rica

Strati OphiûL

Bourgois J. étal 1982

Wildberg H. efaM982

Amer.C Costa Rica Nicoya

Strati Ophioi. Radt

Schmidt-Effing R. 1980

Amer.C. Costa Rica Nîcoya

Jur.-Cret.

Strati Ophioi.

Schmidî'Eriing R_ 1979

Amer.C. Costa Rica Nicoya

Cret.

Strati

Scrimidt-Eftmg R, étal. 1980

Amer.C. Costa Rica Nicoya

Cret.

Strati Radl

Schmidt-Effing R. 1980

Amer.C. Costa Rca. Nicoya

Radt Ophiot. Sedim.

Gursky H.-J, & Schmidt-Effing R. 1983

Amer.C. Costa Rica Nicoya

Jur-Cret.

Radt Ophioi.

Stainherg E. 1908

Amer.C. Costa Rica Nicoya

M.-Cret.

Strati

Sctunidt-Etfing R. 1980

Amer.C. Costa Rica Ncoya

Mzc

Ophioi.

Gursky H.-J. 1988

Amer.C. Costa Rica NW. Nicoya.

Jur.-Cret.

Strati Sedim.

Gursky H -J Qlai 1982

Amer.C. Cuba.

Campan.

Strati

Florez Albin E. 1980

Amer.C. E.Mexico,

Tithonian

Taxon.

Yang Q & Pessagno E. A. 1989

Amer.C. Puerto Rico

Jur.-E.Cret.

Taxon. Strati

Mattson P- H. & Pessagno E. A. Jr 1979

Amer.C. Tethys

Jur.-Cret.

Radt

De Wsvor P. et al 1986a

Amer.C. W.Atlant. Blake Bahama

M.Jur.

Yamamoto H. étal. 1985

Amer.N.

Jur.

Taxon.

Pessagno E A. Jr et al. 1989

Amer.N.

Tr.

Biozon. Taxon. Strati

Blome C, D. I9a4b

Amer.N.

Jur.

Strati Zones

Pessagno E. A. Jr étal. 1987

Amer.N.

Mzc

Taxon. Strati Gener.

Campbell A, S. & Moore R. C. 1954

Amer.N. Alaska

Tr.

Biostr.

Biome C D. et al 1989

Amer.N. Alaska. USA

Earl.Mzc

Paleogeog. Envir.

filome C. D. 1987

Amer.N. Calif. Franciscan

Jur.-Cret.

Strati

Davis E- F 1918

Amer.N. Calif. ex-USSR Asia Japan

Mzc

Bioz.

Vishnevskaya V. S. 1985

Tethys Europe

Amer.N. Calif.

Jur.-Cret.

Taxon.

Pessagno E. A. Jr 1973

Amer.N. Calif.

Cret.

L.Maastrichtian

Taxon. Strati

Foreman H. P. 1968

Amer.N. Calif.

L.Jur.

Ophioi.

McLaughIln R. J. & Pessagno E. A. Jr 1978

Amer.N. Calif.

Czc Mzc?

Sedim.

HindeG. J t894

Amer.N. Calif.

Tr.-Cret.

Taxon.

Pessagno E. A. Jr 1977c

Amer.N- Calif.

LCret.

Taxon.

Pessagno E. A. Jr 1971a

Amer.N. Calif.

Jur.-Cret.

Taxon.

Pessagno E. A. Jr 1971b

Carib. Bla.-Bahama Gr.Valley

Amer.N. Calif. Coast Ranges

L.Jur.-Cret.

Strati Taxon.

Pessagno E. A. Jr 1977a

Amer.N. Calif. Franciscan

Amer.N. Calit. Franciscan Gr.Valley

Taxon.

Riede* W, R. & Schtocker J. 1956

Seidera V M. étal. 1979

Amer.N- Caüt. Fransclscan

Jur.

Radt Ophioi. Strati Lithol.

Murcliey B. 1984

Amer.N, CartI. Gr.Valley Blake-Bahama

Cret.

Taxon.

Pessagno E A Jr 1972

Amer.N. Calif. Gr. Valley California

L.Cret.

Strati Taxon

Pessagno £. A. Jr 1976

Amer.N Calif. Gr.Valley Franciscan

Ë.Cret.

Strati Taxon.

Pessagno E A. Jr 1977b

Amer.N. Calit. Great Valley

L.Cret.

Taxon.

Pessagno E. A. Jn970

370

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

LOCATION

AGE

TOPIC

AUTHOR

Amer.N. Calif. Klamaîh

Perin.-Tr.

N.Sp. Paleoenvir.

Noble P. & Renne P. R. 1988

Amer.N. Calif. S.KIamath

Strati

Irwin W. P. étal. 1977

Amer.N Calif. Teüiys

Pzc-Czc

Skelet.

De WeverP-1986

Europe (Italy. Spam. France)

Amer.N California,

M.-LJur.

Taxon.

Pessagno E. A. Jr & Blome C. D. 1982

Amer.N. California

LCret.

Taxon.

Campbell A. S. ik Clark B. L. 1944

Amer.N. Canada (Br.Columb.)

Devon.-Jur.

Taxon.

Cordey F. & De Wever P. 1988

Amer.N Can. (Br Columb ) CacheCreek

Jur.

Strati

CordeyF-fifaf 1987b

Amer.N. Can. (Br.Columb.) CacheCreek

Perm.-Jur.

Strati

Cordey F. et al. 1987a

Amer.N. Canada Alberra

Cret.

Wall J H. 1975

Amer.N. Canada Oueen Charlotte

Tr. (L. Nor.)

Carter E. S. 1988

Amer.N Canada Oueen CharloHe

Eari.-Mid.Jur.

Biostr, Taxon.

Carter F. S. étal. 1988

Amer N Canada Queen CharioUe

Earl.-Mid.Jur.

Biostr. Taxon.

Carter E- S 19B5

Amer.N. Can. Oueen Charlotle (Kunga)

L.Tr.

Strati

Carter E. S. et at. 1989

Amer N Coiofado, Kansas

Crel.

Strati Taxon

Bergstfesser T J î983

Amer.N. E.AIaska

L.Tr,

NSG N.Sp.

Robinson B E. 8 ^essagno E. A. Jr 1988

Amer.N E Atlantic Europe

Cret.

Strati Taxon.

Forernan H P. 1977

Amer.N. E.Oregon (Blue-Mts E.Oregon)

Pzc-Mzc

Environ. Biostr.

Blome C. D, étal 1986

Amer N E.Oregon W ldaho.

Tr.-Cret.

Biogeo Ecolo. Taxon.

Pessagno E A Jr & Blome C. D. 1986

Amer.N. E-C.Oregon

Lias.'Dog.

Taxon Cladist.

MacLeoci N. 1988

Amer.N. East-C.Oregon

Tr.-E.Jur.

Taxon.

Yoh K. Y. 1987

Amer N. East-C.Oregon.

Mzc

YehK.-H 1989

Amer.N. EasLC.Oregon.

Tr.

Yeh K.-Y 1988

Amer N Europe E Atlantic

Cret.

Strati Taxon.

Forernan H.-P. 1977

Amer.N. NW.Nevada

Jur.-Cret.

Ophiol. Strati

Sûsson M. et al. 1984

Amer.N. Oregon

L.Tr.

Taxon. Strati

Blome C.D. 1983

Amer N Oregon British Columbia-

L.Tr.-Jur.

Taxon. Strati

Pessagno E A, Jr & Blome C. D. 1980

Amer.N. S.AIaska E.Oregon.

Mid.Jur. (Callov.)

Taxon. Strati

Blome C.D, 1984a

Amer.N SW Oregon Strati

Mzc

Carayon V étal. 1984

Amer.N. SW.Oregon Klamath

Tr.

Strati Ophiol.

Roure F & De Wever P. 1983

Amer.N. USA Canada

Jur.

Taxon.

Pessagno E A, Jr étal. 1986

Amer.N. W.Cafii.

L.Mzc

Saiders V M. & Blome C. D. 1988

Amer NW. Amer.N. Calif.

L.Jur.

Strati

Pessagno E A. Jr étal. 1984

Amer.S. Argenlina (Neuquén)

Jur.-Cret.

Biostr.

Pujana 1. 1988

Amer.S. Feuerland

Cret.

Richler M. 1925

Amer.S. Tripoli (Chile)

Czc Mzc

Taxon. N.Sp. Strati

FrenguelliJ 1941

Asia Austral.

Sedim.

Kobayasht T. 1944

Asia China Himalaya Tibet Gyangze

Cret.

WuH.-R.SLiH.S-ig82

S.XIzang (Tibet)

Asia China Himalaya Tibet Xizang

Asia China Himalaya Tibet Yariung

Cret.

Wu Hao-ruo étal. 1977

Wu Hao-ruo 1980

Zangpo

Asia China Japan Sikhote-Aiin

Tr.-Jur.

Kojima S. 1989

Asia China S Tibet

L.Jur.-E.Cret.

Wu H. 1988

Asia China S.XIzang

Tr.-E.Jur.

Taxon.

Yigang W. & Yujing W. 1976

Asia China S Xizang

Asia China Sea

Mzc?

Plankton

Wang Yujing & Sheng Jinzhang 1982

TanZh,&Su X. 1982

Asia China Tibet Himalaya

Cret.

Ophiol.

Wu Hao-ruo 8 Wanming D. 1980

Zangbo Xizang

Asia China Tibet S.Xizang

Cret. Cenom.

Taxon. N.Sp.

Wu H R. 1986

Asia China Tibet Xizang

Jur. E.Tithon.

Taxon.

U H. S. 1986

Asia China Tibet Xizang

E.Jur. (L.Pliensb)

Li H. S. 1988

GEODIVERSITAS • 1997 • 19(2)

371

De Wever P. & Vishnevskaya V. S.

LOCATION

AGE

TOPIC

AUTHOR

Asia China Xish Island

Taxon. N.Sp.

Xinghui S. 1982

Asia China.E

Strati

Zhiyuan T. & Tsorun T. 1976

Asia China.NE.

Tr.-Jur.

Kojima S. & Mizutani S. 1987

Asia China.NE

Tr.-Jur.

Satoru K. & Mizutani S. 1987

Asia ex-USSR Crimea

Ecolo.

TshedlaD, M. 1981

Asia ex USSR E.Sakhalin

Tr.

Strati

Bragin N. Ju. 1985

Asia ex-USSR NW.Uzbek.

Mzc?

Averburg N. V. & Kestner F. F. 1973

Asia Himalaya Tibet, Ladakh

Mzc Eoc.

Biostr. Strati Ophiol.

Coichen M. étal 1987

Asia India

Ophiol.

Gbosh S. efaf. 19B4

Asia Indones. Bornéo Molukken

Jur.-Cret.

Tan Sln-Hok1927

Asia Indones.

Strati Taxon.

Tan Sin Hok 1931

Asia Japan

Strati

Ichikawa K. 1946

Asia Japan

Mzc? Pzc? Czc?

Diagen. Silica

NagaiaK. 1986

Asia Japan

L.Jur.-Cret.

Taxon. Strati

Nakaseko K. & Nishimura A. 1981

Asia Japan

L.Tr.

Taxon. Strati

Nakaselo K, & Nishimura A. 1980

Asia Japan

L.Jur.

Taxon. Strati

MatsuûkaA I984a

Asia Japan

Cret.

Taxon. Strati

Nakaseko K. e/a/ 1979a, b

Asia Japan

Sedim. Mélangé Strati

Nakazawa K. étal. 1983b

Asia Japan

Gen.geol.

Strati

Nakaseko K. étal. 1983

Asia Japan

L.Tr.-E.Jur.

Biostrl

Igo H. 8 Nishimura H. 1984

Asia Japan

Jur.

Zonation Strati

Matsuoka A & Yao A. 1986

Asia Japan

Czc Mzc

Kobayashi T & Kimura T. 1944a

Asia Japan

Jur.-Cret.

Taxon. N.Sp.

Ichikawa K_ & Yao A. 1976

Asia Japan

Mzc

Strati

Ichikawa K. 1986

Asia Japan

PzC'Czc

Ichikawa K. 1953

Asia Japan

Permo-Tr.

Evolu.

Kobayashi T. & Kimura T. 1944b

Asia Japan

Mzc

Mizutani S. 1987

Asia Japan

Tr.-Jur.

Kido S. 1982

Asia Japan

Mzc Pzc

Gener.

Kimura T. 1944c

Asia Japan

Tr.-Cret.

Sedim. Strati

Matsuoka A. 1983b

Asia Japan

Perm.-Tr.

Strati

Koike T. étal. 1974

Asia Japan

Mzc? Czc

Strati

Nakaseko K. 1979b

Asia Japan

Czc

Geol. Strati

Nakaseko K. e/a/ 1979

Asia Japan

Lias.

Strati

Isozaki Y & Matsuda T. 1985

Asia Japan

Cret.

Strati Correl.

Nakaseko K. 1979

Asia Japan

Jur.

Strati Taxon.

IsozaktY état. 1981

Asia Japan

Tr.-Jur.

Taxon.

Yao A- & Ifihikawa K. 1969

Asia Japan

Jur.-Cret.

Extinc. Taxon. Strati

Matsuoka A. l9SÇa

Asia Japan

Jur.

Biostr.

Yao A. 1986

Asia Japan

Sugano K & Nakaseko K. 1970

Asia Japan

Jur.

Environ.

SunouchiH. étal. 1982

Asia Japan

Tr.-Jur.

Strati Taxon.

Yao A 1982b

Asia Japan

L.Cret-Czc

Strati

Nakaseko K. étal. 1965

Asia Japan

Kimura T. 1944a

Asia Japan

Jur.

Taxon. Strati

Mizutani S. ùtal 1984

Asia Japan

Jur.-Cret.

Strati

Fujimoto H. 1933b

Asia Japan

Cret.

Murata M. étal. 1962

Asia Japan

Carboniferous-Jur.

Strati

Naka T. & Ishiga H. 1987

Asia Japan

Tr.-Jur.

Silica Geoch.

Kakuwa Y-1907

Asia Japan

Pzc-Mzc

Strati

KoiKe T S Takashima K. 1983

Asia Japan

History

Sugano K. 1975

Asia Japan

Mzc

Okimura Y. et al. 1986

372

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Plaiform

LOCATION

AGE

TOPIC

AUTHOR

Asiâ Japan

Jur.

Taxon. Strati

Wakita K. 1982

Asia Japan

Strati

Suzuki J. 1939

Asia Japan

Jur.

Taxon. Evolu.

Takemura A. S Nakaseko K. 1983

Asia Japan

Mzc

Sedim.

Sugano K. 1986

Asia Japan

Tr.

Taxon.

SalùT. étal. 1982

Asia Japan

Strati Plankton

Takemura A 1980

Asia Japan

Jur.

Sashrda K, étal. 19823

Asia Japan

E.Jur.

SashidaK étal. 1986

Asia Japan

Tr.-Jur.

Taxon.

Salo T & Nlshizono-Y. 1983

Asia Japan

L.Cret.

Geol.

KurImotoC 1982

Asia Japan

Jur.

Taxon.

Sugano K. & Nakaseko K. 1968

Takemura A & Nakaseko K. 1982b

Asia Japan

Jur.

Taxon.

Takemura A. & Nakaseko K. 1982a

Asia Japan

Jur.

Strati

Mâlsuoka A. 19853

Asia Japan

M.Jur.

Yokota S SSanoH 1986

Asia Japan

Tr.

Takashima K. & Koike T. 1982

Asia Japan

Jur.

Taxon.

Takemura A. 8 Nakaseko K. 1982c

Asia Japan

Jur.

Taxon. Strati

Matsuûka A. 19860

Asia Japan

Mzc Czc

Strati Gen.geol.

Takeshita T. 1982

Asia Japan

Taxon. Skelet. Evolu.

Takemura A. & Nakaseko K. 1986

Asia Japan (Shikoku) Tethys Italy

Mid.Jur.-Earl.Cret.

Biostr. Strati

AilaY 1987

Asia Japan Boso Chiba

Czc? Mzc?

Kanomata N. S Iwashita F. 1964

Asia Japan Chichibu

Taxon. Strati

FujiinotoH. 1939

Asia Japan Chichibu

Mesozoic

Strati

MalsuoKa A. 1986b

Asia Japan Chichibu

Pzc-Mzc

Gen.geol.

Owada K SSakaY 1982

Asia Japan Chichibu Kyushu

Tr.-Jur.

Biostr.

SatoT étal. 1986

Asia Japan E.Hokkaido

Cret.

Kimmami K. étal. 1983

Asia Japan E.Shikoku

Mzc

Strati

IshkJaK. 1986a. b

Asia Japan Gifu

Tr. Jur.

Wakita K.&lsomiH, 1986

Asia Japan Hidaka

L.Cret.

Iwala K. 8 Kato Y, 1986

Asia Japan Hokkaido

Strati

Nagala K. 1982

Asia Japan Hokkaido

Jur.-E.Cret.

Strati

IshizuKa H et al. 1984

Asia Japan Hokkaido

Cret

Strati Gen.geol.

Takotani Y. 1982

Asia Japan Hokkaido

E.Cret.

Strati

Minoura N. étal. 1982

Asia Japan Hokkaido

Aptian

Okada H. étal 1982

Asia Japan Hokkaido

Cret.-Czc

Strati

Nagata K. 1979

Asia Japan Hokkaid

(Mioc.-Quater.)

Cret.

Tajika J. & Iwata K, 1983

Asia Japan Japan.C.

L.Cret.

lyota N, et ai 1984

Asia Japan Kochi

Jur.

Biostr. Strati

AitaY 1982

Asia Japan Kyushu

Mzc

Nishizono Y et ai 1982

Asia Japan Kyushu

Mzc

Sedim.

Nishirono Y. & Muraia M. 1983

Asia Japan Kyushu

LJur.

Tanaka H. étal. 1985

Asia Japan N.Hokkaido

E.Cret.

Strati

Igo H. et al. 1987

Asia Japan N.Shimanto

Cret.

Okamura M. 1981

Asia Japan N.Shimanto

L.Cret.

YamauchI M. 1982

Asia Japan N.Shimanto Shikoku

L.Jur.-Earl.Cret.

Strati

AokiT 1982

Asia Japan Okinawa

Cret.

Taxon.

Fujlta H. 1983

Asia Japan Okinawa

Asia Japan S.Shikoku

Sedim. Gen.geol.

Ujiie H. & Hashimolo Y. 1983

YeharaS, T926

Asia Japan Sakawa Tosa

Asia Japan Sambagawa

Jur.

KImuraT 1944b

Kobayashi T. 1941

GEODIVERSITAS • 1997 • 19(2)

373

De Wever P. & Vishnevskaya V. S.

LOCATION

AGE

TOPIC

AUTHOR

Asia Japan SE.Kanto

Czc? Mzc

Taxon. Strati

Ichikawa K. 1950

Asia Japan Shikoku

Mzc

Nakagawa C. & Nakaseko K. 1977

Asia Japan Shikoku

L.Jur.-Cret.

Strati

Nakagawa C. efai 1980

Asia Japan Shikoku

Jur.

Bioslr, Strati

AltaY. 1985

Asia Japan Shikoku

Suyari K. & Kuwano Y. 1986

Asia Japan Shikoku

Jur.

Taxon. Strati

Matsuoka A. 1982a

Asia Japan Shikoku

Tr.-Jur.

Taxon.

Yehara S. 1927

Asia Japan Shikoku

Tr.-Jur.

Strati Sedim.

tshlda K. 1985

Asia Japan Shikoku

E.Cret.

Okarnuia M. & Ulo H. 1982

Asia Japan Shikoku

Cret.

OkamuraM, & Matsugi H. 1986

Asia Japan Shikoku

LCret.

OKamurà M et ai 1982

Asia Japan Shimanto

Cret.

Strati

Aoki T S Tashiro M. 1982

Asia Japan Shimanto

Mzc

Suyari K. 1986a.b

Asia Japan Shimanto Shikoku

Mzc

Strati

Suyari K. & Yamasaki T. 1988

Asia Japan SW.Hokkaido

Jur.

Tecton.

Ishiga H, & (shiyar»a D. 1987

Asia Japan Tethys

LJur.-Earl.Cret.

AitaY.&Okada H. 1986

Asia Japan. Tethys Europe ex-USSR

Mzc

Bioz.

Vishnevskaya V. S. 1985

Amer.N. Caltf.

Asia Japan W.Shikoku. Chichibu

Jur.

Kashima N. 1986

Asia Japan.C.

Jur.

Taxon. Strati

Mizulani S. & Kido S. 1983

Asia Japan.C.

Tr.

Radt Sedim.

Sugisaki R et ai 1982

Asia Japan.C.

E.Cret.

Wakita K, 1988

Asia Japan.C.

Otsuka T. 1986

Asia Japan.C.

Tr.-Jur.

Taxon.

Yao A- ef al 1980

Asia Japan.C.

E.Jur.

Taxon.

SashkJa K. 1988

Asia Japan.C.

L.Tr.-Earl.Jur.

Biostr.

Yoshida H 1986

Asia Japan.C.

M.Jur.

Biozon. Biostr.

Matsuoka A. 1988

Asia Japan.C.

Jur.

Taxon. Strati

MizutaniS. étal. 1982a

Asia Japan.C. (Mino terr.)

Jur. Mzc

Strati

Adachi M 1982

Asia Japan.C. Fukui

Jur.

Hattort 1.1987

Asia Japan.C. Fukui

Lias.-Dog.

HattOfil 1988

Asia Japan.C. Gifu

Mzc

Sedim.

Wakita K. & Okamura Y. 1982

Asia Japan.C. Inuyama

Lias.

Taxon.

Mon R. â Yao A. 1988

Asia Japan.C. Inuyama

Earl.Jur.

Mon R. 1986

Asia Japan.C. Kanto

Cret.

Htsada K.-l. eial 1986

Asia Japan.C. Kanto

Jur.-Cret.

Hisada K,-l & Kishida Y. 1986

Asia Japan.C. Mino

Mzc

Genesis Silica Radt Environ.

Hattori 1, 1984

Asia Japan.C. Sambagawa

Sedim. Diagen.

Huzimolo H- 1938

Asia Japan.C.

Perm.-Jur.

KoJimaS. 1982

Asia Japan.C.

Tr.

Taxon. Strati

Mizulani S. et ai 1981b

Asia Japan.C.

L.Tr.-E.Jur.

Strati

Kishtda Y & Hisada K. 1985

Asia Japan.C.

M.Tr.-E.Jur.

Taxon,

Yao A. 1982a

Asia Japan.C.

Jur.

Sedim. Radt

WakiiaK. 1983

Asia Japan.C.

L.Jur.-Cret.

Strati

Yamamoto H 1983

Asia Japan.C.

Jur.

Gen.geol.

WakiiaK. 1983

Asia Japan.C.

Strati

Kishida Y & Hisaoa K. 1986

Asia Japan.C.

Jur.

Strati

Mizulani S. et ai 1981a

Asia Japan.C.

Cret.

Taxon.

Sashida K et ai 1984

Asia Japan.C.

Mzc

Sedim Taxon.

Yoshimura M. et ai 1982

Asia Japan.C.

Tr.-Jur.

Taxon.

Yao A. 1972

Asia Japan.C.

Tr.-Jur.

Taxon.

Yao A, 1979

Asia Japan.C.

E.Tr.

Taxon.

Sashida K. 1983

374

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

LOCATION AGE TOPIC AUTHOR

Asia Japan.C.

Asia Japan C.

AsiaJapan.N. Hokkaido

Asia Japan.N. Hokkaido

Asia Japan N. Hokkaido

Asia Japan.N. NE.Hokkaido

Asia Japan NE.

Asia Japan.SW.

Asia Japan SW.

Asia Japan.SW.

Asia Japan SW.

Asia Japan.SW.

Asia Japan.SW,

Asia Japan.SW.

Asta Japan.SW.

Asia Japan.SW.

Asia Japan.SW. E.Shikoku

Asia Japan.SW- Kii

Asia Japan.SW. Shikoku

Asia Japan.SW. Shikoku Awaji

Asia Japan.SW. Shikoku

Asia Pacif. Indones. C.Celebes

Allant.

Allant. Carib. (Bahamas)

Allant. Carib. (La Desirade, Les Antilles)

Allant. Europe

AUanl. Europe N.Sea.

Allant.C. Carib. Barbados

Altanl.NE. (off Africa)

AHanl.SE

Atlantic NE.Méditer.

Tr.-Jur.

Taxon. Strati

Cret.

Taxon. Strati

Strati

Jur.

Strati

LTr.-Mid.Jur.

Strati Tecto.

L.Jur.-E.Cret.

Taxon. N.Sp.

L.Jur.

Ophioi.

E.Cret.

Jur.-Cret.

Mzc

Perm.-Tr.

Tr.-Jur,

Taxon.

Jur.

Tr.-Jur.

Taxon.

Mesozoic

Strati

LJur.

Taxon. Strati

Jur.

Strati

L.Tr.-Eari.Jur.

Biostr

Jur.(Dog.)

Strati

Tr.-Jur.

Taxon.

Strati

Perm.

Envir,

Mzc

Envir, Radt

M.Jur.

Taxon. Strati

L.Tr.

Taxon. N.Sp.

Tr.-Jur,

Strati

Permian

Tr.

Taxon. Strati

Tr.-Jur.

Strati

Mid,L.Jur.

Taxon Strati

Jur.

Strati

Cret.

Envir,

Mzc

Strati

Gen.geol.

Cret.

Taxon. Strati

L.Jur,

Taxon. Strati

M.L.Jur.

Strati

Czc Mzc

Tr.-Jur.

Strati

Mzc

Taxon. DSDP

Cret.

Biostr.

M.Cret.

Sedim. Gen.geol. Strati

Czc Mzc

Taxon.

Mid.Jur.-Earl.Cret

Strati

Earl.Cret.

L.Jur -E.Cret.

Review Biostr.

Mzc

Cret,

DSDP41

Cret.

DSDP40 Taxon. Strati

Cret.Quatern.

DSDP13Taxon. Strati

Mizulani S. S Koike T. 1982

IwasakiT. étal. 1984

KtdoS

MizutantS. 1981

Hattori I. & Yoshimura M. 1983

Kawabata K. 1988

IshizukaH étal, 1983

Kame Y. et ai 1981

Iwaia K. eral. 19S3a,b

Matsuoka A. 1987

Ishiga H. â Kusu T. 1986

Yao A- étal- 1982

SakaY 1983

Yao A. 1983

Nakdseko K. 1381

Maisuoka A. & Yao A. 1985

MatsuoKa A. 1984b

Hori R. 1988

ImolQ N -et al 1982

Yao A. 1981

Ichikawa K. el al. 1985

ImoloN t984a

Imoiû N. 1984b

Matsuoka A. 1985b

Nakaaehû K. & Nishimura A. 1979

Kishida Y, iSi Sugano K. 1982

IsozakI Y. 1986

ISDzaki Y Matsuda T. 1980

Malsuda T. & IsozakI Y. 1982

Matsuoka A 1982b

Hayasaka Y étal, 1983

Nbkazawa K. et al, 1983a

Karnoii M & Takelomi H. 1982

Yanai S. 1983.

Matsuyania H et al. 1982

Matsuoka A. 1986d

MalsuokciA. 1983a

YamafiaMT, 1987

IshidaK. 1983

HindeG J. I917

Rieoel W.-R, 1971a

Cita M B- e/a/. 1970

SchaatA. 1985

Ehrenberg C. G. 1854

Baumgartnor P O 1983

Bouysse P étal 1983

Swain r M. 1977

Dyer R. & Copestake P. 1989

Ehrenberg G. G. 1846

Foreman H. P. l97Sb

Foreman H, P 1978a

Dumitrlca P. 1973

GEODIVERSITAS • 1997 • 19(2)

375

De Wever P. & Vishnevskaya V. S.

LOCATION

AGE

TOPIC

AUTHOR

Atlantic E. Europe Amer.N.

Cret.

Strati Taxon.

Foreman H. P. 1977

Austral. Indones. New Guinea

Strati

Crespin !. 1958

Canada (Queen-Charl.)

Lias. Dog.

Taxon,

Pessagno E. A Jr& Whalen P. A. 1982

Calif. E-C.Oregon

DSOP16

Mzc-Czc

Strati

Dinkelman M. G. 1973

Europe Amer.N. E.Atiantic

Cret.

Strati Taxon.

Foreman H. P. 1977

Europe C. Roland

Cret.

Morphol.

GorkaH. 1988

Europe E.Atiantic Amer.N.

Cret.

Strati Taxon.

Foreman H. P. 1977

Europe England (Kimmeridge)

Jur. (Kimm.)

Boréal

Downie C. 1956

Europe France (Ardèche)

Late Tithon.

Taxon,

Cayeux L. 1896

Europe France (Larzac)

Mzc

Bergounioux F. M. 1950

Europe France (Pans Basin.) Belgium

Mzc

Chalk Sedim.

Cayeux L. 1897

Europe Italy Sicily

M.Jur.

Kilo el ai 1990

Europe

Mzc

Taxon, Evolu. Strat. Techn.

De Wovor P.. Riedel W. étal. 1979b

Europe N,France

Jur. (Oxf.), Eoc.

Cayeux L. 1891

Europe N.Germany

Cret.

Taxon.

Ziltel K A- 1876

Europe Roland Krakau

L.Jur.

Wlsniowskt T. 1889

Europe Slovak. Czcek.

Tr.-Jur.

Ophiol. Radt

Dumilrica P & Meilo J. 1982

(Meliata, Silica, Slovak Karst)

Europe Turkey

Lias.

Taxon.

Pessagno E. A. Jr & Poisson A. 1981

ex-USSR

Mzc Czc?

Strati

Zhamoida A-1,1975

ex-USSR

Mesozoic

Strati

Zhamoida A. 1.1972

ex-USSR

Pzc Mzc

Taxon.

AlanasievaM S 1986

ex-USSR

Mzc

Strati

Zhamoida A. 1. 1981

ex-USSR

Mesozoic

Strati

Zhamoida A. 1 1961

ex-USSR

Mzc

Zhamoida A. 1. & Kazintsova L. 1981

ex-USSR

Cret.

Biostr.

Kazinisova L. 8 Vishnevskaya V. 1988

ex-USSR

Cret.

Strati

Rundyova N P. 8 Jinoridze N. 1975

ex-USSR

Cret.?

Taxon. N.Sp. Strati

Vishnevskaya V. S. 1985a

ex-USSR

Cret.

Taxon. Strati

Vishnevskaya V S. 1981b

ex-USSR

Cret. Cenom.

Kazintsova L 1 1981

ex-USSR

Mzc

Taxon. Skelet.

Vishnevskaya V. S. 1981c

ex-USSR Amer.N. Calif, Asia Japan,

Mzc

Bioz.

Vishnevskaya V S. 1985

Tethys Europe

ex-USSR Carpath. Ukrain.

Jur.

Strati

Lozynyak P. Yu. 1981

ex-USSR Carpath. Ukrain.

Cret.

LozynyakP.Yu. 1975

ex-USSR E. Sakhalin

Mzc

Strati

Zhamoida A I 1968

ex-USSR E.Sakhalin

L.Cret.

Kazintsova L. 1985

ex-USSR E.Siber. Sikhote Alinj

Mzc

Eliseeva V. K. étal. 1976

ex-USSR Far East

Cret.

Taxon. Strati

Vishnevskaya V S. 1981 a

ex-USSR Greater & Lesser Caucasus

ex-USSR Kamchatka

ex-USSR Kamchatka Asia

L.Jur.-Cret.

Biostr.

Vishnevskaya V. S. 1988a-c

RijnevaN-P 1975

Vishnevskaya V S. & Bernard V. V. 1986

ex-USSR Kazakhstan

Czc? Mzc?

Strati

Pupyshev N A 8 Lipman R. 1973

ex-USSR Kodak

Mzc

Strati

Bogdanov N A, étal. 1982

ex-USSR Koryak

Mzc

Strati

VishnevsKaya V. S. étal. 1981

ex-USSR Koryaksk

Valanginian

Strati

Dundo OPA Zhamoida A. 1.1963

ex-USSR Lesser Caucasus

Mzc

Strati

Zhamoida A 1 efa/. 1976

ex-USSR Mid.Asia

Mzc

TshediaD. M, 1984

ex-USSR N Pacif, Bering Polar

M.L.Cret.

Biozon. Strati Environ.

Vishnevskaya V. S. 1986

ex-USSR Olulor

Cret.-Czc

Strati

Vishnevskaya V. S. 1984a, b

ex-USSR Olyutor Koryak

Cret.

Vishnevskaya V. 5. 19B7a, b

376

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

LOCATION

AGE

TOPIC

AUTHOR

ex-USSR Russia

Pzc-Mzc

Gener.

Lipman R. Kh. 1976

ex-USSR Russia

Mzc

Evolu. Taxon.

Lipman R. Kh. 1975b

ex-USSR Russia

Jur.-Cret.

Strati

Lipman R. Kh. 1979b

ex-USSR Russia

Paleogene-L.Cret.

Strati

Lipman R. Kh. 1975a

ex-USSR Russia

L.Cret.

Taxon.

Lipman R, Kh. 1952

ex-USSR Russia Far East

Mzc

Lipman R. Kh. 1953

ex-USSR Russia W.Siberian

L.Cret.

Lipman R. Kh. 1962

Turgaisk N.Peri-Aral

ex-USSR Sakalina Kamtchatka

Mzc?

Runeva N. P. 1981

ex*USSR Sakhalin

Mesozoic

Strati

Zhamoida A L 1969

ex-USSR Siber. Russia

Czc Mzc

Lipman R Kh. 1960

ex-USSR Sikhote

Mesozoic

Strati

Zhamotda A. 1.1968

ex-USSR Sikhote-Alin,

Mzc

TiKhomirova L. B, 1975

ex USSR Tadzhik

Cret. Campan.

Taxon. N.Sp.

Goltman E. V. 1984

ex-USSR Tadzhik

Cret. Senon.

Evolu.

GoHmar. E. V. & Babaeva B. 1985

ex-USSR Tadzhiksk

Cret. Senon,

Strati

Goltman E. V. 1981

ex-USSR Tadzhiksk

Ouater.

Cret.

Goltman E. V. 1973

ex-USSR Tadzhiksk

(Campan. Maastr.)

Strati

Goltman E. V. 1975

ex-USSR Tethys Carpath.

Earl.Cret.

TiKhomirova L. B, 1983

ex-USSR Tethys Caucasia

Jur.

Tikhomirova L. B. 1981

ex-USSR Timan-Ural

E.Kimm.

KûZlovaG. E. 1971

ex-USSR Ukrain. Carpath.

Cret.

Kazinlsova Ll. 1984

ex-USSR Urals

Cret.

Biozon.

Amon E. 0.1988

ex-USSR W.Siberia

L.Cret.-Eocene

Koztova G. E. & Gorbovets A. 1966

ex-USSR W.Siberia

Cret. Turon.

Strati

Amon E. O. 1985

Indian S.

Cret.

Riedel W, R, & Sanfilippo A. 1974

Méditer.

M.Cret,

Ecology Biostr.

Thurow J. &. Kuhnt W. 1988

Mid.East Israël

Earl.Cret.-Czc

Reiss Z. 1952

N.Africa

Turon.

Anoxy

Thurow J 1988

Pacif Indones.

Czc Mzc

Sedim.

Hinde G. J. 1897

Pacif.

Cret.

Strati Taxon.

Schaal A. 1984b

Pacif,

Cret.

Strati Envir. Taxon.

SchaafA I984a

Pacif.

Strati DSDP

Riedel W. R, 1981

Pacif. Amer.C.

Strati

White M. P, 1928

Pacif. Austral.

Pzc-Mzc

Tecton.

Flood P. G. 1988

Pacif. Austral.

Mzc

Sedim. Envir.

Fenlon M- W ef al. \ 982

Pacif. Australia

Czc? Mzc? Pzc?

Sedim.

HindeG. J, 1893

Pacif. Indones. Bornéo

Cret.

Hinde G. J. 1900

Pacif. Indones. Bornéo

Tr.

Taxon.

HindeG. J. 1908

Pacif. Indones. Celebes

Mzc?

Hojnos R. 1934

Pacif. Mariana Leg 60

Cret.

Strati DSDP

Kling S. A. 1982

Pacif. New Zealand

L.Tr.

Blome C, 0. état. 1987

Pacif. New Zealand

Jur.

Feary D, A S Hill P. H. 1978

Pacif. New Zealand

Jur.-Cret.

Strati

Feary D. A. 8 Pessagno E. A. Jr 1980

Pacif.N.

Cret.

Strati Taxon. DSDP32

Foreman H. P. 1975

Pacif.SW.

Plankton Geograph.

StevensG R. i960

Pacific Mid.

Cret. Campan.

Taxon. DSDP

Empson-Mofin K M. 1981

Tethys

Tr.-Cret.

Taxon. Evolu.

De Wever P. 1984b

Tethys

Jur.-Cret.

Taxon.

Fischli H. 1916

Tethys

Mid.Jur.-Earl.Cret.

Strati Taxon

Baumgartnef P. 0.1984

GEODIVERSITAS • 1997 • 19(2)

377

De Wever P. & Vishnevskaya V. S.

LOCATION

AGE

TOPIC

AUTHOR

Tethys

Mzc-Czc

Taxon. Evolu.

Dumitrica P. 1983a

Tethys

Jur.

Environ. Sedim. Biostr

Baumgarlner P. 0.1987

Tethys

Mid.-Tr.

Taxon. Evolu.

Dumitrica P. 1983b

Tethys

Tr.-Jur.

Taxon N-Sp.

KozurH- 19a4b

Tethys

Tr.-Jur.

N.Sp, Taxon.

KozurH. 1984d

Tethys

Mid.Tr.

Taxon. N.Sp.

Dumitrica P, 1982b

Tethys

Tr.

Taxon. N.Sp.

Dumitrica P. 1982a

Tethys

Diagen. Sedim. Silica

Hattorl 1, 1989

Tethys

Tr.-Cret.

Taxon. Evolu. Phylogen.

Kilo N. A De WavRr P. 1988

De Wever R & Origlia !. 1984

Tethys

Tr.-Cret.

Taxon. Evolu. Phylogen.

De Wever P. & Or»glia 1. 1983

Tethys Alpes France Ligurian

Jur.

Strati Ophiol.

De Wever P. & Caby R. 1981

Tethys Alps Austha

Jur.

Taxon. Strati

MuzavorS, N.X. 1977

Tethys Alps Austha N.Kalkalpen

L.Jur-E.Cret.

Taxon. Strati

Holzet H -L 1980

Tethys Alps Europe

Mzc

Taxon.

Donofrio D A. & Mostler H. 1978

Tethys Alps Itaiy

Jur.-Cret.

Strati Taxon. Radt

Kocher R. N. 1981

Tethys Alps N.ltaly (Recoaro) Austha

L.Tr.

Taxon. N.Sp.

Lahm B. 1984

Tethys Alps NW.Carpath. Klippen Z.

Mzc

Hojnos R. 1929

Tethys Amer.C,

Jur.-Crel.

Radt

De Wever P, étal. 1986a

Tethys Budva (Moritenegro. Yugoslavia)

Jur.-Cret.

Taxon.

Gorican S, 1987

Tethys Bulgaria Trekljano S.W.Bulgaha

Tethys Carpalh.

L.Jur.

Biostr.

Zagorcev ). & Tikhomirova L. 1986

Orvoldova L. & Pefercakova M. 1987

Tethys Carpath. Klippen

Jur.

Ozvoldova L & Sykora M. 1984

Tethys Carpath. Klippen

L.Jur.

Ozvoldova L. 1975

Tethys Carpalh. Klippen

L.Jur.

Ozvoldova L. 1979a

Tethys Carpath. Méditer. Lasser Caucas.

L.Jur.-Cret.

Tikhomirova L. B. 1984

Tethys Carpalh. Slovak Klippen Podbiel

Jur.

Ozvoldova L. 1979b

Tethys Cret,

Jur.

Taxon. Evolu.

De Wever P 1983

Tethys Cyprus Oman

Jur.-Cret.

Strati

Blome C. D. & Irwin W. P. 1985

Tethys Cyprus. (Troodos)

Cret.-Czc

Strati Envir Ophiol.

Robertson A. H. & Hudson J. D. 1974

Tethys E.Carpathians S.AIps

Tr.

Taxon. N.Sp. Phylogen.

Dumitrica P- 1982c

Tethys E.Rhodope Bulgaria

E.Cret.

Strati

Lipman R. Kh. & Boyanov 1.1976

Tethys Europe

Cret.

Rüst D-1887

Tethys Europe

Cret.

Taxon.

Rûst D. 1888

Tethys Europe

Tr.(Ladin.)

Taxon. N.Fam.

Kozur H. 1988

Tethys Europe

Tr.

Taxon.

Kozur H- & Mostler H. 1984

Tethys Europe

Jur.-Cret.

Taxon.

RüstD. 1898

Tethys Europe

Jur.

Taxon.

Rüst D. 1B85

Tethys Europe

Tr.

Taxon.

Rüst D. 1892

Tethys Europe (Italy. Spain. France)

Pzc-Czc

Skelet.

De Wever P 1985

Amer.N. Callf.

Tethys Europe Alps

Tr.

Taxon. N.Sp.

Kozur H & Mostler H. 1981

Tethys Europe Alps

Oxf.-Kimm.

Strati Envir Taxon. Ophiol.

SchaafA er ai. 1985

Tethys Europe Alps

Tr.-Jur.

Taxon. N.Sp.

Kozur H. 5 Mostler H. 1979a

Tethys Europe Alps

Tr.

Taxon. N.Sp.

Kozur H. S Mostler H. 1972

Tethys Europe Alps

Tr.-Jur.

Taxon.S N.Sp.

Kozur H & Mostler H. 1978

Tethys Europe Alps Austr»a

Tr.

Taxon. N.Sp.

KozurH. & Mostler H. 1979b

Tethys Europe Alps Austha

L.Jur.

Sedim.

Steiger T. 1981

Kalkalpen Salzburg

Tethys Europe Austha Salzburg

Earl.Lias.

Dunikowski E. V. 1882

Tethys Europe Carpath. Meliata-Serie

Pzc-Mzc

Strati

Kozur H. AMockR 1973

Tethys Europe Corsioa

Jur.-Cret.

Ophiol. Strati

De Wever P, e/a/. 1987b

378

GEODIVERSITAS • 1997 • 19(2)

Mesozoic radiolarians from the European Platform

LOCATION

AGE

TOPIC

AUTHOR

Tethys Europe Eastern Rhodops Bulgaria Earl.Cret.

Boyanov 1. & Lipman R. Kh. 1973

Tethys Europe ex-USSR

Mzc

Bioz.

Vishnevskaya V. S. 1985

Amer.N. Calif, Asia Japan

Tethys Europe Greece

Tr.-Jur.

Strati Envir. Paleogeog.

De Wever P. & Dercourt J. 1985

Tethys Europe Greece Crete

Tr.

Metam. Strati

KozurH. AKrahl J. 1984

Tethys Europe Greece lonian

Callov.-Tithon.

Karakilsios V- et ai 1988

Tethys Europe Greece llaly Siclly Turkey Tr. Lias.

Taxon. Strati

De Wever P. 1982b

Tethys Europe Greece Pindos

Jur.-Cret.

Strati

De Wever P. A Origlia 1. 1982a

Tethys Europe Greece Pindos

Lias.

Taxon. Radt

De Wever P S Orlgria 1. 1982b

Tethys Europe Greece PIndos Olonos

Dogg.-Malm.

Strati

De WevGf P & Cordey F. 1984

Tethys Europe Greece Pirrdos-Olonos

Jur.-Cret.

Taxon. Environ.

De Wever P. & Thiébault F. 1981

Tethys Europe Greece Plndos-Olonos

L.Tr.

Zagofcev 1. et ai 1989

Tethys Europe Hungary

Mzc

Hojnos R 1916

Tethys Europe Hungary Mechek

L.Jur.

Sedim. Strati

Nad| 1.1971

Tethys Europe llaly (Euganei)

Crel.

Taxon.

Squinabol S. 1903

Tethys Europe Italy (Euganel)

Cret.

Taxon.

SqumabolS. 1904

Tethys Europe llaly (Lagonegro)

Tr.-Cret.

De Wever P. & Miconnet P. 1985

Tethys Europe Italy

Jur.

dating

ContiM. efa/. 1988

(Ligur., Apenn.Mt.Alpe)

Tethys Europe Italy (Veneto)

Cret.

Taxon.

Squinabol S. 1914

Tethys Europe Italy Alpes

Jur.

Ophiol.

De Wever P. étal. 1987

Telhys Europe italy Alps Mongmervo

Cret.

Taxon.

SqumabolS. 1912

Tethys Europe Italy Bolognese

Mzc

Taxon.

Neviani A. 1900

Tethys Europe N.Apen. italy (La Spezia)

Tr./Llas.

Taxon. Strati

Ciarapica G. & Zaninetti L. 1982

Telhys Europe N.Hungary

Jur.(Bajoc.)

Taxon.

KozurH. 1985

Tethys Europe N.Hungary

Jur.

Taxon.

KozurH.&MostlerH. 1986

Tethys Europe N.Hungary Rudabanya

Mid.Jur.

Grill H.>1. & Kozur H. 1986

Tethys Europe NW.Yugoslavia

Mid.Tr.

Taxon. Biostr.

Gorican S 1988

Telhys Europe Romania

Jur.-Cret.

Taxon.

Dumitrica P. 1970

Tethys Europe Russia lirais

E.Perm.

Taxon.

KozurH. &Mostler H. 1989

Telhys Europe Slovenia (NW YugosL)

Ladin.(MTr,)

Taxon.

Kolaf-Jurkovsek T. 1989

Tethys Europe Slovenia

Tr.-Jur.

Goncan S, S Kolar Jurkovsek T. 1984

Telhys. Europe Spain, Sicily. SE France

L.Jur.- E.CreL

Biostr,

Manlvil H et al 1986

Telhys Europe Swilzer.

Mzc Czc

Taxon.

Jaccard F. 1909

Tethys Europe

Taxon.

N.Sp., Evolu.

Kozuf H. & Mostler H. 1983

Tethys Europe Turkey

Lias.

Taxon.

De Wever P. 1984c

Telhys Europe Turkey

Lias.

Taxon. N.Sp.

De Wever P 1982a

Telhys Eur. W. Carpath. Kysuca Klippen

Mzc

Biostr

Ozvûldova L. 1988

Tethys Europe W Carpath.

Mzc Jur.

KozurH. & Mock R. 1985

Tethys Europe W.Carpaths Meliata

Jur.

Kozur H. & MocK R. 1985

Tethys France Hles-Alpes

L.Jur.-E.Cret.

Turner J. 1965

Telhys German

Dog.

Heitzerl 1930

Telhys Greece

Late Jur.

Taxon. Strati

Baumgartner P. 0.1980

Tethys Greece

Jur.-Cret.

Radt

Thiébault F. et ai 1980

Tethys Greece (Ewoia, E.Greece)

Late Jur.-Earl.Creî.

Strati Taxon.

Baumgartner P. 0- S Bernoulli D. 1976

Telhys Greece (Peloponnesus)

Jur.

Strati Sedim.

Baumgartner P. 0.1985

Telhys Greece Argolis

Jur.-Cret.

Baumgartner P. 0.1981

Telhys Greece Epireous

Jur.

Taxon. Strat.

Danelian T. 1989

Tethys Greece Epireous

Jur.-Crel.

Strati

DaneHan T et al. 1966

Tethys Greece Europe Asia Amer.

Jur.-Cret.

Radt Climat

De WevBf P. 1987

Tethys Greece Hungary

MidJur.-Cret.

Taxon.

Cordey F. 1984

Tethys Greece Italy

L.Jur.-Earl.Cret.

Strati

Baumgartner P. 0.1980

GEODIVERSITAS - 1997 • 19(2)

379

De Wever P. & Vishnevskaya V. S.

LOCATION

AGE

TOPIC

AUTHOR

Tethys, Greece, Italy

L.Jur.-Earl.Cret.

DSDP

Devos 1. 1983

Amer.C. Costa Rica

Tethys Greece Italy (Sidly)

Jur.-Cret.

DSDP Taxon. Strati

Origlia-Devos 1. 1983

Amer.C. Costa Rjca Indran

Tethys Greece Haly Lombardia

Jur.-Cret,

N.Sp. Taxon.

De Wever P. 1981c

Tethys Greece Méditer Karpathos

Cret.

Vinassa de Regny P. E. 1901-02

Tethys Greece Pindos Europe

Jur.-Cret. Baj.(?)-.

Strati Taxon.

De Wever P. & Cordey F. 1986

Tithon

Tethys Greece PindosZ. (S.peigponnes.) Jur.-Cret.

Thiebault F. étal. 1986

Tethys Greece Sictiy, Turkey.

Tr.

Taxon. N.Sp.

De Wever P-e( a/ 1979a

Tethys Hungary (Dama)

Tr.

Strati

De Wever P. 1984a

Tethys Hungary Bukk

Jur.

Strati Biogeo

Kozur H. 1984e

Tethys Hungary Carpaih. Bükk

Mzc

Strati

Kozur H. 1984a

Meiiata Uppony Mecsek

Tethys Italy

Mzc-Czc

Taxon.

Vinassa de Regny P. E. 1898a

Tethys Italy (Lombardy. Sicily)

Mid.Jur.-Eari.Crel,

Biostf. Strati

Alla Y. 1987

Japan (Shikoku)

Tethys Italy (Sicily)

Jur.-Cret.

Taxon. Bîostr.

De Wever P. et al. 1986b

Tethys Italy (Sicily)

Late.Jur.-Earl.Cret.

Biostrat. Taxon.

De Wever P. étal. 1985

Tethys Italy (Spezia)

Tithon.

Taxon

Vinassa de Regny P.E. 1899

Tethys Italy Alps E.Carpaîhians (Rom.)

Tr.

Taxon. N.Sp.

Dumitnea P. 1978c-

Tethys Italy Appennine

Jur.

Marcucci M, étal. 1987

Tethys Italy Bolognese

Jur.

Vinassa de Regny P. E. 1900

Tethys Italy E.Liguria (Mte Aipe)

Taxon.

Conti M. a Passenhi M. 1988

Tethys Italy Europe

Mzc Czc

Taxon.

Nevtani A. 1901

Tethys Italy Europe C Appennine

Cret.

Biostr

Marcucci Passerini M. étal. 1988

Tethys Italy France Ligury Europe Alps

(Cenom.-Turon.)

Jur.-Cret,

Ophiol. Strati

De Wever P, ef a/ 1987a

Tethys Italy N Apennins Corsica

Jur.-Cret.

Strati

Conti M. étal- 1985

Tethys Italy N.Apennines

Jur.

Stratig. ophiol.

Barrel T J 1902

Tethys Italy N.Apennines

Jur,-Cret,

Strati

Conti M. & Marcucci M. 1986

Tethys Italy S.Tuscany

Biostr.

Conli M. 1986

Tethys Italy Spezia

Jur. Tithon.

Vinassa de Regny P. E. 1898b

Tethys Morocco (Rif)

Jur.-Cret.

Paleogeog. Strati Envir.

De Wever F étal. 1985b

Tethys Morocco N.Rif

Jur.-Cret.

Taxon. Strati Radt

El-Kadiri Kh *984

Tethys NW Greece lonian

Jur.

Biostr.

Danelian T, S De Wever P. 1988

Tethys Oman

Permian-Cret.

Biostr.

De Wevdr P s Bourbillon C. 1988

Tethys Oman

Cret.

Strati Ophiol.

Beurrier M. étal. 1987

Tethys Oman

Perm.-Cret.

Radt Telhys strat.

Bourdillon C et ai 1987

Tethys Oman (Hawasina)

Mzc Permian

Strati Paleogeog.

De Weve^ P étal. 1988

Tethys Oman (Hawasina)

Strati

Blome C. D. e/ al. 1983

Tethys Oman (Samail N.)

Cret.(Senon.)

Radt Taxon. N.Sp.

De Wevar P. S Bourdillon C. 1988

Tethys Oman (Semail)

Cret. Campan.

Strati Taxon. Ophiol.

Schaaî A. à Thomas V. 1986

Tethys Oman (Semail)

Jur.-Cret.

Ophiol.

Tippit P R. étal- 1983

Tethys Oman Hawasina

Mzc

DavisA. G. 1950

Tethys Pannonian Hungary

Mzc

Biogeo Strati

Kozur H. 1984c

Telhys Remania

Jur.-Cret.

Radt

Proiescu O, 1933

Tethys Romania Carpath.

Cret.(Cenom.)

Taxon. Strati

Dumitnea P. *975

Tethys Rotti Europe Italy

Mesozoic

Taxon. Strati

RiedelW. R 1953

Tethys S.AIps.

Mid.Tr.

Taxon. Strat»

Dumitrica P étal. 1980

Tethys Tethys Oman Samail

Cret.(Senon.)

Taxon. Ophiol.

De Wever P. étal. 1988

Tethys Turkey

Lias.

Taxon. N.Sp

De Wever P. 1981 b

380

GEODIVERSITAS • 1997 • 19 (2)

Mesozoic radiolarians from che European Platform

LOCATION

AGE

TOPIC

AUTHOR

Tethys Turkey

Lias.

Taxon. N.Sp.

De Wever P. 1981a

Tethys Turkey

Mzc

Ophiol.

Bailey E. B. & McCallien W. J. 1953

Tethys W.Carpath. Yugosl.

L.Jur.-E.Cret.

(Tithon.-Neocom.)

Sedim.

Misik M. 1973

Tethys W.SIovenia

E.Cret.

Pavsic J. & Gorican S. 1987

Tethys Yugosl.

Mzc

Radt

Obradovic J. & Gorican S. 1987

Tethys Yugosivia Slovenia

Jur.

Taxon.

Gorican S. 1983

W.Pacif.

E.Cret.

DSDP62 Strati Taxon.

Schaaf A. 1981b

W.Pacif. indones. Bornéo

Mzc

Strati Dating Ophiol.

Leong K. M. 1975

W.Pacif. Palawan Block, Philippines

L.Pzc-Earl.Mzc

Strati

Cheng Y.-N. 1989

W.PAcif.E.Australie (New England)

Pzc Mzc

Aitchison J. 1988

W.Pacific, DSDP Leg 61

Czc Mzc Cret.

Strati

De Wever P. 1981d

World

Mzc

Premoli-Silva 1. étal. 1976

GEODIVERSITAS

1997

19(2)

381

Cenozoic radiolaria from

European Platform: a review

Patrick DE WEVER

Laboratoire de Géologie, URA 1761, Muséum national d'Histoire naturelle,

43 rue de Buffon, F-75231 Paris cedex 05 (France)

Irina M. POPOVA

CNRS, URA 1761, Université Pierre et Marie Curie (France)

(permanent address: Far East Geological Institute,

100 yr. Prospect, Vladivostok, Russia).

De Wever P. & Popova I. M. 1997. — Cenozoic radiolaria from European Platform: a

review, in Crasquin-Soleau S. & De Wever P. (eds), Peri-Tethys: stratigraphie corrélations,

Geodiversitas 19 (2) : 383 - 469.

KEYWO^S

radiolarians,

Peri-Tethys,

Cenozoic,

silica,

review.

ABSTRACT

Stratigraphie corrélations beeween western and eastern European areas under

a clear boréal influence are diffîcult because different paleogcographic

domains (boréal w tropical) arc involved in eastern countries and most of the

boréal data which were acquired in eastern countries used technical equip-

ment and méthodologies which are not the same as in western countries, and

also the Russian literature is not easily accessible, is usually in cyrlllic and fre-

quently lacks good illustrations.

From a review of Cenozoic Peri-Tethyan radiolarian investigations, it has

become clear that there are probiems with respect to correlate western and

Russian studies, namely: Russian gcographical and geological terminology,

which is difFicuic for foreign scienrists to understand; differing approaches to

the establishment of a biozonarion and bcnce to corrélations; and species

détermination (and systematics) which were made, in some cases, on the

basis of thin sections, or badly preserved fauna. In this article we givc an

explanation of some Russian geographicai and geological teems. Information

about the âge, précisé locaÜiy (wîch latitude and longitude) of Cenozoic

deposifs discovered in sections and wells of the Péri- fethys basin along with

a brief lithology, strarigraphy and biosiratigraphy, based on micro and

macrofauna investigations, for different region.s, is presenred in tabulât form.

And ail palaeoenvironmental information is shown on the maps. The goal of

this paper is to correlate various biological dmescales from western to east-

ernmost Europe with emphasis on data collection from eastern Europe.

GEODIVERSITAS ♦ 1997 • 19(2)

383

De Wever P. & Popova I. M.

Stratigraphie corrélation of Upper Palaeozoic through Receni high latiiude

rocks has been hampered by a lack of world-widc coopéraiivo studies. Now

that scientific exchange is casier beween Eastern and Western workers, a

rapid solution of many stratigraphie problems inay be achieved through joint

projects. Before startîng on this dccailed comparison of eastern and western

studies we here présent a review of previous works.

MOTS CLÉS

radiolaires,

Péri-Téthys,

Cénozoï(^ue,

silice,

revue.

RÉSUMÉ

Les corrélations stratigraphiques entre les régions d’Europe occidentale et

orientale sous influence boréale franche sont difficiles car différents domaines

paléogéographiques (boréal vs tropical) sont généralement intriqués dans les

pays de l'Est et la plupart des données boréales acquises dans les pays de PEst

le furent avec des moyens techniques et des méthodes différents de ceux des

pays occidentaux, en outre la littérature russe n'est pas aisément accessible,

est écrite en caractères cyrilliques et manque généralement d'illustrations de

qualité.

À partir d’une revue des travaux effectues sur les radiolaires cénozoïques de la

Péri-Téthys, Il est devenu évident que des problèmes majeurs de corrélations

se posaient pour plusieurs raisons. Tout d’abord à cause d'aspects géogra¬

phiques et terminologiques qui sont parfois difficiles à appréhender pour des

scientifiques étrangers. Ensuite parce que les approches diffèrent dans l’éta¬

blissement des biozonations et des corrélations. Les acceptions varient aussi

pour les déterminations spécifiques (et donc aus.si systématiques) qui furent

d’ailleurs effectuées, dans de nombreux cas, à partir de plaques minces, ou de

faunes mal conservées. Dans le présent article nous donnons une explication

de quelques noms géographiques ou termes géologiques. Nous prc.sentons

aussi sous forme de tableaux et de cartes des informatioas à propos des âges,

précisons les localisations (en latitude et longitude) de dépôts Cénozoïques

trouvés sur des coupes ou en forage et appartenant aux bassins

Péri-Téchysiens, accompagnés d'une brève description lithologique, du cadre

stratigraphique et paléoenvironnemencak fondés sur les micro- et macro-

faunes. pour les différentes régions. L’objectif de cet article est de pouvoir

corréler diverses échelles biologiques d'Europe occidentale avec les plus

orientales en mettant l'accent sur les données d'Europe orientale.

Les corrélations stratigtaphiques du Paléozoïque Supérieur au Récent dans les

roches de hautes paléolaiîtiides ont été freinées par un manque de coopéra¬

tion largement internationale. Maintenant que les échanges scientifiques sont

plus faciles entre pays de l'Esi et de rOiicst, une solution à divers problèmes

stratigraphiques devrait pouvoir être obtenue rapidement par des projets

conjoints. Avant de commencer cette étude détaillée entre stratigraphies occi¬

dentale et orientale, nous présentons une revue des travaux antérieurs.

INTRODUCTION

For both the upstream and downstream side of

several studies it is necessary to homogenize dif¬

ferent biological chronometers. The goal of this

paper is to consolidate information so that geolo-

gists interested in basinal deposics can quickly

and easily use the interrelationship of microfos-

sils as a useful tool. Our goal is to correlare, using

modem methods, varions biological rimescales

from western to easternmost Europe wirh empha-

sis on data collection from Eastern Europe.

384

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Plarform

Most srudies in micropalaeontoiogy in the for¬

mer Soviet Union déveloped without rlie know¬

ledge of the western literature and, to some

extent, the reverse was also the case which arose a

problem of consanguinity,

Some fossil groups hâve been studicd for a long

time and are relatively wcll known. Corrélation

between several basins using these fossil groups is

possible, even though still impertect. Planktic

organisms hâve been shown to be more uscful

than benthics. On the contrary, some other

groups, such as radiolarians, hâve been largely

ignored.

Microfossils are important, but some groups are

ofeen overlooked as stratigraphie tools. Their

usefulness for quick analysis in Palaeozoic to

Eocene rocks is excellent if certain sysccmatic

conformicy can be agreed upon. l’he changing

relationships between microfossils groups (dia-

loms, foraminifers, tadkdarians, conodonts,

sponge spicUles, and nannofossils) may signal

changes in basin and océanographie conditions.

Stratigraphie corrélations with castern European

areas under a clcar boréal influence are diffîculc

bccause: (1) different paleogeographic domains

(boréal tropical) are involved; (2) most of the

boréal data has been acquired in easrern coun-

trics where technical equipment and used métho¬

dologies are not che same as in western countries

(use of a scanning électron microscope is still

uncommon jn several countries): (3) the Russian

literature is not easily accessible, is usually in

cyrillic and frequently lacks good illustrations.

The long term objective of our study is to:

1. Re-examine the caxonomy of radiolarians

from western întracratonic basins and from the

Russian Platform, Ca.spian Sea Région, Siberian

Lowlands, Nonh Kazakhstan.

2. Set up a bioscratigraphy of rhese organisms

(quantitative biochronology) with the same

means as that used for the receni Tethyan syn-

thesis (Baumgartner ef/?/. 1995).

The présent paper represents rhe First part of this

final objective.

From a review of Cenozoic Peri-Tethyan radiola-

rian invesugations, it has become clear that there

are problems with respect to correlate western

and Ru.ssian studies, namcly: (1) Russian geogra-

phicai and geological terminology, which is diffi-

cult for foreign scientists to understand; (2)

differing approaches to the establishment ol a

biozonarion and hence to corrélations; (3) spe-

cics détermination (and systematics) which were

made, in some cases, on thebasis of thin sections

(Chediya 1973), or badly preserved fauna

(Subbotina 1960). In this article we givc an

explanation of some Russian geographica) and

geological terms. Information about die age> pré¬

cisé locality (with latitude and longitude) of

Cenozoic deposics discovered in sections and

Wells of the Peri-Tethys basin along with a brief

lithology, srratigraphy and bioscratigraphy, based

on micro- and macrofauna investigations, for dif¬

ferent régions, is preseneed in tabular form

(Table 2) and ail palacoenvironmcntal informa¬

tion is shown on the maps (Figs 6-14).

Future srudies wlll provide:

— Lithologie descriptions of some key sections

and cores that are représentative of some régions

or basins with their précisé locations (latitude

and longitude).

— Microfossil database. A complété computerized

database (with raxonomy, photos, géographie

occurrences, etc.) is being developed.

Other indirect benefits:

— Opportunity co develop doser relationships

between scientists and to hâve easier access to

local literature.

— Understand terminologies in translation such

as chose referring to lithologies (domanikoids

faciès, opoka, aleurolites, menilices) or geography

(Preduralie vx tris-Llral, Zatiralie tfs Tran.s-Ural,

Predmugodzharie vs Cis-Mudjarie, Pri- = nearby,

ex. Pripolar...)

Stratigraphie corrélation of Upper Palaeozoic

through Recent high latitude rocks has been

hampered by a lack of world-w'^ide cooperative

srudies. The reasons include a global political cli-

mate that hampered Technology transfer between

countries and scientists. Now thar scienriFic

exchan^e is easier between Eastern and Western

workexs, a rapid solution ul niany suatigrapliic

problems may be achieved through joint pro-

GEODIVERSITAS • 1997 • 19 (2)

385

De Wever P. & Popova I. M.

jects. Sample and ccchnology exchange will help

researchers to scc a more complété fo.ssil record

and better networking can now allow interested

workers to develop models that will belp to

interpret géologie ba.sins. Before startlng on this

detailed comparison of eastern and western stu-

dies we will présent a review of previous works.

HISTORY OF STUDY ON RADIOLARIANS

A good review of this copie has been published

by Sanfilippo et al. (1985a). Parts of it are quo-

ted in the présent texf.

For a long time (and one can still find it in some

handbooks) radiolarians hâve been regardcd as

being of little use for stratigraphy. For example,

Shrock & Twenhofcl (1953: 67) indicated that

“fossil Radiolaria ... hâve not been found usehil

for age détermination or corrélation, partly

because of che fact that fossil species are much

like exisring ones, and partly because so few

forms hâve been found.” More recently one can

find: “Ce sont de mauvais fossiles ayant peu varié

depuis le hinmire jusqu'à rAciuet' (Encyclopedia

Universalis 1980: 1065b). This revcals how idées

reçues hâve longevity.

In 1950. the reasons for considering radiolarians

co be uselcss a.s a stratigraphie lool seemed

obvious. Ail che literature of die previous years

supporied the idea that che familles and généra

of radiolarians in Palaeozoic rocks are the same as

those in presenr-day pUnkton (Campbell 1954).

Even at the level of specics, many forms in

“Recent” sédiments collecled from the océan

floor by the Challenger expédition werc seen to

be the same as those occurring in Early Terriat)'

sédiments on Barbados (Flaeckel 1887). A chalk

from the i.sland of Rotri, near Timor, dated as

Pliocène, contained a radiolarian assemblage sho-

wing grcater similarities to Mesozoic faunas of

Europe than to Lace Tertiary assemblages and

present'day plankton (Tan 192"^, 1931).

Pessimisni concerning the inurility of radiola¬

rians for stratigraphie purposes was erradicated

by the work of Riedel (1952, 1953). Material

obtained from océanographie cruiscs, such as the

Swedish Deep'Sea Expédition of 1947-1948,

provided the key to understand the urility of

radiolarians for stratigraphy. The lower parts of

severai piston corcs from the tropical Pacific were

found to contain radiolarian asscmblagc.s similar

to those that had been described from the Early

Tertiary of Barbados, or rhe Late Tertiary of Italy

and C'alifnrnia,. The radiolarian assemblages of

the upper parts of ail the cores in the région

contained a constant component, comprising

species described from present-day plankton, and

many contained as wcll a part that varied from

cote to core, but couJd bc marchcd with one or

more of the Tertiary assemblages that had been

encountered a few mètres below rhe sédiment

surface. Evidently, the rates of accumulation of

pciagic sédiments were sufficiently low, and phy-

sical discurlianccs of bottom sedimems were suf-

ficiently common and intense, to cause

widespread admixture of Tertiary radiolarians

with Reccm oncs at the sedimem surface (Riedel

1952, 1957a). lEcrcin lays ihc cxpl;mat[on foc the

laige numher of species in common between recent

assemblages, and those in Tertiary rocks. In faci the

radiolarians ai different Icvels in the Tertiary were

sufficiently different to permit their application in

biostratigraphy. ITcrefore, the ‘"Mesozoic aspect” of

che **Pliocene” assemblage from Rorti bccame

inacasingly odd. Rc-examination by Riedel of the

samples involved led to the solution: the Dutch

expédition had collected samples of pciagic chalks

of rwo different âges. The samples conraining the

rich radiolarian assemblages can be dated as

Crecaceous on rhe basis of their calcarcous nanno-

fossils, and the samples containing Pliocène nanno-

fossils hâve a .spar.se radiolarian fauna that had not

been nociced before.

The development of the knowledge of stratigra¬

phie utility of radiolarians ha.s been recent and

rapid- Now there arc about a hundred paleonto-

logists (academie and industrial) whose principal

involvcmcnr is radiolarian stratigraphy.

Initial studies of radiolarian biostratigraphy were

establishcd gcnerally on simll.arity ar the level of

species, and did not contradict the fixed convic¬

tion rhat most généra and families had persisted

from tire Palaeozoic to the Recent. However,

with the Deep Sea Drilling Project, which has

been coring long columns of peUgic sédiments in

ail major océans since 1968, a better knovvlcdge

of stratigraphie ranges of radiolarian species was

386

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

obtained, and as ancestor-descendant relations

were demonstrated, it became obvions that che

lengthy stratigraphie ranges of généra were unna-

tural.

FROM PLANKTON

TO SEDIMENTARY ROCKS

Radiolarians, a class of actinopods, are marine

protozoa with a capsular membrane which sépa¬

râtes an ectoplasm from an endoplasm.

Polycystines (a Superorder), with thcir siliceoiis

skeletons, are the only radiolarians s.L which are

preserved as fossils, At présent, among

Polycystines, members of che order Nassellaria

are the most diversified, but Spumellarians seem

to be the most abundant (Lombari & Bowden

1982). The skeleron is included within the c>'rO'

plasm, ont of contact with sea water and, there-

fore, is not exposed co dissolution during the

cells life. Scvenil groups hâve a high content of

endoplasmic oil-droplecs and could represent a

primary source of hydrocarbons.

Radiolarians may exist from the pôles to the

cquaton but thcir abundance varies. Like other

planktonic organisras, thcir abundance is more

dépendent upon the suppJy of nutriems than on

the silica suppJy. Most ofthem live in che upper

lew hundred métrés of che water column in ali

océans and seas ot normal marine salinicy. Their

diversity and numhers of individuals décliné in

near-shore watets. in high laiitude.s rhe number

of spccies (diversiry) is much smaller than in low

latitudes, even if the number of spécimen (abun¬

dance) is high. A latitudinaJ distribution does

exist for radiolarian associations. It is also pos¬

sible to differentiare surface from subsurtace

assemblages.

After death, an individual test is at least partially

dissolved during settling and while it lies exposed

on the bottom of the océan. According to

Schrader (1971). Diinbar ôc Berger (1981),

Asper et al. (1992), rhe scftiement of micro-

plankton occurs in faecal pellets. But there were

not much radiolarians records which hâve been

find in them but around them (Nakaseko et al.

1985). Chemical and physical characteristics of

tests vary according to taxa (King 1975, 1977) as

does the dissolution affccting them (Ricdcl 1958;

Renz 1976; Bjorklund & Goll 1986; Swanberg &

Bjorklund 1992). Because of che ubiquity of

radiolarians in plankton, and the fact that che

préservation of thcir skeletons is not controlled

by a compensation depih analogous to chat for

calcium carbonate, one might expect to find

them more commonly in present-day and

ancient sédiments, than is actually the case.

The numhers of individuals and species are lower

m sédiment (and a fortiori in the rock) than in

plankton. Radiolaiians may bc abundant in rela-

tively shaUow basins close to a shorclinc, e.g. the

Santa Barbara Basin, off California under a

depth of 500 m (Kling 1979) and the Norwegian

fjords (Swanberg & Bjorklund 1992). In ail these

régions, radiolarians are accompanied by (and in

the polar régions markedly dominated by) dia-

toms. If, at certain localities in these régions,

radiolarians arc not a prominent component of

the sédiments, it is usually a result of their dilu¬

tion by other constituents, and not of their disso¬

lution.

In oceanic rccerit sédiments (Miocene-Present),

the radiolarian abundance on a site is connected

eirher to high or low stands (e.g. South Atlantic

coa.st off Africa, Walvîs I^jdge; Diester-Haass et

al. 1992; Hay àc Brock 1992).

Less than 1% ot che silica fixed by planktonic

organisms in surface waters is pie.served within

the gcologicaJ record. Silica phase iransforma-

cions are accompanied by porosity réduction.

The original poiosity is higher when the sedi-

menr is richer in silica and during diagenesis

(Isaacs 1981). For rhe gcologist, the porosity

decrease (volume) corresponds ro a diminishing

of the thickness and he has lo cake into account

the imporrant decompaccing factor when making

accumulation rate and palaeopa>duccivicy calcu¬

lations (De Wever et al. 1994).

In addition lo pressure and température, time

favours both opal transformations. Thus cherts

are more prévalent in older sédiments (Palacozoic

and Mesozoic) and porcelanitcs in more recent

ones (Cenozoic). The transformation opal-A to

opal-CT is estimated to occur at 25-50® and

GEODIVERSITAS • 1997 • 19(2)

387

De Wever P. & Popova I. M.

takes 20 Ma in areas of low to moderare sedi-

mentation rares and 5-10 Ma in areas of high

sédimentation rares (Kastner 1981). The

opal-CT to quart'/- transformation occurs wirhin

40-50 Ma (Kcene 1976).

STRATIGRAPHY

Because of the difficulty to extract radiolarians

from siliceous rocks, ihe first zonations were pro-

posed for the Cenozoic only during ihe lace

1970 s.

Some of the most fundamcntal step. that of

recording the earliesi or latest occurrence of a

radiolarian taxon in a sériés of samples, is often

complicated enough to con.strain a part of sub¬

jective opinion. This applies to the fimits of spe-

cies dcBned morphotypically. Morphotypic

limits are perlorce tiscd when phylogcnetic rela-

tionships are gnknown, and may also bc used in

addition to evolutiotiary limits, when lincs of

évolution arc clear.. Under some circumstanccs,

evolutionary limits can bc stratigraphically more

useful than morphotypic oncs. Such is rhe case

when ail members ot a spccies change gradually

to rhe descendant niorphology, as in the spccies

belonging to the genus Diartus (D. pettersoni,

D. hîi^hesi) or Spongaster (.V. tenais S. pentas,

S. benningbami) (Johiutui ik Nigrim 1985a, b).

That maacr is complicated in some cases when

an ancestral form persists to co-occur with a des¬

cendant lincage over some Icngth of lime (as

Pterocorp sahae and P campunulu persisi along

with their ancestor P cLinsus Caulet et Nighni,

1988; or as CLitbrocyclas bicornis persists along

with ils descendants Cycladophora sphacrica

Popova, 1991 and Cycladophora hayesi Lazarus,

1988). These methods produce a lise of stratigra¬

phie e\xnts in each sequence, and the difterenc

succession of ev'enrs are correlaied, In most cases

some of the corrélation line.s cross and ir is ncces-

sary to choose which of the two conflicting

pièces o( evidence (crossing lincs) is to bc accep-

ted. For this purposeï it is licipfui to evaluate ihe

level of reliability of each event, according to a

number of criieria. It Ls worth noting that a dia-

chronism musc be invoked in some cases. This

diachronism has been demonstrated berween dif¬

ferent océans (Indian/Paciflc), in the same océan

(wesiern/eastern Indiaii and Pacific Océans), as

well as for a same phylogcnetic transition

(Johnson &C Nigrini 1985a, b), lu some cases this

diachroneity reaches up to 10 Ma* as for

Acrosphaera rnurroyi gr., or Lithostrobus cf.

L bexagothiUs te Caulet 1992). In some

spécial environments, such as upwelling Systems,

this diachroneity may be considérable:

Lamprocyclas hadros appears more than 10 Ma

ago off Oman, while it firsr occured at 6 Ma off

Péril (Nigrini ti Caulet 1992).

A succession of spécifie events provides the great-

esT stratigraphie resolution, hur it is awkward to

transmit information in this fbrm to biosrrarigra-

phers working with orher fossil gnnips, and par-

ricularly to general geologists. The message is

simplificd by separating ihc succession of events

iiuo clusters, each ol which dclimits a zone.

Evenls used co dcfinc zones are usually sclectcd

on ihe basis of t heir existence rcliably identifiable

over widc géographie areas. Some spécialises of

several microfbssil groups descrîbc as many zones

as arc permirred by the number of events avai-

lablc to them. Such a procedure would be unrea-

listic for radiolarians, especially in the

high'diversity areas of the tropical and remperatc

latitudes, and iherefore only a practical number

of radiolarian zone.s are dcfined ihere (ex. about

thtrt)' for ihc encire Cenozoic by Sanfilippo et al.

1985a).

Ongoing work, espccially on material acquired

during ihe Deep Sea Drilling Project and Océan

Dnlling Program, provides a growjiig number of

radiolarian events. and of scqueiices in which

rhey arc recognized. It has thus bccome impos¬

sible for any individual rcsearcher to organize ail

of the resuJrs for determining whai is rhe most

likely scracigraphic order of events in each bio-

gcographic province, and which variation

requiros interprétation in ternis of environment,

préservation, factors etc, To facilirate this task,

onc may use the method ot probabilistic strari-

graphy described by Hay (1972). The method

involvcs an initial arrangement of the events in a

best esiimated stratigraphie order, and then

inverting the above/below rclation.s of pairs of

adjacent events until the number of contradic¬

tions is the minimum. A major objection to this

388

GEODIVERSITAS • 1997 • 19(2)

Moderate deep

water faciès

Shallow water faciès

Régional plaktonic

Nikitina 1972

Over

zones

Zagorodnuk 1967

Characteristic and concomitant species

(/)

foraminlferal zones

Foraminifera

(Radiolaria)

Foram Inîfera

Radiolaria

J»:

BoIMna antegressa s.s

Bolivina antegressa

Lantlculina

calcariformis

îo

Cenosphaera

Cylindivclavul/na rudHosta. LanticuUm simfsropoHca,

Màrginalina befrrm, BrotTeneita launca taunca,

B. fira^àviwsisuasfi» DKr.tgHaneogmnosa.

t<tonion cufMSopVt. Cafcaai’Ja

Cenosphaora mariae, Porodiscus lurgaJcus,

Dnjppairacttjé éBoteennaa, Cenospnaem mirganae.

Spongoaaajsconcontncui. Cagnospftaea veterj^a,

.ç

.JA

Bolivina jacksonensis

Brozenella tauhca

taurica

mariae

CyclammvraPsBvtfodavuttnacolomi.

Marginylina irirscryttpt^ssa, (auiica acuUfamis,

aocà*fia

PHacoaiscustuTTtetaaus, Tnecospnaera sasbra

Selhtxyrils nuhintus. Ashophacus n sp.

Globfgeraspis

tropicalfs

Brozenella taurica

acutifomis

Spongasteriscus

gorskii

Mar^iJtncpsisf^àgaPus. PtecMfron<iKuiaiis stunata.

BalivinB (BCkBçpensiSi Butunna sculplilts

Cafpospt^Bçra usunartsis, StytoPyctra Ischjebkoi,

Saihcpytamhi vttort, Arrphtstytus ensigec

T7'r>rc'V5 0virr«»s. gcrsHu

>»

(/)

Globigerina

turcmenica

Spiroplectammina

vicina morpha

Lenticul

miera

Xiphatracus visendus

Haplophmgmoides macer.

Caucasina eocaenica

Xiphamsatü h>>ier,a\js Carpofiphaefa usuensis.

Sethopyranus vtesfon. Spongastencus gorskû.

Sivk/ifDcPus (■aaiêtu&, SëtPoeyrits parvr^inHjs.

Porpatscua Af^nu'arius

•O

Hantcenina

alabamensis

Brozenella kerestensis

Pseudocla vulina

subbotinae

Lenticulina

dimorpha

•C

&§■

Phacodiscus

duplus

Lenticutina grodnensis, Anomalinoidespostvulgaris,

Bfottao&ia kBresteoan&is

Pnacoaiscusduptus. Conoea/yorvma aralansrs

Astfophacus duplus, A testatus.

Pnacodtscusaotyaphsspscus. Pnmopyteovata

Acarinina

rotundimarginata

Lenticulina kuberlina

S *0

Phacodiscus sp.

Hopkins/natjykovae. Eponidcsofptbtus. GamaiMes

kaWiSlanKus, Paeudodaviihna HstpraifoxiBs.

(bumna praeficoiptiUs

A$troo^acu9(P.ioio$. Pt'Qi^f'di^tissubsphaer^us,

Çorroca'Ÿ<?mma gralansi^, Lit*iome>sss o.sp

Rcrtasptvtara n set. Sathocyrtis tBmifien^*\,S5p

Acarinina

bulbrooki

Brozenella postacuta

aksuatica

•Î2

qi S ê

•S O

3 C §

Podocyrtis

prvnoformis

Textiiianii tjuÿuistca, Lur4iCülnAeKgr. momata,

TnfrrpiptHtiB aragonm^is caucasica

LycPnocamumbaflum CatpaspTaafa megapon o.ssp.

5^(MctspftdB« rni'tJfrs). SkOtipotlfSCuia/a/Bvisrs.

PoJocyttts prunoformis Lttffalracfus turgatcus

Truncorotalia

aragonensis

Anomalina scrobiculata

O to «n

t s- g

JS -s s

Cenosphaera pila

Ammooacullies pitOwayepsis, Lantk^Hna ergenfca.

Acarviina pentacamgrala Haphnsma compacta

Bulimina mitgamana. Brotzenella postacuta postacuta

k»

Globorotaiia

Lenticulina mexicana

Canosphaea pila. Carposphaara rnicmpofulosa.

Thecosphaeta n.sp.. Cromyodruppa tebesensis,

subbotinae

nudicostata

iS m

«0 3-5

c O 5

Amphicarydiscus

fusoides

Margmuléna Bofraga/ius,

£M|DS 0 S(yJlus lootonsj Amphlbrachium gracilis.

A, pJanum Amphicatidiscus fusoides.

Globorotaiia

Lenticulina mexicana

ÿ i5 ^

^ to -S

O to

LentKutma viatovi

Hiatiastrum paleogenus, Slethostylus acutus

ffi

aequa

praemexicana

Gratits tybiciis. OdhidoidestBxrilîs,

Gaud/ytna navarroana

Fig. 1. — Corrélation between régional zones based on planktonic foraminifers and radlolarian zones on Russian platform (according to Zagorodnyuk 1969).

Cenozoic radiolaria from European Platform

De Wever P. & Popova I. M.

method is that no plan exisrs for taking into

account the tlisparity of reliabilicy, between

recorded data; State of presen^tion». type of bioe-

vent, géographie extension of an evenc...

Differing from occanic data, land-based collec¬

tions of data are frequcntly isolated, scatrered

stratigraphically and geographically and the diffi-

culty there lays in esiablishing corrélation bet¬

ween evenis in spaced sequences. When

information is scarce and scarce ro such a point

that corrélation is impossible or at least délicate,

such as in ihe Mesozoic, some workers use ano-

ther method described as Unicary Associations

(Guex iy87> 1991).

Diachroneity is one of the primar>' factors limi-

ting biostratigraphic corrélations. Independenr

régional calibration of biosiraugraphic eventthus

offers the possibiliry of signtficantly improved

âge model.s. Régional calibration of zonations is

also needed for biostratigraphic events that are

endemic to the région- le lias long been recogni-

zed that radiolarian biogeography, perhaps more

than any other microfossil group, differs between

low and high latitudes, with many endemic spe-

cies occurring within the latitudlnally arranged

biogeographic provinces of the océan. Radio-

larian strarigraphy in the Cenozoie reflects chi.s

distinctive biogeographic pattern, with separate

zonation schemes for the tropics (Sanfilippo et aL

1985a; Johnson et uL 1987), Antarctic (Gauler

1991; Lazarus 1992) and Norwegi-an-Greenland

sea (Goll ôc Bjorklund 1989).

SUMMARY OF STUDIES

The most abundant and used data hâve been

obtained from the océans. în order co position

land-based scudies relative co oceanic ones we

will begin with a short summary of oceanic stu-

dies contriburing to our undetstanding of radio¬

larian occurrences through the Cenozoie. The

most important source of information on the

occurrences and distribution of Cenozoie radio-

larians is the sériés of Initial Reports of the Deep

Sea Drilling Project and Océan Drilling

Prograrn.

A compilation of papers in that sériés, dealing

with Cenozoie radiolarians is provided by

Premoli Silva et al. (1976), for Legs 1-39, by

Sanfilippo et ai. (1985a) for subséquent legs, and

more tecently by Spenccr-Cervato et al. (1993)

for the North Pacific Océan.

Acguisn luNS from ockan.s

Most of the récent studies on Cenozoie radiola-

rian strarigraphy hâve been on samples from tro¬

pical and temperate latitudes, but the First

radiolarian zones were defined from the

Antarctic (Hays 1965). High-latitude radiolarian

a-ssemblagcs contain only 10% of the number of

species found in low-laritudes assemblages, and

iheîr most obvious constituents are spedes chat

are absent or rare in low latitudes. This implies

that radiolarian zonation cstablishcd for high

latitudes diffêr from that applîcd in low Litirudes.

Progress to solve this ptoblcm are expected from

investigation of mid-lacimde ‘sub-boreal” samples

which contain éléments of both cool- and

warm-water assemblages, and parricularly from

régions such as the Southern Russian platform.

Late Miocene - Recent

Neogene radiolarian sedimenrs hâve been repor-

ted off north'West Africa, California and Central

America (l-ancelor, Seibold et al. 1978; von Rad,

Ryan et ai 1979; Lancelot, Winterer et ai 1980;

Rosendahl, Hekinian étal 1980; Ycats, Haq étal.

1981; Warkins, Moore et ai 1982...)

In Récent sédiments Goll (1976a) has shown

that radiolarians are widespread in the Pacific

and Indian Océans (excepr bencaih the central

water masses), and are resrricred ro high Southern

and northern latitudes, and off West Africa in

the Atlantic Océan. The biogeographic distribu¬

tion of distinct assemblages rhroughout the

Pacific and Indian Océans is described by

Sancecta (1978), and for the Pacific by Casey

(1971a, b) and by Moore (19'8). More restricted

biogeographic investigations of the tropical

Pacific hâve been pubÜshcd by Nigrini (1968)

and bv Johnson & Knoll (1974), and North

Pacific distributions are described by Nigrini

(1970), Sachs (1973) and Kruglikova (1977).

Studies of radiolarians from particular régions are

listed on cable 1.

In addition to numerous contributions of the

Deep Sea Drilling Project, the strarigraphy of late

390

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

Neogene nidiolariaris in the tropical Pacific is

dcscribed by several authors (Table 1 ).

The distribution of radiolatian sédiments in the

Indian Océan is considered in some detail by

Caulet (1978. 1991) and Nigrini (1991).

Biogeographic investigations hâve been made iu

the Indian Océan scctor of the Antarctic by

Petrushevskaya (1967), and in lower latitudes by

Nigrini (1967), Petrushevskaya (1972a, b),

Johnson de Nigrini (1980, 1982) and Johnson

et al. (19H7), Latc Neogene Indian Océan radio-

larian stratigraphy in higli latitudes has been des-

cribed by Hays (1965) and Keany (1979), and in

lower latiaides by Caulet (1979).

The general distribution of Recenc radiolarian

sédiments tn the Atlantic Océan is described by

Goll de Bjorklund (1971(2). 1974). Biogeo¬

graphic investigations luve been made lot the

South Atlantic (Morley 1979), the ea.stern tropi¬

cal Atlantic (Labracherie 1978, 1980a, b), the

Gulf of Mexico (Casey et al 1979a, b> c). the

North Atlantic (Peirushmkaya 1969), and the

Norwegian-Grcenland Sea (Bjorkiund 1973;

Petrushevskaya & Bjorklund 1974). Stratigra¬

phies based on sclccted taxa hâve been publishcd

for the Mioccnc-i’lioccnc of the Norwegian-

Greenland Sea by Goll de Bjorklund (1980), and

for the Quaternary of the central North Atlantic

by Morley de Hays (1979b). Radiolarians from

Recent sédiments in the western Meditermncan

are described by Cjulet ( 1974).

Oligocène - Middle Miocene

Deep Sea Drilling Project cores show that the

Middle Terti;uy distribution of radiolarian sédi¬

ments is similar to that of the Latc Tertiary,

except that fewer of these older sequences in the

Indian Océan contain siliceous microlossils, and

their distribution in the eastern Pacific is limitcd

as a resuit of sea-floot spreading. Tn the

Caribbean région, middle Tertiary sédiments fre-

quently contain radiolarians, bur they are iiot

présent in younger sédiments. On the oiher

hand, in the northetn Pacific, siliceous inicrofos-

sils are more prévalent in late than in middle

Tertiary sédiments. Thcyer 6c Hammond

(1974a, b) correlate radiolarian biosrratigraphy

with magnetic stratigraphy in tropical Pacific

cores, and Johnson & Parker (1972) correlate

radiolarian and foraminiferal .stratigraphies whilc

Sanfilippo de Nigrini (1995) correlate radiola¬

rians, nannofos^ils and foraminifers in ihc

Pacific, Atlantic and Indian Océans for ihc

Oligocene-Miocenc transition.

Eocene

In deep-sea sequences, Eocene radiolarians occur

in the central and western tropical Pacific, the

Jasman Sea, scattered patches in the low and

middle latitudes of the Indian Océan, the wes¬

tern Atlantic Trum the vicinicy oT tfie Rio Grande

Rise through the Caribbean lo Nova Scotia, and

in the eastern Atlantic from nurth-we.st Africa to

the Norwegian-Greenland Sea (Bjorklund de

Kellûg 1972; Bjorklund 1976a. b; Bjorklund &

Goll 1986; Lancelot, Seibold et al (19^8);

Montaderi, Roberts ei al 1979; Sanfilippo de

Ricdel 1979; Tucholke, Vogt et al 1979. von

Rad, Ryan et al 1979; Weaver 1976). Sancetu

(1979) has described the biogeography of assem¬

blages in the Pacific and Indian Océans from

Eocene to Miocene and Abelmann (1990) those

for the Antarctic.

Palacocene

Radiolarian occurrences of this âge are very few,

Thçy were encounrered hy the Deep Sea Drilling

Project at isolated sites off eastern America, ofï

Spain and North Africa, in the Tasman Sea. and

scattered through the Indian Océan, In norch-

west Atlantic Palaeocene occurrences are recor-

ded by several Deep Sea Drilling Project Legs.

Ac:qljisitions prom land

Late Miocene - Recent

Ehrenberg published (1854, 1873, 1875) the

results of his radiolarian investigations carried

out on Barbados.

In western America, early reports of land-based

occurrences ol Miocene radiolarians include

Campbell de Clark (1944) in California, Mcrt7.

(1966) in Peru, and Frcnguelli (1941) in Chile.

In Japan, onc may note works published by

Nakaseko {I960, 1963); and in the eastern pan

of the former ÜSSR those by Kozlova (1960)

from Sakhalin, and Runeva (1975) from

Kamchatka. A land-based occurrence of Pliocène

radiolarians is known from Rotti (Riedel 1953).

GEODIVERSITAS • 1997 • 19(2)

391

SCALE

NORTH EURASIA

OCEAN TROUGHS

FORAMINEFRAL ZONES

(MSK1981,

Paleogene commission)

Speeroldfa variabilis

Spiroplectammina

carinata oligocenica

Globigertna otricinaUs

(Lenticufina herrmanni)

BoUvina anteragressa

Qlobigerfna tropicalis

Globigerina turcmenica

Hemhenina afabamensis

Acarinina roîundimarginata

Acarinina bulbrooki

Gioborotalia aragonen^s

Globorotalia subbotinae

Acarinina susphaerica

Globorotalia conicontn/ncata

Globorotalia angulata

Acarinina inconstans

Globoconusa daubjergensfs

Globigerina taurica

RADIOLARIAN ZONES

AND LAYERS

(R. Kh. Lipman)

iayers with Cenodiscidae

NANNOPLANKTON ZONES

(MSK1981.

Paieogene commission)

NANNOPLANKTON AND RADIOLARIAN

ZONES

(A. Sanfitippo, M.J. Westberg &

Np CP I W R-Ri®'*®'1981)

Dorcadospyris ateuchus

Cenospbaera almaensis

Iayers

zone ^

Phacûdisctis Hchareri

H. lentis, T. splendicus, S.tschujenkol

zone Ellipsoxiphus cbabakovi

zone Conocaryomma araiensis

zone $pOT}gurvs biconstricus

Ampriycarfdiscas hisoides -

Amphybrachium gracilis zone

Amphycaridiscus fusoides -

4#?7pniOi3cniatn ^nhJUs zona

lajpers wHh SpcfTg;ciscldae

acre SetJrxXsoLS vialovi

_ Blipscstyli^ tnçfarus _

Croruyodnj^ ^egularia

_ Pü/0(3feCtiS Orff9lUS _

zona Cenosçfyaera caucasfca

zone Cenodiscus magnvs, C. long us

zone l>fK>sph^^ kreguisns \ Iayers

matjifts ' Prurtcidea

_ _ no zone _

_no zone_

Heliocoponthosphaara reticulata

Coccolithus sijhdistichus

r I I

'V^UtVUa I psmtAJomdinnf

ChianHiiiinu&osmaruBnsiS

n^kJuiclenBslrs \jinbiltca

Nannot&trina fulgens

Discoaster Rhobdasphaera mfëtal

subblodoensis -1

15 14

I Lower subzone

Discoaster lodoensts

Marthosterites trib/acbiatus

ÔiscnâstsFdiasiÿ^

Dlscnasler bînoao us

_ M arOiostsrrlBS canfofiüs _

_ Pisçoaslsfmuitiuâjêj^ _

^ r_ HaMa lilhus fiedBi[ _

i Discoaslof gemmeus

I OtscoasTefkioinpàfli

Faseiculites tympanifarmis

Crtaiplacûlitiustsnnurs •f.l

Einpsonnos /nscelûs

14 12

13/ 11

Theocyriis tuberosa

Thyrsocyrtis bromia

_ Podocyrt is goetheana

_ Podo cyrtis chafara

Podocyrtis milra

Podocynls arrpia, rbyrsocyrtis ifiacanina

Theoc a mpe

_ ^socc^ CfHC.'0 » x<yrà _

_ P^ormxy^ m arViafa_

Priormocystîs striata

Buryella clinata

Becoma bidartensis

Heliolithus riedeli

Fig. 2. — a corrélation scheme of zonal division of Paleogene of northern Eurasia and oceanic troughs based on radiolarians. foraminifers and nannoplankton {Lipman 1993).

De Wever P. & Popova I. M.

Cenozoic radiolaria from European Platform

In Europe, Icalian localicies provide che majority

of our information on Neogene assemblages of

the Mediterranean région; summaries by

Sanfilippo (1971) and Sanfilippo et al. (1973,

1985a) cover many of ihc niainland localicies

described by early Italian authors (Vinassa de

Regni 1900; Carnevalc 1908; Principi 1909;

Anelli 1913; Lucchese 1927). In addition Sicilian

Late Miocene and Pliocène occurrences bave aiso

been described since 1880 by Stohr and since

1890 by Dreyer (see also Table 1). Calabrian

occurrences of Pliocène and Quaternary assem¬

blages are also reported by Scguenza (1880)»

Guerrera (1881), Pancanelli (1882). Paraiethyan

Miocene assemblages are described from Central

Euiope: Romama by Dumicrica (1968), the pre-

Carpachians by Runeva (1969) and Austria by

Bachmann, Papp & Stradner (1963).

Oligocène - Middle Miocene

Miocene radiolarians are known from Maryland

in the eastern North America (Martin 1904). A

summary of Caribbean occurrences lias been

compiled by Sanfilippo & Riedel (1976); parti-

cularly significant are the Middle Miocene of

Trinidad, Jamaica and Barbados and the

Oligocène of the Oceanic Formation on

Barbados. Land-based middle Terriary radiola-

rian occurrences are described by Takayanagi et

ai (1976) in the Miocene of Japan, and Runeva

(1975) in the Oligocène and Miocene of

Kamchatka. An Early Miocene assemblage is

recorded (rom the Andamaii Islands (Indian

Océan) by Jacob Ôc Slirivastava (1952).

In Europe, an early Oligocène locality is known

in East Prussia (Eisenack 1954). Early Miocene

sequences are known from Southern Spain

(Berggren et al. 1976) and northern Italy

(Westberg, Sanfilippo & Riedel 1981).

Paratethyan occurrences of Early Miocene are

described by Barwicz-Piskorz (1978) and

Dumitrica (1978).

Lipman (1972) and Ke.stner (1973a,b) describe

Oligocène assemblages from the USSR.

Eocene

Land-based Eocene occurrences in America are

recorded by Clark & Campbell (1942, 1945)

from California, and by Cunningham (1895),

for an occurrence in Mississippi. In rhe

Caribbean région the classic occurrence of

Barbados was described by Ehrenberg (1854,

1873> 1875) and Bütschli (1882a, b). An occur¬

rence on Cuba was reported by Palmer (1934)

and other localicies on Barbados, Trinidad, Cuba.

Grenada and Panama are summarized by

Sanfilippo &: Riedel (1976),

In New Gninea some record.s are cited by

Crespin (1958), in Saipan by Riedel (1957b),

and in Kamchatka by Runeva (1975).

In Europe an occurrence is reported in northern

Getmany by Brandr (1935) and in Israël by Reiss

(1952).

In che former USSR, Eocene radiolarians hâve

been recorded in numerous papers (see Table 1).

Palaeocene

In North America, a Palaeocene radiolarian

occurrence is recorded in Missouri (Frizzell &

Middour 1951), and one in California (Foreman

1968). Sanfilippo & Riedel (1976) recorded an

occurrence in Cuba.

în the former USSR, Palaeocene radiolarians are

reported by several authors (Table 2).

STUDIES ON RUSSIAN PLATFORM

In analyzing Russian literature we discovered

many geographical terms like: Pre-Caucasus,

Zallralie, Povohhe and so on. which are iinfami-

liar lo the western reader. Similady in geological

descriptions there are such term.s as sloP

'*svitd'\ "^horisotP and so on. Here we give an

explanacion of terms which are currently in use

in Russb. For claricy we preserved the original

names of the subdivisions (in brackets in the

text).

Geographical terminology

- Chukotka = Tchouktches = Chukchi.

- Crhnsky. Crimea.

- Pre Black .Sea région: territory 400-600 km to

the north of the Black Sea, Southern Ukraine.

- Pre Carpathianr, Carpathian folded area and

the territory 200-300 km to che east of the

Carpathian mouncains.

- Pre-Caspian (or Pre-Aral): the territory to the

GEODIVERSITAS • 1997 • 19(2)

393

De Wever P. & Popova I. M.

north of the Caspian (or Aral) Sea, but in some

publications it can be the territory to the east

and to the wesr ai Caspian (or Aral) Sea.

- Pre-Cancasus-. the territory lOÜ km to the north

of the Caucasus.

- Povobhe (= Povolshie): territory along the right

and lefi banks of Volga river.

- Predmugüdzhari(f: Cis-Moudjari.

- Preduralie = Pre-Ural = Cis-UraJ = West Ural.

- Priaralir. western Aral Lake région.

- Stepnoi Crimea\ middle part of Crimea penin-

sula, territory near Simferopol.

- Zauralie = ZaUralie: territory to the east of

Ural mountains (= Trans-Ural).

GEOLOGiCM TF.RMINOLOGY

Lithology

- Aleurolices (or alevrolite): scdimeniary silty-clay

rocks, which contai ns. about 45% very fine grains

of sand and more ihan 55% clay.

- ArgUlïie. metamorphosed (low degree) aleuro-

lites.

- Opoka: Russian analog of cherts (diatomite,

radiolarite type) with a high pcrcentage (more

than 70%) of organic silica.

Stratigraphy

(according to A. Zharnoida et ai 1970)

- Otdek a unit oi a common (“chronostratigra-

phic”) scale, translated by the term Sériés

(English).

- Svita-, alwâys translated by the term formation,

although in a strict sense this term “formation”

does not exactiy coincide with its interprétation

by many Russian authors, as formation means

the basic subdivision of the category of lithostra-

tigraphic un its.

- Horizon: layec.

- Pachka: we translated it as a member and it

means literally a member of some larger subdivi¬

sion (formation).

- Sloi and plast\ thcrc is no clear distinction bet-

ween the English terms bed and stratum, which

incidentally is also the case with the Russian

terms sloî and pLtsî.

In the following part the texr is arranged in (1)

geographical order (from the West to the East)

and (2) by the year of publication. The numbers

in square brackets which tollows a référencé cor¬

respond to the numbers used on table 2 and on

corresponding location maps.

PRi.-BLACK Sla région

Pre- Carpathium

Information about Oligocène and Lower

Miocène Radiolaria of the Pre-Carpathîan area

(Vorotyshehe, Slonitsa and lysmenitsa Rivets

sections) can be found in papers written by

Subbotina (1960, [40]) and Runeva (1969,

[39]). In our opinion the assemblage dcscribcd

by Subbotina seems to bc redeposited because

the taxonomie composition of the radiolarian

association discovered in Oligoccnc-Lower

Miocene deposits of the Zagorsky sériés is unu-

sual. The radinlarian association wa.s found in

cxoric pièces of breccia. Ail illustraied specimens

are very poorly preserved and ihe association

contaias some spedes of Dictyomitra. There is a

noie in ihe paper about redeposiiioii of forainini-

fers espccially in sandy siraia. Runeva (1969,

[39]) discusses this problem in her paper where

she iniioduccd the gencric composition (only) of

Lower Miocène radiolarian associations from the

Vorotyshehensky sériés of the l^n^-Carpaihian area.

The conclusion of the author toncerning the

Oligocène and Lower Miocene âge of Radiolaria

bearing deposits from the Vorotyshehe, Slonitsa

and I v'smenitsa Rivers is that the radiolarian com-

plcx is a resuit of ciosion of Crecaccous and

Eocene radiolarian bearing deposits and was trans-

ported with the transgression of these sédiments

from the east or .souih-east.

Lozyn)'ak (1969, 1985, [26)) described Eocene

and Oligocène radiolarian assemblages from the

Maniavskaya sériés (Lower Eocene), Bachinskaya

bed (Middle, Upper Eocene) and Menilitovaya

sériés (Oligocène) ol the Carparhian folded area.

South-îoestern Ukraine

'Lhe hisiory of Palaeogene radiolarian studies in

the Ukraine begins with Gurov’s publication in

1893 (Gorbunov 1971, [9]) where he memioned

the prcsence of Haliomna sp. in Kharkov rocks

from the Southern areas of ICharkov Province.

Information about the existence of Palaeogene

radiolarian associations in deposits from Kiev,

Chernigov and Poltava Provinces (Koryokovka,

394

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

Kholm villages, Volynsk), the Odessa area, the

Pre-Black Sea troughs, the Verino pôle, and

along the Lopanj, Uda, Severskii, Donets and

Melovaya Rivers cornes from the publications of

Titkovsky (Î90la), Uspenskaya (1930, 1950a),

Kaptarenko-Chernousova (1936, 1948), Pechen-

kina (1964) (ail rcferences from Gorbunov

1971). The most complété data about Paleogene

radiolarians of this région can be found in the

Gorbunovs monography (1979).

Borisenko (1958, [2]), working in the Krasno-

darsky région and Seversky, Abin.sky and

Psobaisky Districts, has dcscribcd foriy new tîoea

from a shallow water radiolarian assemblage of

Palaeogcne deposits of the Psecupskaya For¬

mation (svita). Ten new taxa were described by

her (Borisenko I960b> [3]) from the Upper

Palaeoccne rocks of the Abasinskaya Formation

(svita) of eastern Kuban. The Lower-Middle

Eocene deposits of western Kuban (Psecups

River, interflow ot the Shebsha and Shibica

Rivers) contain a shallow water radiolarian asso¬

ciation discovered in the Zybzinskaya, Kutais-

skaya and KaJuga Formations (svita) (Borisenko

1960a, [4]). The same tetritory lias been studied

by Krasheninnikov (1960, [!5]) and he presen-

ted the description ot forty-two new radiolarian

taxa (two gênera and forcy-two species) from

Lower, Mtddle and Dpper Eocene deposits from

chc western Prc-Caucasus (MoldavanoTsifsk and

Zybzinsk area). The associations of radiolarians

wcrc found togetherwirh foraminifers bclonging

CO the Glüborotalia suhbotinae and Globorotalia

aragonensh Zones. The first radiolarian assembla¬

ge from the Zybsinsk sériés indicaics shallow

water conditions and rhe second onc, from the

Kutaissk sériés, deep water conditions.

Crimea Pemmula

A Lare Palaeoccne radiolarian association from

the Kachinskaya layer (horizon), an Early Eocene

association from Simferopolsky and a Late

Eocene association from Bodraksky layer (hori¬

zon) of Crimea havt been studied by Chedyia

(1973 [6], 1981 [8]), The invesiigacor concluded

that; (1) therc is no corrclation between the

radiolarian association from Stepnoi and Sou¬

thern Crimea; (2) the Palaeogcne assemblages of

Radiolaria from Crimea can not be correlated

wLth the same from Middie Asia using normal

corrélation techniques bascd on the taxonomie

composition of assemblages; (3) the assemblage

can be correlated only by cycles of sédimenta¬

tion, Corrélation with Foraminifers .showed that

the radiolarian association from the Kachin.sky

horizon occurs with rhe Acarinia aca7’jjuita

assemblage, the association from Bakhehisaraisky

layer (horizon) occurs with *he Opereuhna

semiurvoluta assemblage, and the association

from chc Alrninsky laver (horizon) with lhe

Glohigempsis mdtx assemblage.

Lipman (1982, [22]). working with the deposits

ol the Rubanovskaya formation in the Lower

Serogorsk}' région of ihc KJicr.sonslcy district, has

invesiigoled Oligocène Radiolaria from the nor-

thern Pre-Black Sea area and Crimea. She intro-

duced two new radiolarian taxa, The âge of the

shallow water radiolarian association was confit-

med, using foraminifers and molluscs. The

rcsuJts of an investigation airricd ont by Lipman

on Radiolaria from eighr sections of Palaeogcne

deposits in the Rakhenisaraisky district were

published in 1984a [23|. She discovered as.socia-

tions of Radiolaria in ouccrop.s of Upper

Palaeoccne to Lower Oligocène deposits from the

Kasha Rivei and Suviy-Kayà Mountain (Upper

Palaeoccne), the Belbek River (Lower Eocene),

the Alma River (Middle-Upper Eocene) and

Kizil'Djar Mountain (Upper Eocene-Lower

Oligocène). Ail assemblages of Radiolaria occur

lugcther with foraminiferal zonal associations;

Acarinina suhsphaeHcit, Globorotalia suhbotniae,

Hühtkenma nlabmnemüy Gbhtgcrapsis tropîcnlis^

Bolivina ar^tegt'esi^a and Lenticulina hermamn In

a second paper published by Lipman (1984b,

[24]) corrélation of zonal siratigraphical schemes,

based on radiolarian and ioraminifers, from the

Palaeoccne and Floccne deposits of the Pre-

Caucasian and Apsheron peninsulae was introdu-

ced. The investigator applied her own zonal

subdivision, based on radiolarian data toc the

Cherkessky key-scction of the Prc-Caucasus and

made a corrclation between zonal radiolarian

associations and assemblages described by

Borisenko (1960a, [4J) and Krasheninnikov

(1960j [15]) for western Kuban and by

Mamedûv (1970, [30]; 1973b, [32]) for the

Apsheronian peninsula.

GEODIVERSITAS • 1997 • 19(2)

395

De Wever P. & Popova I. M.

North> Caspian

Area

Don River

Middie Volga

Area

East Ural

Slope

West Siberian

EOCENE

<1^

T. andriashevi

r '

■L±

E. polysiphonia

C. alta

H. quadratus

L separatum

L separatum ?

H. hexasteriscus

H. lentis

S. paciferus

P. fiscella

f ?

P. fiscella

PALEOCENE

û.

Ph. cubensis

P. foveolata

T. sengilensis

P. foveolata

T. sengilensis

B. tetradica

MP- 't;.

B. tetradica

T. lamacium

ÛC

3 iW

B. alifera

Fig. 3. — Corrélation of radiolarian zones among North Caspian, Don River, Middie Volga, East Ural and West Siberian areas ( from

Koziava 1993).

Russian Platform

Upper Palaeoccne and Lower to Upper Eocene

radiolarian bearing deposits from the Voronesh

anticline hâve been studied by Tochilina (1969,

[41]; 1975). Radiolaria were not found in

Oligocène deposirs from thac région. The shal-

low water radiolarian associations occur together

with foraminifers and molluscs. Three faunal

periods closely connected with transgressions and

régressions are escablished m ehis papcr:

1. Late Palaeocene (Veshenskaya formation

\svita\) - Early Eocene (Sheprukhovskaya forma¬

tion [svita]);

2. Late Eocene (Tishkinskaya formation [svita\)\

3. Late Eocene (Kasianovskaya formation [svita\).

The author compared faunal associations in

deposits of the Voronesh anticline (Russian

Platform) with that of the Pre-Caucasian and

eastern slope of the Ural mountains and found

many common species.

The Southern part of Russian Platform has been

studied by Zagorodnyuk (1969. [43]; 1975,

[44]; 1981, (451), She also investigated

Radiolaria from the Asovo-Kubansk trough,

Salo-Manyhsk interflow and the basin of the

norrhern Emba (Pre-Caspian lowland). She reco-

gnized three different radiolarian associations for

the Lower flow of die Don River and four assem¬

blages in the Pte-Caspian lowland. Investigating

the transition between some représentatives of

396

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

Amphihrachhim and Hhtiastrum she found ouc

that: (1) apparently they hâve a common ances-

tor; and (2) préservation of the shells improves to

the north.

The Lower Don basin and norrhern Pre-Caspian

Eocene deposits served as a basis for Nikitina and

Zagorodnyuk’s (1981, 137]) study in which thcy

carried out a corrélative anal>^is of foraminiferal

and radiolarian distribution within these rocks.

The authors givc a corrélation berween régional

zones based on planktonic foraminifers and

radiolarian zones, proposed by Zagorodnyuk

(1967) for shallow waier associations.

The scheme proposed in this paper does not cor-

relace with the zonal subdivision based on

Radiolaria data established by Lipman (1972,

[20]; 1993, [25]) for Palaeogene deposits of the

former USSR.

Palaeogene deposits of the samc territories hâve

been studied by Kozlova (1990, [13]; 1993,

(I4])î she established nine zonal subdivisions

which correlared with radiolarian zones proposed

by her for the Middle Volga, East Ural slope and

West Siberia.

The existence of three zonal schemes for the

same région reflects the différence in approach co

the establishment of radiolarian biOvStratigraphi-

cal zonal .subdivisions- First there is a problem

because of the large number of hiatuses in ihe

studied sections. Second thcrc i.s a problem in

deciding which species tn use as a basis for a

zonal .scheme. This question was not clearly dis-

cussed by Nikiüna & Z.agorodnyuk (1981, [37])

or Zagorodnyuk (1981, [45]).

Lipman (1993, [25]) and Kozlova (1990, [13|;

1993, [14]) suggGsted thar the number of events

in the association of Radiolaria .should be the

main charactcrisric for the zonal boundary.

However, Lipman tried co apply to the ga*Don

Basin the scale she established for the western

Siberia lowland and then tried to trace ir to

many régions of the counrry; whereas Kozlova

attempted to apply (partially) the scale proposed

by Forcman (1973) for the Gulf of Mexico. Il is

difficult to say now wbich actempt is the best

and will be the most fruitllil. In our opinion it is

an important problem to be studied within the

Peri-Tethys programme.

MiDDt.E Part of Volga River Flow

(Middle Povolsh’e)

Radiolaria from this région have been studied by

Lipman (1969, [19]) and Kozlova (1984a, b,

[121; 1990. Ii3]î 1993, |14]). For the Upper

Palaeoccne-Middlc Eocenc three versions of a

zonal subdivision have been suggested. First,

Kozlova (1984b. [12]) attempted to apply some

biüstratigraplucal subdivision.s suggested by

Foreman (1973) for the Gult of Mexico. Second,

Kozlova (1990, [13]) proposed a zonal scheme

based on morphotyplc lineages of the gênera

Axüpruïmm, Heliodiscus, Tripodtsdnus, Clathro-

cyclas^ Lychnovajiium and Photmocyrtis. This

investigation shovved the impossibilicy of using

Buryella clinata and SponguU'ochus puciferus as

indeX'-spccies for this région. Insiead Kozlova

suggested Phormocyrth striata and fleliodistas

lentls zonal subdivisions for the Lower Eocene

tinie iriterval. The fîrst one {P. striata) of tire

index species is absent in a third version biostra-

tigraphical scheme (Kozlova 1993, [14]). A new

zone. Heliodistus hexasterisetm. was .suggested for

the upper Lower Eocene and lower Middle

Eocene dcpo.siis and the author puts a question

mark tbr rhe Middle liocene L sepatatum Zone

in the middle Volga area indicating that the esta¬

blishment of this zonal subdivision is still under

discussion.

TüliRGAlSK TROUGH AND NORTHERN PrE-Ar.AL

The Oligocène radiolarian association was di.scû-

vered by Kesrner (1973).

Investigations of Eocene Radiolaria in this area

were carried out by Lipman (1965a, b, [17, 18];

1969. [19]; 1972, [201; 1975a, b, [21]) and

Kozlova (1990, 1993). The most complété infor¬

mation about Palaeogene Radiolaria from the

Tourgaisk Trough and northern Prc-Aral région

is given in papers writteu by Lipman (1965,

1969, 1972, ig75a):

1 . The distribution of ninery-eight radiolarian

species in the Tourgaisks drough and northern

Prc-Aral Eocene deposits is shown in the first

paper (Lipman 1965a) of this sériés.

2 . Two zonal subdivisions based on radiolarian

data are established: Spongurus biconstrictus -

Middle Eocene (lower part of Tasaransk sériés)

and Ellipsoxiphus chabakovi - Upper Eocene

GEODIVERSITAS • 1997 • 19(2)

397

De Wever P. & Popova I. M.

FORAMINIFERAL ZONES OF

THE SOUTHERN USSR

(Krasheninnikov 1971 ;

MSK USSR 1981, 1985)

RADIOLARIAN ZONES

LATE

EOCENE

Globigeraspis tropicalis

Theocyrtis andriashevi

MIDDLE

EOCENE

Globigerina turcmenica

Ethmosphaera polysiphonia

♦

Cyrtophormis (?) alta

♦

Hantkenina alabamensis

Heliodiscus quadratus

Acarinina rotundimarginata

□

Lychnocanium separatum

■

Acarinina bulbrooki

□

Heliodiscus hexastericus

■

EARLY

EOCENE

Globorotalia aragonensis s.l.

Heliodiscus lentis

♦

Globorotalia subbotinae s.l.

•

Petalospyris fiscefla

LATE

PALEOCENE

Acarina acarinata

^ Phormocyriis

^ cubensis

P. foveolata

T sengilensis

Acarinina subspherica

Buryelfa tetradica

Globorotalia angulata s.l.

Thecosphaera lamacium

EARLY

PALEOCENE

Buryella (?)

alitera

Cromyocarpus

(?) ovatus

Spianktonic foraminifers ^Nannoplankton ^Dinoflagellates

Fig. 4. — Foraminiferal zones of South Eurasia comparée! to radiolarians zones (from Koziova 1993).

(upper part of Tasaransk sériés).

3. Spongurus hiconstrictus association of

Radiolaria occurs together with loraminifers

Nummulites distam, N., murchisso/ii, Cibicida

eocaenuSi Bulimina mïtgarsînae. She believed

these sédiments to be analogous to the Alaisk

stage of Central Asia, and co the Buchagsk sériés

of the Russian pktform.

4. Ellipîoxiphîis cbahakovi occurs together with

the foraminifer Spiroplectammina spectabilis, The

radiolarian association can be correlated with

Upper Eocene deposits irom the Turkesian Stage

of Turkmenia, Kyzyl-Kum, and from the

Ljulinvorsk Sériés of the western Siberian lowland.

5. In the deposits from the Saksaul Sériés one

can see a third association of Upper Eocene

(shallow water association) Radiolaria. The

Upper Eocene âge of the stratum is confirmed by

molluscs {Pectunculiis aralcmh), and by foramini¬

fers {Bolhdnopsis carimtifbrmis tic).

6. The fifst assemblage of radiolarians was dîsco-

vered in the deposits of the nonhern Aral Sea

coast sections and on Cape fsendy-Aral in thin

layered dark, greyish-grey clays, which were

deposited above the nummulilic limcstones, and

also in marly clays and in the maris trom wells of

the Chagraish plateau, in the Tumaly-Kolj village

at Lake Tebez, in Chelkar, on Mount Tas-Aran,

398

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radioiaria from European Platform

Paleontological characteristics of zone

Foraminiferal zone

Radiolarian zone

Upper

Coun

BoIMna - Nonion curviseptum

Û.

û.

Globigerinoita index

Cromyocarpius echinatus

Middle

Coun

Globigehna turcmenica

Sethopyramis victori

Stylatractus pictus

UJ UJ

Globlgerinoides

subconglobatus

Azerbaidjaniyus compositus :

Styfoirochus schweeri

û UJ

9 5^

V O

2 UJ

Globorotalia

Lower

crassaformis

Ar)thocyrtidfum apsheronense

Comutalla fimbnata

Globorotalia

LOWER

EOCENE

Coun

aragonensis - caucasica

Globorotalia subbotinae

Astrosestrum dtaliensis

Ellipsostylus ancorarius

UPPER

PALEOCENE

•Je

«9

fts

Globigerina ve/ascoens/s

and agiutinised foraminifera

Fig. 5. — Scheme of Radioiaria and Foraminifera’s zonal corrélation in Shemakhino-Kobistanskaya and Apheronian péninsule areas

of Azerbaidzan (Mamedov 1973b).

in the Turgay and in several wells along the River

Ashchis and in the Irgis area. This complex is

also traced in the Buchagsk Sériés in the South¬

ern part of the Russian Platform,

7- The second assemblage of radiolarians was

encountered in sections of Mount das-Aran, on

the northcrn coast ofTschc-Bas Bay, the Aral Sea

and in several wells located on the Chagraisk

Plateau in the Tumaly-Kolj village at Lake Tebez,

in Chel-kar and in Turgay.

8, According to Lipman, the majority of radiola-

rian assemblages she invcstigated are characteris-

tic of a shallow water basin. In addition to tins

general conclusion we should say, that in Middle

Eocene radiolarian assemblages studied one can

see many représentatives of Nassellaria, which are

not présent in Late Eocene associations and this

might indicate a différence in water depth.

The investigation carried out by Lipman on the

Palaeogene biostrangraphy of this région was

taken inro account by Kozlova (1984, [12]). In

her study of Palaeogene Radioiaria from the East

Ural slope she Incorporated in her new zonal

.scheme some zonal subdivisions proposed by

Lipman. However, she referred her Upper

Eocene Heliodisvits lentis Zone to the Lower

Eocene and subdivided the EUipsoxiphus chaha-

kovi Zone inro rwo new zones, the Petalospyris

fiscclla Zone and Spongotrochus paciferus Zone.

She also introduced four new radiolarian species.

PRE-CaSHAN REGION

The Pre-Caspian cerricory is very large wirh its

eastern part belonging to Turkestan, its western

GEODIVERSITAS - 1997 • 19(2)

399

De Wever P. & Popova I. M.

part to Azerbaidzan, and the northern part to

Russia. We start our description with the western

part.

The western part of Pre~Caspian région

(Azerbaïdzan)

ShemakhinO'Kobistanskaya and Apsheronian

peninsula areas sen'^ed as a basis for Mamedovs

(1969a, b, c. |27'29]; 1970, [30); 1973a. b, [3U

32]; 1975, [33]) investigations of Palaeocene-

Eocene Radiojaria discovered in the Lower-

Upper Coun Formation. Twenty-nine new taxa

were desccibed in his papers, and the First divi¬

sion of Eocene deposits according to radiolarians

was established (Mamedov 1973a, [31]).

Species ntenrioned by Mamedov as characteristic

of the western Pre-Caspian région are not lound

in the zonal scheme established by Lipman for

the Apshenni Peninsula and Prc-Caucasus, despitc

the fact ütat bodi biostratigraphical subdivisions

are based on radiolarian data and werc correlated

with the samc foraminifcral zones. However, ic is

possible to carry an indirect, but not pure gra-

phical, corrélation between these rwo zonations

for Lower-Upper Eocene deposits. Unfonun-

ately, we can not say the samc about the biostra-

tigraphical schemc established for the northern

Pre-Caspian région by Koziova (1993. [l4]).

In this case it is possible to use graphical corréla¬

tion methods only since the author gave a coni-

parison bciween hcr radiolarian biostrari-

graphical zonation with that based on foramini-

fers, which had been suggested by

Krasheninnikov (1971) and appiovcd by MSK

USSR (1981, 1985) for the Southern part of for¬

mer USSR lerricory (rhis scheme is different to

the one gîven in Mamedovs paper).

In a previous article Koziova (1984a). using the

same scale, corrclatcd some. but not ail, radiola¬

rian zones with some diatom zones. Thus,

Bîiruella tetradica zone (Foreman 1973) has been

correlated with lower part of the Trinacria ven-

triculosa àiàxovw zone (Gloser 1979). Pemlospyris

fiscella ( Koziova 1984a) with Coscinodiscus payeri

(Gleser 1979). Spongotrochus padferus (Koziova

1984a) with the lower pan of Pyxilla gracilis (?),

and Helîoducm lenth with the upper parc of

Pyxilla gracilis (?).

l'he easiern part of the Pre-Caspian région,

Middle Asia

Radiolaria were found and studied in the

Palaeogenc deposits of Middle Asia (Lipman

1950, [16]; 1953; Chediya 1957. 1981;

Moksyakova 1961. [35]; 1965. 136); Kreidenkov

& Chediya 1971; Kestner 1971, [10]) in expo-

surcs and wells of eastern lurkmenia, Bukharo-

Khivinsk dépréssion and south-western spur.s of

the Gissarsk mountain range. Tadzhiksk déprés¬

sion and Fergana. Eocene Radiolaria from the

Turkestanian Suge hâve been studied by Lipman

(1950, [16]). 8he described eighteen new spccies

found in outerops in Kyzyl-Kum. Tamdy.

Shchulj trough, western slopc of Tamdinsk stage,

Alt-Oi, and in the wclls near Dzhanhoi, L^sun-

Kuduk and Cher)T [16]. The next investigation

of Upper Eocene radiolarians from Kumsky hori¬

zon of Western Turkmenia vzas carried out by

Moksyakova (1961, [35]). The investigator des¬

cribed eighteen new taxa. Neverrheless the radio¬

larians association cannot be referred to a typical

shallow water assemblage, because of the eight

spccies of Nassellaria présent The next paper of

Moksyakov.i (1965, [36]) was devoted to Upper

Eocene Radiolaria from the Kuberlinsk and

Kerestinsk horizons of south-easrern Turkmenia,

Kyzyl-Kum and western Turkmenia (Ustyurt and

Krasnovüdsk plateau). The descriptions of ren

new radiolarian taxa are given in this paper. The

author présents a corrélaiioa (on the contrary to

Chediya (1981) between ihe Bodraksky Stage of

Crimea stratotype seciioa and Kyberlinsky,

Kerestinsky and Kymsky horizons ol 3'urkmenia.

She referred the Beloglinsky horizon of

Turkmenia to Alminsky in Ciimca. Kestner

(1971, [10]) discovered twelve généra of

Nassellaria {Tripospyns^ Lychnocanium, Setho-

pyramiss Sethocyrtis^ Lophophaena, Podocyrtis,

Theocorysy Theocyrtu^ Truolocanipe, Theocampe,

Lithostrobus, Eucyrtidinn/) in Lower-Upper

Eocene deposits of Beloglinsk, Kuberlinsk-

Keresrinsk and Kumsk horizons, He referred

Lower Eocene deposits to Bakhehisaraisky,

Middle Eocene lo Simferopolsky and Late

Eocene to Bodraksky stages of rhe Black Sca stra-

[orype section. The majority of ihese généra (cle-

ven) were found in Upper Eoccnc deposits

together with the following foraminifers:

400

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

Acarinina rotirndimarginata, Htinîkenina atxtba-

rnensis and Globigcrinoules subconglobatus, One

genus wa.\ found in Early Eocene deposits toge-

ther with Globorotalia accjua and G. mhbotinae.

The Middie F.oeene radiulart-an association

occurs together with Globorotalia aragonemis and

Acarinina crassaformis. In the paper written by

Averburg & Kestner (1973) one can find the cor¬

rélation made beiwecn radiolatian and hiramini-

fer zones ot thU région.

Chediya (1973, [6]) investigated an Early Eocene

association of Radiolaria in the Suzaksk area, a

Middlc Eocene association in the Alaisk area,

and a Late Eocene association in deposits of the

Bukharo-Khivinsk dépréssion. Judging from

lithologie composition of the rocks and fauna

described in this publications, the sea in this area

was during the Early Eocene a shallow water

basin, which became deeper in the Middie

Eocene and reached its maximum depth in the

Late Eocene.

Unfortunately, information about Palaeocene

radiolarian associations discovered in this area is

incomplète. We found only one paper (Chediya

et al, 1971. [5]) dealing with micro- and macro-

faunal studies from the Bukharsk layers exposed

in the mountain ranges of Peter-che-Firsc,

Khodzha-IOsiati, Aryk-Tan, Istum-Tay and in

the area Kichik-donguz élévation. Three new

radiolarian taxa hâve been described in it, The

association of Radiolaria occurs together with

foraminifers. Underlying and ovcrlapping layers

contain coral, pelecypods, gastropods, brachio-

pods, ostracods, other macrofauna and small and

large foraminifers.

CONCLUSION

As mentioned previously by Sanfilippo et al.

(1985), in comparison with the amount of évi¬

dence available for calcareous microfossil groups,

there are few localiries for which tlic change from

the Mesozoic to the Cenozoic radiolarian fauna

can be traced. The available evidence indicates a

profound décline in radiolarian diversiry at ihe

Cretaceous-Terriary boundary- A high propor¬

tion of Mesozoic gênera and familles became

extinct with only a few surviving into the Early

Palacoccnc. By early Eocene time, however,

radiolarian généra and specics had aitaincd die

diversity that they exhibited during the

Cretaceous and throughout the later Cenozoic

(Riedel & SanPilippo 1981). Thiis the radiola-

rians clearly fulfil one ol the requîrcments for

stratigraphie utility, namely taxonomie diversity -

but whai about ilieir rate of evolucionary change ?

Due CO the great taxonomie diversity of the

Ççnozoic radiolarians, if is not wise to expect

that ail species will be comprehen.sively known in

the neai* future, l'herefore choices will hâve lo be

done on which ways the pos.sible reseaah will be

conduct for radiolarian knowledge. Taxonomy

must rcflcct phyJctic rclationsbips, not géométrie

ones as in the Haeckelian system. Wc arc approa-

ching this capabîlity in somc families but are

from i[ for most of the spumellarian families. To

achieve such goals, h is necessary to record diver-

sily and stratigraphical ranges from couniries,

which were somehow' ncglected untÜ now, such

as the Russiaii platform.

Studying the available literature in this field we

hâve been faced with some problems. The majo-

rit)- of them dcal with the establishment of a

biostratigraphical scheme. Some of the problems

hâve ‘objective’’ reasons:

’f'hc connection beeween some parts of Peri-

Tethys was not constant during Palaeogenc.

2. Ail processes of sédimentation were strongly

intlueneed by transgressions and régressions

within che basin; therefore chere is ver)' limited

number of sections within ihe former Peri-

Tethyan basin m which one does not find nume-

rous hiatuses in radiolarian distribution.

3. Some parts of dic Peri-Tethys at that time had

long-lived basins with a well dcveloped shallow

water radiolarian fauna and this phenomena

makes corrélations between distant parts more

diffîcult and indirect.

Besides the.se objective reasons there are some

“subjective” reasons:

1 . Scientists hâve been using different bases for

the establishment of a hiostratigi-aphic zonation.

2. The âge détermination of Palaeogene deposits

in some régions (for example in Middie Asia)

should be redone because the radiolarian assem-

GEODIVERSITAS • 1997 • 19(2)

401

De Wever P. & Popova I. M.

blage was studied in tliin sections only» or becau-

se the radiolarian association was described only

at the generic level.

3. Long distance corrélations requîtes that the

taxonomy of many species be revised, as many

identifications wcrc based only on drawing.

Resolution ot the difficulties mentioned above

may help us to understand the reasons for the

existence of two different zonal scales, one pro-

posed by Lipman (1993) and the other by

Kozlova (1993).

During the présent review it became apparent

that:

1. The presence of Oligocene-Lower Miocene

radiolarian assemblages in the deposits exposed

in Carpathian tolded area had not been proven.

2. There was a contradiction betvveen the

palaeoenvironmental reconstructions of Lipman

(1965) and of Kestner (1971). both of *which

were based on radiolarian associations from

Eocenc deposits of the Bükharo (Khivinsk

dépréssion and south) western spurs of the

Gissarsk mountain range. According to Lipmans

data the Upper Eocene radîolarians belong to a

shallow water assemblage, but Kestners data sug-

gest that the Upper Eocene radiolarian associa¬

tion is characterisfic of deep water conditions.

Finding lhe solutions to these two relevant pro-

blems would be appropriatc and fruitfui Unes for

future research whbin the Peri-Tethys project.

Acknowledgments

This study was carried out during the Peri-Tethys

programme (Project 94-72) and ni ihe GDR 88.

It was financed by these programmes and by the

URA 1761. We arc also grateful ro C. Nigrini

(USA) and other reviewers who crincized and

painstakingly helped ro improve ihe manuscript,

as well as to M. Baconat (MNHN, Paris) for

bibliography. The stay of one of us (L Popova)

for one year in France during the présent work

was financed by che Centre National de la

Recherche Scientifique (CNRS-SDU, section

11 ).

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Lvov: 107-112.

— 1975 . — PccLiliarifics of thc structure of some

Sphaeroidea and Di.scoidca from deposits of Low

Don river basin. 'Systematic and Stratigraphie stgni-

ficancc of Rtidiolaria" [Sistematica t stratigraficheskoe

znacf.fenie Radwlarii], Leningrad, new séria 226:

48-52

— 1 975 . — K vnprosy o granitsc srednego i verkhne-

go cotsena po dannym izucheniya radiolyarii bassei-

na nlzhnego Dona i Vostochnogo Prikaspiya.

Trudy Vsesoyuznogo Ordena Na uchno-

hsleeiovatelskogo Geohgicheskogo Instituta (VSF.GEI),

novya seriyu, 226: 84-87.

— 1981- — About rhc position of thc T.owcr-Middle

Eocene boundary by mean of Radiolarians, in

Sistemaiika, Evolutsia i Stratigrafitcheskie

Znatchenie of Radiolarii [Systemaric, Evolution

and Stratigraphie Importance of Radiolaria],

Âcademy 0 ] Sciences of ÜSSR. Nauka, Moscow:

95-97 [in Russianj.

Zharaoida A. 1. 1984. — Somes resulrs and problems

of lossii Radioiarians Study, in Petiushevska M. G.

& Srepanjams S. D. (rds), Morphology, Ecology

and Evolution of Radiolarian.s, Proceedings of we

Fourrh Lurorad Conférence, 15-19 October,

Academy oj Science, l eningrad: 54-63 lin English].

Zhamoid.! A. I., Kovalevsky N. I. &: Moiseeva A. I.

1970. — Obsof zarybeshnikh stracigraficheskikh

kodçksov. Trtidi Aeadernii Nayk,\c}\y.\u\c 1, 182p.

Zhiyüan T. & Ts^^run T. 1976. — Studies on the

Radiolaria of fhe Easr China Sea. Studia Alarina

11:217-310.

Zhit'uan T. & Xinghni S.. 1981. — Two nev'species

of Liriospyns (Radiolaria: IVissocyclidae) from the

Xisha Islands, China, with a discussion on rheir

skcletal structures. Acta Zootaxonomica Sinica 6 (4):

337-343.

Zhiyuan T.. Hongxu G. & Xinghui S. 1978. — The

quantitative distribution of Stkholanchc zandca in

the western Part of ihe east China Sea. Oceanobgia

et Limnologia Sinica^ (1): 64-66.

Submitted for publication on 15 Februaiy 1996;

accepted on 15 September 1996.

432

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

Table 1. — Publications on Cenozoic radiolarians ordered by geographical régions (except publications dealing with the European

part of the former Soviet Union [see Table 2]).

LOCATION AGE

TOPIC

AUTHOR

Ouater.

Cachon J. etaJ. 1978

Ouater.

Evolut. Cytol. Ultrastruct.

Cauhon J. & Cachon M. 1978a

Ouater.

Biol. Cytol. Ultrastruct.

Cachon J. & Cachon M. 1978b

Ouater.

Taxon. Evolut.

Cachon J. étal. 1977b

Ouater.

Biol. Cytol.

Cachon J. & Cachon M. 1977

Ouater.

Biol. Cytol.

Cachon J. & Cachon M. 1976a

Czc

Taxon.

Goil R. M. 19723

Recent

Biol. Cytol. Physiol.

Cachon J. étal. 1977

Ouater.

Biol. Cytol.

Cachon J, S Cachon M. 1979

Recent

Biol. Cytol. Physiol.

Cachon J. & Cachon M. 1980

Czc

Evolut.

Kellogg D. E. 1983

Czc

Evolut.

Kellogg D, E. 1980

Ouater.

Sedim. Climat. Season. product. Ecot.Casey R, E. ét al. 1971

Czc

Evolut.

Kellogg D. E. & Hays J D. 1975

Czc

Taxon. Strat.

Campbell A. S. 1954

Recent

Biol. Atlas General

Cac^l 0 n J. & Cachon M. 1982a, b

Recent

Ultrastruct, Reproduct. Biol. Cytol.

Cachon J, étal. 1985

Czc

Taxon. N.Sp.

Campbell A. S. 1951

Ouater.

Biol- Cytol.

Cachon J, & Cachon M. 1975

Ouater.

Biol. Cytol.

Cachon J. & Cachon M. 1974

Czc Mzc

Biostrat

Boltovskoy D. 1988

Recent

Preserv.

King K. 1977

General Technics Préparation

BollûvsKoy D. et al 1983

Ouater.

Currenl Sedim.

Boltovskoy D. 1988

Recent

Biol. Physiol. Reproduct.

Klings, A. 1971a

Mzc-Czc

General Strat- Evolut.

Kling S. A. 1978

Preserv. Plankt.

Boltovskoy D, 1981

Czc Mzc

DSDP6

Kling S. A. 1971b

Recent

Physiol. Cytol.

King K. 1975

Recent

Biol. Physiol. Cytol. Diagen.

King K. 1974

Recent

Biol- Cytol- Skelet.

Cachon J. & Cachon M. 1972a, b, c

Ouater.

Biol. Skelet. Physiol.

Cachon J. & Cachon M. 1971b

Ouater.

Cytol- Biol.

Cachon J. & Cachon M. 1971a

L.Eoc.

Taxon. N.Sp.

Brandi R. 1935

Czc

Taxon Evolut.

Kellogg D. E 1975

Neogene

Strat. Environ.

Casey R. E. & Reynolds R. A, 1980

Taxon. Biol. Strat. General

Goll R. M. & Mehnield E. G. 1979

Czc

Taxon. N.Sp.

Haecket E. 1881

Czc

Taxon. Evolut. Skelet.

Dumitrica P. 1983

Czc

Taxon. N.Sp.

Haecker V. 1908

Czc

General Taxon.

Dumitrica P. 1979

Czc Ouater.

Taxon. N.Sp. Oc.

Haeckel E. 1887

Czc

DSDP1

Ewing M. étal. 1969

Taxon. Strat. General

Funnell B. M. & Riedel W. R. 1971

Slral Taxon. DSDP9

Goll R. M. 1972b

Czc

Taxon. Evolut.

Goll R. M. 1976a

DSDP38 Taxon.

GoH R. M. 1976b

Recent Ouater.

Plankt, Biol Physiol.

FebvreJ- 1982

Neog.-Ouater.

Evolut. Taxon.

Goll R. M. 1979

Biol. Ecol.

Flarbison G. R. eîal. 1977

GEODIVERSITAS • 1997 • 19(2)

433

De Wever P. & Popova I. M.

LOCATION AGE

TOPIC

AUTHOR

Czc-Quater.

Taxon. N.Sp.

Dreyer F. 1889

Paleog.

Biozon. Strat.

Cavelier C. & Pomerol C. 1977

Czc-Quater.

Biol. Evolut. Taxon. Cytol.

Hollande A. & Enjumet M. 1960

Eoc.

ChediyaD. M. 1973

Czc-Quater.

Biol. Cytol. Physio.

Hollande A. & Hollande E. 1976

Mzc-czc

General review Sedim.

Hlll W. 1912

Quater.

Biol. Physiol.

Herrîng P, J, 1979

Czc

Evolut. Extinct. Quater.

Hays J. D. & Shackleton N. J. 1976

MzC'Czc

DSDP16 Strat.

Dlnkelman M- G. 1973

Czc

Taxon.

Deflandre Rigaud M. 1969

Dedandre G. 8 Deflandre-Rigaud M. 1958

MzC'Czc

Distrib. Sedim. Paleog.

Hein J R, & Parrish J. T. 1987

L.PIeist. Quater.

Evolut.

Knoll A. H. 8 Johnson D. A, 1975

Quater.

Biol. Cytol.

Cachon J & Cachon M. 1976b

Climat. Ecol. Environ.

KrugtikovaS, B, 1969

Czc? Mzc?

Ecol. Oceanol. Biogeog.

Kfuglikova S. B. 1984

Mioc.-Quater.

Strat. DSDP12

Benson R- N 1972

Quater,

Biol, Physiol.

Anderson R. 0.1980

Quater.

Biol.

Anderson R 0.1978b

Biol.

Anderson B. 0.1978a

Quater.

Biol. Cytol.

Anderson R. 0. 1976a

Ouater.

Biol. Cytol.

Anderson R. 0.1976b

Quater.

Biol. Cytol.

Anderson R. 0. 1977a

Quater.

Biol. Cytol.

Anderson R. O. 1977b

Quater. Recent

Ecol. Strat.

Kruglikova S. B. 1901

Skelet. Physiol. Biol.

Anderson R. 0. 1986a, b

Biol. Skelet.

Anderson R. 0. et al. 1989a, b

Quater.

Recent Biol.

Anderson R. 0. & Rottger R. 1986

Quater.

Biol. Skelet.

Anderson R. 0. étal. 1986b

Biol. Cytol. Physiol.

Anderson R. 0. 1983

Neog.-Quater.

Evolut. Taxon. Skelet. Strat. Oceano.

Lazarua D. B. e/a/ 1985

Biol. Cytol.

Anderson R. O 1984

Evolut.

Lazarus D. B. étal. 1982

Czc Quater.

Biol. Physiol, Cytol.

Anderson R. 0. i985b

Evolut. Taxon. Biol. Biogeog.

Baker C. W. & Johnson D. A. 1982

Biol. Evolut.

Anderson R. 0.1985a

Quater.

Biol. Skelet.

Anderson R. 0 1981

Czc-Quater.

Biol. Physiol.

LecherF 1978

Biol. Cytol.

Anderson R 0 1976a

Quater.

Ecol. Biol.

Anderson R. 0. étal. 1985

Recent Quater.

Biol. Skelet. Cytol.

Anderson R. 0 Â Botfield M. 1983

Skelet, Biol,

Anderson R. 0. & Swanberg N. R. 1981

Quater.

Biol. Cytol.

Anderson R O. e/a/. 1983

Quater.

Biol. Skelet.

Anderson R O. S Bennett P, 1985

Quater.

Biol.

Anderson R. 0. e/a/. 1984

Quater.

Skelet. Evolut.

Bjorkiund K. R. & Goll R. M. 1979b

Quater.

Biol.

Anderson R. 0. e/a/. 1986a

Quater.

Sedim.

Anderson R. O. l9B6b

Biol. Ecol. Physiol.

Anderson R, O, étal. 1989b

Czc

DSDP31

üngH, Y. 1975

Czc

DSDP40

Pisias N G. & Moore T.C. Jr 1978

Quater.

Biol. Taxon Skelet.

Pelrushevskaya M. 0. étal. 1976

434

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

LOCATION AGE

TOPIC

AUTHOR

Taxon. DSDP14

Petrushevskaya M. G. & Koziova G. E. 1972

Taxon. Strat.

Riedel W. R. & Sanfilippo A. 1977

Czc

Taxon. Strat Evolut.

Riedel W R. S Sanfilippo A. 1978a

Eoc.'OIigoc.

Geochron.

Riedel W. R. Sanfilippo A. 1986

Recent

Phaeodar. Preserv.

Runeva 1. P. & Resheinyak V. V. 1979a. b

Taxon. Strat. Evolut.

Riedel W R. 1 Sanfilippo A. 1982

Taxon. Strat. Evolut. Skelet.

Riedel W, R. & Sanfilippo A. 1981

Recent

Plankt. Sedim. Environ.

Riedel W- R SSaitoT 1979

Czc

Skelet. Taxon. Ontog. Phylo.

Petrushevskaya M. Q. 1987

Pzc Mzc Czc

Taxon. Skelet.

Petrushevskaya M. G. 1986

Czc

Strat. DSDP

Oison R. K. SGollR. M. 1970

Czc Ouater.

Skelet.

Nishimura A 1982

Mioc.-Quater.

Bibliog.

Nigrini C A. & Moore T. C. 1979

Mioc.

Taxon.

Nakaseko K. étal 1983

Biol. Taxon. Plankt.

Page F 1984

Taxon. Skelet

Petrushevskaya M. G. 1975b

Pzc Mzc Czc

Taxon. Evolut. Skelet.

Petrushevskaya M- G. 1981a

Taxon. Skelet,

Petrushevskaya M. G. 1975a

Ouater.

Taxon. Paleogeog. Plankt.

Petrushevskaya M- G. 1972b

Ouater.

Taxon. Plankt.

Petrushevskaya M. G. 1972a

Recent

Sedim

Takahashi K, & Ling H Y. 1984

Recent

Sedim. Preserv

Takahashi K. 1984

Recent

Preserv Sedim.

Takahashi K. 1983

Paleog. Geogr.

Worsiey T. R. S Jorgens M. L. 1974

Mzc Czc

Techn.

Yogo S. 1982

Recent

Biol

Swanberg N. R. et ai 1986a, b, c

Recent

Biol. Skelet. Taxon. N.Sp.

Swanberg N. R. et ai 1985

Neog.

Taxon. Strat. Zones

Sanfilippo A. et ai 1985b

Taxon. Skelet.

Schaal A. 1981

Neog.

Taxon.

Sanfilippo A, & Riedel W. R. 1980

Neog.

Taxon. Strat.

Sanfilippo A Riedel W. R. 1970

Neog.

Taxon. Strat.

Sanfilippo A. 1980

General

Shrock R R. & Twenhofel W. H. 1979

Recent

Biol.

Swanberg N. R. & Anderson R. 0. 1985

Czc Recent

Biol.

Swanbeig N. R. 1984

Czc

Biol. Environ.

Swanberg N. R. 1983

Mzc Czc

Environ. Ecol. Geogr. Current

Spaw J. M. et ai 1979

Czc

DSDP27

RenzG W, 1974

Oligoc.-Mioc.

Evolut.

Moore T. C. 1972

Czc

Strat. Taxon. DSDP8

Moore T. C. 1971

Czc Mzc PZ

General

Lipman R. Kh, étal. 1979

Paleogene Mzc

Strat.

Lipman R, Kh. 1979b

Czc Mzc

Evolut. Taxon.

Lipman R Kh. 1975c

Czc Mzc PZ

General Taxon. Evolut.

Lipman R. Kh. 1979a

Czc-Qualer

Biogeog. Ecol. Climat.

Morley J. J. 1980

Czc Ouater,

Biogeog. Plankt.

Mast H. 1910

Czc Ouater.

Plankt. Evolut. Taxon.

MerinfeldE. G. 1978

Eoc.

Taxon. Strat.

MatoC- Y-&TheyefF-1980

Cret.-Czc

Taxon. Strat. DSDP10

Foreman H. P. 1973

Cret.-Czc

Taxon. Evolut.

Dumitrica P. 1985

Czc

General Taxon.

Foreman H. P. & Riedel W. R. 1972

Czc Mzc?

Levykina I. E. 1984

GEODIVERSITAS • 1997 • 19(2)

435

De Wever P. & Popova 1. M.

LOCATION

AGE

TOPIC

AUTHOR

Czc? Mzc?

Plankt.

Meyen F. J. F. 1961

Paleog.-Ouater.

Taxon. Strat.

Sanhlippo A & Riedel W. R. 1982

Pzc Mzc Czc

Taxon.

RiedelW. R. 1967a

Pzc Mzc Czc

Taxon.

Riedel W, R. 1967b

Ouater.

Skelet. Preserv.Struct

Strat. Taxon. DSDP17

Bjorkiund K. R iü Goll R, M. 1985a. b

MoofeT C 1973a

Allant.

Taxon, Strat. DSDP1

Riedel W, R- 5 Sanfilippo A. 1970

Amer.C. Allant.W. Carib.

Taxon. Strat. DSDP15

Riedel W. R. à Sanfilippo A. 1973

Amer.C. Barbados Les Antilles

Paleoc.-Mid.Miocene

Bi|u Duval B- efa/. 1985

Amer.C. Carib.

Czc

Taxon.

RiedelW. R, â Hays J. D 1969

Amer.C. Carib.

Eoc. Oligoc.

Strat. Tektite Extinc.

Maurrasse F & Glass B. P. 1976

Amer.C. Carib.

Czc

Paleog. Ecol. Climat. Sedim.

Manrrasse F. 1976

Amer.C. Carib. Médit. Pacif.

Paleoc.-Neog.

Taxon. Strat. DSDP10

Santuippo A, & Riedel W. R. 1973

Amer.C. Carib. Cuba

Czc

Albin E-F, 1986

Amer.C. Carib. Cuba La Habana

Paleoc.-Eoc.

Albin E.-F. Fernandez G. 1985

Amer.C. Costa Rica

L.Miocene

DSDP 69

Hein J. R et al 19a3b

Amer.C. W.Costa Rica.

Crel.-Paleog.

Sedim.

Hein J. R,e/â/. 19e3a

Amer.C. Barbados

L-Eoc.-E-Olig.

EvoluL DSDP 77B 289

Sanfilippo A 1988

Amer.C Barbados Atlant.W. Carib.

Eoc.

Evolut.

Sanfilippo A-et a/ i985a

Amer.N.

Eoc.-Oligoc.

Extlnct. Evolut. Biozon.

GlasfiB, P, et ai. 1978

Amer.N.

Eoc.-Oligoc.

Tektite Evolut Extinct.

GlaasB P & Crosbie J, R. 1982

Amer.N. Alabama Mississippi

Eoc.

Taxon, Strat.

Cunningham K, M ^ 895

Amer.N Asia Auslralia Africa

Eoc.

Extincl. Evolut. Tektite

GlassB P, Blâl 1979

Amer.N, C.Calil.

Eoc.

Taxon. Strat. Environ.

Siusfofd J- R-1988

Amer.N. Caüf.

L.Eoc.

Taxon. N.Sp.

Clark e. L. 8 Campbell A. S. 1942

Amer.N. Calîf.

Eoc.

Taxon. N.Sp.

Clark B L, S Campbell A. S. 1945

Amer.N. Calif.

Czc

Sedim.

Conrad C S Ehlig P. L. 1983

Amer.N. Calif.

Czc Mzc?

Sedim.

HIndeG. J. 1894

Amer.N, Calif.

Mioc.

Taxon. N.Sp.

Campbell À. S. & Clark B. L. 1944

Amer.N. Calif.

Recent

Current Climat. Biogeog. Environ.

Boltovskoy D. â Riedel W. R. 1985

Amer.N. Calif.

Biogeog. Ecol.

KlingS. A 1977

Amer.N. Calif.

Recent

Current Climat. Environ.

BottovsKoy D â Riedel W. R, 1987

Amer.N. Calif.

Czc Mioc.

Strat.

Poore R Z. er al. 1981

Amer.N. Calif.

M.Mioc.

Strat.

Price A. B 1975

Amer.N, Caiil. Anlar C

Neogene

Strat. Climat. Environ. Ecol.

Casey R, E, 1972

Amer.N. Caiil Barbados

Paleog.

SaondersJ- Q-etal 1984

Amer.N. Calif. Francise.

Czc

Taxon.

Riedel W. R & Schlocker J. 1956

Amer.N. Caiil. Pacif.

Ouater.

Strat. Taxon.

Benson R N. 1966

Amer.N. Calif. Monterey

Mioc.

Strat.

Price A. 0 1975

Amer.N. CaJil, Monterey Baja

Mioc.-Plioc,

Strat- Environ-

Weaver F- M. étal -1981

Amer.N. Carib. Allant Mexico

Extinct Tektite Evolut.

GlassB P S Zviiart M. J. 1979

Amer.N.

Eoc.-Oligoc.

Evolut. Extinct.

Glass B, P & Zwarl M. J. 1977

Amer.N. Maryl.

Mioc.

Taxon.

Martin G. C, 1904

Amer.N. N.Calif.

Eoc.

Strat.

Blueford J. R. & Brunner Ch. 1984

Amer.N. S.Calif. Pacif.

Neog.

Ecol- Environ.

Casey R E-e^3M972

Amer.N. SE.Missouri

Paleoc.-Eoc.

Taxon.

Frlzzell D. L. S Middour E. S, 1951

Amer.N. USA

Neog,

Palmer A, 1984

Amer.N, W.C.Calif.

Eoc.

Environ. Oceano.

Blueford J- R. & White L D. 1984

Amer.S. Chile Tripoli

Taxon. N.Sp. Strat.

Frenguelli J. 1941

Amer.S. S.Brasil

Ouater.

Kotzian S. C. B. 1964

Amer.S. Peru Pisco-F^

Mioc.

Sedim.

MertzD, 1966

Antar.

Czc-Quater.

Climat. Environ, N.Sp.

HaysJ, D. 1965

436

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

LOCATION

AGE

TOPIC

AUTHOR

Antar.

Ouater.

Sedim.

HaysJ. D. 1967

Antar.

Plioc-Quater.

Climat.

Keany J. & KennettJ. P. 1972

Antar.

Cenozoic

Strat. Biogeog.

Kennet! J, P. 1976

Antar.

Ouater.

Environ.

KennettJ, P, 1979

Antar.

Plioc.

Taxon. Strat.

KeanyJ.1979

Antar.

Neog.

Taxon.

Coco B- C 1982

Antar.

Mioc.-Quater.

Strat.

Nakaseko K. 1959a

Antar.

Mioc.-Ouater.

Strat.

Nakaseko K. & Nishimura A. 1982

Antar.

Czc Ouater

Plankt.

SchroaerO 1906

Antar.

Czc

Taxon. Phaeodar.

Popofsky A. 1908

Antar.

Ouater.

Taxon. Climat.

RiedeiW- R 1958

Antar.

Czc-Recent

Popotsky A. 1917

Antar.

Czc-Recent

Ecol.

Popofsky A. 1913

Antar.

Czc-Ûuater.

Taxon. Plankt.

Petrushevskaya M, G. 1967

Antar.

Czc

Taxon.

Popolsky A. 1912

Antar. Arct. Polar.

Czc-Recent

Climat Ecol

Popofsky A. 1920

Antar Atlantic

Plio-Pteist.

Neog. Ouater.

Strat. Antar.

Abelmann A & Gersonde R. 1988

Antar, Pactf.S.

Ouater.

Taxon. Plankt.

Petrushevskaya M. G. 1979b

Antar. SE.Indien Oc.

Ouater.(L.PIeisI.)

Environ. Biogeog.

Dow R L 1978

Antar.lndian Oc.

Ouater.

Taxon. Skelet.

Petrushevskaya M G. 1975c

Antar.S.

Ouater.

Taxon

Boltovskoy D & Vrba A 1988

Antarct.

Ouater.

Taxon. PianHt.

Petrushevskaya M. G. 1974

Antarctic

Ouater.

Earîh Rotation Cyclicity

HaysJ-D e/an976

Antarctic

Ouater,

Climat. Extinct.

Hays J. D. & Donahue J. G. 1972

Antarctic

Biosiral DSDP

ChenP H 1975

Antarctic

Oligoc.-Neog.

Taxon Slral. DSDP

Chef! P H. 1974

Antarctic

Ouater.

Climat Biozon.

HaysJ. D. ÂOpdykeN. D. 1967

Arctic

Ouater.

Taxon. N.Sp.

Hulsemann K 1963

Arctic Pacif.? Boréal

Paleog.-Recent

KozIovaQ. E. 1984a

Asia Australie

Czc? Mzc?

Sedim.

KobayashiT 1944

Asta Centr.Japan

Miocene

Taxon.

Tanaka H. étal. 1983

AsIa China

Taxon. N.Sp.

Xinghui S. 1982

Asia China

Czc

Biol.

Xinghui S. & Zhlyuan T. 1985

Asia China

Mzc Czc

Taxon. Skelet. Evolut.

Tan Z, Y. Su S-H, 1981

Asia China Gyangze Xizang

Plankt.

WangYuling & Sheng Jinzhang 1982

Asia China Himalaya Tibet Xizang

Czc

Wu Hao-ruo 1980

Asia China Sea E.

Czc Ouater.

Environ Taxon.

ChenWenbin-Wang Baoyong 1982

Asia China Xisha Islands

Czc

Taxon, Skelet.

Zhiyuan T. & Xinghui S. 1981

Asia E.China Sea

Czc

TanZh. SuX. 1982

Asia E.China Sea

Strat. Geogr.

Zhiyuan T- et al. 1978

Asia E.China Sea

Czc

Strat.

Zhiyuan T. & Tsorun T. 1976

Asia Eurooe ex-Ussr pre-Causasus

Paleoc.-Eoc.

Lipman R. Kh. 1984b

Asia ex-Ussr N.Sakhalin

Neog.

RunevaN. P 1984

Asia Himalaya Tibet LadaKh

Eoc.

Strat.

Colchen M. étal 1987

Asia Indones. S.China Sea

Czc Ouater.

LingH. Y. 1972

Asia Japan

Czc

Biozon. Strat.

Kitazato H. 1975

Asia Japan

Czc Mzc Pzc

General

Kimura T. 1944

Asia Japan

Czc Mzc

Kobayashi T. & Kimura T. 1944

Asia Japan

Czc Mzc

Strat.

Ichikawa K. 1946

Asia Japan

Czc Mzc

Ichikawa K. 1953

Asia Japan

Neogene

Sugano K. & Nakaseko K. 1971

GEODIVERSITAS • 1997 • 19(2)

437

De Wever P. & Popova I. M.

LOCATION

AGE

TOPIC

AUTHOR

Asia Japan

Neogene

Sugano K. & Nakaseko K. 1970

Asia Japan

Mioc.-Quater.

Sîrat.

Nakaseko K. 1956

A$iâ Japan

Neogene

Sugano K. & Nakaseko K. 1973

Asia Japan

Neogene

Sugano K. S Nakaseko K. 1972

Asia Japan

Mzc? Czc?

Sedim.

Sugano K. 1986

Asia Japan

Mioc.

Strat.

Nakaseko K. 1954

Asia Japan

Mzc Czc

Review

Sugano K. 1975

Asia Japan

Czc

UngH. Y. a Kurthara K. 1972

Asia Japan

Mioc.

Strat.

Nakaseko K. 1955

Asia Japan

Neog.

Sugarro K. & Nakaseko K. 1968

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K. 1953

Asia Japan

Mioc.

Strat.

Nakaseko K. & Nishimura A. 1974

Asia Japan

Neogene

Strat.

Nakaseko K. & Sugano K. 1973

Asia Japan

Neogene

Strat.

Nakaseko K. e( ai 1972 a, b

Asia Japan

Geol. Strat.

Nakaseko K. étal. 1979a

Asia Japan

Czc

Strat.

Nakaseko K. étal. 1979b

Asia Japan

Czc

Takayanagi V, étal. 1978

Asia Japan

Mioc.

Taxon. Strat.

Nakaseko K. étal 1982

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K, Sugano K. 1972

Asia Japan

Czc

Strat.

Nakaseko K. 1979

Asia Japan

Neogene

Sugano K & Nakaseko K. 1975

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K. & Chiji M. 1964

Asia Japan

Cret.-Czc

Strat.

Nakaseko K. étal. 1965

Asia Japan

Neogene

Taxon.

Nakaseko K. & Nishimura A. 1971

Asia Japan

Strat.

Nakaseko K. & Sugano K. 1970

Asia Japan

Plioc.-Quater.

Strat.

Nakaseko K. 1964

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K. 1971 a. b

Asia Japan

Plioc.-Quater.

Nishimura A. & Yamauchi M. 1984

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K T959b

Asia Japan

Okada H. et a/. 1982

Asia Japan

Czc

Sugano K. étal. 1980

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K. 1969

Asia Japan

Neog. Ouater.

Sugano K, & Nagata K. 1978

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K. 1963

Asia Japan

Mioc.-Quater.

Strat.

Nakaseko K 1960

Asia Japan

Mioc.

Strat.

Takayanagi y. et ai 1976

Asia Japan C.Pacif. Amer.N. Calif.

MIoc.-Plioc.

Strat.

Nagata K. 1982b

Asia Japan

Czc

Skelet.

Nishimura H. 1986

Asia Japan E.Hokkaido

Biostrat. Preserv. Diagen.

Nagata K. 1986

Asia Japan Equat.Pacif.

Strat. Plankt.

Takayanagi Y. et ai 1979 a. b

Asia Japan Hokkakjo

Mioc.

Strat.

Nagata K. & Ichinoseki T. 1982

Asia Japan Hokkaido

Mioc.-Quater.

Strat.

Nagalâ K. 1979

Asia Japan Honshu

Mioc.

Biozon.

Oda M efa/ 1983

Asia Japan Honshu

Czc

Strat.

llpmaA- e/a/. 1981

Asia Japan NE.Honshu

Strat.

Amano K. 1980

Asia Japan Pacif.

DSDP56 Strat.

Barron J. A. état. 1980

Asia Japan Sendai

Czc?

OdaM, SSakaiT 1977

Asia Japan Shimanto

Czc

Taxon.

IshikawaT. 1982

Asia Japan W.Hokkaido

Strat.

Nagata K. 1982d

Asia Japan

Oligoc.-Neog.

LingH Y. 1987

Asia Japan.C.

Neog.

Sugano K. 1982a

Asia Japan.C.

History Review

Sugano K. 1982b

438

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

LOCATION

AGE

TOPIC

AUTHOR

Asia Japan.C.

Mioc.

Sugano K. 1976

Asia Japan.SW.

Czc Mzc

Ishida S. 1979

Asia Japan.SW. Shikoku

YamasakI T. 1987

Asia Japan.SW. Maizuru Qr.

Biostrat.

Nishimura K, & Ishiga H. 1987

Asia Pacif.

SakaiT e/a/. 1981

Asia Pacif. Celebes Indones.

Hinde G. J. 1917

Asia SE.Middie Tadzhikistan

Paleog. Eoc.

ChediyaD. M. e/a/. 1971

Allant Norway

Ouater.

Skelet. Taxon.

BjorkIundK. R 1974a

Atlant.

Mzc?

Taxon.

Ehrenberg C. G. 1854

Allant.

Ouater.

Sedim.

Cauiei J. P. & Cloccialli M. 1975

Atlant.

Ouater.

Environ. Biogeog.

Bjorkiund K. R, & Swanberg N. R. 1987

Atlant.

Ouater.

Kozlova G. E. 1980

Atlant.

Recent

Biol.

Kleijne A. 1907

Atlant.

Cret-Ouater.

Strat. DSDP2

Cita M.B. efa/.19ro

Atlant.

Czc

Biogeog.

Casey R- E. & McMillen K. J. 1977

Allant.

Ouater.

Strat. Climat-

Morley J, J, & Shackieton N. J. 1978

Atlant. Açores

Czc-Recent

Plankt.

Muzavor S. N X, 1981

Allant. Amer.C. Carib.

Ouater.

Environ Biogeog.

Casey R E. 1971a

Atlant. Amer.C. Carib.

Recent

Biol.

Swanberg N. R, ûtal 1986 a, b, c

Atlant. Amer.C. Carib. Guif Mexico

Ouater.

Ecol. Biogeog.

Casey R. E. Qtal 1979a

Allant. Amer.C. Carib Gulf-Coasl

Ouater.

Environ. Ecol. Current Plankt.

Casey R. E. eial. 1961

Atlant. Amer.C Carib. S.Texas

Ouater.

Ecol Énvifor> Current

Leavesley A et al. 1976

Allant. Boréal Norway

Ouater.

Current Biogeog. Sedim.

Jansen E. fit Bjerktund K. R. 1985

Atlant. Boréal Nonway

Strat. DSDP38

Dzinoridze R. N.elal- 1976

Allant. Boréal Norway Greenland

Neog.-Ouater.

Evolul. Strat.

Goll R, M. & Bjorkiund K. R. 1980

Atlant. Boréal Norway Groenland

Taxon. N.Sp.

Goll R. M- & Bjorkiund K. R. 1985

Atlant. Carib.

Ouater.

Environ. Ecol.

Casey R E. 1971b

Allant. Carib. Barbados

Ehrenberg C. G 1846

Atlant. Carib. Blake Bahama

Czc

DSDP44

Weaver F M. & Oinkelinan M. G. 1978

Allant. Europe

Czc Mzc

Swain F- M. 1977

Atlant. Rochall Plateau

Mioc.

DSDP81 Strat.

Weatbarg-Smith M, J & Riedel W. R. 1984

Atlant. S.Brasil

Czc

KoizianS. B, 8 Eilerl V. P. 1985

Allant W.Norway

Czc Ouater.

Sedim.

BjorkIundK. R, 1973

Allant Antar.

Neog.

Biostrat.

Abeimann A, 1988

Atlant.E Angola

Ouater.

Biogeog. Environ.

BjorKIund K. H & Jansen J. H. F. 1984

Atlant.E. Morocco

Mioc.

DSDP5D Strat

Westberg M. J. étal, ’Ô80

Atlant.E- NW.Africa

Ouater.

Biogeog. Ecol

Labracherie M. 1900a

Atlant.E. NW.Africa

Ouater.

Current

Labracherie M. 1980b

Atlant.E.Tropic.

DSDP41 Strat Taxon.

Johnson P-A-1978

AUanl.N Borea! Norway

Ouater.

Biol. Skelet. Plankt.

Swanberg N R. & Bjorkiund K. R. 1987b

Atlant.N, Boréal Norway

Recen!

Plankt Ecol- Environ.

Swanberg N R & Bjorkiund K. R. 1986

Allant.N. Boréal Norway

Ouater.

Biol. Plankt. Ecol.

Swanberg N. R. S B/ofklund K. R. 1987a

Atlant.N.

Ouater. Recent

Biogeog.

Kloijne A. 1984

Atlant.N.

Ouater.

N.Sp, Biogeog Skelet.

Bjorkiund K R. 1976a

Atlant.N.

Ouater.

Biogeog Sedim

Goll R. M. & Bjorkiund K. R. 1971

Atlant N.

Strat. Taxon.

Riedel W R. 1957a

Atlant.N.

Czc

DSDP94

Westberg-Smith M, J. étal. 1986

Atlant.N.

Czc-Ouater.

Taxon. Plankt. Skelet.

Pelfushevskaya M. G. 1969

Atlant.N. Aniar. Pacif.N.

Neog.

Lonbari G. & Lazarus D. B. 1988

Atlant.N. Boréal Norvegian Sea

Strat.

Bjorkiund K. R- 1976b

Atlant.N. Boréal Norway

Ouater.

Jôrgensen E. 1900

Atlant.N. Boréal Norway

DSDP Taxon.

Petrushevskaya M. G. & Kozlova G. E. 1979

GEODIVERSITAS • 1997 • 19(2}

439

De Wever P. & Popova I. M.

LOCATION

AGE

TOPIC

AUTHOR

Atlant.N. Boréal Norweg.-Greenland

Ouater.

Taxon.

Petrushevskaya M. G. & Bjorkiund K. R. 1974

Atlant.N. Boréal Norwegian Sea

Ouater.

Climat. Environ.

Bjorkiund K.R. état. 1979

Atlant.N. Boréal Norwegian Sea

DSDP38

Jouse A. P, étal. 1979

Atlant.N. Boréal Norwc^gian Sea

Eoc.

Taxon. N.Sp.

Bjorkiund K. R S Kellogg D. E. 1972

Atlant.N. Boréal Norweg.-Greenl. Sea

Ouater.

Climat. Environ.

Bjorkiund K- R.&GollR, M. 1979a

Atlant.N. N.Sea

Recent

Slral.

Bjorkiund K R, 19B5

Atlant.N. N.Sea (Skagerrak)

Ouater.

Environ. Sedim.

Bjorkiund K- R, étal. 1985

Atlant.N. N Sea (SkagerraK)

Ouater.

Strat.

Bjorkiund K. R. 1985

Atlant.N. N.Sea

Ouater.

Strat. Biogeog

Bjorkiund K. R 1983

Atlant.N. Norwegian-Greenland

Ouater

Evolut.

KozIovaG. E S Petrushevskaya M. G. 1979

Atlant N. Reykjanes Ridge

Czc

Slral. Taxon. DSDP49

LIng H, Y. 1979

Atlant.N. W.Norway Biogeog.

Recent

Season product. Climat.

Bjorkiund K. R, 1974b

AtlantNE,

Ouater.

Curreni

Labracherie M. A Moyes J. 1978

Atlant.NE.

Neog.

Taxon. Strat. DSDP48

Santilippo A. & Riedel W. R. 1979

Atlant.NE. Méditer.

Cret.'Quater.

DSDP13 Taxon. Strat.

Dijmitrica P 1973a

Atlant.NE. S.Norwegian Sea

Ouater.

Biogeog. Ecol.

Labracherie M. 1978

Atlant.NW.

Czc

DSDP 93

Nishimura A. 1987

Atlant.S.

Environ. Ecol

BoltovsKoy D. î980

Atlant.S.

Ouater.

Sedim. Biogeog,

Goll R. M. & Bjorkiund K. R. 1974

Atlant.S.

Czc-Quater.

Biogeog Ecxil. Climat.

MorleyJ i, 1979

Atlant.S- Antar. S.W.Indian. Oc.

Biogeog Current Sedim. Environ.

Lozano J. A. A Hays J. D. 1976

AtlantSW.

Biogeog.

BoltovsKoy D. 1981a, b

Atlant.SW.

Ouater.

Receni Biogeog.

Boltovskay D. 1978a, b

Atlant.SW.

Ouater.

BoltovsKoy D S Riedel W. R. 1980

Atlant.SW.

Recent

Plankt. Biogeog.

BoltovsKoy D. 1982

Atlant.SW.

Recent

Biogeog. Current Environ.

SüllovskQy 0. 1986

Atlant.SW. Antar.

Ouater.

EilenV. P-1985

AtIant.SW.

Receni

Plankt. Biogeog.

Boltovskoy D. 197Ô

Atlant.W Carib. Amer.C Barbados

Eoc.

Evolut.

Santilippo A. étal. I985a. b

Atlant.W. Amer.C. Carib. Mexic.

Ouater.

Ecol. Biogeog, Sedim. Plankt.

McMillen K. J. S Casey R. E. 1978

Atlant.W. Amer.C. Carib. Mexico

Ouater.

Ecol. Biogeog, Preserv.

McMitlen K. J. 1977a

Atlant.W. Amer.C. Carib. Mexico

Ouater.

Ecol. Biogeog Preserv. DSDP66

McMillen K. J. 1982

Atlant.W. Amer.C Carib. Mexico

Czc Ouater

Ecol Biogeog, Presenr.

McMillen K. J- 1977b

Atlant.W. Barbados Antilles

Czc

DSDP

RenzG, W 1984

Atlant.W, Carib.

Neog.

Taxon. Strat.

Santilippo A- 8 Riedel W. R. 1976

Atlant.W. Carib. Guif Mexico

PliO'Quater.

Plankt. Taxon. Environ.

Casey R. E. étal. 1979c

Atlant.W. GuIf Mexico

Ouater.

Ecol- Sedim.

Casey R E. e! al. 1979b

Atlant.W. Guif Mexico Carib. Calif.

Czc Ouater.

Strat. Environ. Plankt. Ecol.

WigleyC. R, 1982

Allant.W. Guif Siream

Receni

Biol.

SwanbergN. R. & Anderson R. 0.1981

Atlant. W.Tropic.

Ouater.

Flux Sedim. Current Preserv. Skelet.

Takahashi K & Honjo S- 1983

Atlant. W.Tropic.

Ouater.

Flux Sedim. Current Preserv.

Takahashi K. & Hon|o S. 1981 a. b

Atlantic

Recent

Ecol. Biol.

Swanberg N. R; & Harbison G. R. 1980

Atlantic

Czc-Quater.

Strat.

MorleyJ. J. 8 Shackleton N. J. 1978

Atlantic

Czc

Taxon DSDP

Riedel W R_ l971a

Atlantic Antar.

Plio-Pleist. Neog.

Strat. Antar.

Abelmann A. & Gersonde R, 1988

Atlantic.S.

Ouater.

Biogeog. Ecol. Climat.

Moriey J J, & Hays J. D. 1979a

Banda

Taxon. N.Sp. Sedim.

Harting P. 1863

Calif. El Nino

Ouater.

Climat. Current Environ. Ecol.

Casey R. B. étal. *987

Eurasia ex-Ussr

Paleog.

Boréal Strat.

üpman R. Kh. 1985

Europe Austria

Mioc.

Taxon.

Bachmann A, ét al. 1963

Europe Belgium leper

Eoc.

Willems W. 1981

Europe Carpathian Roland

Mioc.

Barwicz-Piskorz W. 1978

440

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolarîa from European Platform

LOCATION

AGE

TOPIC

AUTHOR

Europe France (Paris Bas.) Belgium

Czc

Sedim. Petro.

Cayeux L. 1897

Europe Italy Calabria

Plio-Quater.

Tripoli Strat. Sedim.

Guerrera F. 1881

Europe Italy Calabria

Plioc.

Sanfilippo A. 1988

Europe Italy SIcily Tripoli

Mioc.

Stohr E. 1880

Europe Italy Sicily Zancle

Plioc.

Taxon Strat.

RiedelW, R. ef al 1974

Europe Médit.

Ouater.

Preserv. Sedim. Taxon.

Caulet J. P. 1972

Europe Médit.

Recent

Plankt Climat Season Ecol.

Massera Bottazzt E. & Andreoli M. G. 1977 a, b

Europe Médit.

Czc Recent

Biogeog. Current Environ.

Massera BottazzI E. étal. 1986

Europe Médit.

Czc Recent

Plankt Environ. Ecol.

Massera Bottazzi E. el al. 1984

Europe Médit. Tirreno

Ouater.

Taxon.

Poluzzi A. 1982

Europe N.France

Eoc.

Sedim.

Cayeux L, 1891

Europe.E. Brno-Kralovo

Mioc.

Taxon

Slama P. 1982

exUssr

Czc

Goltman E, V. 1970

ex-Ussr

Eoc.

Taxon. N.Sp.

Lipman R Kh, 1969

ex-Ussr

Paleogene Czc

Eoc.

Lipman R. Kh. 1972

ex-Ussr

Eoc.

Biozon.

Zagoradnyuk V 1.1981

ex-Ussr

Paleogene

Strat.

Lipman R, Kh, 1975b

ex-Ussr Crlmea Minor Asia

Ecol.

TchedyaD M. 1981

ex-Ussr Don River N.Emba

L.Eoc.

Strat.

ZagorodnyuK V 1.1969

ex-Ussr General

Czc Mzc Pzc

Lipman R. Kh. 1976

ex-Ussr Kamtchatka

Runeva N P 1975

ex-Ussr Kamtchatka

Taxon. N.Sp.

Balley J. W. 1856

ex-Ussr Kuban

Paleoc,-Eoc.

Taxon. N.Sp.

BonsenkoN. N. 1960a

ex-Ussr Kuban

Eoc.

Taxon.

BorisenkoN N. IQBOb

ex-Ussr Mid Asia.

Czc Mzc

TsdhôdiaD. M. 1984

ex-Ussr N.Sakhalin

Mioc.

Koztova G, E, 1960

ex-Ussr NE.Azherbaidjan

Eoc.

Strat. Evolut.

Mamedov N A. 1975

ex-Ussr Pacif.

Ouater.

StreIkovA- A S Reschetnyak V. V. 1971

ex-Ussr Paleoc. W.Kuban

Eoc.

Taxon. N.Sp.

Borlsenko N. N. 1958

ex-Ussr Pre-Aral

Eoc,

Taxon. N.Sp

Lipman R. Kh. 1975a

ex-Ussr Pre-carpath.

Mioc.

Runeva N. P, 1969

ex-Ussr Pricaspian

Czc Eoc.

Strat.

Zagorodnyuk V. 1.1975

ex-Ussr Priscaspia.

Eoc.

Strat.

Nikitma 1- P. & Zagorodnyuk V. 1.1981

ex-Ussr S.Sakalina W.Kamlchatka.

Mzc?

Runeva N. P. 1981

ex-Ussr Sakhalin

Neog.

N.Sp. Biostrat.

Popova 1. M-1988

ex-Ussr Shemakh.-Kobyst. Azerbaid.

Eoc.

Strat.

Mamedov N. A. 1973a

ex-Ussr Siberia

Czc Mzc

Lipman R. Kh. 1960

ex-Ussr Sikhote-Alinj

EliseevaV. K. et a/. 1976

ex-Ussr Tadjiksk,

Czc

Strat.

Goltman E. V. 1981a

ex-Ussr Tadzhiksk

Maastr.-Ouater.

Goltman E. V. 1973

ex-Ussr Tadzhikski

Czc

Goltman E. V. 1971

ex-Ussr Tadzhikskoi

Strat.

Goltman E- V-1975

ex-Ussr Tadzhikskoi

Ouater.

Strat.

Goltman E, V. 1981D

ex-Ussr Turgay Pre-Aral.

Biogeog.

Lipman R. Kh. & Kbokhlova A. 1.1964

ex-Ussr Turkmen.

Czc? Mzc?

Strat.

MoksyakovaA- M- 1965

ex-Ussr Turkmen.

L.Eocene

Strat.

MoksyakovaA. M. 1969

ex-Ussr Ukrain. Carpath.

Paleog.

Lozynyak P. Yu. 1985

ex-Ussr Urals

Skelet.

Amon E. fi Kovallchuk A. 1.1988

ex-Ussf W Pre-Caucasus

Eoc.

Krasheninnikov V, A. i960

ex-Ussr W.Siberian

L.Eoc.

Taxon. N.Sp.

GortrovelzA. N. 1972

ex-Ussr W.Siberian

Paleog.-Recent

Biogeog.

Gorbovelz A. N. et al. 1972

ex-Ussr W.Siberian

L.Eocene

KozlovaG. E. & Gorbovets A. N. 1966

GEODIVERSITAS • 1997 • 19(2}

441

De Wever P. & Popova I. M.

LOCATION

AGE

TOPIC

AUTHOR

ex-Ussr W.Turkmen.

L.Eocene

MoKsyakovaA. M. 1961

ex-USSR Crimea Tadzhiksk

Paleog. Eoc.

Chediya D. M. & Chediya 1. O. 1973

ex-USSR N.Kamtchatka Bering S.

Paleog.

Averina G. Y. 1988

Faroe Channel

Ouater.

Taxon.

Haeckel E. 1882

General

Ouater.

Taxon.

Haeckel E. 1862

General

Czc-Quater.

Biol. Skelet.

Haeckel E. 1866

General

Mzc Czc

Taxon. Skelet.

Petrushevskaya M G. 1979a

General

Mzc Pzc

Taxon.

Petrushevskaya M. G. 1984

General

Czc Mzc?

ZhamoidaA. 1.1984-

General

Taxon.

RIedelW. R. 1971b

General

Mzc Czc Ouater.

Taxon.

Petrushevskaya M. G. 1975d

Global

Ouater.

Ecol. Environ. Biogeog.

Casey R, E. 1977

Global

Czc Ouater,

Biogeog. Ecol. Evolut.

Casey R. E. 1982

Global

Biogeog. Current Environ.

Casey R. E. sfa/, 1982

Indian

L.Eoc.

Taxon. Strat. Biogeog. Oc.

GollR, M.&CauIetJ. P. 1985

Indian Antarct.

Czc-Recent

Taxon. Planki.

Petrushevskaya M. G. 1971c

Indian E.Arabia Peru

Mioc.-Recent

ODP

CauM J, P- & Nigrini C. 1988

Indian Oc.

Neog.

Environ, Ecol, Season Current

CauletJ, P 1977

Indian Oc.

Pleistocene

Biosîr.

CauletJ, P-1986

Indian Oc.

Neog.

Sedim, Environ.

CaulelJ. P. 1973

Indian Oc.

Strat. Taxon, DSDP22

Johnson D. A.1974a

Indian Oc.

Sedim. Minerai. Mn

LeclaireL. et a/. 1976

Indian Oc.

Czc-Ouater.

Taxon Biogeog. Current Plankt.

Pelrushevskaya M, G. 1973

Indian Oc. Antar.

Ouater.

Taxon. Plankt.

Petrushevskaya M- G. 1977b

Indian Oc. Antar.

Taxon. Plankt.

Petrushevskaya M. G. 197la

Indian Oc. Antar.

Ouater.

Taxon, Planki.

Petrushevskaya M. G. 1977a

Indian Oc. Antarctic

Ouater.

Taxon. DSDP29

Petrushevskaya M. G. 1975c

Indian Oc. Atlant.

Plankt.

Nigrini C. A. 1967

Indian Oc. Indon. Burma Andama Isl.

Czc

Strat.

Jacob K. & Shrivaslava R. N. 1952

Indian Oc. Pacif.Tropical

Neog.

Evolut. Strat.

Caulet J. P. & Nigrini C. 1988

Indian Oc.C.

Plioc. Ouater.

Strat.

CauletJ. P. 1979

Indian Oc.E.

Ouater.

Strat. Biogeog.

Johnson D ,A, 8 Nigrini C. 1982

Indian Oc.S.

Paleoc.'Eocene

CauleiJ P 1988

Indian Oc.S.

Neog.

Skelet. Ecol. Environ. Climat.

Granlund A. H-1986

Indian Oc.S.

Ouater.

Climat- Strat-

CauletJ P 1982

Indian Oc.S.

Neog.

Skelet. Environ. Ecol. Climat.

Granlund A. H. 1984

Indian Oc.S.

Taxon. Strat, DSDP26

RIedelW. R. & SanMippo A. 1974b

Indian Pacif.

L.Neog.-Ouater.

N-Sp- Phylog.

Nigrini C. & CauletJ- P. 1988

Indian W.GuIf Aden

Taxon. Strat. DSDP24

RiedelW, fl. & Sanlilippo A. 1974a

Indian.S.

Paleoc.

Ecol. Climat.

Morley J J, 1989

Indian.W.

Neog.

Taxon. Strat. DSDP25

Sanlilippo A. & Riedel W. R. 1974b

Indian.W. GuIf Aden

Neog.

Taxon. Strat DSDP24

Sanlilippo A. & Riedel W. R. 1974a

Indian.W. Oc.

Ouater.

Biogeog.

Johnson D A 8 Nigrini C. 1980

Indian.W. Oc. Arabian Sea

Ouater.

Strat. Taxon.

Nigrini C. A 1974

Indian.W. Oc. E.Somaty Basin

Ouater.

Sedim.

CauletJ. P. étal. 1988

Indonesia

Czc? Mzc?

Strat, Taxon.

Tan Sin-Hok 1831

Médit.

Czc

Taxon N Sp

Haeckel E. 1861

Médit.

Czc

Taxon. N.Sp.

Haeckel E. 1860

Médit.

Czc-Quater.

Acanth.

Muller J. 1858

Médit.

Czc-Recent

Acanth.

Muller J 1856

Médit.

Neog.

Taxon. Strat.

Sanfilippo A. et al. 1973

Médit.

Neog.

Taxon. Strat- DSDP42A

SanfiHppo A, ei al. 1978

442

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

LOCATION

AGE

TOPIC

AUTHOR

Médit. Pacif.

Czc

Biogeog. Taxon.

CauletJ. P. 1971

Médit. Pacif. Amer.C. Carib. Guff Mex. Paleoc.-Neog.

Taxon. Strat. DSDP10

Sanfilippo A. & Riedel W. R. 1973

Médit. Pacif.W.

Neog.

Taxon. Strat.

SanfilippoA. 1971

Médit. Tethys

Taxon.

CauletJ. P. 1974

Middle*East Israël

Eoc.

Reiss Z. 1952

Pacif

Czc-Quater.

Sedim. Preserv.

Hurd J. D-1973

Pacif.

Ouater.

Preserv.

Hurd D. C. & Takahashi K. 1983

Pacif.

Czc

Strat DSDP55

Koizumi 1. étal. 1980

Pacif.

Czc-Quater,

Strat. Taxon. DSDP30

HoldsworthB K, 1975

Pacif.

Plioc.-Quater.

Evolul. Taxon.

Kellogg D. E.1976

Pacif.

Climat. Biozon

Hays J. D étal. 1972

Pacif.

Paleoc.Eoc.

Taxon. DSDP21 Strat.

Dumilrica P. 1973

Pacif.

Plio-Quater.

Strat. Climat.

Hays J. D, étal. 1969

Pacif.

Czc

Strat. Taxon.

Riedel W. R. & Funnell B. M. 1964

Pacif.

Mzc Czc

Strat- DSDP

Riedel W. R. 1981

Pacif.

Paleoc.-Eoc.

DSDP S.384

Nishimura A. 1986

Pacif.

Mioc.'Chjater.

Strat.

SailoT efaf-1975

Pacif.

DSDP56, 57

Reynolds R. A. état. 1930

Pacif.

Mioc.

DSDP Sirat,

Westberg M- J. & Riedel W. R. 1978

Pacif.

Czc-Quater.

Biogeog, Ecot Oimat.

Moore T. C. 1978

Pacif. Amer.C. Carib. Guif Mex. Médit. Paleoc.-Neog.

Taxon. Strat DSDP10

Sanfilippo A. & Riedel W. R. 1973

Pacif. Amer.N. Calif.

Ouater.

Strat. DSDP65

Benson R. N. 1983a

Pacif. Allant- Antar.

Plioc.

Strat. Climat.

Keany J. 1976

Pacif. Austraiia

Sedim. Environ.

Fenton M, W e/af. 1982

Pacif. Austraiia

Sedim.

HindeG, J, 1893

Pacif. Carib. Allant.

Taxon. Evolut.

Goll R. M. 1968

Pacif. Carib. Allant.

Taxon. Evolut.

Goll R. M. 1969a

Pacif. Equatorial

Strat.

Johnson D. A. & Parker F. L. 1972

Pacif. Equatorial

Ouater.

Biogeog. Climat

Johnson D. A. & Knoll A. H. 1974

Pacif. Indian Oc.

Paleog.

Environ.

Sancefta C. 1979

Pacif. Indones. Bangka

Czc Mzc

Sedim.

HindeG. J 1897

Pacif. Indones. Celebes

Padf. Indonesia Philippine Sea

Paleog.-Neog.

Biozon. DSDP59

Hojnos R. 1934

Theyer F. & üneberger P. 1981

Pacif. Mariana

Cret.-Czc-Quater.

Strat, DSDPeo

KlingS. A. 1982

Pacif. Okhotsk Sea

Biogeog.

KrugliKovaS B 1975

Pacif. Tahiti

Strat PlanM

Takayanagi V. et al. 1982

Pacif tropical

Czc

Strat. Taxon.

Frîend J.K. & Riedel W. R. 1967

Padf.C.

Sedim. Biogeog. Environ.

Leinen M. 1979

Padf.C.

Ouater.

Planki. Sedim. Ecol Biogeog. Preserv

. Renz G.W- 1976

Padf C. Equaior.

Mioc.

Strat.

BiuetordJ. R. 1962

Padf.C. Equatorial

Ouater.

Environ. Sedim.

BluelprdJ. R. 1980

Padf.C. Tropical

Ouater.

Taxon. N.Sp.

DeflandreG. 1972

Padf.Cent.

Ouater.

Taxon. Plankt

Petrushevskaya M. G. 1971b

Pacif-E.

Recent

Plankt. Oceano.

Boltovskoy D. & Jankllevich S. S. 1985

Padf-E.

Ouater.

Sedim.

Johnson D. A. 1974

Pacif.E.

Strat DSDP 16

Bukry D, étal. 1973

Pacif.E-

Plioc.-Quater.

Taxon. Siraf. DSDP54

Goll R. M. 1980

Pacif.E.

Ouater.

Environ. Current Strat.

Romine K. 8 Moore T. C. 1981

Pacif.E- Amer C. Carib.

Neog.

Taxon Sfrat. OSDP68

Riedel W. R. & Westberg J. M. 1982

Pacif.E. AmerC. off Guatemala

Mioc.

DSDP67 Strat.

Westberg M. J. & Riedel W. R. 1982

Pacif.E. Amer.S. Peru

Czc-Ouater.

Current Environ

Molina-Cruz A 1984

Pacif.E Calif. Peru

Recent

Plankt. Oceanot Upwell. Ecot

PisiasN. G. étal. 1986

GEODIVERSITAS • 1997 • 19(2)

443

De Wever P. & Popova I. M.

LOCATION

AGE

TOPIC

AUTHOR

Pacif.E. off Peru

Mioc.-Ouate

Stratig.

De Wever P. étal. 1995

Pacif.E. off Peru

Neog.

Strat.

De Wever P. et al. 1990

Pacif.E. Peru

Mioc.

Sedim, Environ.

Marty R. C. étal. 1987

Pacif.E. Peru E.Arabia

Mioc.-Recent

OOP

Caulel J. P- & Nigrini C. 1988

Pacif.E. Peru Nazca

Ecol. Current Environ. DSDP34

Sachs H M. 1976

Pacif.E.tropic.

Plankt.

NignniC. A. 1968

Pacif.Equat.

Ouater.

Strat. Plankt.

Nignni C. A. 1971

Pacif.N. Bering Sea

Ouater.

LingM. Y étal. 1971

Pacif.N, SE.Bering

Ouater. Recent

Sedim. Product.

Banahan S & GoenngJ. J. 1986

Pacif.N.

Strat. Evolut.

HaysJ. D. 1970

Pacif.N.

Mzc Ouater.

Sedim. Preserv.

Erez J- et ai 1962

Pacif.N.

Czc

Biol. Sedim.

KruglIkovaS. B. 1973

Pacif.N.

Ecol. Current Environ.

Sachs K M-1973

Pacif.N.

Ouater.

Plankt.

Nigrini C. A, 1970

Pacif.N.

Taxon. Evolut. Skelet. Ecol.

Sachs H. M. & Hasson P. F. 1979

Pacif.N. (boreai-subtrop.)

Czc Ouater.

Environ. Biogeog.

KruglikovaS. B. 1977

Paof-N. Amer.C. Calif.

Neog.

DSDP63

Wolfarl R. 1981

Pacif.N. Antar. Allanl.N

Neog.

Lombari G A Lazarus D. B. 1988

Pacif.N. Navarin Bering Sea

Ouater.

Biogeog. Environ.

BluefordJ R. 1983

Pacif.N, S.Bering Sea

L.Czc

DIagen. Sedim.

Hein J. R. et ai 1978

Pacif.N.

Strat.

Ouinlerno P 6 Theyer F. 1979

Pacif.N.Centr.

Recent

Ecol. Distrib.

Kling S. A. 1979

Pacif.NE.

Czc

DSDP18

KlingS A. 1973

Pacif.NE.

üngH. Y. 1966

Pacif.NE.

Ouater.

Preserv.

Kadko 0. étal. 1983

Pacif.NE.

Czc-Quater.

Current

Moore T. C 1973b

Pacif.NE.

Recent

Sedim. Oceanog.

Yamauchi M. 1986

Pacif.NW,

Czc

Strat. DSDP55

ÜngH Y 1980

Pacif.NW.

DSDP56

SakaiT. 1980

Pacif.NW.

Czc

DSDP56,57

Reynolds R A, 1980

Pacif NW

Plioc.-Recent

Climat- Environ.

MorleyJ- J 1987

Pacif.NW. Sea Okhotsk

Czc Ouater.

üngH. Y. 1974

Pacif.NW, Kamtchat. Kuroshio

Czc

Sedim. Current

Popova 1. M 1986

Pacif.S.

Mzc Czc

Plankt. Geogr.

Slevens 198Q

Pacii.S.

Plioc.-Ouater.

Lukanina 1. V. 1985

Pacif.SE.

Ouater.

Environ. Biogeog. Current Ecol.

Molina-Cruz A. 1977

Pacif.SE. Antar.

Czc

DSDP35

Weaver F. M. 1976

Pacif.Tropic. Indo.

Neog.

Strat-

Johnsor>D- A et ai 1987

Pacif.W Saipan Mariana

Eoc.

Strat.

RiedelW. R i957b

Pacif-W Tropical

Ollgoc.-Mioc.

Taxon.

RIedei W. R. 1959

Pacif.W.

Taxon. Strat. DSDP7

RiedelW R & Sanfilippo A. 1971

Pacif.W.

Czc

Strat. DSDP61

De Wever P 1981

Pacif.W.

Ouat

Biogeog. Paleocean. Sedim.

BoltovsKoy D 1907

Pacif.W.

Czc

Taxon.

RiedelW. R. 1952

Pacif.W. Philip. Indian Oc. Indon. Pacif.

DSDPSa

Sloan J. 1980

Pacif.W.

Paleog.-Ouater.

Strat.

Sanfilippo A. atal, 1981

Pacif.W.Centr.Equat.

Biozon.

KobayashfK ôfa/ I971

Pacif .W.C. Taiwan

Czc Recent

Sedim

ChBf>g y.-N. & Yeh K.-Y. 1989

Pacific

Sedim. Oceanol. Miner.

Baker E. T ét al. 1979

Pacific

Neog.

Earlh rotation

Hammond R. S. et ai 1979

Pacific Antar.S.

Ouater.

Skelet.

BoltovsKoy D. & Vrba A. 1989

Pacific Centr.

DSDP33 Stral.

Johnson D. A. 1976

444

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

LOCATION

AGE

TOPIC

AUTHOR

Pacific Equat.

Mid.Mioc.

Strat. Biozon.

Johnson D. A. & Wick B. J. 1982

Pacific Indian Oc.

Neog.

Environ.

Sancetta C. 1978

Pacific Equat.

Ouater.

Sedim. Current Ecol. Environ. Skelet. Takahashi K. & üng H. Y. 1980

Pacific Equatorial

Ouater.

Sfral. Biozon.

Johnson D A. & Knoll A. H. 1975

Red Sea

Season Environ. Biogeog.

GollR, M 1969b

Ross Sea

Neog.

Climat. DSDP 274

Robed C. étal. 1988

Sidly

E.PIioc.

Taxon- Strat. DSOP

Riedel W. R. & Sanfilippo A. 1978b

Tethys

Tethys Alps Carpath. Klippen

Czc

Taxon. N.Sp. Evolut.

Dumitrica P. 1983a

Hojnos R 1929

Tethys Carpat. Romania

Mioc. (Torton.)

Dumitrica P. 1968

Tethys Carpath.

Mioc.

Dumitrica P. et al. 1975

Tethys Cyprus.

Cret.-Czc

Strat. Environ.

Robertson A. H. F & Hudson J. D. 1974

Tethys Europe Cyprus

Paieoc.-Eoc.

Biozon.

KhokhlavaL. l E. 1988

Tethys Europe Italy

Mjoc.(Tofton./

Messin.)-Plioc.

Strat.

Coalongo M- L e/a/. 1979

Tethys Europe Italy

Mioc.

Taxon. N.Sp.

Carnevale P. 1908

Tethys Europe Italy

Mzc Czc

Taxon. N.Sp.

Vinassa de Regny P. E. 1898

Tethys Europe Italy

Czc

Taxon.

Neviani A. 1901

Tethys Europe Italy

Mioc.

Vinassa de Regny P. E. 1900

Tethys Europe Italy Calabria

Czc

Strat.

Seguenza Q. 1880

Tethys Europe Italy Napoli Messma

Czc Ouater.

Biol.

Cienkowski L 1871

Tethys Europe Italy Rotti

Czc

Strat. Taxon.

Riedel W. R. 1953

Tethys Europe Italy Sicilla (Tripoli)

Mioc,

Taxon. Strat.

CoccoL 1905

Tethys Europe Italy Sidly

Mioc.

Taxon.

Dreyer F. 1890

Tethys Europe Paratethys

Mioc.

Environ. Crisis DSDP42

RogI F. et al. 1978

Tethys Europe Slovakia

Mioc.(Badenian)

Taxon. Strat.

Dumitrica P. 1978

Tethys Europe Spain

Mioc.

Environ.

Berggren W. A. et a/. 1976

Tethys Europe Switzerl.

Mzc Czc

Taxon.

Jaccard F, 1909

Tethys Médit.

Tethys Oman

Ouater.

Environ, Preserv Anoxia

Bjorkiund K. R. & De Ruiter R. 1987

Hudson R. G. et ai 1954

Tropic-Padf-

Neog.

Evolut.

Levykina I, E. 1985

Tropical

Recent

Sedim. Preserv. Ecol.

Takahashi K, 1981

Tropical

Recent

Plankt. Sedim.

Takahashi K. 1982

Tropical Padf.

Mioc.-Ouater.

Taxon. Plankt.

NigriniC- A. 1977

Valdivta

Ouater.

Taxon, N.Sp. Biogeog. Skelet.

HaeckerV 1907

W.Norway Fjord

Ouater.

Sedim. Environ.

Aarseth 1. B. étal. 1975

World

Czc Mzc

Premoli-Silva 1 étal. 1976

World Océan.

Taxon. Skelet.

Petrushevskaya M. G, 1981b

Zealand SE.Otago

New sp.

BensonW N. & Chapman F. 1938

• 1997 •

GEODIVERSITAS

19(2)

445

GEODIVERSITAS • 1997 • 19(2)

Table 2. — List of publications dealing with Cenozoic strata of the Russian platform. Each publication has a number which corresponds to that on figures 6-14. For each publication

the âge, région, longitude and latitude, subject of investigation, paleoenvironment and other involved fossil groupe is given.

Author

Age

Région

Longitude

Subject of

Paleoenvironment

Other

Latitude

investigation

fossils

Amon &

Kovaltchuk

1988

Paleocene

Eocene

Eastern Ural

Turgay

62°30'1-65°00'1E

48“00'1-50°00'1N

Radiolarian zonation

established by Lipman

for Talitskaya,

Serovskaya & Irbitskaya

formations.

Talitskaya formation

(Paleocene): recrystal-

lized association of Ra

dioiaria. Serovskaya

formation (Late Eoc.)

shailow waler asso¬

ciation. Irbitskaya for¬

mation (Mid.-Up. Eoc.)

pelagic association.

no data

Borisenko

1958

Paleocene

Western Kuban

Northern Caucasus

1 ) Beslineevsko-

Shedok région

2) AbinsK région

(Goryachiy Klyuch)

3) Seversky disiricl

(balKa Kipashaya)

1) 40“00'1-41"00'1E

44°00'1-45“00‘1N

2) 38°30'1-39"30'1E

44“00'1-45^'00'1N

3) 38^00-38=30TE

48“50'1-49“00'1N

Radiolaria from llskaya

and Psekupskaya

formations.

40 new taxa described

Shailow water

association

no data

Borisenko

1960b

Upper Paleocene

Éasfem Kuban

1 ) Cossak village

(bouiidary between

Azovsky and Kras-

nodarsky district)

2) river M. Zelanchuk

(StavropolsKy dlsfrict)

1) 37'’30'1-40°00'1E

46“15'1-47"30'1N

2) 42“00'1-42“30TE

43"30'1-44'’00'1N

Radiolaria from Abasinskaya

formation

10 new taxa described

Shailow water

association

no data

Borisenko

1960a

Lower-Middie

Eocene

Western Kuban

1) Babakov George

(trubutary of r, Psek-

ups), 2) district Kipu-

ashaya (GluboKy jar)

3) r. Shebsha-Shibika

interflow

1) 38°30'1-39°00'1E

44°00'1-45°00'1N

2) 38°00'1-38°30'1E

48°50'1-49°00'1N

3) not found

Radiolaria from Zubzinskaya,

Kutaisskaya, Kaluga forma¬

tions. 15 new taxa described

Shailow water

association

no data

De Wever P. & Popova I. M.

GEODIVERSITAS • 1997 • 19(2)

South-eastern Mtddie

1) not found

Chediya

Paleocene

Asta 1) Mountain

2) Khodzha:

Kreidenkov

range Peler 1sl

70"58'E

Ashurov

2) Khodzha-Kasian

40°45'N

1971

3) Aryk-Tau

3) not found

4) Istum-Tay

4) not found

5) Kichik-Donguz

5) not found

A- Mid.Asia

A-

Chediya

Eocene

1 ) south-western

1)67"35’-67M5'E

1973

spufs ot the GissarsK

37"30-37‘'40'N

mouni range

2) no précisé data

2) Tadzhiksk depres*

3)7ri9'E:40^23'N

sion

B-

3) Fergana

1)60“30-65“00'E

B- E.Tufkmenla

1 ) BukharO'Khiva

dépréssion

40“00'-4r00'N

Crimea

33“00'-33"30'E

Chediya D. M.

Late Paleocene-

Bakhchisaray strato¬

44°30'-44M5'N

& Chediya 1. 0.

Early Eocene

type section

1973

(Simferopol région)

Middie Asia

1)64"00'-66 00'E

Chediya

Early Eocene

1) E. Turkmenia

38“00'-40"00'N

1981

Middie Eocene

{Bukhâfo-Khivinsk

2) 33''00'-33'*30 E

Late Eocene

dépréssion),

SE ot Mid. Asia

(SW spurs of GissarsK

mountain range),

Tadzhiksk dépréssion

and Fergana

2) Simleropolsky

région

44°30'-44=45 N

Jurassic

Ukraine

1) 32'’10'-32°20'E

Gorbunov

Cretaceous

1) Kiev (Koryukovka v.)

51°15'-51°30'N

1971

Paleogene

provinces

2) 32°30'-32°40'E

Neogene

2) Chernigov

(Khoimy v.) prov.

51°45'-5r50'N

Paleocene Radiolaria

from Bukharsk layers

Pélagie

association

Pelecypods

gastropods

brachiopods

foraminifers

ostracods

corals

Eocene Radiolari, are

studied In thin sections

from deposits of

Kuberlinsk,

Kerestinsk &

Kumsk

horizons

no data

Radiolaria in rocks

analogues to

Globorotalia aequa,

G. sübubotinae

Globigerina ara-

gonetisis etc.

forams’s zones

Radiolaria (bad preserv.) from

KashinsKaya formation (Late

Paleocene) and BaKhchisaralsky

horizon (Early Eocene),

no description.

Shallow water

association

no data

Radiolaria from 1, Kath«nsKy,

2. Bakhohisaralsky. 3. Atmifrsky.

4. Simferopolsky. 5 Bodraksky

formations of Simferopolsky

région and 1. SuzâksK. 2. AlaisK,

3. Turkeslanian 4. Rishtansk,

5. fsfarinsk horizons of Middie

Asia

Alternatinn of shallow

ar>d deep water asso¬

ciations in Simfero¬

polsky région and

shallow water asso¬

ciations in Middie

Asia

Forams

associations

1. Acarima acahnata

2. Opereuhna

serr}iiyoHta

3. Gltybigarapsis

index zones

Radiolarians of Jurassic,

no data

Cretaceous. Paleogene and

Neogene summary of the

history of the investigations,

no description or plate.

Cenozoic radiolaria from European Platform

GEODIVERSITAS • 1997 • 19 (2)

Author

Age

Région

Longitude

Latitude

Subject of

investigation

Paleoenvironment Other

fossils

3) Poilava

3) 34'^00 -35"00'E

(Vûlynsk) provinces

49=00-50"00'N

4) Odessa

4) 30 ^30'-31 ^00'E

(Khollodny v.) provinces

46=30'-47’00'N

Middie Asia. BuKharo-

1 ) no précisé data

Eocene Radiolaria

Pélagie

E. Eocene:

Kestner

Eocene

Khivinsk depres&ion

2) not found

from Beloglinsk,

association

Globorotalia-

1971

(1-5) and

3) not found

Kuberlinsk,

in Upper

aequa^

SW spurs ot the

4) not found

Kerestinsk

Eocene

G. subbotfna.

Gissarsk mounialn

5) territory between

horizons

shallow water

M- Eocene:

range (6-7)

Khiva

in Lower

Globorotalia

1 ) Kushab

(60'’49'E;41'’25'N)

Eocene

aragonansis,

2) Khalar

and BüKhara

Acarinina

3) Pamuk

(64°26'E;39=47'N)

crassaformis.

4) Lakkent

6) 66=30'E:38'’24 N

L. Eocene;

5) Razak

7) no précisé data

Acarinina

6) Dekhanobad

rotundimarginata.

7) Toichisai

Ust Yurt

no précisé data

Oligocène Radiolaria

Shallow

L. Eocene

Kestner

Oligocène

Aidzhankos area.

water

Lenticulina

1973 a

Barsâkeijmesski)

association

hermanni +

trough

Oligocène

BoHvina

antegreassa

Middie Povolshie,

1)48° 25'-48° 30'E

9 radiolarian assem-

Alternation

L. Paleocene diatoms

Kozlova

Upper

Eastern Ural.

53® l5'-53'' 2Û N

blages are given,

of shallow

zones:1 ) Trinacria

1984a

Paleocene

Western SIberla

2)48' 45 -48 48 E

7 rad zones esfablished

and deep water

herbeigiâna,

Lower

1 ) Syzran

53'^50'-53'-57N

in different formations

associations

2) Tnnacna

Eocene

2) Sengiley

3) 48^22-48‘'25 'E

from Povolshie. E. Ural

of Radiolaria

ventnculosa

3) Oulianovsk

54“ 19 -54“ 20 N

W Siberia

3) Coscinodiscus

4) Korsbevka

4) 48' 10'-4a" 15 E

4 n. sp. are described

uraiensis

5) Insa

54“ 15'-54= lO^N

Early Eoc. Z.;

5) 46° 20'-46°21E

1 ) Coscinodiscus

53 '-'SO -SS'’ 51 N

payer!. 2) Pyxilla

gracilis

Pre-Caspian région

1)53“ 56'E:

Phylogeny and description

Kozlova

Upper

1) Miyalinskaya-r.Uil

48° 55 N

of Axoprunum. Heliodiscus,

data

1990

Paleocene

V. Miyaly

2) 53° 00 -53"-30 E

Tripodiscinus.

Lower,

2} Kamiskolskaya

48° 30 -49° 30'N

Clathrocydas. Lychnocanum

De Wever P. & Popova I. M.

GEODIVERSITAS

A 14

CD Koziova

'T' 1993

Middie,

{near Akshatau{?))

3) 54° 13'E:

Upper

3) Lybenka

50° 22'N

Eocene

Voronesh anticline

4) 39° 52'E

4) Kantemirovka

49° 4Û'N

5) River Don bassin

5) no précisé data

1-9)

1)36°44'E:49°51'N

Upper

Voronesh anticline

2) 36°44'-37°30'E

Paleocene

10-19)

49°51'-49°30'N

Lower,

Middie Povolshie

3 ) + 4 ) not found

Middie,

20- 28)

5) 39°52'E;49°40'N

Upper

Eastern Ural

6) 41°15'-41°80'E

Eocene

29- 34) Pre-Caspian

50°10'-50°20'N

58- 60) W.Siberia

7) not found

8) 33°49'E;45°5rN

1 ) Russkie Tishki

9) 42°00'-42°10'E

2)-h3) River Oskol

49°40'-49-'50'N

4) Deresovka

10) 46°50 E:49°25'N

5) Kantemirovka

11) 12) 13): =2) 4) 5)

6) Nikolskoe

14) 47°09'E;53°40'N

(near Kalach)

15) 46°35'E:53°08'N

7) Baltinovsk

16) see Syzran n°1

8) Vorobjevka

17) 18) 19) :

(n.Vorontsovka)

45°00'-47°30'E

9) River Mishkova

52°00'-52°30'N

(near Meshkovskaya)

29) +30) +31):

10) Dzhanybek

54°30'-57°30'E

11 ) Korshevka

47°00'-49°00N

12) Sengiley

32) 57°06'E;49°09'N

13) Insa

33) 61°14'E:48°36'N

14) Balashejka (near

34) 62"30'-65°00'E

Barysh-Kuzovatovo)

47 30'-48 OO'N

15) Kuznetsk

58) + 59) see loc. n°2, 3 in

16) Suchanovka

Koziova 1984 loc.n°12)

17) Kiselevka+18.r.

60) no précisé

Alaj +19.Diupa

location

29) North Emba

55°00'-57°00'E

30) Emba

31) South Emba

32) Ternir

33) Irgiz

34) West Kazachstan,

welt 125

58) +59)

60) Uspenskaya well

48°30-49°00'N

& Phormocyrtis of

Eocene-Upper Paleocene

deposits is given

The biozonation for

boréal province is introduced

Radiolaria of boréal no

Corrélation

province data

of zonal subdivision

The scheme of

based on

Upper Paleocene

radiolaria,

Eocene Radiolarian

planctonic,

zones corrélation

foraminifera.

is given for

nannoplankton

North Caspian Sea,

and dinoflagellates

River Don, River Volga

middie flow,

East Ural slope

Western Siberia

is given

Cenozoic radiolaria from European Platform

GEODIVERSITAS • 1997 • 19(2)

Author

Age

Région

Longitude

Subject of

Paieoenvironment

Other

Latitude

investigation

fossils

Pre-Caucasus

1 ) no précisé data

42 new

Shallow

Early Eocene

Krasheninnikov

Lower,

west

2) no précisé data

species and

water

foraminHera zones

1960

Middie,

1 ) Moldavano-Psifsk

3) no précisé data

2 new généra

association

Globorotalia subbotinae

Upper

2) Zybsinsk area

4) 42^ 25'-42" 30'E

are described

Low-Middle Eocene

Eocene

3) ravine Kjpyachaya

46^15'-46^ 30'N

and Mid. Eocene Rad's

4) ravine Solenaya

assemblages are

discovered within

foraminilera's zone

Globorotalia

aragonensis

Turkesîan, central

1) Tamdybulak(?)

18 new taxa described

Shallow water

Lipman

Eocene

Kyzyl-Kum:l) Tamdy

64"36'E;4r46N

in Eocene association

association

data

1950

2) Shchulj trough

2), 3) not found

of Radiolaria

3) Chetyr well

4) TamdytauK?)

4) W. slope ol Ihe

63''20'-63“30'E

Tamdinsk stage

41-15-41‘’25'N

W. Kyzyl-Kum

5) 34»20-E

5) DzhânKoi

45"40N

6) Ak-Oi

6) not found

7) Usun-Kuduk.

S.-W. Kyzyl-Kum

7) not found

SE&W

1)63“40*E

1 ) The distribution

Alternation of

Spongurus

Lipman

Maestrichtian

Turkmenla

SS^'ISN

of 98 species is

deep water

biconstrictus

1965

Turgai.

2) 64'’06'E

given in the Eocene

and shallow

association

Danian

Northern Pre-Aral

52'^22N

deposits

water

occurs

1 ) Kustanai

3) 61'-'06 E

2) Two zona! subdivi¬

Radiolarian

together

Paleocene

2) Semiozernoe

46"07'N

sions based on Radio¬

association

with

Eocene

3) Saksayl’sk

4) 59^29 E

laria are estâbli-

foraminifera

4) Mis IzyrHly-Aral

45"48'N

shed a) Spongurus

Nummulites

5) Baikonur

5) e6“03'E

biconsthdus

disîans

6) fiver Turgaj

47’50N

b) Ellipsoxiphus

N. murchissoni

{middIe flow)

6+15) 60'’12 E

chabakovi in

etc.

7) AralsK

48'^49‘N

Tasaransk sériés

8) Kushmurun

7) 6r43'E

9) Semiozernoe

46=56'N

Ellipsoxiphus

10) Amangeidy

8) e4'’37’E

chabakovi

11) Chelkar

52^30'N

association

12)Togyz

9) 64‘’06'Ë

of Radiolaria

13) Mountalns

52"22'N

occurs together

De Wever P. & Popova I. M.

GEODIVERSITAS • 1997 • 19(2)

Tas-Aran 10)65°irE

14) Tshchebas guif 50°12'N

15) Aktogai 11 ) 59°39'E;47°48'N

16) lrgiz 12) 60°32'E:47°32'N

17) Turgai 13) 59‘'20'-59°40'E

46°15'-46°20'N

14) 59“40'-59“45'E

46“05'-46°10'N

16) 6ri4'E

48"36'N

17) 63“25'E

49“ 38'N

Northern Pre-Aral

1) not found

Lipman

Paleocene

TurgaiskTrough

2) 57°30'-58"30'E

1976

Eocene

1) Mount Tas-Aran

45''45'-47“00'N

2) Chagrayskoye

3) 59°39'E

Maestri-

Plateau

47“48'N

chtian,

3) Chelkar village

4) not found

Danian

4) Lake Tebes

5) not found

5) Tumaly-Kolj vil.

6) 63'’25'E

6) Turgai village

49“38'N

7) Saksaulskiy

7) 61“06'E:47“06'N

8) Belgorod

8) 36“36'E;50°38'N

9) Astrakhan

9) 45“30'-46“30'E

10) Krasnovodskoe pl.

46°00'-47'’00'N

11 ) Kustanai

10)52''35'-52°40'E

12) Emba

40“10'-40°15'N

13) Bukhara (région)

11)62“30'E

14) Chardzou (?)

52°25'-52°35'N

Komsomolsk

12) 54°30'-57“30'E

(between Ashkhabad

47“00'-49°00'N

and Bukhara)

13) 64“10'-64°30'E

39“20 -39“30'N

14)63“34'E;39°01N

Turgaisk Trough,

locations are the

Lipman

Eocene

Northern Pre-Aral

same as in

1969

Lipman 1965

4:^.

with

foraminifera

Speroplectammina

spectabilis

The map with no no

Conocaryomma data data

aralensis

occurrences is given

New Family-Conosphae- no no

ridae, new subfamily data data

Conocaryomminae, new

genus Conocaryomma

and 2 new species

C. aralensis, C. lentis

Cenozoic radiolaria from European Platform

GEODIVERSITAS • 1997 • 19(2)

Author Age Région Longitude Subject of Paleoenvironment Other

Latitude investigation fossils

Lipman

1972

Eocene

TurgaiskTrough.

Northern Pre-Aral

ail location from

Lipman 1965

Lipman

1975a

Middie

Eocene

Northern Pre-Aralie

1) Izyndy-Aral

1)59"29'E

45‘-48'N

Lipman

1982

Oligocène

Northern Pre-Black

Sea

1 ) Lower Serogozsky

région of Khersonsky

district

1) 32'’00'-32“30'E

46°25'-46°50'N

Lipman

1984a

Paleocene

Eocene

Oligocène

Nonh Western

Caucasus and

Apsheron

peninsula

Crimea.

1) 33^53'E

Lipman

Upper

Bakhchisaray area

44M4'N

1984b

Paleocene

1) Bakhchisaray

2) 33"50 -34"10'E

(v, Slaroselie)

44’30'-44“40'N

2) r. Kacha

(V Predusheinoe)

3) SuvIuKaja Mounl.

4) r. Belbek

(near Bakhchisaray)

5) Bakhchcsaray

(quarry ot cements

factory)

6) Kizii Djar Mountain

(v. Pochtovoe)

3) not found

North Eurasia

no précisé data

Lipman Paleocene

1993 Oligocène

Eocene

11 new species and

Shallow

11 new genus are

water

data

described

association

4 new species of

Shallow

Nummulites

Radiolaria are

water

introduced

association

Foraminifera

2 new species of

Shallow

Foraminifera

Radiolaria are

water

described

association

mollusc fauna

Corrélation of the

Shallow

Foraminifera

stratigraphical divi¬

water

scale

sion of the Paleocene

and Eocene stages based

on Radiolarians and

Fora minifera

association

is provided

Pg Radiolaria.

Shallow

Foraminifera

conclusion: impossible

water

scale

to compare rad's asso¬

ciations of Crimea and

Middie Asia.

No Radiolaria record

hâve been found in the

sections of r Belbek,

cernent quarry near Bakh-

chisarai, m. Kizil-Djar

(near v. Pochtovoe)

and V. Staroselie

association

is provided

Radiolarian zonation

Corrélation

for the North Eurasia

data

with

is provided and foraminifera’s

correlated with the

rad’s zonation sugges-

ted by Sanfilippo,

De Wever P. & Popova I. M.

GEODIVERSITAS • 1997 • 19(2)

Westberg & Riedel. and

1981 for the Paleogene nannoplankton’s

deposits of the zonation

océans tropical realm is made

Lozyniak

1985

Eocene,

Oligocène

Ukranian Carpatians

Skybe zone

1 ) river Cheremosh

2) r, Prut

3) r. Stryy

4) r. Dnestr

1) 26=00'-25"30'E

48i0'-48-30'N

2) 25"00 -26 OO E

48’30'-48 35'N

3) 23^30 -24WE

49‘^10‘*49“30'N

4) 24“10'-24‘’30'E

49'^20'*49''40'N

Poor to moderate

preserved radiola-

rian associations

hâve been studied

data

Mamedov

1969a

Eocene

Azerbaidjan

1 ) Shemakhino-

Kubâstanskaya area

2) Apsheronian

peninsula area

1) 48‘‘25-48*30'E

40W-41-30'N

2) 49"30'-50"30'E

40M0'-40 40 N

6 new radiolarian

species are described

data

Globorotali

crassaformis,

Globiger inoita

index,

Globigerina

turkmenika,

Globorotalia

aragonensis

Azerbaidjan

1)a- 48°37'E

6 new radiolarian

Mamedov

1969b

Eocene

1) South-Eastern

Caucasus

a- Shemakhino-

Ismaillinsky. b- Kubastan

2) Apsheronian

peninsula

40°38'N Shemakha

48"10'E;40°46'N

Ismailiy.

b- 48"33'E;4r23N

Kubastan

2) 49^30“*50"30'E

40"10'-40‘40'N

species are described

data

Azerbaidjan

1)48°45'-49"30'E

6 new radiolarian

Mamedov

1969c

Eocene

1) Sumgait river

40"30'-40°50N

species are described

data

Azerbaïdjan

1) not found

6 new radiolarian species

Mamedov

1970

Middie

Eocene

North-East part

1 ) village Kirovka

are described from deposits

of Low. Coun formation

data

Azerbaidjan

1). 2) see Mamedov

5 new radiolarian

Globorotalia

Mamedov

1973a

Up. Paleocene

Low.. Mid..

Up. Eocene

ail locations ot

the samptes are

from previous

publications

1969b

3-7) no précisé

data

species are described

data

crassaformis

Cenozoic radiolaria from European Platform

GEODIVERSITAS • 1997 • 19(2)

Author

Age

Région

Longitude

Latitude

Subject of

investigation

Paleoenvironment

Other

fossils

Azerbaïdjan

1), 2) see

5 radlolarian associa-

8 biostratigraphical

Mamedov

1973b

Eocene

1) Shemakhinskaya

area

2) ismaillinskaya area

3) Kirovka village

4) Agdara

5) Gadshili

6) Khiljmili

7) Dijally

loc. n’’ 28

3-7) not found

tive zones are esta-

blished in Sumgaits-

kaya and Low , Mld.,

Up. Coun formations

and correlated

with 6 Foraminiferal

biostratigraphical

zonation

data

subdivisions

based

foraminifera's

data

Azerbaïdjan

AH locations

3 stages in the deve-

First stage coïncides

Mamedov

1975

Lower

Middle

Upper

Eocene

are from

publications

lopment of Eocene

Radiolarians are given

1- Early Eocene. 2- Mid.

Eocene, 3 - Late Eocene

data

with Globorotalia

suboîinae

Second stage

with Globorotalia

crassaformis

Third stage with

Globigennoila index

Mamedova.

Mamedov

1970

Azerbaïdjan

1 ) Gadzili village

2 ) Shemakhinsk area

no précisé data

Plates with the âge,

lilhology and Radiola-

rian assemblages are

provided

data

Correlalion

with foraminifera

data is made

Western Turkmenla

1) not found

18 new species of

Deep water

Moksyakova

Upper

1) Southern Usi Yurt

2) 54“30'-54‘’50’E

Radiolaria are de-

association

data

1961

Eocene

2) Maili and Boishoi

BalKhan

3) Koimal-Dag

4) KrasnovodsKoe

plateau

5} Usbolsk corridor

6) Efbent Tashaus

(Contrai Karakums)

39=10 -39 30'N

3) not found

4) 52=30 -53 OO'E

40 10 -40 20'N

5) 55"00 -SS^SO E

39 00 -39 20'N

6) 59'58'E:4r49 N

scribed from Kumsky

horizon

alternating

with shallow

water asso¬

ciation

Turkmenia

1)52'=55'-52^57E

10 new radlolarian

Deep water

Moksyakova

Upper

l)hole 304(Kara-

41 ■10-41 -ISN

species are descri-

association of

data

1965

Eocene

Bogaz-Gol gui()

(N-W bay)

2) exp.S |Kara-6ogaz-

Gol gulf] (South pari

Omchali)

2) 53H4'£

40*^38 N

3) 53=45 -53'50 E

40"05'-40^’10'N

4) 59 WE

bed from Kerestinsky

and Kyberlinsky

horizons

Radiolaria

De Wever P. & Popova I. M.

GEODIVERSITAS • 1997 • 19(2)

4:x

Nikitina,

Zagorod-

nyuk

1981

Radionova

Khokhlova

1994

3) hole 3 (150 km to

42=28'N

the West from Kras*

5) 59"58 E

novodsk)

41‘'49'N

4) Nukus

6) 58^24'E

5) Tashauz

40“12'N

6) Darvaza

7) 58'18 Ê

7) Sernyy Zavod

40^00'N

8) Chardzhou

8) 63"34 E:39°09'N

9) hole 35

9) 63^00-63^10'E

37"30'*37"40'N

1) Lower Don bassin

1)40'^00 -4rOO'E

Eocene Radiolaria and

Plate illustrâtes

Zonation

Eocene

2) Norrhern Pre Caspian

47''00'-48"00'N

Foramlnlfera. 1 ) Range-charts

shaliow water-

based

(rivers Sagiz* Emba)

2) Emba (see loc n 18)

of Eocene benihic loram*nifera

radiolarians

on Foraminifera

50^00'-55^00'E

from South Sagîz - Easfern Pari

and

data is

3) Ergen-eastern Pre-

47''30'-48'30‘N

of Russky plattorm and

foramini feras

give

Azov (western part

3) 37"30'-40''00'E

Serfsky plate is given,

associations

of Karpinsky swell)

45^00'-47-30'N

2) Corrélation of radiolarian

and foramlrrtferal biostratl-

graphic zones is made

A- Crimea

1)33"20'E:45''12'N

a) Nannoplankton and

Radiolarian

Nan no-

Up.Paleocene

1) Eupatoria

2) near Feodosiya.

foraminifera's biostrati-

as semblages

plancton

formations

2) Nasypnoe

no précisé data

graphy. b) Paleogene

are of

foraminifera

Goryachii

B- Caucasus

35^23‘E:45^03'N

épisodes of biogenic

shallow-water

silicoflagellates,

Klyuch.

3) Anapa

3) 37"20'E:44 54 N

silica accumulation

origin except

diatom

and Abaza

C- Western Ukraina

4)100-200 kmSof

correlated with trans-

Mid.Eocene

Lower Eocene

4) Shibik river

Novor ossiysk

gressive-regressive

association

Formations;

5) Glubokil Yar

37=46'E;44M4 N

cycles c) The list of

discovered

Cherkess, Zybza.

6) Balka Kipyach'ya

no précisé data

Radiolarian taxa, found

in Dagestan

Kutaisi (r. Belaya)

7) Balka GluboKaya

5) no précisé data

in Dp. Paleocene

(Rubas-Chai r.)

Mid. Eocene

8) Pshish river

6) no précisé data

Low. and Mid.

Formations:

9) Kurdzhips river

7) no précisé data

Eocene and Oligocène

Kaluga and

10) Laba r.

8) near GoryachI

deposits is provided

Khadyzhensk

11) Belaya r.

Klyuch,

(western Kuban)

12) Kuban r.

39^'18'E;44''36'N

Oligocène

13) Kheu r.

9) no précisé data

Khadsum

14) Unjkh r.

40'--44’E.:44°39'N

horizon of the

15) Rubas-Chai r.

10) near Labinsk

Maikop Group

16) nofthern Kobystan

and Shedok

(15,16) western part

40"50'E:44°13'N;

of Casptan Sea

11-17) no précisé data

17) Karagje dépréssion

18) 55"30'-55“20'E

13) Bol'shoi Balkhan

mountains

39"00‘-39°20'N

Cenozoic radiolaria from European Placfoi

GEODIVERSITAS • 1997 • 19 {2)

v-n

Author

Age

Région

Longitude

Subject of

Paleoenvironment

Other

Latitude

investigation

fossils

Neogene

Pre Carpatian

1)24"20'E:49"02N

Lower Miocene generic

Runeva

Miocene

1 ) Kalush'Zoljny»

(Kalush)

composition ot the

data

1969

zone

2) no précisé data

radiolarian association

2) Vyrva r

3) no précisé data

from Vertwvelsk iayers

3) Banevichi v.

4) no précisé data

of Vorotyshchensky senes

4)TarnavKar,

is provided

Paleogene

Pre Carpatians.

1)23°31 ■E;49=16'N

6 radiolarian taxa were

Oligocène Globo

Subbotina

Neogene

East Carpatians

2) no précisé data

found. Préservation is

data

rotalia

1960

Oligocène

1) Vorotyshche r.

3) no précisé data

very poor.

denseconnexa

Lower

Pollanltsky,

(near city

Redeposition

subbotinae.

Miocene

Vorotyshchensky,

Truskavets)

Gtobigerina

Zagorsky

2) Stonilsa r.

pseudoôdita

sériés

3) Tysmenitsa r.

Miocene

redeposition of

Foraminifera has

been observed.

Voronesh anticline

1)40°35';50°2rN

Early, Middie, Late

Tochilina

Upper

1 ) Russkaya

2) no précisé data

Eocene radiolarian asso¬

data

1969

Paleocene,

Zhuravkav,

3) no précisé data

ciations are given, no

Lower

2) Eryshevka v.

4) no précisé data

Radiolaria in Oligocène

Middie

3) Semenovka v.

5) 40"07'E;50‘^28 N

sédiments

Upper

4) Gavniinsk

Eocene

5) Pavlovsk

Voronesh anticline

1) Rossosh-39'’35'E

Up. Paleocene

Alternation

Up. Paleocene

Tochilina

Upper

1 ) tôrrilory wlthin

50’12N

(Sumskaya form.)

of shallow

alternation of

1975

Paleocene

square; Rossosh v.-

Losevo- 40'02 E

Low. Eocene

and deep

radiolaria &

Lower

Losevo V. KalâOtv

50'41 N

(Kanevskaya f )

water

Molluscs bearing

Eocene

Boguchar v

Kaiach- 41'02E

M. Eocene (Kie^«'

radiolarian

deposits

MIddte

2) near Chuguev v.

50''26N

kaya form.), Up.

associations

Low. Eocene

Eocene

3) near Belgorod v-

Boguchar- 40“34 E

Eocene (Kharkov-

Radtolarians

Upper

4^ near Obojan v.

49 5S N

skaya formation)

with Foraminifera

Eocene

5) near Kantemirovka v.

2) 36^44'E;49"5rN

Three penods ot radio¬

Mid. Eocene

6) near Veshenskaya v

3) Belgorod

larian fauna develop¬

Radiolarlans. with

4) no précisé data

ment are established

Foraminifera &

36-36 E;50^38 N

(• Late Paleocene-

Molluscs

5) 39 ■52 E

Early Eocene

Up. Eocene

49 -40 N

K- Late Eocene-Klevsky

alternations of

6) 41^45'E;49'39 N

III- Late Eocene-Kharkovsky

Molluscs & and Rad.

bearing deposhs

De Wever P. & Popova I. M.

GEODIVERSITAS • 1997 • 19(2)

Russian platform

1) 40°00'-41°00'E

3 different Radiolarian

Deep-water

Zagorodnyuk

Upper

1) Lowerflow of the

47"30'-47“45'N

associations for the

and

1969

Eocene

Don river

2) see loc n°14

Lower Don river flow

shallow

Pre-Caspian lowland

3) a- Sal’sk-

and 4 assemblages for

water

2) the bassin of the

4r33'E:46°30N

Northern Emba (Pre-

Radiolarian

Northern Emba

b- Alexandrovskoe

Caspian) hâve been

association

Azovo-Kubansk

(Stavropol)-

described

through and

42'’59'E:44M5'N

Kuberlinsk, Ke-

3) Azov

c- 38"57'E:46-^05'N

restinsk, Kumsk

élévation

d- 39"45'E:47'’15'N

and Beloglinsk layers

a- Sal’sk

4) (North Pre-Caspian)

from Emba and

b- Alexandrovskoe

a- 40M0'-40“40'E

(Northern Pre-Aral)

c* Kanevskaya

47°10'-47°00'N

Tasaranskaya,

d- Rostovskaya

b- 44°52'E;46°17'N

Saksaylskaya,

4) SalO'Manych

inter-fluve

a- r. Manych

b- western Ergen

(Ulan Erge)

Cheganskaya

Russian platform

no précisé data

Peculiarities of the

Zagorodnyuk

Eocene

Lower flow of the

morphological struc¬

data

1975a

Don river

ture of some Sphaer-

oidea and Discoidea

1 ) South-Eastern part

no précisé data

The taxonomical compo¬

Shallow

Zagorodnyuk

Mid.,Up.

part of Russian

sition of radiolarian

water

1981

Eocene

platform

assemblages from

radiolarian

boundary

2) Eastern Pre-

Bakhchisaraisky and

associa¬

Caspian

Simferopolsky layer

tions

is described

data

corrélation

with

biostratigraphical

zonation based

on foraminifers

data is provided

Cenozoic radiolaria from European Platform

De Wever P. & Popova I. M.

Fig. 6. — General map of eastern Peri-Tethys domain showing the investigated régions listed on Table 2. Main areas of investigation

are marked with grey zones. The numbers refer to those given on Table 2. Detail maps are provided from west to east on Figs 7-22.

458

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radiolaria from European Platform

ROLAND

• Berdichev

\Drogobych

U K R

I N E

\ ^

, Dnestr

Chernovtsy^

• Vinnitsa

40 ) ''"'mir"'\

'-J/

R O U M A N I A

^ MOLDAVIA

-v

Fig. 7. — Location map of sites used in previousiy published investigations of Ukraine, south of Lvov (25'’E, 50°N)

Voznesensk

Krivoy Rog

• )

-^r 7

^ Réservoir lake

ofKAKHOVKA

iNicoiaye V

' iiiiÉliiiiiiiii ^ oM

_ / I Black Sea ~~ _ I _1_

Fig, 8. — Location map of sites used in previousiy published Investigations of Ukraine, northern Black Sea région, near Odessa

{31'’-34''E. 45“N) .

GEODIVERSITAS • 1997 • 19(2}

Fig. 9. — Location map of sites used fn previousJy published investigations ol the northern Black Sea région Crimea (31°-36“E).

Détroit ■—

-Kéré~Bogéé~

Z KrMnov^%ÏR,2

tjl •K-iindihlk

TURKMENISTAN

/ Kari'Kila

GREAT/DESERT SALT

Fig. 10. — Location map of sites used in previousiy published investigations of the east Caspian Sea, Krasnovodsk area {55°E).

460 GEODIVERSITAS • 1997 • 19(2)

Fig. 11. — Location map of sites used in previousiy

De Wever P. & Popova I. M.

37*E 38^E 39^E

Fig. 13. — Location map of sites used in previousiy published investigations of the northern Black Sea région in the

Lougansk-Stakhanov area (37°-39°E, 48”-49“N).

Fig. 14. — Location map of sites used In previousiy published investigations of eastern Ukraina and south-western Russian platform,

Kharkov-Volgograd area (40°-45°E, 50°N).

462

GEODIVERSITAS • 1997 • 19 (2)

Cenozoic radiolaria from European Platform

41®E 42*E 43*E

GEODIVERSITAS • 1997 • 19(2)

463

-vJ

Fig. 16. — Location map of sites used in previousiy published

investigations of the north-eastern Black Sea, Krashnodar-

Maïkop-Stavropol area (37“-43®E. 44'’-45^N).

Korenovsk

Cenozoic radiolaria from European Platform

40*E

Fig. 17. — Location map of sites used in previousty published investigations of the eastern Black Sea, and eastern Ukraina-south-

western Russla: Kharkov, Rostov-on-Don and Volgograd régions (40“-45°E, 50‘"N).

GEODIVERSITAS • 1997 • 19(2)

/.rc

De Wever P. & Popova I. M.

466

GEODIVERSITAS • 1997 • 19(2)

Cenozoic radioiaria from European Platform

45*E 50*E

Fig. 19. — Location map of sites used in previousiy published investigations of the middie Volga between Saratov and Kuvbishev

(40°-50°E, 52"N).

46*30’E

48*E

49«3n'P

42*N

41»N

Fig. 20. — Location map of sites used in previousiy published investigations of Azerbaidzan, Baku area {46°-50"E, 40°-42°N).

GEODIVERSITAS • 1997 • 19(2)

468

GEODIVERSITAS • 1997 • 19(2)

Magnetostratigraphy of the Pliocène deposits

in Black Sea, Caspian régions

and adjacent areas

Edward A. MOLOSTOVSKY

Institute of Geology, Saratov State University,

Moskovskaya Street, 161,410750 Saratov (Russia)

Molostovsky E. A. 1997. — Magnetostratigraphy of the Pliocène deposits in Black Sea,

Caspian régions and adjacent areas, in Crasquin-Soleau S. & De Wever P. (eds), Peri-

Telhys: stratigraphie corrélations, Geodiversitas 19 (2) : 471-495.

ABSTRACT

The results are summarized of paleomagnetic studies of the Pliocène deposits

from Kcrch Peninsula, western Gcorgia, Azerbaijan, Turkinenia, Norrh Cis-

Caspian and Lower Volga régions. Information from a number of researchers

was used alongsidc with the author’s data obtained earlier and in the course

of research within the frarnework of the IVri-Tethys Programme. Composite

paleomagnetic sections from the areas lisied were correlated and relared co A.

KEYWORDS Cox (Harland e( al 1^)82) magncrochronologic salle and to the paleomagne-

magnetostratigraph), scheme of the Ncoecnc deposits from rhe Mcditerninean région. On the

polarity, basLs of the paleomagnetic data, rhe views on chronologie rclationships

paleomagnetism, among some local stratigraphie units were corrected; main development

rémanent magnétisation, riii j jr c rmic a ■

Para-Tedivs mollusk and osrracode raunas rrom the Black bea and Caspian

Plioccne. régions were analyzed.

MOTS CLÉS

magnétüstrati^raphic,

magnetozone.

polarité",

paléomagnétisme,

magnéti/tation rémanence,

I^ara-Térhys.

Plioccne.

RÉSUMÉ

Les résultats provienneiir d’érudes paléomagnétiqiics dans les dépôts plio¬

cènes de la Péninsule de Kerch, de Géorgie occidentale, d'Azerbaïdjan, de

furkménie, du nord de la Cis-Caspienne cl de la région du cours intérieur

de la Volga. Les informations provenant d'autres chercheurs sont utilisées,

ainsi que des données de l’auteur au sein et antérieures au Programme Péri-

Tethys. Les coupes paléomagnétiques composites provenant des régions

citées sont corrédées avec l'échelle magnétochronologique (Harland et ai

1982) du Neogène de Méditerranée. Sur la base des données paléomagné¬

tiques, des corrélations chronologiques entre différentes unités locales sont

revues. Les principaux stades de développement des faunes d^■)S^Tâcodcs et de

mollusques de la mer Noire et des régions de la Caspienne sont analysés.

GEODIVERSITAS • 1997 • 19(2)

471

Molostovsky E. A.

INTRODUCTION

The lon^ process clisintegration of the Tethys was

finisheci at the end of the Early Pliocène with che

isolation of the Pontic and Caspian basins, after

which thcir interconnections were but short and

incidenral. The independent development of the

post-Tethyan water bodics has affcctexl che compo¬

sition of ihcir faunal conimunitics. Faunal ende-

mism makes il difilculr to divide and corrclatc the

Plio-Pieistocene Fonnaüons in the Black Sea and

Caspian régions. Some local unies stlll lack any

commonly ateepted scheines of derailcd division,

many boundaries remain rather unclear, corréla¬

tions among the local unies and with the Neogene

beds of rhe Mediierranean are anibiguous.

The paleomagneiic scudies that have been perfor-

ined in the last forty ycars. hâve played an

important part in solving che problems of the

Pliocène stratigraphy of ihe eastern Para-Tethys.

During ihis period some dozens ut natural sec¬

tions and Wells in Turkmenia, Georgia,

Azerbaijan and the north-wcstcni Cis-Poncic

région were invesrigated, which has resultcd in a

vast palcomagnetic data array systemaiizcd on

the basis ot A. Cox magnecochronologic scale

(Harland et al. 1982). The most significanr

results of magnetostratigraphic rescarch are ana-

lyzed in ihe présent paper

The palcomagnetic rescarch in Azerbaijan and

western Turkmenia was carried out by Khramov

(1963), Frubikhin (1977), lsmail-/ade (1967)

and Pevzner (1973). Their data was used as the

basis for rhe corresponding parts of the présent

paper. The macerials from orher régions were col-

lected and analyzcd under direct supervision of

the auihor. The sections from Kerch Peninsula

and the North Cis-Caspian were studied within

the framework of the Peri-Teth}^ Programme.

While summarizing the results on Kerch and

West Georgia, the authors inform,uion was sup-

plemented by the data from Molostovsky et al.

(1982, 1983).

Of principal importance for the Pliocène magne-

tostratigraphy in the eastern Para-Tethys, was

A. Cox magnetochronologic scalc, used as the

basis for élaboration of stratigraphie relations

among local units and their position in the gene¬

ral magnetic polarity scale. The magnetostrati-

graphy of the Plioccne beds from the Black Sea

and Caspian régions, was cs.sentially formed on

die basis of A. Cox scalc^ and ihi.s is reflecicd in

ihc prcscnt paper.

The information on laboratory methods and for

the nature of natural rémanent magnetism

(NRM) can he found eisewhcre and are not

considered here givc référencés, the only excep¬

tion bcing ihe authors macerials on Georgia,

Kerch Peninsula, North Cis-Caspian and Volga

régions, wherc the Works were conducted under

his direct guidance (Fig. 1).

RESKARCH METHODS

The principal attention was focuscd on référence

sections paleonrohtgically wdl characterized.

Thcy were invesrigated in coopération wirh geo-

logists and paleonrologisis, Paleomagneric sam-

pling was made in parallel with fossil collection

which provided reliable stratigraphie référencé

for magnetozoncs. The “top-bortom” oriented

corcs were selecred from wells at the cime of their

extraction from the corers.

The sample rémanent magnetizarion was mcasu-

led with ION-1 and JR spinner rnagnetometers.

Température magnetic cleaning was performed

in rhe furnace.s wirh m-metal screens hy means of

successive heating iip to 400-500 ‘^C. Heating

régimes were sclecicd expcrimcntally with Ica-

ding collections ot 20-25 sampics. No less than

two cubes were selected ior thermal cleaning

from every level; their position in furnacc was

anti the parallel. Some sample.s were subjected to

control cleaning with alrernating field within a

Helmholtz coü System in the range of

16-40X lO -M/m,

To diagnose the compositions of magnetic

phases, oprical and X-ray structural analyses

alongside wirh diffcrenrial thermomagnetic ana¬

lyses (D FMA) were used, normal magnetizarion

CLirves, )r and Jrs, were mcasured, destroying

fields ol .saturation magnetizacions (H’es) were

determined.

Tlie characreristics listed above allow to judge

upon Curie points (Cp), rhe spcctra of blodcing

températures, sizes and oxidation degrccs of

magnetic particles and, as the resuit, upon chemi-

472

GEODIV6RSITAS • 1997 • 19(2)

Magnetostratigraphy of the Pliocène in Black Sea and Caspian régions

cal compositions of che principal magnctic phases.

To déterminé the natiiral rémanent magnetiza-

tion componenrs and their directions, ihe

samples were heared successively (in fifty incre-

menrs) iip ro 40(1-600 ®C. The. process of dema-

gnerizarion was analyzcd by means of Zijderveld

diagrams.

It is practically impossible to perform che labour-

consuming experiments on cach samplc, if large

collections arc being studied, with hundreds of

sampling Icvcis from many sections represented.

rherefore, to study the NRM component

contents and to make minéralogie analyses,

15-25 samples with varions lithologie composi¬

tions were selectcd from normal and reverse

magnetizarion zones in cach section, which made

about 20-25% of tlic overall amounts of the col¬

lections. ’l'he results thus obtained were c.vtrapo-

lated, each magnctozonc being providcd with

magnetic-mineralogic déterminations frorn at

least 5-10 stratigraphie levels, and narrow events

from at least 2-3 oncs.

rhrec types of NRM-carriers hâve bcen revealed:

1. Detrital magnetite constitutes the principal

magnetic phase in the Pliocène deposits of wes¬

tern Georgia and partially oi the Kcrch Peninsula

and the Low Volga région. It fonns angular and

subroundcd grains of 0.01-0.1 mm size. On

35* 40* 45* 50®

Fig. 1. — Location map showing studied sections. Sections: 1, well 1, 5, 13, 14, 15, 18, 19 (Samara Région). 2, well 3 (Saratov-

Volga région). 3, well 20 (Saratov-Volga région). 4, well 13 (Kalmykia). 5, well 48 (Kalmykia). 6, Kerch Peninsula. 7, West Georgia.

GEODIVERSITAS * 1997 • 19(2)

473

Molostovsky E. A.

0 100 »oo aoo 400 soo eoo roo C*

sam. 810/26 (Arahintsevo, Kerch PenInaulaJ

Fig. 2. — Differential curves of thermal demagnetization of

Pliocène samples: A. B, magnetite samples; C, hydroxyde

samples; D, authigenic greigite and pyrrhotite samples.

ContinuoLis line, first heating; pecked line, second heating.

DMTA curves ir h markcd wirh sharp Js dip at

570-580 °C. It does not display anyclear cfFect in

Cp in l^inely dispcrsed fracrions and is characte-

rized by a wide range of blockiag températures

with the Joss of Js et around 570 ”C (Fig. 2A, B).

2. Iron ores from tke Kerdt région and some red

clays from the Volga région possess rémanent

magnetiz^tion duc to findy disperscd iron oxides.

DMTA curves of thc.se rocks slmw |s dips in the T

range of 150-250 and at hématite Cp (Fig, 2C)

Normal magnetfzadon ctirvc.s for ihc rocks of the

first and second groups arc presented in figure 3A.

3. Wirhin a substanrial portion of the PÜoeene

clays from the North Cis-Caspian and Volga

régions, rhe chief Jn carriers atc tcpfcscnccd by

authigenic iron sultidcs of the FeSx type with

1.1 <x^ 1.6.

Authigenic magnetic sulfides are morphologically

diverse and occur ;is rounded, tubular or irregu-

lar aggregates that concentratc in accumulation.?

close to vcgccabic détritus, frequendy in associa¬

tion with pyrite. Optical and X-ray analyses hâve

proved them to be melnikovlte (greigite) from

1rs

Fig. 3. — Curves of normal magnetizatlon. A, magnetite

samples; B, hématite samples.

the Cp of 380 and 420 (Fig. 2D). Magneto-

thcrmal analyses occasionally reveal hexagonal

pvrrhotine among the sulfide.s, producing cha-

racteristic peaks m the 260-300 “C range (transi¬

tion to monodirui modification).

A sériés of paleoinagneiic-sample thermal clea-

nings wirhin the température range up to 500 ®C

was petformed for the analyses of rémanent

magneti/.arion componenr vectors. The resulcs

werc used to construct Zijdervekl diagrains.

Twü components are characteristic of derrital

NRM-carriers in the sections from western

Georgia: che primary component. synchronous

with sedimeni génération, and the secondary

one, viscous, formed dunng subséquent géologie

epochs. The mcrachronous secondary magnetiza-

tion is completely cleared away when rock

samples are heared up to 100-200 °C (Fig 4A-

D), leaving behind the truc direction of the pri¬

mary rémanent magnecization.

Three N RM-components are characteristic of

the Pliocène day.s from dic norchern Cis-Caspian

and Volga régions (Fig. 4E-H). The viscous

secondary magnetization isv as a rule, cleared

away when a rock sample is heared up co 100 “C.

The primary magnetization, synchronous with

scdinienc déposition iS associated with authigenic

sulfidcs and does not change its direction mar-

kedly when heaied up ro 200-300 “C When a

sample is heated above 300-400 metachro-

nous stable magnetization Is displayed, a.s.sociated

with the secondary minerais magnetite and

hématite which arc formed wiihin rocks as the

resuit of primary sulfide oxidation. These com-

pojients are inost clearly seen in the samples

from R-zones (Fig. 4E-H).

474

GEODIVERSITAS • 1997 • 19(2)

Magnetostratigraphy of the Pliocène in Black Sea and Caspian régions

Fig. 4. — Zijderveld diagrams of thermal demagnetization of the Pliocène samples. West Georgia (A-B) and North Cis-Caspian

région (E-H).

GEODIVERSITAS • 1997 • 19(2)

475

Molostovsky E. A.

A similar proccss is' observed in laborarories

when collections are storeci for long periods.

Reversely magnetized sanrples in such cases ffe-

quently acquire stable normal rnagnetization.

The change of magnevi/.ation polarirv' resulring

trom the innuctice of the secondary magnetic

phases afrcr the destruction ol primary sulfides is

clearly demonsirated m figure 4E, H.

The basic problcm of any paleomagneric study

(providing evidence for NMR prîoricy and geo-

physical nature of magnecozones) can t be ulri-

mately solved tluough laborarory experiments.

Some indirect tests prove to be helpful, which to

a certain degtee help to dernonstrate the validiry

of conclusions on NRM primary nature.

To achieve rhis» beside the conventional tests

(Khramov & Sholpo 1967; Khramov 1982), a

number of additional features were used, appli¬

cable to the séquences wiih various compositions

and dislocation dcgrccs:

1 . The closeness of Jn veccor distributions was

compared berween rocks from various lithologie

groups. In case of detrical magnétisation, close¬

ness of Jn vectors in psammire-class rocks should

gencrally bc less chen in aleuro-peliies.

2. Jn polaricy independence of lithology faciès

and magnetic phase compositions was esrimated.

Association of various-rype rocks to the zones of

the same rnagnetization, and on the contrary,

alternation of diverse-polarity zones within the

monofacies sections, were regarded as indicative

of the primary nature ol NRM.

3. Geophysical nature of magnetozone^s is indica-

ted by their latéral scabilir 3 % consistency within

certain straiogenctic sériés: marine, dcltaic, allu¬

vial and othcT faciès, Testing of outer convergence

with corresponding paléontologie and radiome-

tric controlsj is probably the srrongest argument

for confirming the primary characrer of NRM.

Some results of magnetostrarigraphic research of

the Pliocène dept^site from individual régions are

presented below

REGIONAL MAGNETOSTRATIGRAPHIC

SCHEMES

Western Georgia (Guria)

The author in coopération with paleontologists

Kitovani and Imnadze has examined forteen sec¬

tions. The whole of the western Georgia’s

Pliocène is presented in dear sequence with mul¬

tiple overlappings: from the ba.se of the Pontian

through the top of ihe Gurian Chauda. This

chick complex of lerrigenous scdimenis is radier

tnonotonous lithologically. Bluc and dark-grey

massive clays ajid alcurites prevaÜ over subordi-

natc inicrlaycrs of polymiccic sandscones.

Stratigraphie division of the sequence îs perfor-

med according to oscracode and mollusk faunas.

In the présent paper it is .subdivided from the

boitom to the top of the section according to the

schemes by Kitovani and Imnadze (Kitovany

1976).

The PontUm stage ( 180-210 m)

Characieri.scd by a spécifie mollusk fauna:

Congetia digitifera Andrussow, Paradaena ahichi

R. Hoernes, Monodaena psciuiocafdns Barbot de

Marny, etc,

The Kimmeriart régional stage

According lo the mollusk fauna, ii is subdivided

into a lower (Azov) horizon (8-12 m) with

Linmocardinm Andrussow et al. The middle and

the upper horiz.ons are not divided (30-70 m)

but established from the appearance of Dreissena

ptdyntorpha Pallas, T>. angusta (Roussean),

Didacfia cnmatelhta Oeshayes, etc.

The Kuyntnikian régional stage

Represented by layers with mixed Kimmerian-

Kuyalnikian malacofau na and typically

Kuyalnikian bedding with Dldacna medea

Daviaschvili, Suhmodaena plevnexia Daviaschvili,

Monodaena posidonacotdes Daviaschvili. etc. The

overall ihickncss of the Kuyalnikian thus defmed

con.stirures 15-20 m.

The Gurian horizon (80-90 m)

Begins with lieds conraining Dreissena ex gr. ros-

trijhiinis Dcsliaycs. The main part of the section

is charactcrizcd by Digressodanta minor Kitovani,

D. digressa (Livental)j D. Kitovani, etc.

The Nagobilei^sky (Chauda) horizon (50-90 m)

Is at the top of the Pliocène section in western

Georgia and may be lowermost Pleistocene in

476

GEODIVERSITAS • 1997 • 19(2)

Magnetostraiigraphy of the Pliocène în Black Sea and Caspian régions

part. The (juri.in Chauda \a characteri/ed by rich

and diverse malacofauna: Digressoducna graciüor

Daviaschvili, TshaudiDUssa T guriana

Livental, Didacna (yseudocrassa tipica Liventah

etc.

The Pleistocene

A 90 m thick sequence of sands with subordinate

clay interlayers cxposed in nvo sections studied

containing ostracodes that are characteristic of

ancien t euxinic beds: Caspiola gracilis hacuana

(Lubimova), C acronasuta (Livental), Lepto-

cythere bkornis Asianova, etc.

Comparison

The Pliocène deposits from svestern Georgia are

charactcrized by high magnetism with regitlar

distribution of Jn and æ values over the stratigra¬

phie section. I he lowcr parc of rhe [*ontian is

relatively low inagnctic (Jn = 3-17 X 10-^ A/m,

ar = 10-50 x 10*^ SI units), In the Llppcr Ponuan

and Kimmerian beds, these parameters are

20-40 X 10 -’ A/m, æ = 100-280 X lO^'' SI units.

The Upper Pliocène parc of the section, rock

magnetism rcaches ilic maximum values: Jn =

40-150 X lO-^ A/m, æ = 300-1400 x 10 ^ SI

units.

Optical methods and DTMA hâve revealed

detrital magnetire grains of 0.1-0.005 mm size in

ail lithologie rock variecies. It may bc présent as

even smallcr, dust-like particles. No other pro¬

bable NRM-carrieis wcrc detected in rocks.

Detrital ongin of the optically diagnosed magne-

tite is esiahlishcd from angular grain outlines,

wacer-tran.sportation marks in ihe form ot

scracches and scores, aggregations with silicate

minerais. There is the dependence of magneric

fraction distribution on the rock tcxrural fea-

tures: accumulation within oblique sandstonc

interlayers, duc to nauiral lewashing of sédi¬

ments, inercased concentrations in basal layers,

accumulation.s of dusL magnetite particles on

lamination plane.s.

The share of metachronou.s viscous magnetiza-

tion reaches 60-70% of lhe sum Jn, but in most

samples it is redueed upon heating up to 200 °C.

No peculiariiies wcrc observed in the behaviour

of NRM vcctors relative to rock lithologie or

faciès compositions. Just a wider dispersion in Jn

directions is observed in sandstones compared to

aleurolites and clays. At the samc cime, regular

distribution of normal and reverse magnetizarion

intcrvals îs ob.scrvcd along the rime scale, as well

as their récurrence in the sections, rcliably refe-

renced according to fauna.

Paleomagnciic zonaliiy peculiaritics in the

Pliocène and Quaternary deposits from sonie

refemnee .sections are presented in figures 5, 6,

paleomagnctic corrélation of the sections in

figure 7.

Comparisons of the individual columns make it

possible to discinguish four magnetozoncs, com-

plicated with narrow opposite-polariry sulr/ones,

within the recenr deposits Irom western Georgia.

The fîrst from below Rn zone includes the whole

of the Ponrian plus the Power and the Middle

Kimmerian. In rhe upperniost part of tlie

Ponrian and in rhe Power Kimmerian from

Khvarbcti IP Makharadze and Gogoreri-Meriya

sections, four n-subzones are traced, each orie

from 3-6 m thick. The middle Kimmerian depo¬

sits arc reversely magnecized everywhcre. On the

wholcv rhe structure of ilie lower Rn intcrval, as

well as the stratigraphie range occupied, make it

possible to refer the interval to the Gilbert Zone

in the general magnetochronologic scale.

The lowcr Kuyalnikian and upper Kimmerian

parts of the section, redueed due to ancient éro¬

sion, are relatively less well known The upper

Kimmerian in rhe Khvarberi 11 oiitcmp is com-

posed of normally magneri/.cd beds with the

apparent thickness of about 5 m. The lower

Kuyalnikian horizon aiso reveals normal polarîty

Jn within outerops along rhe Skurdiibi and

’Psina-Gele rivers and in some other localities

where the apparent thicknesses at outerop cons-

rittite 6-8 m (Fig. 7).

Zubakov (1990) establishcd the stratigraphie

range of this N-zone within parallel sections with

the upper Kimmerian and the lower Kuyalnikian

and identifîed it with Gauss Zone.

Srratigraphically higher, thece is a large reverse

polarity intcrval cmbraclng the Nagobilcvsky

(Chauda), Gurian and tlu* upper hait of the

Kuyalnikian and unambiguousaly identified with

ihc Matuyama Zone. Four successive N-sub-

zones were recognized and traced along the sCrike

within this zone: from the middle of the Chauda

GEODIVERSITAS • 1997 • 19(2)

477

Molostovsky E. A.

KHVARBETI II

ë I 3

^ O

« g X

PALEOMAGNSTIC

CHARACTERISTICS

D I

ZiQ 0 60 120-90 0 ^90

FOSSIL REMAINS

MOLLUSK:

Dreissenaex gr. rostreformis Desh.,

Pyrgula sp-, Micromelania sp.

OSTRACODE:

Pontoniella acuminata (Zal.),

Pontonielfa pcntica Agal.,

Caspiotls acronasuta (Liv.),

CaspioHa venustâ (Zal.),

CaspioHa Oalcanica (Zal.),

Caspiolla karatengiaa Mand.,

Caspiocypris labiataiZa\.),

Bacunella dorsoamiata (Zal.),

Paracanriona aff varrncossa (Stant.),

Leptocythore bosquaU Liv.,

Leptocyîhare guriana li-nn.,

C^^fwrisii t) 0 gatshovi Liv.,

Turrt^enocymerp pstudoconvexa (Liv.),

Turrhanocytherc rfawctii Imn.,

Loxocrmchà caliokyi Rtep.,

Loxoconcha paraflela Muller

Loxoconchapesata Liv.,

Loxoconcha tshaudae Imn.,

Xesioleberis chanakovi Liv.,

LoxocornocuUna tf/a/yarov/Schn.,

Pontoleberis pentica (Stan.).

MOLLUSK;

Dreissena anisoconcha chohensis Tset,

Didacna mediae David., Ecericardium sp.

OSTRACODE:

Pontoniella acuminata (Zal.), Caspiolla

venusia (Zal.), Bacunella dorsoacuata

i (Zal.). Caspiocypris reticulata Krst.,

\Leptocythôre andrussovi Liv.

MOLLUSK;

Dreissena anisoconcha chonensis Tsel.

Pseudocatillus pamau (Shwets.).

Zagrabicê sp.. Macradacna sp.

OSTRACODE:

Pontoniella acuminata (Zal.), Pontoniella

ponUca Agal., Casp)of(a liventali (Evn.).

1 Caspiocypris latiai3{Za\). Bacunella

\dofsoarculata (Zal ), Cythenssa

Ipoga^shoW Liv

MOLLUSK;

Dreissena decipiens M.

IISI

Fig. 5. — Paleomagnetic section of the Pliocène deposits of western Georgia.

478

GEODIVERSITAS • 1997 • 19(2)

Magnetostratigraphy of the Pliocène in Black Sea and Caspian régions

in the top of thc Gurian, at the Gurian-

Kuyalnikian boundary, in the iipper part of the

Kuyalnikian (Fig. 7).

The first, third and fourth subzone.s are most

logically intcrprcrcd a.s bcing analogous to the

Jaramillo, C31duway and Réunion épisodes. The

second subzone, from thc uppermost Gurian

with the Kwcmo-Natancbi épisode, has also been

recognized by Zubakov 6c Kochegura (1976) at

the same stratigraphie Icvel in western Georgia.

The age of ihe later according to ihermolumines-

cent analysis is 1,1-1.2 Ma; chronologically simi-

lar N-subzones hâve bcen found within basaltic

covers of Madeira l.sland and in California

(Mancinen 1978).

The upper zone of normal magnetization corres¬

ponds CO the ancient euxinic beds aitd from its

stratigraphie position may bc idcntificd with the

middlc part ol the Brunhes Zone. It is coraplica-

ted with a reverse-sign subzone, most possibly

LEGEND FOR FIGS 5-8, 11

Natural rémanent magnetization

Magnetic susceptibility

N, n

Normal polarfty Jn

R. r

Reverse polarity Jn

Intervals of normal polarity (N)

□

Intervais of reverse polarity (R)

Absence of deposits or absence

of polarity data

—

Clay

UT U

Aleurolite

Sand

Sandstone

Limestone

1-1

Iron ore

P Q O ol

Pebble and gravel

K—1

Gap

|A|

Mollusk

1^1

Ostracode

analogous to the Lower Khazarian (Dnieper) épi¬

sode with thc absolute thermoluminescent

datingof 0.35 Ma (Zubakov 1990).

THF. NORTH-WESTEKN CiS-PoNTIC REGION

The recenc deposics from Taman> Kerch

Peninsula and norchern Cis-Azov région were

paleomaguerically studied by Tretyak 6c Volok

(1976), Semenenkü 6c Pevzner (1979),

MoJostovsky étal. (1984) and Zubakov (1990).

Individual portions of the section are presented

hcre from natural ourcrops. A continuons succes¬

sion was studied by Semenenko & Pevzner

(1979) from the well cores. Up lo now, practical-

ly the whole of the Pliocène sequeiicc trom the

base of the Pbnrian stage rhtough the overlaying

Picistocene loams has been characterized paleo-

magneticallv (F.ber/in 1940).

The Pontian stage

With the characteristic malacofauna of Para'

dama. Valenàennius and Congeria, it is represen-

ted h)' 20-120 m thick monotonous grey clays.

The Ktmmerian stage

The Kimmerian stage, as distinct from the

Pontian, is lithologicaJly well dilFercntiated. Its

lower (Azov) horizon, when présent, îs distingui-

shed by its variable composition. Thi.s consists of

clays, iron sands and poor iron ores in Taman; in

the Chegerclia synclinc in Kerch Peninsula, it is

recognised witliin a clayey monofaciaJ .seccion by

the substitution of tJie Pontian Parndaena abkhi

R. Hoetnes by the Kimmerian Paradaena defbr-

misy Drehscnn rostriformis Deshayes, etc.

The middle (Kamyshburun) horizon is built of

massive iron ofe.^ tonraining al?undant Dreissenay

ParadaenUy MunodacnOy etc.

The top (Panrikapei) horizon is composed of

grey and olive clays with thin interlayers of poor

iron ores.

The thickness of the Kimmerian does not exceed

20 m wichin the zones of shallow-water sédimen¬

tation and increases up to 220 m in the axial

parts of the synclinal basins.

The Kuyalriikian stage

The Kuyalnikian stage in the easrern part of the

Kerch Peninsula lies unconformably upon

GEODIVERSITAS • 1997 • 19(2)

479

Molostovsky E. A.

STAGE

LITHOLOGY

FAUNA

POLARITY

PALEOMAGNETIC

CHARACTERISTICS

O f

150370 0 90 '900 *90

MAKHARADZE

FOSSIL REMAINS

lij

to-

15-

20-

25-

30-

40-

50.

■

MOLLUSK: Dreissena polimorpha veberiSer).,

A Dr. andrus (Ronss.), Phyllocardium planum Desh.,

\ (Pall.), Limnocardium {Tauricardium) sguamulosum

\ Desh., Didacna {Crassodaena} crassatefeta Desh.,

\ O. crassafeteta tigona Andrus., Monoofaena

\ polemonts Schwels,

r=:

\ MOLLUSK. L/VT?noca/-d/üfn sguamulosum Desh.,

\ Phyllocardium planum Desh, Phyllocardium alaîoplanum

\ Andr., Stenodaena anguticostata Ronss.

MOLLUSK: Dre/ssena aff. iniguivalnis Desh.

Didacna multicriata Ronss., D. depressa Desh.,

Paradaena abichiP. Horn., Plagiodacna carinita Desh.

Fig. 6. — Paleomagnetic section of the Pliocène and lower Pleistocene deposits of western Georgia. Legend: see figure 5.

480

GEODIVERSITAS • 1997 • 19(2)

Magnetostratigraphy of rhe Pliocène in Black Sea and Caspian régions

Fig. 7. — Paleomagnetic section and corrélation of the Pliocène deposits of western Georgia. Legend: see Fig. 5.

GEODIVERSITAS • 1997 • 19(2)

481

Molostovsky E. A.

various Kimmerian horizons. le is represented by

a 12-16 m thick unit of bluisb-grey clays and

sands. The thickne.s.s of ihe Kuyalnikian beds is

as high as 80 m in tlie Chegercha .synclinal fold.

The Dreisstna (and Lymnovardiitm) containing

bearing layers belong to the lowcr Kuyalnikian

here, and the ovcrlying Taman layers with

Avimactra mbcaspia Andrussow and Cardium

dombra Andrussow to the upper Kuyalnikian

(Nevesskaya étal. 1986).

Continental analogues of rhe marine

Kuyalnikian are common in rhe Cis-Azov région,

wirh the well-.studied sequences of small mam-

mal from the lower (Kuyalnikian) and the upper

(Odessian) parts.

The Kuyalnikian scquence is succeeded by the

Tyup-Djankoi beds; rke Pliocène section is crow-

ned with a clay member atrributed to rhe

“Gurian" layers. The Tanianian beds may serve

as a good corrélation référencé; chey overlie older

deposirs and are recognized by the Actchagylian-

rype mollusks.

Cornparhon

The Pliocène deposits from Kerch Peninsula and

rhe adjacent areas are generally low magnetic:

Jn = 0.3-0.8 X 10-^ A/m, æ = 10-15 X 10'^ SI

units. In the iron ores Jn reaches 1-2 X 10 X

10 ^ A/ni,. æ =r 20-55 X 10 *’ SI units.

The magnetic pvoperties of chc bulk of the rocks

are derernuned by fine clastic tnagnecite. In iron

ore layers, NRM is mainly canied by authigenic

FeO.OH and FC 2 O 3 developcd over siderite and

chlorite.

Substantial metachronous magnetization, coinci-

Fig. 8. — Paleomagnetic section of the Pliocène deposits in Kerch Peninsula. Legend: see figure. 5.

482

GEODIVERSITAS • 1997 • 19(2)

Magnetostratigraphy of the Pliocène in Black Sea and Caspian régions

ding with the reccnc field, is présent practically

in ail the rocks. \xs main pari is destroyed in the

200-300 température. Jn components allow

to judge on the seaion magnetic zonalities quite

confidently. Tt is necessary co note chat the distri¬

bution of the normal and reverse magnétisation

intervals doesnV dépend on lithology, faciès or

composition of magnetic minerais. It is seen

from figure 8, chat the layers with detrital

magnerite from varions pans of the section are

characrerized by NRM of various polarities. At

the same time, within the middlc Kimmerian,

the ore horizons with chemicai rémanent magne-

tization reveal the same Jn polarity as the hosting

clays with allothigenic magnetite.

Paleomagnetic columns for the principal sections

Fig. 9. — Paleomagnetic section and corrélation of the Pliocène deposits of north-western Cis-Pontic région. I, Chegercha synclinal

fold (Semenenko & Pevzner 1979): II, Tobechnik; III. Arshintsevo (II, III: Molostovsky 1986): IV, Arshintsevo; V, Lubimovka

(Sevastopol); VI, Krasny Kut; Vil, Babach-Tarama; VIII, Kryjanovka; IX, Liventsovka (IV-IX: Treyak & Volok 1976); X, Taman

Peninsula (Zubakov & Kochegura 1976).

GEODIVERSITAS • 1997 • 19(2)

483

Molostovsky E. A.

from the Crimca and Taman are shown in

figure 9. l'heir coinparison demonsiratcs a simi-

lar sequence in magneiic polarity changes along

the stratigraphie seule.

The Pontian .stage is evcrywhere characterized by

reverse magnciizatiüii. 1 he niain part of the

Kimmerian section is composcd of the rocks

wich dominating reverse polarity Jn; four normal

polarity subzones are distinguishcd there

(Semenenko & Pevzncr 1979), Highcr in the

section, a normal magnctizarion inccrval is rccor-

ded, embracing the mo.st of the upper

Kimmerian and tlie lower Kuyalnikian. In the

upper Kiirimerian part of the section, two reverse

polarity sub/ones are documented in the Pake

Tobechik section. The upper Kayalnikian

(Taman layers) is everywhere composed of rever¬

se polarity Jn rocks.

The similar paleomagnetic column structure is

characreristic of ihc continental analogues of the

Kuyalnikian régional stage. The lower horizon

with the Kuyalnikian microtheriofauna rhere is

characterized by normal magnetizaiion, the

upper one, characterized by the Odessa small

mammal complex, is revcrsely magnetized

rirccyak & Volok 1976).

The rcverse-polarity intcrval passes on from the

lamanian layers to the Tyup-Djankoian and

Gurian beds and terminâtes in the lowcrmost of

the covering loam séquence, the major portion of

which forms a part of Prunhes magnetozone.

The order revealed in the Pliocène magnetozone

strarigraphy (R, N, R), combincd with reaso-

nable rcliablc paléontologie control, allows corré¬

lation of the magnctozoncs with Gilbert, Gauss

and Matuyama zones. Their stratigraphie équiva¬

lents are:

1. For Matuyama Zone the upper Kuyalnikian,

Tyup-Djankoian and Gurian beds.

2. For Gauss Zone the upper horizon of the

Kimmerian and the lower Kuyalnikian; r-sub-

zoncs of the Paniikapci horizon probably corre-

lacc with the Kacna and Mammoth épisodes.

3. Gilbert Zone may involve the hulk of the

Kimmerian and the Pontian srage as it is seen in

the north-western Cis-Pontic région. N-subzones

of the Kimmerian pan of the section may bc as a

group identified with Gilbert-zone épisodes.

Thï. north^kk Cis-Casi'1An and

l.OW Veux. A RF.r.lON

'Fhe Pliocène deposiis fmm ihis vast région are

poorly .srudied palcumagnctically, and at présent

the data on just eight référence wells are avai-

lable. The principal Upper Pliocène unies from

the Caspian région hâve been rccognized thcrc

according to ostracode aitd mollusk fàunas. The

sections were paleomagnetically studied by

Er>'omin under the guidance of Molostovsky;

mollu-sks wcrc defined by Fcdkovich and ostra-

codes by Karmishina. 'Fhc principal stratigraphie

and paleomagnetic data on ihe sequence are

given belüW (Ki>lesriikov 1940; Nevesskaya et al.

1986; Muratov & Nevesskaya 1986).

The AetchagylitiH régional stage

Is xiibdivided iiuo threc substages according to

die existing stratigraphie scheme, but the lower

Aetchagylian deposits in the Volga région are

sporadic. In the sections studied, they hâve been

registered only in well N3, wliere a 17 m thick

clay member concaining Dreissena polymorpha

Pallas, Pisidittm arnnicion Muller Planorbis pla-

mrhh Linné, was assigned to the lower substage.

Fhe middle substage, built of clays and aleuro-

liccs is common; it ovcrlies various formation

unconformably right down to the Upper

Cretaceous and is characcenzcd hy rich and

diverse mollusk complex: Cerastoderma vodgù

(AndrussowO, C konschini (Andrussow), C. pseu'

daedfilc (Andrussow), Avirardiiim tnkttini

(Andru.ssow'), Avimnetra venjukovi (Andrus.sow),

Ao. suheaspia (Andrussow') and by ostracodes;

Loxoconcha varia Suzina, Candona convexa

Livcncal, C Livental, Leptocytheregubkini

(Livcnial), etc, l’he middle Accchagylian is

14-125 m thick.

The upper Actchagyhan substage conformably

ovcrlies the middle one and is represented by

20-70 m thick interbedded aleurices and sands.

Small Dreisscnar Avimnetra subcasptn (Andrus-

sow)^ Ceraswderrna dombra (Andrussow) are

known as well vis ostracodes: Paracypridcu napha-

tntîchobinn (l.ivenraJ), Cyprideistorosa (Jones), etc.

The Apsheroninn régional stage

Division of this into three parcs is commonly

accepted. The lower substage is restricted to che

484

GEODIVERSITAS • 1997 • 19(2)

Magnetostrarigraphy of the Pliocène in Black Sea and Caspian régions

South of thc icrnrory (wells Ni, 123)* where it

conformably overlies the Accchagylian Jeposics

and is separated Irom the later ones by a mono-

tonous, poorly fossiliferous sériés cont-aining

mainly re[ncscnt.ittvcs ol Dreissena Qcn\is: D. dh'

tincia Andrussovv, D. polymorpha (Pallas),

D. eichwaldi Andrussow, etc.

The lower Apsheronian are lithologically repre-

sented by grey aleuriric clays 14-18 m thick in

thc wells invcstigated.

The middie Apsheronian over most of the région

transgressively overlies the erodcd surface of the

Actchagylian structures. It i.s coniposcd ol grey

calcareous-clays, aleurires and sands containing

rich mollusk assemblages: Pampscheronia rarico'

stata (Sjogeren), P. eurodtsma (Andrussow),

Monodacna rninor Andrussow, etc; its thickness

ranges from 60 to 330 m.

The upper Apsheronian is lithologically similar

CO rhe middJe Apsheronian and rhere is a graduai

iransition hctwcen chem. This intcrval of thc sec¬

tion is characterized by sharp déplétion of mala-

cofauna dominated by small Dreiisena. Rare

remains ol Â'înnüdacua, smooth Apschenmia,

Pseudocatillus occur. The upper Apsheronian

deposits are 20-40 m thick.

Comparison

In many sections, the rhythmic character of sédi¬

mentation is well pronounced. Each rhythm

includes a sandy (régressive) and a clayey (trans¬

gressive) member, with a sum thickness of

30-50 m. Among the autlugcnic minerais, sidc-

rite and iron hydroxides are characreristic of

régressive lacies. wbile magnetic iron sulfides and

pyrite are characteristic of transgressive unes.

Fine clastic (0.05-0.001 mm) magnetite in

varions amounts is présent in ail rhe faciès.

WELL n^13 s. KUMSKOY, KALMYKIA

FOSSIL REMAINS

MOLLUSK:

Pseudocatillus sp.. Dreissena sp., Adacna sp.

OSTRACODE;

Aurilfa aierdajdjanica (Lw.). Laxoconçha ex

gr. rugosa Step., Leptocythere pirsagatica (Liv.)

MOLLUSK:

Parapscheronia rancostata (Sjoegr.L Pseudosatillus

dubius (Andfüs.). Monodacna sjoegreniumAnôrus.,

M. laevigata Andrus.

OSTRACODE:

Aurilla azerbajdjàOtcâ (Liv.J. Caspfalta acronasuta

Liv., Cyprideis torcsa Jones, Cryptocypnd&s

bogatsbov'f (Uy.) _

MOLLUSK: Dreissena carinatocurvata Sinz..

Micromefanatà subcaapfa Andrus .

Monodacna sp-, Pseudocatillus s\).

I OSTRACODE:

\ Paracyprideis naphtschclana (Üv.), Casploila

\ acronasuta (Uv ). Leptocythere

\ multftuberculaiailW.].

MOLLUSK:

Pseudocatillus sp., Dreissena so.,eic.

OSTRACODE:

Casprolla acronasuta Liv., Paracyprideis

naphtatsholana (Liv.). Cypridefs torosa Jones.

OSTRACODE:

Caspiolla acronasuta Liv., Paracyprideis

naphtatscholana (Liv.), Cryptocyphdeis

bogatshovi {Uv.), etc.

Fig. 10. — Paleomagnetic section of the Pliocène deposits of the wells (settlement Kumskoy, Kalmykia).

GEODIVERSITAS * 1997 • 19(2)

485

Molosrovsky E. A.

Transgressive and régressive sédimentation stages

are recorded by sharp variations of scalar magne-

tic characteristics. )n rransgressive clay faciès, rhe

values of Jn = 20-150 X 10*^ A/rn, æ =

80-500 X 10 ^ SI unies. In regre-ssive sand faciès

Jn = 0 5 X 10'^ A/m, a! = 10-30 x 10 '' SI unies.

The magnetic-mineralogic anal}^cs bave revealed

aurhigenic iron sulfides of the pyrrhotinc-greigite

(melnilcovire) group to bc the main NRM-car-

riers in ehe transgressive parts of the chythms. In

IWELL 3 KOSHELf

FOSSIL REMAINS

MOLLUSK: Dreisena polimorpha Pall.

OSTRACODE: Paracyprideis strachanensis Karm.

MOLLUSK: Cerastodffrna psoudoadule (Andrus.),

C. vogdti f Anda»ï> ). Avicardium kfi^^elini (Andrus.),

Avtmacifs ossosküvi (AndruB.i

OSTRACODE; Candona canvcMLly..

Prntymnocyther^ ^ 0 ? , Cyptideis torosa

Jones-, C. pitoceniciî Roe.. Qf-

pseudoarmaM. Rop.. Loptocyih^rff gubkini

Liy/., Loxoconcha vana Suz..

Paracypndeis ex rjr. asttanbansis Karm.

MOLLUSK: Dreisena polimorpha Pall., Pisidium

amnicum Mull., Planorbis planorbis 01.

PALEOMAGNETIC CHARACTERISTICS

J-10-3A/m

WELL 20 ALEXANDROV GAY

FOSSIL REMAINS

OSTRACODE: Leptocyîhere martha (Liv.).

Paracyprideis atf. astrachensis Karm.

MOLLUSK: Parapsihoronta rancostata (Sjoegr.),

Pseudocatillus (Andrus.). Monodaena sp..

Addcna sp. Inder. Hyrtaniasp., Dreissena distincta

(Andrus.). Caibicula ^minalts apscheromca

/Andfus.j

OSTRACODE: Lôptocyîhere camelii {LN.),

Loxoconcha petasa Liv - Caspiccypris mandelstanv

{â:hw.). Advenocypriskurovdagensts Klein.,

Pioiimnocythete aW scharapovae (Schw.)

MOLLUSK: Avimacira subcaspla (Andrus.),

Cerastodermacl dombra (Andrus.)

OSTRACODE; Paracypndeis naphtatscholana

(Liv.), Prolimnocythers tonnireticulata (Suz.)

MOLLUSK: Cerastodermâ vogdl/(Andrus.),

C. ((onsert/nr(Andrus.). Avicaidfum nikitini

(Andrus.), Awmacira veryv)cov/(Andrus.). Av.

kobsnikûvi (A A Z.). Av. iriostranzevi (Andrus.),

Clessiniola

ulvensis (Andrus.), Pirenella caspius (Andrus.)

OSTRACODE; Loxoconcha varia Suz.,

Prolimnoeyihere ischaplyg\r\ae (Suz.), Candona

convexa Liv,. Leptocythere gubkini (Liv.),

Paracyprideis naphtatscholana Liv..

Cyprideis rorosa Jones., etc.

Fig. 11. — Paleomagnetic sections of the Pliocène deposits in Saratov-Volga région.

486

GEODIVERSITAS • 1997 • 19(2)

Magnetostratigraphy of the Pliocène in Black Sea and Caspian régions

régressive sand fades, rnagncnzation is determi-

iicd hy chistic magneute. l’hus, in mosi sections

of marine Pliocène froin the North Cis-Caspian»

alcernating intervals are observed: these oi domi¬

nant décrirai ur cheniical rémanent magnetiza-

tions.

One should be especially cautions while interpre-

ting the data on the rocks Avirh rheir magnetiza-

tion caused by auchigenic sulfides. The lutter

ones are quickly oxidized under atniospheric

conditions, thus, lhe cores should be analyzed

nor later than in mo lo thrcc weeks afrer extrac¬

tion froin the Wells. Wltilc anulyzing the results,

those ol" the frrst rhcrn'ial cicaning srep (below

350 “C) and ihu.se of the second one (550-

580 ”C) separacely. At rhe frrst stage, chemical

rémanent inàgtietizaiion is dominant in such

rock types; ai the second stage, afrer pa.ssing the

Curie point for sulfides, magnetite remuins the

only NRA1 carrier.

To coDStriicr rhe paleomagnetic colurnns, rhe

only samples used were chose with the chemical

and detrital Jn componeius revealing rhe same

type of oricncaticm in space (Fig. 4E-M),

Noiwithstanding the différences in lithology,

faciès and compositions of magnetic phases,

therc is a stable temporal regularity in the beha-

viour of narural rémanent magnerizacion in the

rccent dcposics from the North Cis-Caspian and

Volga régions.

Within rhe range from the lowermosi part of the

Pleistocene to the lower Actchagylian inclusive,

two large paleomagneric intervals are omnipré¬

sent: the upper, reverse polarity one, and the

lower, normal polarity one. The revcrse-polarirv

zone accounts for the whole of the Apsheronian

and the upper half of rhe Actchagylian stages and

the normal-polarity zone corresponds to the

lowermost middie and lower Actchagylian

(Figs 10, 11).

Matuyama and Gauss zones raay be considered

as their analogues in magnetochronologic scale.

Within rhe Maruyama Zone, snme narrow nor-

mal'sign zones hâve been revealed, whidi may be

correlared according to their srraiigraphic posi¬

tion with Reunion (middlc-upper Actchagylian

boundary), Olduwai (the base ot the Apshe¬

ronian) and Jaramillo (the uppeimosi middie

Apsheronian) events.

W£;s‘iTiw Fukkmknia

Paleoinagnctic .srudics of the Plioccne deposits in

the Trans-Caspian région were carried ont sepa-

rately by Khramov (1963) and ‘frubikhin

(1977). Rhmmov (1963) has investigated rhe

Middie Püoeene red-bed (Chclcken) Formation,

Actchagylian and Apsheronian régional stages.

Frubikhin has examined the Upper Pliocène

seqtience comprisiag the Apsheronian and

Actchagylian stages.

The Chclcken Formation

The Cheleken Formation is composed of red and

grey clays, aleurolites, sandstones and contains

rare remains of rnollusks Turrucaspia sp.,

Hyrobin sp. and hrackish-waier o^stracodes of the

généra Hiocyprh, Lirnuocythere^ Cyprinottis.

Maximum ihickncsscs occur in the Cheleken

PeninsLila (2600 m) and they reduce to

200-300 m to the east (Muraiov & Nevesskaya

1986).

The ActchagyUiin and Aspheronian régional stages

It is commonly accepted rhat, within rhe sections

studied by Khramov, the Actchagylian bed.s

conformably overlic the Cheleken Formation

delete. *l'hcy arc gcncially composed of rocks

witii reverse rcmaJicnt magnetization; the over-

lying lower and middie Apsheronian beds are

aiso rcvcrsely magnerîzed.

Trubikhin has performed complex smdies (paloo-

inagnctiL and liilTologic-mineralogic) of rwenty

sections of the Actchagylian and Apsheronian

Stages in the western Turkmenian Dépréssion

and Kopet-Dag foothtlls (Ttiibikhin 1977).

Fhick (200-700 m) Upper Pliocène séquences of

marine and continentHl origin are develuped in

rhese régions. In rhe sections studied, grey clays

and sand-interlaid aleurolites dominatc; ihcy

were divided in detail according co the mollusk

faunas. Nevesskaya has revealed the following

from Trubikhin's collections;

1. In the lower Actchagylian, Mactra suheaspia

Aadrussow, M. carabugasica Andru.ssow,

M. avala Tscheizov and Cardiurn dornbra

Andrussow.

2. In the middie Actchagylian, multiple Mactua

suheaspia Andrussow, M. instranzevi Andrussow,

M. aviculoides Andrussow, Cardiurn dornbra

GEODIVERSITAS • 1997 • 19(2)

487

Molostovsky E. A.

AndrUvS.sow, C cucurtenme Andrussow, C. kofi-

ir/?/>z/Andru-Ssow, etc.

3. The Lippcr Actchagylian substage is characreri-

zed by brackish-water Dreissena, Clessionola,

Micromelania and feodoxiis along with depleted

Cardiiim and Màcirâ assemblages.

Représentatives of Dreissena^ Aiicromelanin^

TeodoxiiSy Didacnonija^ Pseudoceitilus and other

généra are characteristic of the Lower

Apsheronian. The middle Apsheronian is charac-

cerized by diverse Curdium Apscheronia^

Paraapscheronia, Monodaena and other généra.

Hypanisy Hircania, Micromelanuiy Monodaena^

Dreissena occur Jn the upper Apsheronian.

Comparison

Principal magnerostrarigraphic sections for the

Upper Pliocène in western Turkmenia are pre-

senred in figure 12. They clearly demonstrace the

bizonal structure of the paleomagnetic column,

CHELEKEN

Fig. 12. — Paleomagnetic corrélation of sections of the Pliocène

and Plelstocene deposits of eastern Azerbaijan and western

Turkmenia (Khramov 1963).

with the lower, normally-magnetizcd zone

cmbracing the lower and the lowermost middle

Accchagylian. The stratigraphie range of the

upper, reversely polarized zone is wider and

includes the upper part of the Accchagylian plus

the whoJe of the Apsheronian. Trubikhin (1977)

interprets the régional N and R zones as being

analoguous ro Gauss and Matuyama zones in

standart magnctostradgraphic scale.

Kliramov’s paleomagncric coJumn exrends

Trubikhins scheme within the Middle Pliocène.

Il pecLiliarities of paleomagnetic section structure

are considered, it seems possible rhat the Gauss

Zone is not confined to the Actcliagylian, but

includes the nomially magneiized uppennost of

ihe Cheleken .sériés séquence. The predominant-

ly reversely magnecized middle and lower parts of

the Cheleken may be correlated with Gilbert

Zone.

The paleomagnetic data avaÜable evidemly do

not conform ro the tradidoual concept of the

Aachagylian discordantly overlying the red-bed

and tlie Torongly .suites. This conclusion may be

explaincd by dic absence of the lower, normally

magnetized Aachagylian beds (Accchagyllan-

Gauss) in the highs of the Cheleken Peninsula,

where the red-bed suite is overlain by the

Atrchagylian beds with rever.sely-polarized naiural

rémanent magnetlzation (Actchagylian-

Matuyama). Hence, the cotreetness ol the

conclusion on the lower Actchagylian horizons is

thinning on the ancient structure during the

period before rhe second Actchag)dian transgres¬

sion.

In the more easterly réglons of the Turkmenian

Dépréssion, the normally magnetized, lower part

of rhe Actchag}Tan i.s avaiUble, but the Cheleken

part of rhe Gilbert Zone halls ont ol the section

and the marine Actchagylian with latent discor¬

dance overlies the reversely magnetized Torongly

Formation, assigned tü the Gauss Zone by

Trubikhin (1977).

AZERRAlj.AN

Eastern Azerbaijan is among the most paleoma-

gnetically-studied régions. Following Khramovs

pionccring works (1963), the majority of the

most représentative sections hâve been studied

488

GEODIVERSITAS • 1997 • 19 (2)

Magnetüstratigraphy of the Pliocène in Black Sea and Caspian régions

including the Lower Pleistoccne, Apsheronian,

Actchagylian beds and the Balakhan (productive)

sequence of the Middie Pliocène.

The producni>e snjuencc

Il is formcd bv the sediment accumulations of a

brackish'Water basin; ihey are represented by

aicernating aleurolites, clays, sands and sand-

stones with the total thickness up to 2500 m.

Theseaion issubdivided inco several parts,

The upper part of the sequence, right ro the base

of che Balakhan suite, is characterized by a relier

ostracode laiina of Bakunella^ Pontoniella and

Caspiola^ gênera commun in the Pontian stage.

The Balakhan, Sabunchi and Surakhaiiy suites,

constituting the upper part of the productive

sequence, conrain the Actchagylian ostracodes:

Limnocytherey Leptocytherey etc. (Nevesskaya et al.

1986; Muratov Nevesskaya 1986).

The Actchagylian stage

It is represented by grey aleurolites and clays with

sand and rate limestone and congloinerare icer-

layers. The thicicness of the Actchagylian varies

berween 50-70 and 600-800 m and ir is subdivi-

ded into threc parts according to malacofaunal

composition. The criteria used lor this division

arc the saine as for the frans-Caspian région: a

depletcd assemblage in the lower Actchagylian

(Cerastodermay Clessintolay Phcnella, Mûcrra)^ a

rich assemblage of rhe middie Actchagylian

Cardiumy a depletcd assemblage of Mactra and

Cardium in the upper Actchagylian (Ali-Zadc

1954; Muratov 6c Nevesskaya 1986).

The Actchagylian beds transgressively and uncon-

formably overlie ancient deposics of the Middie

JuraSvsic. The Balkhan sériés is che only exception

and is believed to be connected with the

Actchagylian chrough graduai intercransitions.

The Apsheronian régional stage

It is lithologically similar to the Actchag>'lian and

differs in paléontologie nanire. The Apsheronian

deposit thicknesses do not exceed 250-300 m on

the highs and arc as high as 1500-2000 m in the

dépréssions. The Apsheronian is divided into

three substages- according to the composition of

mollusk fauna (Muratov & Nevesskaya 1986).

The lower Apsheronian is characterized by

Monodücnay Üreissena. Hyrcaniay Corbiciila and

other gênera. The middie substage is distingui-

shed by the development of Monodaena and

Didaenaides gênera, and foi origination of new

-species of Hircania and Apscheronia généra.

The upper Apsheronian is characcerised by the

disappearance of rhe ribbed apsheronids

{Apscheronia) widely common in the mïddie sub¬

stage (Nevesskaya et ai 1986; Muratov

Nevesskaya 1986).

Comparison

In Khramovs magnetostratigraphic scheme

(1963), based on the sections from the Apsheron

Peninsula and Kobysran, magnccic zones of the

Ap.sheronian and Actchagylian ace recognizcd, as

well as chose in die upper part of che productive

sequence within the Surakhan, Sabunchi and

Balakhan Formations (Fig 12).

According ro Kliramovs and Ismail-Tlades data,

rhe Actchagylian and Apsheronian stages in eas-

tern Azerbaijan are united by a common zone of

reverse polarity. The underlying beds of rhe

Surakhan are marked with dominant normal

magnetizacion both in rhe Apsheron Peninsula

and Kobysran. A large inierval ot stable reverse

polarity is regiscered downwards rhrough che sec¬

tion; It includes che Sabunchi and Balakhan

suites (Ismail'Zade étal 1967; Khramov 1963).

A relarively dctailed survey of the Upper Pliocène

part of rhe section was presenred by Ali-Zade et

al (1973) and Asadulayev & Pcvzner (1973),

who ha.s confirmed the blzonal structure of the

Actchagylian palcomagnccic .section. As in wes¬

tern Turkmenia, thç lowçr half of the

Actchagylian stage is compo.sed of normal-polari-

ty rocks, whereas the upper horizons of the

Actchagylian ,and the whole of the Apsheronian

are revcrsely magnetized.

Two normal subzoncs arc recorded within the

Apsheronian part of the section, CJnc of them js

associated with the Accchagvliaa-Apsheronian

boundary, the other one almost coïncides with

the middle/upper Apsheronian contact.

Four magnero'zones are documented within the

composite palcomagnctic section through the

Plio-Pleistocene in Azerbaijan. The top normally

GEODIVERSITAS • 1997 • 19 |2)

489

Molostovsky E. A.

[International

jPALEOMAGNETIC

I _SC ALE _

VOLGA'CASPIAN

_REGION_

WEST^MOLOSTOVSKY

GEO RGfA (THIS WORK)

Fig. 13. — Paleomagnetic corrélation of the Pliocène and Pleistocene deposits of Black Sea and Volga-Caspian régions.

magnetized zone, équivalent to the Pleistocene, is

clearly identified wirh che Brunhes Zone. The

underlying R-zone, which includes che

Apsheronian and the upper half of the

Actchagylian, is referred to Maruyama Zone by

analogy with adjacent régions.

Based on the régional scale pattern, the Gauss

Zone shoiild unité the lower half of the

Accchagylian and rhe Surakhan suite.

Such a combination of marine and brackish-

water tacies within ihe Gauss Zone is similar to

that obscrvcd bctwecn the Accchagylian and the

Cheleccn suite in western furkmenia. Similarly,

a stratigraphie discordance is rcvealed berween

the Actchagylian and rhe productive sequence

within the section lacking the lower part of the

stage and with the Surakhan suite overlain by the

reversely magnetized Actchagylian (Fig. 13).

CORRELATION OF THE PLIOCENE

DEPOSITS FROM THE BLACK SEA

AND CASPIAN REGIONS

BY PALEOMAGNETIC DATA

Corrélation of rhe data from western Turkmenia,

Azerbaijan, western Georgia, norch'Wesrern

Ponde and norchern Cis-Caspian régions, shows

pracncally identical successions" in airernation of

large normal and reverse-polariry incervals

through the whole of the Pliocène section, from

the base of the Pontian through the base of the

Pleistocene. U should bc noted that the same

type ol magnetic zonation lias been reveaJed

within coeval deposits of different origins, irres-

pective of magneric phase minerai composition

or of the character of narural rémanent magneti-

zation.

490

GEODIVERSITAS • 1997 • 19(2)

Fig. 14. — Corrélative scheme of the Pliocène deposits of Caspian and Black Sea régions (Karmishina 1975).

Molostovsky E. A.

The Matiiyama-Brunhes inversion should be

considered the niosr reliable référencé Icvel for

inter-rcgional corrélation. The conclation bci-

ween local stratigraphie imits and the paleoma-

gnetic scale is prvsented in figure 13.

The summary of the biostratigraphic corrélation

schemes for the Pllocene of the Pontic-Caspian

région is shown in figure 14.

Compati,son of the schemes makes it possible to

consider ihc révisions inrroduced by paleoma-

gnetic data înro ihc iraditional concepts of

Pliocène stratigraphy;

1. The Kimmerian stage cannot be correlated

with the middle-lower Actchagylian due to

magnetic polariry différences.

2. Paleomagneric dara eliminate the idea of refer-

ring the Taman layers to the lower Kuyalnikian

(Buryak 1969) due co different polariry Jn of

these stratigraphie unies. For the same reason, the

lower Kuyalnikian cannot be correlated with the

upper Actchagylian.

3. Magnetozonc corrélation beiwccn the

Pliocène sections froni Azerbaijan and

Turkmenia does nor confirm the tradicional ide.i

of the Actchagylian confirmably overlying the

productive and red-bed séquences, 1 he

Actchagylian overlies varions Middie Pliocène

horizons transgre.ssively, with clear stratigraphie

unconforniicy.

l'he proposed paleomagnctic modifications of

biostratigraphic schemes do not iisually encoiin-

ter significant objections, the only exception

being the Pontian stage and its position witliin

the magnerostratigraphic scale bas been deba-

table for rwo décades.

There are ihree published points of view on the

problem ol the position of the Poncîan. Two of

them prefer the idca of a "short” Ponrian

(0.6-0.8 Ma), and corrclarc the Pontian stage

with the lowcrmost pan ni Gilbert Zone

(Trubikhin 1977: Molostov.sky et al 1982) or

with zone 6 (Semenenko & Pev/ner 1979) of the

general paleomagnctic scale. Afrcr numerous

changes ol opinion. Zubalcov has assumed of a

"long” (about 2 Ma) polyzonal Pontian wichin

rhe lowermosr Gilbert Zone plus the wholc of

zones 5 and 6 (Zubakov 1990).

The idea of “a long Pontian” seenis somewhat

spéculative, because within the sections from the

Crimea, Taman. Georgia and Roumania, the

Pontian stage or ics analogues correspond to the

monopolar R-zone, which is more in accord with

the idca of a “short” Pontian.

The idca of correlating the Pontian with the

sixth epoch of die paleoniagnetic scale originated

after NN11 zone nannofossils were found within

the lower (Azov) horizon of the Kimmerian and

those of the NN12 zone in the Middie

Kimmerian.

Based on the nature of nannoplankron and

magnetozone distributions within océan sédi¬

ments and the stratotype section of the Neogene

in Iraly, Semenenko Pcvzncr (1979) hâve com-

pared the lower Kimmerian Wich zone S and che

upper Mcssinuin. and the Pontian with zone 6

and the lowcrmost part of the Messinian. The

Mioccne/Plioccne boundary in the castern

Para-l'cthys was, accordingly, removed from the

base of the Pontian to the bottom of the middie

Kimmerian.

The>e idexs were questioned (Trubikhin 1986)

on the bas’is ol paleomagnctic data for the réfé¬

rencé sections of the Mio-Plîocene from

Roumania and this présent authors data from

western Georgia, with the magnetic zonation

indicating the conespoiideiKe of the Pontian

and the lower Kimmerian to the Gilbert Zone

and hence U) the lowermost Pliocène.

Both models arc subject to correction after addi-

tjon.ll paléontologie and paleomagnctic studies

hâve been carried our.

The study of cores from the équatorial Pacific

has shown D/scoaster (juinquerumus to di.sappear

at various stratigraphie Icvcis. In rhe well

PC-12'66, the boundary between zones NNll

and NN12 occurs within the upper third of the

foraminifer zone NI7, which corresponds to the

middie of the palcomagnetic scale fifth epoch^ In

Wells 77 and 158 this change is recorded at a

higher stratigra ph ic level, within zone N18,

which is usually correlated with the Gilbert Zone

(Dunn &c Moore 1981). Tliiis, the defînirion of

ihe index-species for ihe NN 1 1 zone in the

Poncic Azov horizon has lost its relcrarne, bccau-

sc it cannot .serve as a corrclaiion index for the

Lower Kimmerian and the fifth epoch of the

paleomagnctic scale.

The position of Gilbert Zone within the strati-

492

GEODIVERSITAS • 1997 • 19(2)

M^netostradgraphy of the Pliocène in Black Sea and Caspian régions

graphie scale for tlie Mcditcrranean has altcred in

recent yearu. It fbllnws from Cita (1983) that the

conclusions of Ryan et ul. (1974) on the corréla¬

tion of the Messinian to magnetozones 5 and 6

were only tentante, because the Messinian stage

stratotype has nor been sruJied paleomagneti-

cally due to weak magnetization of the rocks.

Research in castern Crete has shown that the

upper Messinian (evaporites plus mare" for¬

mations) corresponds to rite lowermost part of

the Gilbert Zone and the middle and the lower

parts of the stage to magnetozones 5 and 6

(Langereis et 1977).

From the evidence dîscussed above, it seems

mosr reasonable to refer the Pontian to the

lowermost part of the Gilbert Zone and correlate

it with the upper Messinian and» parttally, with

the lower Zanclian. In this case the Miocene-

Pliocene boundary, .ivS it is accepted in the

Mcditcrranean, should occur within the Pontian

stage.

Paleomagnetic corrélation of the Pontian with

the Mcditcrranean unies reduces the level of

uncertainty arlsing fioni biosrrangraphic scheme

comparisons. Nevesskaya et ai (1986) believe

that the Pontian may correspond to the

Messinian in the Mediterranean, in full or in

part, or the lowermost part of the Zanclian, or

the uppermost Messinian and lowermost

Z^anclian.

Magnerostratigraphic corrélation of the Pliocène

beds from the eastern Para-Tethys and the

Mediterranean région is shown in figure 15.

PALEOMAGNETIC CALIBRATION OF

OSTRACODF. AND MOLLUSK FAUNAS

FROM THE PONTO-CASPIAN REGIONS

Unification of régional paleomagnetic schemes

on the basis of A. Cox scaJe has provided the fra-

mework lor a comparative analysis of oscracode

and mollusk faunas de\elopment stages within

the Pontic and Caspian régions. According to

Karmishina (1975). ihrce stages niay bc recogni-

zed in the development ol the Plioccne basins

and their ostracode biota; the Pontian,

Actchagylian and Apsheronian lor the Caspian;

the Pontian, Kimmerian early Kuyalnikian and

Fig. 15. — Paleomagnetic corrélation of sections of the

Neogene of Mediterranean (I) and eastern Para-Tethys (II).

lare Kuyalnikian Gurîan for rhe Euxinic. The

Pontian stage is accepted as common for both

régions, and the Actchagylian is generally correla-

ted with the Kimmerian early Kuyalnikian

Gurian.

Projection of rhe biostratigraphic scheme on ro

the paleomagnetic scale reveals the chronologie

asyachroneit}' of a number of evolutionary boun-

daries (Fig. l6).

Within the Euxrnic Basin, the Pontian stage

came to an end in the middle of the Gilbert

epoch, probably after rhe Tver épisode. The

Actchags'Iian ostracode complex supplants the

Pontian onc at about the samc level within the

lowermost part of the Balakhan suite (Karmi¬

shina 1975; Mura-tov & Nevesskaya 1986).

rhe Actchagylian stage in the Caspian corres¬

ponds to the whole of the Gauss epoch and to

GEODIVERSITAS • 1997 • 19(2)

493

Molostovsky E. A.

I : Black sea région M : Casplan région

Fig. 16. — Principal studies of development of the Pliocène

ostracodes and mollusks of eastern Para-Tethys corrélation with

paleomagnelic scale (ostracodes: Karmlshyna 1975. mollusks:

Nevesskaya étal. 1986).

the carly Matuyama up to Olduwai épisode; it

covers the rime interval of 3.4-1.9 Ma Its presu-

med analogue in the Pontic région, the

Kimmcrian early Kuyalnikian stage, occupies a

different magnctochronologic interval: the major

part of fhe Gilbert epoch and the vvhole of the

Gauss epoch (4.57-2.47 Ma).

The Ap.sheronian and the lace Kuyalnikian

Gurian siage.s hâve different durations: their rime

ranges constiture 1.89-0.73 and 2.47-0.73 Ma

respectively. Comparative analysis ol rhe évolu¬

tion of che Pontic-Caspiaii malacofauna demons-

trates diat rhe Apsheconian stage is équivalent co

the Gurian and Cliaudian stades collectively in

duration, and the Kuyalnikian stage is shorter

than the Kimmerian.

In prindple, similar relaiionships based on the

magneric polarity scale may be determined bet-

ween the Pliocène taunas from eastern and wes¬

tern Para-Techys as well as between them and the

fauna of the Mediterranean région.

CONCLUSION

In the Pliocène sections from the Black Sca and

Caspian régions, three major zones of the general

magnctochronologic scale are rccognizcd and tra-

ced consisrently; they are complicated by a num-

ber of subordinatc subzoncs. The Upper Pliocène

R-zone is idcntificd wich the Matuyama Zone

(0.73-2.47 Ma) and comprises the most of the

Upper Pliocçne + Eopleistocene. The middle,

Gauss N Zone (2.^7-3,4 Ma)> comprises the

Middle and the lowcrmosr part of the Upper

Pliocène. The lower, Gilbert Zone (3.4-'5.3 Ma),

corresponds to chc most of the Kimmcrian part

of the Middle and Lower Phocene,

Llnification of local stratigraphie schemes, corré¬

lations among the régional géologie evencs and

comparisons of marine sections from the eastern

Para-Tethys and the Mediterranean région, these

are the obvions positive resutes obtained from

many years of paleomagneric researci).

The mo.st urgent task for the neaic.st future i\ to

perform corrélations among chc marine and

continental Plio-Piciscocene Formations from che

norrhern Pcri-Tcthys on the basis of paJeomagne-

tic zonalitics. l'hcrc are most re;d prcrcquisites

available for broad corrélations of such type.

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of magnetostratigraphy. Transactions of XXVII

Geological Congress, Moscow 1: 16-24 [in Russian|.

Muratov & Nes'esskaya L, A. 1986. — Strangraphy of

the USSR: 1-^12 [in Ru&sianl. in Mui.itov tk

Nevesskaya L. A. (ed.s), The Neogene System.

Volume L Nedra, Moscow.

Nevesskaj.'a L. A., Goncharova |. A. & Ilyina L. B. et

ah 1986- — J hr history ttj hJeogtnc niùlluiks fiom

the Para-Tt'thys. Muukâ) Moscow, 208 p- [in

Russian].

Ryan W, B-, Cita M. B., Drciftis R., Burckie L. H. &

Saito T. A. 1974. — Paleomagnetic assignment of

Xeogene stage boundaries and the development of

isochronous datum-planes berween the Medirer-

ranean. the Pacific and Indian océans m order to

investigate the response of the World océan ro the

Mcdiicrratican Salinity Crisis. Rtvista Jialiana di

Paleontoh^t e Strat/grafra 80 (4): 631-688.

Senienenko V. N. <k Pevzner M. A. 1979. —

Corrélation ofthe Upper Mioccne and Pliocène in

the Poiuic-Cispiaii by hiosiratigraphic and paleo-

rnagnetic data. USSR /l.V Proceedtngs^ Geological

Sériés 1: 5-15 [in Russian].

l reryak A. J. & Volok Z. E. 1976. — Paleomagnetic

stratigt'aphy of the Pliocene-Quatvrnary sequences in

the Ukraine. Naukova dumka, Kiev, 86 p. [in

Russian],

TrubikJiln V. M. 1977.— Paieomagnetism anditrad-

graphy of the .^ctchagylian depoUts tn western

Turkmenia. Nauka, Moscow, 79 p. [in Russian],

— 1986. — Neogene magnetubtriuigraphic seule of

easfern Para-'J'ethys: 206-207 |in Russian], in

Petrova G, N. (ed.), U! conférence ofGeomagnetRm.

AS USSR, Kiev.

Zubakov V. A. 1990. — Global rlimatic events tn the

Neogene. Gjdromcieoizdat, Leningrad, 220 p. [in

Russian j.

Zubakov VL A. 6c Kochegura V- V. 1976. —

Magnetochronalogic scalc of rhe modem stage

(5 Ma). Geomagneiic rescarch 17; 37-43 [in

Russian].

Submitted for publication on 15 January Î996\

accepted on l October 1996.

GEODIVERSITAS • 1997 • 19(2)

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Références bibliographiques

Denison R. II. 1978. — Placodermi, in Schultze

H. P. (cd.)j Handbook of Paleoichthyology,

Volume 2. Gtiscav Fischer» Stuttgart» 128 p.

Marshall C. R. 1987. — Lungfish: phylogeny and

parsimony» in Remis W. Ê», Btirggren W.

& Kemp N. R. (eds), l’he Biology and

Evolution of Lungfishes, lournal of Morphology

1:151-162.

Schultze fl. P. & Arsenaiilt M. 1985. — Fhc pan-

derichthyid fish Elpistostege\ a close relative to

tetrapod-s? Paleontology 2S: 293^309.

Schultze M, P. 1977a. — nte origin of the tetra-

pod limb within the rhipidistian fishes:

541-544. in Heclit M. K., Goody P. C. &

Hecht B. C. (eds), Major Patterns in Vertebrate

Evolution. Plénum Press, New York and

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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. — Lungfîsh; phylogeny and

parsimony, in Remis W. Ë., Burggren W. W.

& Kemp N. E. (eds), The Biology and

Evolution of Lungfîshes, Journal of Morphology

l: 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 rhe tetra-

pod limb wilhin the rhipidistian fishes:

541 - 544 , Hcchc M. K., Coody P. C. &

Hechr B. C. (eds). Major Patterns in Vertebrate

Evolution. Plénum Press, New York and London.

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follows:

Vai G. B. &; Venturini C. 1997. — Moscovian

and Artinskian rocks in the frame of the cyclic

Permo-Carboniferous deposits of the Garnie

Alps and related areas, in Crasquin-Soleau S. &:

De Wever P. (eds), Peri-Tethys: stratigraphie

corrélations, Geodiversitas 19 (2): 173-186.

GEODIVERSITAS • 1997 • 19(2)

499

Mise en page

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geodiversitas

1997 • 19 ( 2 )

Peri-Tethys: stratigraphie corrélations 1

edited by Sylvie Crasquin-Soleau & Patrick De Wever

Crasguin-Soleau S. & De Wever P.

169 • Corrélations stratigraphiques de la plate-forme européenne dans le cadre du Programme Péri-Téthy!

(Introduction générale)

Vai G. B. & Venturini C.

173 # Moscovian and Artinskian rocks in the frame of the cyclic Permo-Carboniferous deposits of the Garnie |

Alps and related areas r ^

187

Pasini M. & Vai C. B.

Review and updating of the Moscovian to Artinskian marine rocks in Peninsuiar Italy

193 •

203 •

217 •

221 •

229 •

235 •

Di Stefano P. & Gullo M.

Permian deposits of Sicily: a review

Cassinis G.

Review on continental Permo-Carboniferous deposits in Italy

Cassinis G. & Ronchi A.

Upper Carboniferous to Lower Permian continental deposits in Sardinia (Italy)

Vai G. B.

Late Carboniferous to Early Permian palaeogeography of the Italian and central Mediterranean area

Geluk M.

Palaeogeographic maps of Moscovian and Artinskian; contributions from the Netherlands

Makhlina M. Kh., Solovieva M. N. f & Goreva N. V.

On the biostratigraphy and cyclostratigraphy of the Moscovian Stage in the type area

Molostovskaya I. I.

247 • Stratigraphie corrélation of the Upper Permian deposits from the south of the Cis-Ural marginal

Trougn and the adjacent areas of the Russian Plate W r#

Molostovsky E. A., Molostovskaya I. I. & Crasquin-Soleau S.

761 • Depositional conditions in the Southern Cis-Urals basin during Late Permian (biostratigraphic,

lithofacies and petromagnetic data)

Mtnikh M. G. & Minikh A. V.

279 • Ichthyofaunal corrélation of the Triassic deposits from the northern Cis-Caspian and Southern

Cis-Urals régions

Amon E. O., Blueford j. R., De Wever P. & Zhelezko V. I.

293 • An essay on régional geology and stratigraphy of the Upper Cretaceous deposits of Southern Urals

territories

319 # Wever P. & Vlshnevskaya V. S.

Mesozoic radiolarians from the European Platform: a review

383 • Wever P. & Popova I. M.

Cenozoic radiolaria from European Platform: a review

471 • Molostovsky E. A.

Magnetostratigraphy of the Pliocène deposits in Black Sea, Caspian régions and adjacent areas

Conception Graphique : Isabel Gautray

ISSN : 1280-9659

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