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Zitteliana 10 467-483 München, 1. Juli 19S3 ISSN 0373-9627

To the „Neocomian“ biostratigraphy in the Krizna-Nappe of the Strázovské Vrchy Mountains

(Northwestern Central Carpathians)

By

ZDENEK VASICEK, JOZEF MICHALIK & KAROL BORZA*)

With 8 text figures, 1 table and 2 plates

ABSTRACTThe paper deals with the newest results of detailed strati-

graphical research in nine Lower Cretaceous sequences in Western Carpathians. The correlation of several parabiostra- tigraphical schemes based on several groups of organisms, allowed to elaborate a local biostratigraphy, applicable in the

whole area, and relatively reliable date most of the lithological horizons. Moreover, the detailed lithostratigraphical correlation enables us to reconstruct sedimentary and paleotectonical development of the Krizna (= Fatric) basin.

KURZFASSUNGIn dieser Arbeit werden die Ergebnisse der biostratigraphi

schen Untersuchungen in den Ablagerungen des höchsten Jura und der unteren Kreide im Gebiet des Sträzov-Berglan- des (Krizna-Decke = Fatrikum) vorgestellt. Sie stützen sich auf neun Profile, die lithofaziell und auf ihren Mikroplankton- und Cephalopoden-Inhalt hin untersucht wurden.

Die bisher gewonnenen Ergebnisse zeigen, daß die Entwicklung des Fatrikums komplizierter ist, als bisher angenommen wurde. Die ältesten Ablagerungen der ,,Neo- kom“-Schichtenfolge gehen aus silifizierten Tiefwasserkarbonaten hervor. Tithon, Berrias und Untervalangin sind vor allem mikrofaunistisch belegt, die Makrofauna ist gewöhnlich nur durch Aptychen dokumentiert. Obervalangin bis unterstes Apt enthalten stellenweise ziemlich reiche Cephalopo- denfaunen, besonders Ammoniten, die mediterranen Cha

rakter besitzen. Höheres Apt und Unteralb läßt sich nur durch Mikroplankton und stellenweise durch orbitolinide Foraminiferen identifizieren.

ACKNOWLEDGMENTS

We acknowledge Dr. E. Köhler, CSc. for determination of orbitolinid foraminifers and for stimulating comments to the Aptian stratigraphy. We thank also Mrs. M. Ruzovä for the drawings, Mrs. M. Grmelovä for the photos of the macrofossils, Mrs. H. Brodnianska made the photographs of the microfossils. We are indepted to Academician B. Cambel, Director of Geological Institute Slovak Acad. Sei. for the permission to publish the results of our research.

1. I N T R O D U C T IO NLower Cretaceous carbonate sequences form considerable

part of the rock sequence in the Krizna nappe of central Western Carpathians (Czechoslovakia). During the last years we

*) Z. VaSICek, Dept, of Geology and Mineralogy, Mining University, 708 33 Ostrava-Poruba VI, CSSR; J. M ichalIk , K. Borza , Geological Institute Slovak. Acad. Sciences, 81473 Bratislava, CSSR.

happened to enrich our recent knowledge (M ichalIk & VASiCEK 1979, Borza et al. 1980, M ichalIk et al. 1980, V aSiCek & M ichalik 1981, Borza et al. 1982) by adding of further, more completely known new sequences. Our newest localities and the application of several modern literary data (among them Busnardo et al. 1979 predominantly) made the knowledge of Upper Valanginian - Upper Barremian interval biostratigraphy more refined.

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Stratigraphical research in the West Carpathian Lower Cretaceous sequences is complicated by an intricated tectonical structure of the terraine, forming a part of the Centrocarpa- thian nappe front, by lack of completely incovered sections, as well as by its considerable facial variability. This is why our research cannot be considered as to be finished and some of our conclusions as to be definitive. As a result, we could not define ammonite zones, valid in the whole area.

Northwestern part of Strázovské vrchy Mts. forms southern rim of the Middle Váh-river basin (Fig. 1). Complica-

tely deformed frontal part of the Krizna-nappe, extending oyer great part of this area, consists mostly of Lower- and Middle Cretaceous sediments. In spite of incomplete exposure, several outcrops in quarries, creeks and road’s cuts offer possibility of detailed stratigraphical study. This paper is based on the study of nine detailed documented sections, evaluated from both the macro- and micro-lithofacial point of view, according to the content of microplankton and cephalopod macrofauna, as well as nannofloral remains, studied in several places.

2. PALAEOGEOGRAPHICAL SETTINGMediterranean segment of the Mesozoic Tethys has re

ached the maximum of its diversification during Late Jurassic and Early Cretaceous. Although the recent knowledge of paleogeographical relations between individual elements of the European Alpides does not allow unambiguous conclusions (cf. M ichalik & KovaC 1982), West Carpathian area may be roughly characterized as an extensive, paleogeographically and paleotectonically veiy diversified area, extending on the west from the mouth of Danish-Polish trough, thus in close neighbourrough of the East European platform (Fig. 2).

The northernmost zone (nowadays Outer Carpathians and Klippen Belt) belonged to the margin of North-European shelf, influenced by Kimmerian tectonic movements. The central West Carpathians, on the other hand, were part of intraoceanic (Kreios) shelf fragment, deformed during Austrian otogenic phase. Both the regions were mutually separated by the Jurassic-Cretaceous Penninic oceanic zone. West Carpathian paleogeographical and paleotectonical development has been strongly influenced by these pecularities.

Fig. 1. Geographical localization of studied sections. Legend: 1: Lower Cretaceous deposits of the Krizna-nappe, 2: the same deposits covered by younger sediments or by higher tectonic units, 3: Klippen Belt, 4: faults, 5: limits of distribution of Krizna Lower Cretaceous. Numbers in circles: 1: Nozdrovice section, 2—6: Mraznicke luky sections (2: Kamenna, 3: Pod Strane, 4: Pod Stupikmi, 5: Pod Svinornym, 6: Pod Mraznicou, cf. Fig. 6), 7: Horna Poruba section, 8: Strazovce section, 9: Butkov quarry.



FENNOSARMATIA

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Fig. 2. Albian paleogeographical situation of the Mediterranean Tethys (Michalík & Kovác 1982). West Carpathian area denoted by quadrangle. 1: continental, 2: epicontinental and shelf seas, 3: troughs and rifts, 4: deformed zones, 5: carbonate platforms with adjacent basins, 6: deep-sea basins, 7: oceanic bottom, 8: recent coast-line of Europe and North Africa (for correlation), 9: plate motion vergence.

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Scdim ciit.n y .irc'.i u l (In- ( .cm m ca i pal Inan K i i /n a nappc s. I. ( h i i i i c acLord ing lo A ndkusov; ImisAn {V llvs iim i.s

\')7}) lo rm cd pari u l I » w r i ( ic iaccns (?b ,uk .h l )

baxinal System, scp.irnlcd Im in ( I i l s o i i i Ik t h b o id c r u l IV nn i

n ii uLiMii liy i l ic T .m iL / u i k ( M a i i i f \'>7'>). l l ie x iibsidcncc u l lins I>.isin, isol.ned 11um le rrig c iin tis snpport, eonsidcrable .iLLcIcr.il e iI dm in j; ( „ t lln v i.in ,iii<l (. >x lnrd i.m , vvlicii th ick fe il

.Hui g iccn f.icli<il . ir11c sctpicnce Ins s«dim cm cd lic ic . I Ins sc

ipiciiLC md¡L.ncs “ ( , ( . l ) crisis” or tiic “ Juiassic tull.ipsc” uf T d liy s . lis end is d.ncd by lin d in g o l Oi/m m i/i/iiHT.i jil>r,ihi ( N a i.v) in llie nppcnnusi radiolaritc layers ,md in above-lying nodnlni linicstuncs ( Upper ( Vxlordi.tn). I’clagic carbonate se dim cnt.iliun j; i ,uIu.i11y st,iliili/cd in lilis li.isin and llie l .i Il Íi Íl sli el I reina ins lieeame mu re and mui e 11 cipicnl I v preser ved in

lis se(|iiences.

nP/. H'J" i Inn rjl« Milfnrn F» I I'!) «I rriMUlif' pHnrj« boom

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fdRpriitp,

i p l V i i " , i i , i

I í^ . V A p n . in l> ,i i l iy i iu ' l i k si Ik 'MH’ o I i Ik* M iu l icd .írc.i» . i lo tig w n l i l i t lm s i i.n ij; i.ípl iy n i I o w n O r i . u r n i i s

deposits.

3. STRATI G RA l’-H VV I U I T h R JU K A S S K

Sedimenls ol llie J i i i .is s íl / ( relaeeuns bonm l.iry are vei y

puui in inaLrulannal remuants in uni seeliuns. S indving lilis sapience, we musí use a p>ai asi t .il iy;t apli na I selieme, el .1 llora ted un tlie liase ol tin liiin id and prulilcinalie m icioorganism distribution, as llie eeplialupud remains (aplvelii, am m uniles and lieleinniles) hemme reliahle hiostratigi .iplheal (uul sinee

Uppei V ,ilaiiy;ini.in.

U p p e r J n ra s s ie s e d im e n ls w c i e d u L i i m e m e d m l l i e S u a

/< )v r e s e c t i o n ( lu e . H u n l l i e In j ; . I . ; b ig . 4 ). R e d a nd g ra y

m a i l v l im e s iu n e s u l d ie i i i . i l i n n ¡ i Z o n e c o n t a i n I r c i p i c n t ap

l y c l i i l . tiH icILip ly i hn\ 1’t‘v m h i f r c y r i t b i ( O i t i i ) am ! I ’m n l . i/ i ty<hn\ i>ini<l,itiiï ¡ u n i t l, t i n s ( V m i v ) , m i c r o c r i n o i d s (.Sncoi

{tiiHit s p . ) , o i l i e r i n i c r n p l a n k t n n as l >,n,i\lii)mi>s¡>l.>,ic>d » i d l - i i i i i ' . i ( I 'k i k / a ) , ( ,o / i n i / / s / i / ) , i t ,i , i n i i t i n i im t i n d ( C m u m ), (

¡>iill,i ( U m t / A ) , < . f ,n ¡> , i lh i t , i ( R o h m ), e te , , e l . U m < /A et a l.

I ‘4X2 . I l ie h i g h e r p a n u f m . i r l y l im e s t u n e c o m p l c x L u in a in s

M i d d l e T i t l i o n i a n spec ies ( ¡ h i l i w m i c l l d h o n c l i D o i i i n , ’ l l i e

a p p e a r in g u l l ' ) , )v ln i l i t ino j> ' i c lL i sp , e i t n a e t e i i / e s th e hasa l

l J p p c r T i l l t o n i . m g re e n g i a y m a r l v l im e s tu n e s , w l i i l e l l ie lu ; ;

l ie r a s s o c ia t i o n , c o m a i n i i i g C r,tssn<>ll,iri,t i n W r» i i ' ih , i ( D u

k a n 11 D u t , a ), ( ' . I » c v t s R i m a n t , C.,ilj>io>icll,i d l f w t d I . o h i n / ,

( oloinisj>l>,w>,i > n i ) in l i t i h n , i ( C o i u m ) , e te . ( i l . I ig . 4) , i i u l i

ca les d ie U p p e r T i t l i u n i a n ,

V 2 D1 • R K IA S I A N

l l u t l i ( l ie n p p e r m o s t p .n t o l d ie g r a y m a i l y l im e s t o n e c o n t -

p le x a n d a h o v e - l y i n g t l n c l i l a y c i c d g r a y “ h i a n c o n e - t y p c ” l i

m e s to n e s h e l o n g t u t l ie U p p e r T i t h n n i a n / R c r r i a s B l s icco r -

d i n g t u ( l ie m i c r o l o s s i l c o n t e n t ( d d S S H o l l d r i d />,irvnl,i R i m a

NI . ( tll/IIWIcILl dl j'IHd I a l l l l N ' / , C . l ' I l l f ' t i ïd C A O I S t a i , l i t l t lU -m i / n c / i i c . i r/ i . i lh iu i ( M n i n . i a n u î V I ;ii i i' i isi u ) , l o n g , ! ( C n

i d m ) , l\i‘» i , i n i c l l , i o n l i s t hi , i i i . i ( ( n i n w ) , C o l o ) i i i s l ’h , i c r , i » r i ntil is s iîN,i ( C o i u m ) a n d M m i m u m m a l f , s t a n u t d u n i K a m p 'i

n i h ). N e i t h e r m i c t o l a i t n a l , m t r d ie m a c r u f a i i n . i l c o n t e n t , si

m i l a r l y p o o l as in t h e U p p e r J n ra s s ic d e p o s i t s , a l l o w e t l exact

d é l i m i t a t i o n o l t h e T i d i u n i a n / R c r i ias ian b o n n d . i r y in t h e stn




Saccocoma sp. • * • • ■ ■— • • •• • • • — ♦ . Colomisphaera minutissima

* Cotomisphaera carpathica• **• Parastomiosphaera malmica• Stomiosphaera moluccana

••C h iftn o id e lla sp.«■.Chitmoidella cf- bon e ti

Cadosina fusca fusca* *P raetin tinnopsella sp. •Crasstcolana in term edia«* *

Catpronella alpina .......... . • • • •Tintmnopsella carpatbica * • • • • • • * • — • • • • • • • •

Crassicolana brevis .Crassicolana p ra v u la „,Remamella cadischiana * * * ♦ * *Calpionetla e l l ip t ic a • • . «»

Nannoconus sp * ♦ ♦Tlntinnopsella longa* ♦

C alp ionellopsis simplex Lorenzieüa hunganca

Calp ione llopsis oblonga C a lp ione llites d a rden * ♦ • •

Colomisphacra helipsphaera •Colomisphaera vog leri ,

C a tp ione llites coronataCadosina fusca cieszymca

Cadosina semiradiata olzae , Stomiosphaera echmata

Oiazomatolithus subbeficus • Cyclogelosphaera m argereli ,

Podortiabdus sp, *Ellipsagelosphaera b n ta n n ica ,

Cyclagelosphaera ro ta d yp e a ta Hicranthohthus

Stomiosphaera wanner i •Stomiospbaera alpina

crenu la tus * Ellipsagelosphaera kefta lrem pti •

Podorhabdus dietzmanni * Ellipsagelospbaera

Lameüaptychus beyrichi beyrichi tychus s i ................ ' '

o va ta « .

, Lamellaptychus submortilleti V e tro flexus• • • Punctaptychus punctatus punctatus

Lamellaptychus m o rtil le t i noricus .Lamellaptychus studen studeri .Lamellaptychus m o rtille t i m o rtit le ti . •

Lamellaptychus noncus «m « «• * «mLamellaptychus didayi . .... ................... ............... ....................

Lamellaptychus m o rt il le t i re tro fle xu s « .Lamellaptychus m o rtille t i ssp, 1 Lamellaptychus beyrichodidayi . # ***•*•• * •

Lam ellaptychus seranoms seranoms • * * . .Lamellaptychus angulicostatus ssp. TTTtTTr , ,

Lamellaptychus angulicostatus lonqusB e rn a se lla sp. •P ro te trago m tes quadrisulcatus . . *

Neocomites cf, trezanensis •Phylloceras sp • • ♦ ♦ •

Bochiam tes oosten . • — • .Oleostephanus sp. . . • • • • «

Bochianites neocomiensis . * , ^Haploceras grasianum • » •«

Neocomites ex gr, neocomiensis . +Haploceras desmoceroides » » .

Neocomites /Teschenites / sp. « * •O lcostephanus psilostom us • • •

7 Himantoceras sp * *S p itid iscus sp. •

7 Judd iceras sp- «C rioce ra tites /C r io c e r a t ite s /s p . *

C riosaras ine lla sp .** , Barrel

Conobelus sp,Duvalia la ta «

Pseudobelus bipart i tus •Duvalia b ila ta ta bmervioides *

Duvalia d ila ta ta d i la ta ta • Pseudobelus brevis

‘(pites /B a rre m ite s /s p . * Partschiceras sp. ,

Barrem ites /C a ss id o ice ra s / sp

Karstemceras sp S iles ites vulpes

Duvalia grasiana

Fig. 4. Lithostratigraphic correlation and distribution of organic remains in the Strazovcc-section (cf. loc. 8, Fig. 1).

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Fig. 5. L ithostratigrjphn.al correlation and distribution of the mam fossils in the Nozdrovice-section (loc. 1, Fig. 1).

died sections. The ammonites occur sporadically, being represented by mostly indeterminable fragments in Strazovce and Nordrovice section (loci 1 and 8 in Fig. 1; Figs. 4 and 5). Infrequent aptychi are usually small [Lamellaptycbus studeri stitd en (O oster), L. m ortilleti m ortilleti (P ictet & Lo- rioi ), L. m ortilleti noricus Trauth etc.].

The “biancone limestones” are characteristic lithostratigraphical unit, Upper Tithonian to Upper Berriasian in age. They represent a typical product of the pelagic bathyal environment, being characterized by facial uniformity, abundance of nanno- and microplanktic remains, but by scarcity of the macrofossils (among them dispersed aptychi dominate).

The Upper Berriasian Calpionellopsis Zone could be proved in several sections, being represented by the upper “Biancone” (loc. 8), by yellowish light-gray (marly) limestones (loc. 1), or by light-gray spotted limestones (loc. 3). The microfossil association in all the sections is nearly identical, but quantitative representation of individual taxa moderately changes (cf. Figs. 4, 5, 6).

3.3 VALANGINIAN

The lower part of the above-lying marly spotted limestone complex in several sections (loci 1, 8, 9) contains “Nozdrovice Breccia Horizon”, consisting of irregular angular limestone clasts, mostly Upper Tithonian/Berriasian (Calpionella zone), but also older (Cmssicollaria Z.) and younger (Cal-

p ion ellites Z.) in age. The origin of the Nozdrovice Breccia could has been connected with probable Valanginian sedimentary gap in the northernmore Manin unit (influence of the Late Kimmerian tectonic deformations).

The Valanginian sediments contain a rich spectrum of microplanktic remains (C alpionellites darderi [C olom], C . co-

ronata Trejo, C . caravacaensis A llf.mann, Calpionella a lpina Lorenz, Calpionellopsis ob lon ga [C adisch], Tintinnop- sella carpatbica [M urgeanu & F11 ipescu], T. lon ga [C oi.om], LorenzielLi bnn gan ca K nauf.r & N agy , L. cf. plica ta R emane, Colom isphaera behosphaera [Vogeer], C. v o g le r i [Bor- za], Stom iosphaera ech inata N ow ak , Cadosina fitsca cieszynica N owak etc.). However, the recent microbiostratigraphi- cal knowledge do not allow to divide the Valanginian sequence more in detail.

Our macrofaunal findings enabled us to recognize the uppermost Lower Valanginian in the Butkov section (Fig. 7, probable equivalent with upper part of the French Busnardoi- tes campylotoxus Zone), containing ammonite fragments, resembling Kilianella pex iptycha (U hlig) and Busnardoites N ikolov, aptychi Lamellaptycbus aplanatus aplanatits (Gil- eieron), L. aplanatus retroflexus Trauth, L. m ortilleti m ortilleti (P ictet & Loriol).

Zonal ammonites lack also in the Lower Upper Valanginian Saynoceras verriicosm n Zone). However, several localities yielded ammonite remains, similar to N eocom ites n eo com ien - sis (d ’O rbigny), N. tescben ensis (U hlig) and Bochianites




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H1 -U• Lorenziella phcata• * • Calpionella alpina• • — •Remamella cadischiana• ----- ♦ —«**• Lorenziella hungarica• ----- •---- — **«•• Calpionellopsis oblonga• -------•----- • » » Tm t innopse 11 a carpahhica

•— ♦— Tin tinn op se U a lonqa •— •—•■*■** Calplonelites darden

Calpionellites coronata Calpionoltites caravacaensis

Colomisphaera ^hefjospTa^a

Calpionellopsella maldonadoi Colomiella recta

Colomiella semiloncata Parachitinoidella cuvilien

Colomiella mexicana •Oeflandronella veracruzana

Praecolomiella trejoi Pienima oblonga

Cadosina semiradiata olzae•---------- ^.Stomiosphaera wannen»»— ........................ ..................Nannoconus

ëcïïlnâtaStomiosphaera

-olomisphaera vogler•Cadosina fusca cieszynica

sp.-X -X -X — - - x-x

Cadosina fusca fusca

Hedbergetla sp

* --------------- ♦♦— »Lame lia ptychusL. angulicostatus ssp 1 • -** - - * --------• - —Lamellaptychus did ay i * * ~ *Lamellaptychus aplanatus • • -----•Lamellaptychus bey nchodidayi -Lamellaptychus m orti lie 11 sspl.--------------Lamellaptychus mortilleti retroflexus • Lametlaprychus angulicostatus fractoco*status

noncus

Lamellaptychus

Nautilcculina sp. •______*__ *Patorbitolina cf. lenticularis , , . v_v v

Orbitolina /Mesorbitolma/ minuta O rbitolm a/ Mesorbitolma/ parva x-x-x--x

Orbi tol inopsts reticulata x-x-x—xSabaudia minuta x-x-x--x

angulicostatus longus

» Otcostephanus aff. astienanus►----------•••Bochiamtes neocomiens|s

• Bochiamtes oosten-------Protetragomtes quadrisulcatus

.haploceras desmoceroides ------------- • Neocomites /Neocomites/ teschenensis

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Neocomites /Neocomites/ neocomiensis •** Haploceras /Neolissoceras/ grasianum

Neocomites /Teschemtes/ cf. muretensis Cnocerantes /C no cera tites / nolani

Subsaynella saym •Ptychoceras inostranzewi •

Cnoceratites /C noceratites/ majoricensis •— ♦ — —Cnoceratites /C n o ce ra tite s / quenstedti •-----------

Cnoceratites /C n o cera tites / ernenn Cnoceratites /Pseudothurmanma / mortilleti Cnoceratites /Pseudothurmanma/ belimelensis

Partschiceras intundtbulum Barremites /B arrem ites/ aff. psilotatus

Barremites /B arrem ites/ waagem Barremites / Barremites/ d itfm h s

.Hamulimtes

• Protetragomtes crebnsulcatus• Costidiscus recticostatus •Eulytoceras phestum

Silesites seranoms

parvulus

Fig. 6. Lithostratigraphical correlation of Mrâznické lûky-sections and distribution of the main fossils (loci 2-6, Fig. 1).

oo sten Sarasin & Schöndelmayer, B. neocom ien sis d ’O rbigny, co-occuring with primitive aptychi L. n on cu s (W inkler), L. aplanatus (G illieron), L. ex gr. m ortilleti. The latter forms differ from the typical subspecies L. m. m ortilleti (P ictet & Loriol) by more complicated course of ribs and we ascribe them to L. m ortilleti retroflexus T rauth and to L. m ortilleti ssp. (Fig. 6).

Spotted limestone complex of the Strâzovce section (8), we earlier considered to be Lower Hauterivian in age, relying on findings of the first crioceratiform ammonites in its close

overlie (M ic.halIk & V aSi’Cek 1979, Borza et al. 1980), belongs evidently also to the lower Upper Valanginian.

The horizon with the last primitive aptychi, is covered by layers probably equivalent to the H imantoceras trinodosum Zone with arcuate bended fragments fH im antoceras T hieuloy and with incomplete free-coiled shells, ribbed similarly to the Upper Hauterivian A egocrioceras Spath, or to Upper Valanginian Judd icera s Spath (however, both the genuses were described from the Boreal realm until only). The sole well determinable specimen of H imantoceras acuticostatum T hieu-




loy comes from a little outcrop near Zemianska Zavada (SSE from Povazska Bystrica, cf. Fig. 1).

The aptychi, found in this level, are represented exclusively by forms with backward to the umbo bounded nbs. Further free-coiled ammonite types with ribs bifurcated on the circle of ephebic coils appear in overlying horizons (Stra- zovce section, loc. S, Fig. 1; Fig. 4). According to the Butkov-material (loc. 9, Fig. 1; Fig. 7) they are identical with Cnosarasinella h eterocosta ta (M andov) (sensu J.-P.

T hifuloy 1977). This species occurs in the Tescbenites ca lli- discus Zone of lower Uppermost Valanginian. Interestingly, neither this zonal species known from the Silesic unit of Outer West Carpathians, nor other Tescbenites have been found in this horizon in the Strazovske vrchy Mts. Scarce belemnites Pseudobelus b rev is Paquier, D uvalia dilatata (Blainville), D. binervia (Raspail) and H ibolites ciga retu s Stoyanova- V ergilova accompany this fauna.

VALANGI NI AN H A U T E R 1 V I A N B A R R E M I A N A P T I A N ALBLOWER ¡UPPER LOWER 1 UP P ER LOWER | U PPER c o r

LameUaptychus aplanatus aplanatus ---------- • L.aplanatus retroflexus

• L.mortilleti L beyrichodidayi

L. didayL seranoms seranoms

mortiltetiDTJ

'C

L angulodidayi L seranoms fractocostatusLongulicostatus fractocostatus

l martilleti longus •L. ongul(COstatus longus

Di =r

L angulicostatus anguiicostatus*—--------------------• Olcostephanas sp.---------------------------------♦ — ^ l i > i i l Hapioceras grasionum• Busnardoites sp.• Kibanella e* gr pexiptycha• PtychophyHoc eras sp

Lyticocfras ex gr crypt oceras• Neocomites (Teschemtes )c t • pachydrcranus

•Cnosarosinelta hetercx:ostota• Lytoceras ex gr sutile

10lcostephanus(0.) psiloslomus iBochtanites oosten ► Neocomites (T) neocomiensiformls

Leopold« sp. •Etemceras cftctiechitev ••

O tcostephanus{0)cf astierianus M M Sarasinella off vonans •Crioceratites (C-) nolani •♦♦—♦•

Abrytusttes sp • ------------------------------------------------------ • -• -NeocomitesiT) ct jodariensis •

Eteniceras cf mkolovi •Spitdsscus cf nodosus •

Lytoceras subfimbnatum ••—•---------------------------•Spitrdiscus cf meneghim •—•

Crroceratites C-) lory i •

D

3

3

oD

(D

in

o tno3

OPc7TO<

l/lfDao'Dl/l

• Costidiscus recticostatus ► Valdedor sella sp.

• Holcodiscus perezianus ----------------- •—•Barremites (Cossidoiceras) sp

Anahamuhna sp • 7 Leptoceras sp.»Crioceratiles{C .)cf. mojoricensis

• Ptychoceros sp► Barremites (B) sp-

►Partschiceras infundibulum

Hibolit« cigoretusPseudobelus brevis •-------------------Vounagites pistil (if a r m is •--------- • —Ouvalia binervia ♦ —Duvalia dilatata dilatata •-------- •—■

Hi bo l i t es l o n g i o r •

—• Criocerotdes (C.) duvali----- • Euphyl loc eras sp• Plesiospitidiscus sp

• — • — •

Hibolites cf. jaculoides •------------ •-Mesohibolites cf.uhligi* Hibolites mirificus

I---------- “•Duvalia grasiana•Mesohibolites varians

• M.minaret• — • • M gladnformis

• M.platyurus • M. garshmi

C5~fD

fD

3Z3

fD

Fig. 7. Lithostratigraphical correlation of the section, incovered in the individual Burkov quarry-floors and fossil distribution in the incovered sequence (loc. 9, Fig. 1).




3.4 HAUTERIVIAN

The Valanginian/Hauterivian boundary cannot be exactly delimited neither on the base of microfossils, nor by macrofauna. We consider the micritic nannocone limestones with abundant T eschenites n eo com ien sifom iis (U hlig), T. cf. j o - dariensis (D ouville), T. cf. pacbyd icranu s T hieuloy, Spiti- discus m en egh in ii (Z igno), Eleniceras cf. t cb e cb ite v i Bres- kovski etc., with microplankton like N annoconus steinm anni K amptner, N. co lom i (de Lapparent), N. globu lu s B roni- mann, N. kamptneri Bronimann, less frequently with Glo- bo cha ete alpina Lombard, Cadosina fu s e a fu sca W anner, C. cf. cieszynica N ow ak , C. sem iradiata olzae N ow ak, C olo- mispbaera heliospbaera (V ogler), C. v o g le r i (), Stom iospbaera eebinata N ow ak , S. w ann eri , G em eridella m inuta & M iSIk , D idem noides m oreti (D urand D elga), D idemnum carpaticum M iSi'k & , rarely with Tininnopsella carpatbica (M urgeanu & F ilipescu) and with the foraminifers (Spirillma sp., Patellina sp., Lenticulina sp., H eterobelix sp.) belonging to the Lower Hauterivian.

An expressive complex of rhythmically bedded organode- trital, cherty and marly limestones with marly intercalations (Strazovce Formation) characterizes the deeper basinal slope (Strazovce section, loc. 8 in the Fig. 1, or Fig. 4). The base of each rhythm consists of detritic, gradationally bedded horizons with frequent clasts. Organic remains are fragmentary, often reworked. They frequently belong to shallow-marine organisms (gastropods, solenoporid algae, bryozoans etc.). The formation originated in turbiditic sedimentary regime.

Thin turbidites have been found in Butkov Lower Hauterivian sequence. However, a horizon of carbonate breccia, analogical to the Valanginian Nozdrovice Breccia occurs here, too. The first representatives of C rioceratites (C. nolani ¡Lilian, somewhat higher C. lory i Sarkar) and A brytusites sp. appear above the horizon with the last T eschen ites (Fig. 7).

The uppermost Lower Hauterivian (both the French O lco- stepbanus jea n n o ti and L yticoceras nodosop lica tus Zones) is not faunistically proved by us. However, according to several authors (Trauth 1938, Stefanov 1961, G asiorowski 1962) the occurrences of frequent aptychus L. d idayi (C oquand) terminates just at the end of the Lower Hauterivian. Therefore, we used this criterium by delimitation of the Lower/Upper Hauterivian boundary in both the Strazovce- and Butkov sections.

The overlying deposits of such delimited Lower Hauterivian contain aptychi with angularly broken ribs like L. angu - licostatus (P ictet & Loriol), similar to the typical subspecies, or to L. angulicostatus longus Trauth. Moreover, C riocera tites du va li LEveille and E uptychoceras sp. co-occur with this aptychi in the Butkov section, and sole specimen of Sub- saynella sayni (Paquier) - the index ammonite of the French basal Upper Hauterivian according to Thieuloy (1973) have been found in an equivalent level of the Kamenna section (loc. 2, Fig. 1).

The uppermost Hauterivian Plesiospitidiscus ligatus Zone has not been safely macrofaunistically documented.

3.5 BARREMIAN

The macrofaunistically richest complex of the Carpathian Lower Cretaceous, the Pseudothurmannia Horizon appears in several sections (loci 1, 2, etc., cf. A damikova et ah, in press), above the deposits of Hauterivian s. str. It consists of 6-10 m thick complex of brown-gray micritic limestones with rich cephalopod fauna. The main part of microfossils belongs to nannocones, along with them more sporadically occur Stom iospbaera alpina L eischner, Cadosina sem iradiata olzae N ow ak , Colom isphaera v o g le r i (Borza), G lobocha ctc alpina Lombard, calcified radiolarians, ostracods and foraminifers (“H edb erge lla ” sp., Spirillina sp., Patellina sp., Lenticulina sp., Frondicularia sp., Fleterobelix sp.) and many others. C rioceratites s. str. prevail over infrequent Pseudo- thurmannia in the ammonite fauna. Last lamellaptychi with angularly broken ribs co-occur with these ammonites. In agreement with Lapeyre & T homel (1974) and A damikova et al. (in press) we consider this association to be Lower Barre- mian in age. However, the last occurrence of aptychi, closely connected with the underlying Hauterivian associations and the sudden disappearing of all the crioceratids above the Pseudothurmannia Horizon indicate a close connection of this horrizon with the Upper Hauterivian sequence.

The equivalent of the Pseudothurmannia Horizon behind the limits of its typical development can be recognized by monotonnous aptychi with angular ribs association and, probably also by appearing of H ibolites ja cu lo id es Swinnerton- like belemnites.

The higher Lower Barremian horizons are in all the studied sections indicated by expressive deepening of the basin. The crioceratid fauna, inhabitor of relatively shallow bottom has been in short time span completely substitued by monotonnous barremitid ammonites - good swimmers, able to live in a free pelagic environment. The latter fauna occurs in black marlstones, micritic and spotted limestones with distal turbiditic structures. Ellipsagelospbaera dominates in the low-diversified nannoplankton associations, the microplankton consists of Stom iospbaera w ann eri Borza, S. alpina L eischner, and of other forms (cf. Figs. 4, 5, 6), the foraminifers comprise frequent H edbergella sp ., Spirillina and Lenticulina. Lower part of the barremitid horizon yielded infrequent aberrant shells of Hamulina lorioli (U hlig), Hamulim tes parvu lu s (U hlig), Anahamulina sp., Karsten iceras sp., more rarely spirally coiled Pulcbellia compressissima (d ’O r- bigny), H olcod iscu sperez ianus (d ’O rbicny), etc., solely also the belemnite M esohibolites sp.

The zonal species Silesites seranonis (d ’O rbigny) and C o- stidiscus recticosta tus (d’O rbigny) occur in the Upper Barremian deposits, while M esohibolites (M. gladiiforrn is U hlig, M. p la tyuru s D uval- J ouve, M. m inaret R aspail and other) dominate in the belemnite fauna.

3.6 APTIAN

A complex of black-gray and gray detritic cherty limestones with characteristical breccia horizon on their base represents the products of Aptian sedimentation in the Butkov section (loc. 9 in the Fig. 1; Fig. 7). Gray silky marls with inter-




;;

::

E <■Z3

vP~

t/> ro\ ia oj ' 1/1 —

a . o ° ‘- czJ T™ =Jdi ajoo

I o«500 GJ QJ

E ooCJ

roCD

f

cLoo

cloo

oo<u

i

Fig. S. Lithostratigraphic correlation and the distribution of main fossils in the Horna Poruba-section (loc. 7, Fig. 1).

calations of black-gray detritic limestone, lime breccias and paraconglomerates, tuffites and basic volcanics represent this level in other sections. They contain microfossils Praecolo- miella tre jo i Borza, P. b on eti Borza, D eflandronella v e ra - cruzana (Trejo), ParachitmoidelL 1 cf. ciiv illier i T rejo etc., foraminifers (b lcd b erg e lla sp., Sabaudui m inuta [Hofker], Nautiloculina sp., Palorbitolina cf. len ticu laris [Blumen- bac.h], etc.). The Aptian macrofauna has been found in sole horizons of Horna Poruba section (Fig. 8), being represented by incomplete specimen, similar to D esbayesites invohitiis Spath.

Fragments of bivalve shells, conoids, solenoporids, serpu- lids and orbitolinid foraminifers in the biopelsparitic and bio- intrasparitic limestones in higher pan of the Butkov detritic complex (Fig. 7) and in the conglomerate horizons in other localities indicate Upper Aptian age (cf. Fig. 6).

3.7 LOWER ALBIAN

The uppermost horizon in the Butkov detrital complex consisting of light-gray micritic limestones contains a rich microfossil assemblage (ColomielLi recta Bonet, C. mexicana Bonet, Piemnia ob lon ga Borza & M iSIk etc.) and foraminifers Sabaudia m inuta (Hofker), O rbitolina texana (R oemer) and others, indicating its Lower Albian age. Hard ground with borings of benthic organisms is developed on the surface of this horizon, covered by Upper Albian shally complex.

The complex of spongolithic micrital limestones near the base of Albian shales in Mraznicke luky region (loci 2-6) and Horna Poruba (loc. 7) with Calpionellopsella maldonadoi Trejo & Colom iella recta Bonet represents the last episode of carbonate sedimentation in the studied area. The environment of carbonate sedimentation definitively turned into a flysch basin, controlled by an active tectonic pulse of folded orogen.




4. SUMMARYDevelopment of the Lower Cretaceous Krizna-basin has

been more complicated than usually treated. Remarkable occurrence of Lower Valanginian Nozdrovice Breccia indicate an effect of Late Kimmerian deformation of external zones. The clastic and turbiditic horizons, incorporated in Hauteri- vian, Barremian and Aptian sequences, indicate an increasing tectonic pulse, a symptom of Austrian orogenic phase, culminating during Albian/Cenomanian.

The combination of several parastratigraphical schemes, based on several organic groups (ammonites, aptychi, belemnites, micro- and nannoplankton) gets over the gaps in the recent biostratigraphical division of the Jurassic-Lower Cretaceous deposits of Krizna nappe. Particularly expressive advance has been achieved in the division of Valanginian and Hauterivian sequences (Tab. 1).

Table 1

A M M O N I T E S A P T Y C H I B E L E M N I T E S

APTIAN D esbayesites ex gr. in v o lu tu s Spath

BARR

EMIA

N

UPP

ER

S i le s i t e s seranon is (d'Qrbigny) B arrem ites Sp.Costidiscus r e c t ic o s ta tu s (d'Qrbigny)

M e s o h ib o lite s g la d iifo rm is (Uhlig) H ib o l i te s m ir i f ic u s Stoyanova-Vergilova M e s o h ib o lite s p la ty u ru rs (Duval-Jouve) Mesohibolites m inaret (Raspail)

LOW

ER

B arrem ites (B.) ex gr. d i f f i c i l i s (d'Qrbigny)

Hamulina l o r i o l i Uhlig H am ulin ites parvu lus (Uhlig) P u lc h e l l ia com pressissima (d'Qrbigny) C r io c e r a t i te s (C.) m a jo r ic e n s is

(Nolan)C r io c e r a t i te s (C.) e m e r ic i Lêveillé Pseudothurmannia m o r t i l l e t i (Pictets

Loriol)Lam ellaptychus a n g u lico s ta tu s longus

Trauth

D uva lia b in e rv ia (Raspail)D uva lia grasiana (Duval-Jouve) H ib o l i te s lo n g io r Schvastzoff H ib o l i t e s cf. ja c u lo id e s Swinnerton

HAUT

ERIV

IAN

UPP

ER

C r io c e r a t i te s (C.) du va li Léveillé Subsaynella c f. sayni (Paquier)

L . a n g u lic o s ta tu s a n g u lico s ta tu s (Pictet & Loriol)

D u va lia d i la ta ta d ila ta ta (Blainville)

LOW

ER

C r io c e r a t i te s (C.) l o r y i (Sarkar) C r io c e r a t i te s (C.) n o la n i (Kilian) A b ry tu s ite s sp.E le n ice ra s tc h e c h ite v i Breskcwski Neocom ites (T e s ch e n ite s ) c f. jo d a r -

ie n s is (Douvillé)S p it id is c u s c f. m enegb in ii (Zigno) Neocom ites (T e s ch e n ite s ) neocom ien-

s ifo rm is (Uhlig)

L. d id ay i (Coquand)

L . a n g u lic o s ta tu s fra c to c o s ta tu s Trauth

Pseudobelus b re v is Paquier

VALA

NGIN

IAN

UPP

ER

C r io s a ra s in e lla h e te ro co s ta ta (Mandov)

Him antoceras sp. ,Jud d iceras Sp. B o ch ia n ites neocom iensis d'Qrbigny Neocom ites (N.) neocom iensis

(d'Qrbigny)Neocom ites (N.) teschenensis (Uhlig)

L. seranon is (Coquand)L . a ff. m o r t i l l e t i L . m o r t i l l e t i SSp. 1.L. m o r t i l l e t i r e t r o f le x u s Trauth

Hibolites c ig a re tu s Stoyanova-Vergilova Duva lia d i la ta ta (Blainville)

LOW

ER

K i l ia n e l la ex gr. pex ip tych a (Uhlig) B usnardoites sp.

L. aplanatus r e t r o f le x u s Trauth L . aplanatus ap lanatus Gilliéron

L. n o r ic u s (Winkler)

BERRIA-SIAN

TITHO- NI AN

L . m o r t i l l e t i m o r t i l l e t i (Pictet S Loriol)

L . m o r t i l l e t i n o r icu s Trauth L. s tu d e r i s tu d e r i (Qoster)L. b e y r ic h i b e y r ic h i (Oppel) Punctaptycbus puncta tus punctatus

(Voltz)

Duva lia la ta (Blainville)




5. REFERENCESA damikOVA, G., M ichalik, J., V aSiCek Z. (in press): The composi

tion and ecology of the fauna of “Pseudothurmannia Horizon” (Lower Barremian) in the Krizna-nappe of Strâzovské vrchy Mts. - Geol. zborn. Geo], Carpath., Bratislava.

A ndrusov, D., Bystrickv, J., FusAN, O. (1973): Outline of the structure of the West Carpathians. Guide-book for geological excursion X. Congr. Carp.-Balk. geol. Assoc., 1973, 5-45, 5 figs., Bratislava.

Borza, K., GaSparikova, V., M ich a u k , J., VaSiCek., Z. (1980): An Upper Jurassic-Lower Cretaceous sequence of the Krizna-nappe (Fatric), Strâzovské vrchy Mts. - Geol. zborn. Geol. Carpat., 31 (4), 541-562, 4 figs., 7 pis., Bratislava.

— MiCHALiK, J., V aSiCFK, Z. (1982): Lithogenesis, paleoeco- logy and biostratigraphy oi the Jurassic and Lower Cretaceous deposits of the Krizna-nappe in Strâzovské vrchy Mts. (in Slovak). - Nafta a plyn, 26, 4, 625-638, 8 figs., Hodonin.

Busnardo, R., Thieuloy, J.-P., Moullade, M. (1979): Hypostratotype Mesogeen de l'étage Valanginien (sud-est de la France). - Comm. Franç. de Stratigr., Les Stratotypes Français, 6, 5-143, 9 tabs., 10 pis., 35 figs., Paris.

G asiorowsm, S. M. (1962): Aptychi from the Dogger, Malm and Neocomian in the Western Carpathians and their stratigraphical value. - Stud. geol. Polon., 10, 144 p., 10 figs., 6 tabs., 8 pis., Warszawa.

Lapi YRh, J.-F., ThoMEL, G. (1974): Consideration sur la valeur et la situation stratigraphique précise de la Zone â Anguhcostata (Néocomien). - C. R. Acad. Sci., 278 D, 2889-2892, Paris.

M aheL, M. (1979): Paünspastic picture of the West Carpathians in the basic evolutionary stages. In : Geodynamic investigations in Czechoslovakia, final report, SIov. Ac. Sci., 179-186, Bratislava.

M ichalik, J., VaSiCek, Z. (1979): To the problems of palinspastic and paleogeographic reconstruction of Lower Cretaceous sedimentary area in Strâzovské vrchy Mts. (in Slovak.). - In: Vâznejsie problémy geologického vyvojaetc., Smolenicecon- ference 14-16.11.1979, Oil and gas geology, C, 265-290, Bratislava.

-------&: Borza, K., Puti , M., Rakus, M. (1980): A guide to theStrâzovské vrchy Mts. and the neighbouring Klippen Belt zone (in Slovak.). - In: Materials of 23. Slovak geol. Soc. Conf. 1980, 67-93, Bratislava.

— — & KovaC, M. (1982): To several problems of palinspastic reconstruction and Meso-Cenozoic development of the Western Carpathians. - Geol. zborn. Geol. Carpat., 33, 4, 145-192, Bratislava.

STEPANOV, 1. (1961): Ammonite opercula (aptychi) of the Bulgarian Lower Cretaceous. - Trudy geol. Bulg. druz., paleont., 3, 209-235, Sofia, (in Bulgarian).

Thieuloy, J.-P. (1973): The occurrence and distribution of Boreal ammonites from the Neocomian of Southeast France (Te- thyan Province). - Geol. Journ. spec, iss., 5, 289-302, Liverpool.

------- (1977): La Zone â Calhdiscus du Valanginien supérieur (sud-est de la France). Lithostratigraphie, ammonite fauna, limite Valangmien/Hauterivien, corrélations. - Géol. Alp. 53, 83-142, Grenoble.

Trauth , F. (1938): Die Lamellaptychi des Oberjura undderUnter- kreide. - Palaeontographica, A 88, 118-240, Stuttgart.

VaSiCek., Z., MiCHALîK, J . (1981): Remarks to the Lowei Cretaceous stratigraphy and paleogeography of the northern part of the Western Carpathians. - Geol. zborn. Geol. Carpat., 32/1, 143-153, Bratislava.




Fig. 1.

Fig. 2.

Fig. 3.

Fig. 4.

Fig. 5.

Fig. 6.

Fig. 7.

Fig. 8.

Fig. 9.

Fig. 10.

Fig. 11.

Fig. 12.

Plate 1

Kdiattella ex gr. pexiptycba UHLIG, x l . Specimen BK 8-565/7. Butkov quarry, 8. floor upper Lower Valanginian.

Himantoceras sp., x2. Spec. ZC-2522. Strazovke section, 2522 m, Upper Valanginian.

Juddiceras sp., x 1. Spec. ZC 2995/8, Strazovce section, 2995 m, Upper Valanginian.

Himantoceras acuticostatnm THIEULOY, x 1. Spec. ZZ-5/1. Zemianska Zavada.Upper Valanginian.

Criosarastnella heterocostata MANDOV, XL Spec. BK 8-510/2. Butkov quarry, 8. floor uppermost Valanginian.

Crioceratites (Cnoceratites) nolam KiLIAN, x l . Spec. BK 8—140. Butkov-quarry, 8. floor Lower Hauterivian.

Neocomites (Tescbenites) cf. jodartensis Douville, x 1. Spec. BK 8—170/16.Butkov-quarry, 8. floor, Lower Hauterivian.

Spitidiscns cf. meneghmu ZiGNO, x 1. Spec. BK 6-80/2.Butkov quarry, 6. floor. Lower Hauterivian.

Cnoceratites (Cnoceratites) ditvalt Leveii LE, x 1. Spec. BK 8—100/2.Butkov quarry, 8. floor, Upper Hauterivian.

Pnlcbellia compressissima D’Orbigny, x 1. Spec. BK 8-170/9.Butkov quarry, 8. floor, Lower Barremian.

Hamidina lonoh U hlig , X 1. Spec. PL 1-4/7. Polomec, Zabukovinske quarry near Lietavska Lucka, Lower Barremian.

Desbayesites ex gr. involntus SPATH, x 1,5. Spec. HP-580, Horna Poruba-section,Lower Aptian.



Zitteliana 10, 1983 © Biodiversity Heritage Library, http://www.biodiversitylibrary.org/; www.zobodat.at

V aSiCek, Z ., M ichalIk , J . & Borza Plate 1




Plate 2

all magnifications 285 x

Fig. 1. Cbitinoniella boncii Doben, thin section 7587, Strazovce section, 2025 m, Chitinoidclla Zone, Middle Tithonian.

Fig. 2. Calpionella alpina LoRENZ, thin section No 7589. Strazovce section, 2060 m, Calpionella Zone, Tithonian/Berriasian.

Fig. 3. Crassicollana parvnla REMANE, thin section No 7588, Strazovce section 2050 m, Calpionella Zone, Tithonian/Berriasian.

Figs. 4-5. Tintinnopsella carpathica Murg. & Finn., thin sections 7590, 7592, Strazovce section 2060, 2090 m, Calpionella Z., Tithonian/Berriasian.

Fig. 6. Calpionellopsis simplex COLOM, thin section No 7593, Strazovce section 2100 m, Calpionellopsis Z., Berriasian/Valanginian.

Fig. 7. C. oblonga (Cadisch), thin section No 7594, Strazovce section 2110 m, Calpionellop- sis Zone, Berriasian-Valanginian

Fig. S. Remaniella cams chi ana (Colom), thin section No 7593, Strazovce section 2100 m, Calpionellopsis Zone, Berriasian-Valanginian.

Fig. 9. Tintinnopsella longa (COLOM), thin section No 7681, Pod Svinornÿm Gorge-section, Calpioncllites Zone, Berriasian-Valanginian.

Fig. 10. Calpionelhtes darderi (COLOM), thin section No 7596, Strazovce section 2140 m, Calpioncllites Zone, Berriasian-Valanginian.

Fig. 11. Praecolomiella trejoi Borza, thin section No 7710. Pod Mriznicou Gorge-section, Praecolomiella Zone, Aptian.

Fig. 12. Deflandronella veracruzana Trejo, thin section 7710, Pod Mraznicou G.-section, Praecolomiella Zone, Aptian.

Fig. 13. Colomiella mexicana BONET, t. s. No 47a/8, Butkov section, Colomiella Zone, Aptian-Albian.

Figs. 14-15. Colomiella recta BONET, t. s. No 47a/8l, Butkov section, Colomiella Zone, Upper Aptian-Albian.

Fig. 16. Colomispbaera mimttissima (COLOM), t. s. No 7587, Strazovce section 2045 m, Calpionella Zone, Tithonian/Berrasian.

Figs. 17-18. Parastomiospbaera malmica (Borza), t. s. No 2005 (g), Strazovce section, 2005 m, Lower Tithonian.

Fig. 19. Cadosina minuta BORZA, t. s. No 7703, Pod Strane Gorge-section, Calpionellopsis Zone, Berriasian/Valanginian.

Fig. 20. Didemnum carputicum MlSlK & BORZA, t. s. No 7652, Strazovce section 3270 m, Barremian.

Fig. 21. Stomiosphaera echmata Nowak, t. s. No 7607, Strazovce section 2605 m, Valanginian.

Fig. 22. Colomispbaera vogleri (Borza), t. s. No 8E-320/81, Butkov quarry, 8. floor, 320 m, Hauterivian.

Fig. 23. Colomispbaera beliospbaera (VOGLER), t. s. 8E-290/81, Butkov quarry, 8 floor, 290 m, Hauterivian.

Fig. 24. Cadosina fusca cieszymca Nowak, t. s. No 8E-5/81, Butkov quarry, 8. floor, 5 m, Aptian.

Fig. 25. Cadosina semiradiata olzae NOWAK, t. s. 8E-5/81, Butkov quarry, 8. floor, 5 m, Aptian cherty limestones.



Zitteliana 10, 1983 © Biodiversity Heritage Library, http://www.biodiversitylibrary.org/; www.zobodat.at

V a SICf.k , Z., M ichalik, J. & Borza, K. Plate 2



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