Jurassic–Cretaceous controversies in the Western Carpathian Flysch: the “black flysch” case...

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Cretaceous Research 25 (2004) 89e113

JurassiceCretaceous controversies in the WesternCarpathian Flysch: the ‘‘black flysch’’ case study

Nestor Oszczypkoa,), Ewa Malataa, Lilian Svabenickab,Jan Golonkaa, Frantisek Markoc

aInstitute of Geological Sciences, Jagiellonian University, Oleandry 2a, 30-063 Krakow, PolandbCzech Geological Survey, Klarov 131/3, 118 21 Praha, Czech Republic

cDepartment of Geology and Paleontology, Faculty of Science, Commenius University,

Mlynska Dolina, 842-15 Bratislava, Slovak Republic

Accepted 15 October 2003

Abstract

The age of the ‘‘black flysch’’ deposits in the Polish sector of the Pieniny Klippen Belt (Western Carpathians) has been a subject

of a long lasting controversy. References to both the Middle Jurassic and the mid-Cretaceous have been made. The ‘‘black flysch’’ aswell as overlying deposits, exposed in two sections located in the Slovakian and Polish segments of the Pieniny Klippen Belt(Western Carpathians), are the subject of this paper. A detailed examination of their foraminiferal and calcareous nannofossil

content, carried out on 59 samples, has revealed in most samples the presence of redeposited Jurassic and Cretaceous microfossils.Analyses of our results and other published data have proved an AlbianeCenomanian age for the ‘‘black flysch’’ deposits andbrought to light new information on the reworking processes of the Jurassic and Lower Cretaceous sediments and fossils whose

presence has led to previous misinterpretations of the biostratigraphic record.� 2004 Elsevier Ltd. All rights reserved.

Keywords: Western Outer Carpathians; Pieniny Klippen Belt; Magura Nappe; Jurassic; Cretaceous; Black flysch; Foraminifera; Calcareous

nannofossils; Redeposition

1. Introduction

Horwitz (1929), during his early investigations on thePieniny Klippen Belt (PKB) (Fig. 1), distinguished blackshales of the Wierzowice (Verovice) type with interca-lations of thin- and thick-bedded sandstones rich inmuscovite flakes. These beds were described as the‘‘Black Cretaceous’’ of Barremian to Albian age. Thisage determination was based on sparse occurrences ofmacrofauna (inoceramids, belemnites and crinoids). Afew years later Horwitz (1933) revised his formeropinion and assigned the black shales to the MiddleJurassic as the ‘‘Dogger Flysch’’. In Birkenmajer’s(1960) early stratigraphical scheme of the PKB, thismember was called the ‘‘Aalenian Flysch’’.

) Corresponding author.

E-mail addresses: [email protected] (N. Oszczypko), malata@

ing.uj.edu.pl (E. Malata), [email protected] (L. Svabenicka), golonka@ing.

uj.edu.pl (J. Golonka), [email protected] (F. Marko).

0195-6671/$ - see front matter � 2004 Elsevier Ltd. All rights reserved.

doi:10.1016/j.cretres.2003.10.006

According to Sikora (1962), at least a part of the bedsassigned to the Aalenian Flysch that crops out in Polandis also Cretaceous in age. Sikora’s (1962, 1971a,b) andBlaicher and Sikora’s (1969) ideas on the age of the‘‘black flysch’’ of the PKB and their concept of theSztolnia beds were rejected by Birkenmajer (1963) andBirkenmajer and Pazdro (1968). In reply to Sikora(1962) they argued that the microfauna from the shalesclearly indicated a Middle Jurassic age, whereas theCretaceous planktonic foraminifera reported by Sikora(1962) were the result of contamination. This opinionwas supported by the presence of the Middle Jurassicostracods, bivalves and ammonites (B1aszyk, l968;Birkenmajer and Myczynski, 1977). Sikora (1971a,b)and Blaicher and Sikora (1969) disagreed with thesecritical papers and explained that the presence of theJurassic foraminifera in the Earlyemid-Cretaceous‘‘black flysch’’ was caused by redeposition. Golonkaand Raczkowski (1984a) noted several species of

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90 N. Oszczypko et al. / Cretaceous Research 25 (2004) 89e113

Fig. 1. A, geological map of the middle part of the Western Carpathians (compiled by Oszczypko-Clowes, 2001, simplified). B, position of the Polish

and Slovak Flysch Belt in the Carpatho-Pannonian system.

agglutinated, calcareous benthic and planktonic fora-minifera found by Blaicher in the black flysch in Poland(namely Rotalipora spp., Praeglobotruncana cf. stephani(Gandolfi) and Hedbergella spp. among others) whichsupported an AlbianeCenomanian age for these depos-its. In 1977 Birkenmajer established in the Magurasuccession (Fig. 1) of the PKB the Lower AlbianWronine Formation (of black flysch development) andthe Upper AlbianeMiddle Cenomanian Hulina Forma-tion. Gedl and Gedl (2001a) studied the dinocystassemblages in the Hulina and Wronina formations.According to their investigation LowereUpper Ceno-manian, uppermost Albianeuppermost Cenomanian,uppermost CallovianeOxfordian, and BathonianeCallovian assemblages were found mixed in the section.According to Sikora (1971a,b) the Albian/CenomanianSztolnia beds were underlain by the Wronine beds, andfollowed by the Sprzycne beds (Cenomanian).

Ksia_zkiewicz (1977) shared Sikora’s (1962) point ofview, and based his opinion on the fact, that the ‘‘blackflysch’’ deposits formed a consolidated and mappableunit, which almost always dipped beneath the Creta-ceous variegated shales. Therefore on the GeologicalMap of Poland the ‘‘black flysch’’ was assigned tothe AlbianeCenomanian (Golonka and Raczkowski,1984b).

The latest discovery of a new section in the Slovaksector of the PKB (Fig. 1) renewed the discussionpresented above. We decided to conduct detailedmicropalaeontological studies based on different groupsof microfossils. A range of palaeontological investiga-tions is particularly important in orogenic suture zonessuch as the PKB, which is located along the boundarybetween the Inner Carpathians and the Outer Carpa-

thian accretionary wedge where undisturbed stratigra-phic sequences are scarce and correct age determinationis critical for the reconstruction of the basin andorogenic development. In our opinion the black flyschstudies provide a perfect example of redeposition offossils within flysch sequences, which can lead tocontroversial conclusions from the palaeontologicalrecord.

2. Black flysch within the Pieniny Klippen

Belt framework

The Carpathians (Fig. 1) form a part of the great arcof mountains that stretches to more than 1300 km fromAustria to the RomanianeSerbian border. In the westthe Carpathians are linked with the Eastern Alps, and inthe east pass into the Balkan chain. Traditionally theNorthern Carpathians are subdivided into an olderrange known as the Inner Carpathians and the youngerone known as the Outer or Flysch Carpathians(Ksia_zkiewicz, 1977). The Pieniny Klippen Belt (PKB)is situated at the boundary of these two ranges. TheInner Carpathian nappes contact along the Tertiarystrike-slip boundary with the PKB. The PKB isa narrow, elongated tectonic unit 800 km long and1e20 km wide, which follows the Carpathian suturezone or an ancient subduction zone. The PKB iscomposed of several successions, covering a time spanof Early Jurassic to Paleogene. The Late JurassiceEarlyCretaceous Pieniny Basin (Fig. 2) is well marked bySWeNE-trending facies zones (successions), whichcorrespond to ridges and troughs on the sea floor.Reorganization of plate systems, which followed the

91N. Oszczypko et al. / Cretaceous Research 25 (2004) 89e113

EUROPEAN PLATFORM

Helvetic Kurovice Racza Grajcarek Czorsztyn

NiedzicaZawiasyUdol

Pieniny Zlatna Klapa Manin

CONTINENTAL CRUST BASALT

LIMESTONE MARLFLYSCH

CHERT

NW SECzertezik

Fig. 2. Highly schematic cross-section (not to scale) showing the Pieniny and Magura basins during the Albian.

Eo-Cimmerian orogeny, resulted in rifting and incipientspreading in the AlpineeCarpathian area and gave riseto the PKB Basin. A restricted environment prevailed inthis newly formed basin. Black Posidonia shales, spottymarls (Fleckenmergel) and presumably some synriftturbiditic black deposits known from the PKB Basinindicate oxygen depleted conditions (Birkenmajer, 1986;Tyszka, 1994).

During the MiddleeLate Jurassic there was a spread-ing phase with rapid subsidence and extremely con-densed sedimentation in the basinal parts. The PieninyBasin was divided by the Czorsztyn Ridge into sub-basins (Fig. 2). The deepest part of the south-easternbasin is documented by extremely deep-water JurassiceEarly Cretaceous deposits (Sikora, 1971b; Golonka andSikora, 1981). Transitional slope sequences were situ-ated between the ridge and the basinal parts. Theshallowest ridge sequences are known as the Czorsztynsuccession. Dark grey Early Jurassic deposits in thissuccession are followed by Middle JurassicelowermostCretaceous crinoidal and nodular limestones and UpperCretaceous variegated marls. During the AptianeAlbian complex tectonics in the zone of the futureAlpine belt commenced, marking the beginning of thesynorogenic stage in the Pieniny/Magura Basin man-ifested by deposition of the black flysch.

Anoxic conditions occurred twice, first during theEarly Jurassic and then in the AlbianeCenomanian,leading to deposition of similar deposits. The ‘‘blackflysch’’ deposits could have belonged to both of theseanoxic sequences. The boundary between the LowerCretaceous black flysch and underlying deposits isuncertain. The black flysch deposits are usually overlain

by green shales and higher up the section by UpperCretaceous red marls and shales.

According to Krawczyk and S1omka (l986) the blackflysch in the Jaworki area is composed of shales,sandstones, mudstones, siderites, thin coal intercala-tions, and fragments of exotic rocks. A thin-beddedturbidite succession in the formation is dominated bydark-coloured, micaceous and calcareous shales in-tercalated by fine, horizontally laminated, relativelycoarse-grained, thin- and very thin-bedded sandstones.Among the thick-bedded, coarse-grained sandstonestwo varieties were recognized: Tab turbidites, and layersof structureless sandstones with shale clasts (fluxoturbi-dites) up to 4e5 m thick. The coarse and very coarse,poorly rounded material could suggest short transportfrom a low, subaerial, denuded source area (Krawczykand S1omka, l986). This may also be inferred from theabundance and relatively well-preserved remains ofcrinoids, indicating short transport (see G1uchowskiet al., 1983).

3. Sections studied

3.1. Udol (Ujak)

The Udol section is located in the LubovnianskaVrchovina highland (Figs. 1, 3, 4) close to a contact zonebetween the Magura Nappe and Pieniny Klippen Belt(PKB). In this area, according to Nemcok (1990a; b,p. 130) the PKB ‘‘is represented by predominantlymonadnocks surrounded by sediments between theMagura flysch and Inner Carpathian Paleogene’’. The


Fig. 3. Geological sketch map of the Lubovnianska Vrchovina highland and the eastern part of the Malde Pieniny Mountains (compiled after

Nemcok, 1990a and Golonka and Raczkowski, 1984b).

section studied (road-cut exposure) is situated 1 kmnorth of the centre of Udol (Ujak) village, near the smallchapel (N 48( 18,207#, E 20( 47,623#) (Figs. 1, 3).Exposures are visible on both sides of the road. A 180-m-long eastern wall has revealed four sub-verticallydipping thrust-sheets (Fig. 4). The first thrust-sheet onboth sides of the road is composed of black and darkgrey shales with intercalations of thin- and very thin-bedded (up to 10 cm), coarse- and very coarse-grainedcalcareous sandstones rich in mica and coalified flakes.The sandstone layers display parallel lamination (Tbturbidites). Thin layers of sideritic limestones occursporadically. At the top of the black flysch component,up to 20 m thick, a coarse-grained sandstone andgranule conglomerate, rich in crinoidal grains and clastsof grey limestones has been observed. Higher up thesection CenomanianeCampanian (?Maastrichtian) redand grey marls and marly limestones up to 25 m thickoccur. In these deposits the following successions havebeen recognized (Fig. 5), from which 16 samples werecollected (Fig. 4):

1. In the first thrust-sheet (east and west walls) theblack flysch is overlain by 10e12 m of soft red marls(samples U4, U5) followed by a 10-m-thick packet

of chaotic deposits (sedimentary breccia) composedof red clay matrix (U15) with well-rounded pebbles,cobbles and blocks of white crinoidal limestones(Bajocian) up to 1 m in diameter, and of cherry-red-brick limestones (?Kimmeridgian) and chertylimestones (TithonianeBarremian). This chaoticcomponent is overlain by layers of red and greymarls (U6), 1e3 m thick.

2. The east wall of the second thrust-sheet is built up offolded black flysch with imbricate synclines com-posed of red and grey marls. The lower part of thesemarls comprises 1e3-m-thick layers of soft redmarls (U8) followed by 2e12-m-thick massivesedimentary blocks of light grey, marly limestones(U10). Higher up the sequence there are 2e3 m ofred marls, 4e6 m of grey marls (U11a) and 25 m ofmassive red marls (U11).

3. In the west wall of the second thrust-sheet, the blackflysch is overlain by 10 m of light grey marlylimestones and 6e10 m of red marls. In this sequencethe chaotic member has not been observed.

In both sections (Fig. 4) the Upper Cretaceous marlsare tectonically bounded from the south by two thrust-sheets composed of Middlee?Upper Eocene variegated


Fig. 4. Geological cross-section through road-cut near Udol (Ujak). Lithostratigraphic units: 1, ‘‘black flysch’’ (AlbianeCenomanian); 2, grey and

variegated marls (CenomanianeMaastrichtian); 3, variegated marls (MiddleeLate Eocene); 4, Malcov Formation (Oligocene); samples: U1eU15.

marls and grey marly shales with intercalations of thin-bedded micaceous sandstones of the Malcov Formation(Oligocene).

The black flysch deposits in the Udol section may bewell correlated with an element described on thegeological map of Nemcok (1990a; b, p. 42) as ‘‘flyschdevelopment: sandy limestones and dark grey claystonesof AptianeCenomanian age’’ as well as with the similarrocks in the Polish sector of the PKB determined byBirkenmajer (1977) as the Szlachtowa Formation(ToarcianeLower Aalenian). The red and grey marls

of a Scaglia Rosa-type are identical to the so-calledPuchow Marls (CenomanianeCampanian), knownfrom the Slovak part of the PKB (Nemcok, 1990b)and with the Jaworki Formation (CenomanianeCampanian) in Poland (Birkenmajer, 1977, 2001).According to our observations the Upper Cretaceousmonomictic and chaotic deposits of gravitational origincan be described as olistrostromes with blocks (olisto-lites) derived exclusively from the Czorsztyn successionof the PKB. These chaotic deposits can be correlatedwith the Gregorian Breccia (Coniaciane? Palaeocene)

Fig. 5. Lithostratigraphic logs of the Udol and Sztolnia sections.


distinguished on Nemcok’s (1990a,b) geological map(Fig. 3) and with the sedimentary breccia of the JarmutaFormation at Jaworki (Birkenmajer, 2001).

3.2. Jaworki area

In the Polish sector of the PKB the black flysch wassampled along the Grajcarek, Krupianka and Sztolniacreeks in the Jaworki area of the Ma1e PieninyMountains (Fig. 2). From the Grajcarek and Krupiankasections 13 samples were collected (Fig. 6), while in thelower course of the Sztolnia Creek only two samples weretaken. Thirty-two samples were collected from the lower,middle and upper courses of the Sztolnia Creek (Figs. 6,7). The exposures in the upper course of the SztolniaCreek are located along a 250-m cross-section, whichcomprises two sections (A and B) previously studied bySikora (1962, 1971a) as well as by Birkenmajer andMyczynski (1977), and Ksia_zkiewicz (1977). Section B (asmall waterfall), ca. 40 m long, was discussed by Sikora(1962, 1971a), and Birkenmajer andMyczynski (1977). Itis presented in Fig. 7 based on our measurements made in2001. It differs in detail from the interpretations of bothSikora (1971b) and Birkenmajer and Myczynski (1977).This is probably a result of changes in the state of theexposures during the last 40 years.

The Sztolnia section represents a contact zonebetween the Magura Nappe and the Pieniny KlippenBelt defined by Birkenmajer (1977) as the GrajcarekUnit (‘‘Peri-Klippes zone’’; see Ksia _zkiewicz, 1977). This

zone displays intensively folded EarlyeLate Cretaceous,mainly clayey deposits squeezed between more rigidrocks of the Jarmuta (MaastrichtianePaleocene) andMagura (Eocene) formations (Figs. 6, 7). The section inquestion is built up of several narrow, imbricated thrust-sheets and folds, mainly with sub-vertical tectonicboundaries between the lithostratigraphic units studied.The following LowereUpper Cretaceous formationswere sampled (numbered as in Fig. 7): 3#, black flysch ofthe Szlachowa Formation (ToarcianeAalenien afterBirkenmajer, 1977, 2001), samples 14e18; 4#, dark greyshales and spotty marls of the Opaleniec Formation(lower Bajocian after Birkenmajer, 1977, 2001), samples20, 26, and 30; 5#, green and black bituminous shaleswith manganese oxide coatings of the Hulina Formation(Birkenmajer, 1977) or the Cenomanian key horizon (seeSikora, 1962, 1971a), samples 3e5, 9e11, 21, and varie-gated shales of the Malinowa Formation (Birkenmajer,1977; Birkenmajer and Oszczypko, 1989), samples 6e8,12e13, 25, 28; additionally the cherty limestone wassampled, sample 22.

4. Biostratigraphy

4.1. Methods

4.1.1. Calcareous nannofossilsSuspension slides were prepared from 50 samples using

a decantation method (separated fraction 3e30 mm) inthe followingway: the heavy fractionwas allowed to settle

Fig. 6. Geological sketch map of the Jaworki area in the Malde Pieniny Mountains (compiled after Birkenmajer, 1979 and Golonka and Raczkowski,

1984b).


Fig. 7. Geological cross-section through the upper part of Sztolnia Creek (A, after Birkenmajer and Myczynski, 1977, modified). Lithostratigraphic

units: 1, Czajakowa Radiolarite Formation; 2, Czorsztyn Limestone Formation; 3, Szlachtowa Formation; 4, Opaleniec Formation; 5, Hulina

Formation; 6, Malinowa and Jaworki formations; 7, Jarmuta Formation.

for 3 min in a 45-mm water-column, the fine fraction for45 min. Slides were inspected with a Nikon light-micro-scope at 1000! magnification. Quantitative data onnannofossil taxa were obtained by counting the numberof specimens per field of view under the microscope (fordetails, see explanation of Table 1). Biostratigraphic datawere correlated with the Jurassic nannoplankton NJzones of Bown et al. (1988, 1998), the Lower Cretaceousnannofossil BC zones of Bown et al. (1998), and theUpper Cretaceous zones of Burnett (1998).

4.1.2. ForaminiferaForty samples for foraminiferal studies were disag-

gregated by repeated boiling and freezing using sodiumcarbonate solution. They were then washed overa 63 mm screen and foraminifera were picked from theO125 mm fraction. The 63e125 mm fractions were alsoexamined but they did not contain identifiable forami-nifera. The number of specimens, species diversity andstate of preservation varied from sample to sample. Inthe case of poor samples the whole sample wasexamined for foraminiferal content. The tables depictingforaminiferal and nannofossil contents contain onlythose samples that yielded more biostratigraphicallysignificant microfossils.

4.2. Biostratigraphy of the Udol section

In the Udol (Ujak) section 12 samples were pickedfrom ‘‘black flysch’’ deposits and from red and greymarls of the Jaworki Formation. The locations of thesamples are given in Figs. 3 and 4, and the nannofossiland foraminiferal contents in Tables 1 and 2, respect-ively. The most important species are documented inFigs. 8 and 9.

4.2.1. ‘‘Black flysch’’4.2.1.1. Calcareous nannofossils. These deposits yieldednannofossils of exclusively Jurassic age in a fair or poorstate of preservation. The nearly monospecific assemb-lages are characterized by blooms of Lotharingiuscontractus. The genus Watznaueria occurs either rarelyor has not been observed at all. On rare occasions, otherspecies such as Lotharingius crucicentralis, Watznaueriabarnesae, W. britannica, Carinolithus magharensis, Dis-corhabdus striatus and Ethmorhabdus gallicus, and theevolutionary plexus of the LotharingiuseWatznaueriatransition were recorded. These fossils indicate an agerange of Late Aalenian up to earliest Bajocian.

4.2.1.2. Foraminifera. Poorly preserved assemblageswere recovered. These have a low species diversity andcomprise a low number of specimens. In sample U2 thepresence of the agglutinated taxa Haplophragmoides cf.nonioninoides (Reuss), Trochammina cf. vocontianaMoullade and Gerochammina stanislavi Neagu mayindicate an Albian age (Geroch, 1966; Neagu, 1990).Scarce specimens of Lenticulina andMarginulinopsis andmore numerous sponge spicules seem to representreworked Jurassic fossils. Sample U3 yielded a mixedassemblage of scarce, mostly tubular agglutinated taxaand some planktonic foraminifera with Hedbergellaplanispira (Tappan), Rotalipora appenninica (Renz), R.brotzeni (Sigal), and R. greenhornensis (Morrow) in-dicating a Cenomanian age (Caron, 1985). The othersamples consist of poor and non-diagnostic foraminif-era, and some crinoids, sponge spicules and echinoids.

4.2.2. Olistostrome of red and grey marls4.2.2.1. Calcareous nannofossils. Sample U10 yieldedrich but poorly preserved nannofossils of remarkably


Table 1

Calcareous nannofossil distribution in the Udol (Ujak) section

Udol Jurassic Jurassic?

Cretac.

Late Cretaceous

?Aalenian Early

Bajocian

Early Bajocian Cenom. Turon.

Coniac.

Coniacian Campanian

Middle Late

Calcareous nannofossil zones

NJ8b NJ9 UC3aed UC9aec UC10 UC11 UC14beUC15UC zones (Burnett, 1998)

NJ zones (Bown and Cooper, 1998)

Sample nos. U2 U2a U1 U3 U9 U14 U15 U10 U8 U5 U4 U6 U11a

Sample abundance VL L M M L L L H L L L L M

Preservation VP M P M P P VP P VP P VP VP VP

Cretaceous nannofossil taxa

Amphizygus brooksii VR VR

Axopodorhabdus albianus f

Biscutum ellipticum F R R

Braarudosphaera-Micrantholithus VR

Broinsonia parca constricta R

Broinsonia parca parca VR R

Broinsonia signata VR VR

Chiastozygus litterarius VR R F F

Corollithion kennedyi VR

Cribrosphaerella ehrenbergii R F F

Cylindralithus sculptus VR

Eiffellithus eximius VR R R VR R

Eiffellithus gorkae R R R

Eiffellithus turriseiffelii F R F F F F

Eprolithus floralis F R R F F

Eprolithus moratus VR

Gartnerago obliquum R R R R

Gartnerago theta VR

Grantarhabdus coronadventis VR VR VR

Haqius circumradiatus R VR

Helicolithus trabeculatus VR

Hexalithus gardetiae VR

Liliasterites sp. ?

Lithastrinus grillii VR

Lithastrinus septenarius VR VR

Lithraphidites acutus VR

Lithraphidites carniolensis F VR

Lucianorhabdus ex gr. cayeuxii VR

Marthasterites furcatus R C VR F

Micrantholithus obtusus r

Microrhabdulus attenuatus R

Microrhabdulus decoratus VR R

Micula decussata C R VR F

Micula praemurus ?

Micula swastica VR

Nannoconus elongatus VR

Nannoconus sp. VR

Placozygus cf. fibuliformis VR

Prediscosphaera columnata F R R

Prediscosphaera cretacea F F F R C

Prediscosphaera grandis s.s. R

Prediscosphaera grandis

(sensu Burnett, 1998)

VR VR R

Prediscosphaera ponticula VR F R

Quadrum-Uniplanarius VR

Retacapsa angustiforata F R

Retacapsa crenulata F R F R R

Reinhardtites anthophorus R

Reinhardtites levis F

Rhagodiscus angustus R


Table 1 (continued )

Udol Jurassic Jurassic?

Cretac.

Late Cretaceous

?Aalenian Early

Bajocian

Early Bajocian Cenom. Turon.

Coniac.

Coniacian Campanian

Middle Late


NJ8b NJ9 UC3aed UC9aec UC10 UC11 UC14beUC15UC zones (Burnett, 1998)

NJ zones (Bown and Cooper, 1998)

Sample nos. U2 U2a U1 U3 U9 U14 U15 U10 U8 U5 U4 U6 U11a

Sample abundance VL L M M L L L H L L L L M

Preservation VP M P M P P VP P VP P VP VP VP

Rucinolithus hayi F

Rucinolithus sp.

(sensu Burnett, 1998)

? F

Tegumentum stradneri VR VR VR R R

Tranolithus phacelosus VR

Watznaueria biporta VR VR R R

Zeugrhabdotus bicrescenticus R R VR R

Zeugrhabdotus diplogrammus F R F F R

Zeugrhabdotus spiralis VR

JurassiceCretaceous nannofossil taxa

Cretarhabdus conicus VR VR VR

Cyclagelosphaera margerelii VR

Manivitella pemmatoidea f VR F R F R

Watznaueria barnesae ? VR VR R F C A C A A C C

Watznaueria britannica ? VR VR R

Zeugrhabdotus embergerii R VR VR R R

Zeugrhabdotus noeliae R R

Jurassic nannofossil taxa

Carinolithus magharensis VR f

Carinolithus suberbus VR

Carinolithus sp. f

Crepidolithus sp. f

Discorhabdus striatus VR VR VR VR R F r

Ethmorhabdus gallicus ? f

Lotharingius contractus B B B B B B R r

Lotharingius crucicentralis f F R VR R r

LotharingiuseWatznaueria VR R VR R R R

Estimated abundance of nannofossil taxa: B, bloom; A, abundant (O5 specimens/one field of view); C, common (1e5 specimens/one field of view);

F, few (1e9 specimens/10 fields of view); R, rare (1e9 specimens/20 fields of view); VR, very rare (!1 specimen/20 fields of view); ?, questionable

species; r, reworked specimen. Estimates of the abundance of nannofossils in samples: H, high (O15 specimens/one field of view); M, moderate (5e15

specimens/one field of view); L, low (1e5 specimens/one field of view); VL, very low (!1 specimen/one field of view). Preservation of nannofossils:

M, moderate (overgrowth; etching or mechanical damage is apparent but majority of specimens are easily identifiable); P, poor (etching and

mechanical damage is intensive making identification of some specimens difficult); VP, very poor (some specimens cannot be identified). Categories

after Burnett and Whitham (1999), modified.

small size. The occurrence of Corollithion kennedyi,Axopodorhabdus albianus and Lithraphidites acutus isevidence of a MiddleeLate Cenomanian age. Sample U8yielded strongly mechanically damaged and etched nan-nofossils; unidentifiable fragments prevail. The presenceof Lithastrinus septenarius and Marthasterites furcatusindicates zone UC9, which is attributed to the time in-terval of Middle TuronianeEarly Coniacian. Sample U5yielded extremely poorly preserved (mostly etched) nan-nofossils. Micula decussata, Lithastrinus septenarius andrelatively common Marthasterites furcatus support aMiddle Coniacian age. Poorly preserved nannofossils,mostly in fragments, were found in sample U4. The pre-

sence of Lithastrinus grillii, Marthasterites furcatus andMicula decussata proved a Late Coniacian age. Neverthe-less, the rare occurrence of enigmatic hexagonal frag-ments of ?Rucinolithus sp. may indicate a Santonian age.

4.2.2.2. Foraminifera. The foraminiferal assemblagesare rich and relatively well preserved with a considerableamount of planktonic forms. However, in most samplesthe mixture of taxa of slightly different ages, and speci-mens displaying various colours and state of preserva-tion have also been noted, indicating some redepositionwhich probably involved only marly deposits. The for-aminifera from sample U10 represent a rare example of


Table 2

Distribution of foraminifera in the Udol (Ujak) section

Udol Lithostratigrapy Black flysch

Late

Cenomanian

Red and grey marls of Jaworki Fm

Age Albian Cenomanian Coniacian Santonian

(uppermost part)

Campanian Campaniane

Maastrichtian

Samples U2 U3 U10 U8 U4 U5 U11a U6

Agglutinated foraminifera

Nothia excelsa vr

Rhizammina indivisa F vr

Psammosphaera sp. R vr

Hyperammina gaultina vr F

Ammodiscus tenuissimus vr vr

Glomospira gordialis vr

Haplophragmoides cf. nonioninoides vr

Haplophragmoides sp. vr

Recurvoides cf. imperfectus vr

Recurvoides sp. vr

Spiroplectinella praelonga vr

Trochammina globolaevigata R

Trochammina cf. vocontiana vr

Gerochammina stanislavi vr

Uvigerinammina jankoi vr F vr

Gaudryina cretacea R

Gaudryina laevigata R vr vr

Pseudoclavulina amorpha R vr vr

Pseudoclavulina carinata vr R

Pseudoclavulina gaultina R vr R vr vr

Pseudoclavulina subparisiensis R R

Pseudoclavulina sp. vr vr

Dorothia crassa R

Dorothia oxycona vr

Goesella rugosa R

Benthonic calc.

Lenticulina spp. vr vr vr

Marginulinopsis sp. vr

Pullenia cretacea vr

Globorotalites sp. R

Gyroidinoides globosus vr

Gyroidinoides sp. R

Planktonic foraminifera

Heterohelix globulosa F

Heterohelix pulchra F

Globigerinelloides ultramicrus R

Planomalina buxtorfi R R

Planomalina praebuxtorfi vr

Hedbergella delrioensis vr vr

Hedbergella planispira vr vr F

Hedbergella simplex F

Hedbergella sp. vr R F R vr

Whiteinella sp. vr

Praeglobotruncana gibba A F

Praeglobotruncana stephani vr A F

Praeglobotruncana sp. vr F vr R R

Rotalipora appenninica vr R F F F

Rotalipora brotzeni vr R R

Rotalipora cushmani C R F

Rotalipora gandolfii R

Rotalipora greenhornensis vr R vr

Rotalipora montsalvensis R vr

Rotalipora cf. reicheli vr

Rotalipora sp. R R R R

Globotruncana arca vr vr R vr

Globotruncana cf. bulloides vr

Globotruncana sp. cf. G. falsostuarti vr



Udol Lithostratigrapy Black flysch

Late

Cenomanian

Red and grey marls of Jaworki Fm

Age Albian Cenomanian Coniacian Santonian

(uppermost part)

Campanian Campaniane

Maastrichtian

Samples U2 U3 U10 U8 U4 U5 U11a U6

Globotruncana linneiana R

Globotruncanita elevata A vr

Marginotruncana coronata R

Marginotruncana pseudolinneiana R vr vr

Marginotruncana sinuosa vr vr

Marginotruncana sp. R vr

Dicarinella hagni R

Dicarinella sp. R R

Contusotruncana fornicata vr vr C vr

Archaeglobigerina cretacea vr

Key: vr, very rare; R, rare; F, few; C, common; A, abundant.

an assemblage with no mixture of taxa with respect toage, but the position of this sample in the successionsuggests that these sediments have also been displaced.A Late Cenomanian age has been assigned to this as-semblage on the basis of planktonic foraminifera such asPraeglobotruncana gibba Klaus, P. stephani (Gandolfi),and Rotalipora cushmani (Morrow) (Caron, 1985).Sample U8 consists of some reworked specimens ofCenomanian Rotalipora as well as younger planktonicforaminifera such as Marginotruncana pseudolinneianaPessagno, M. sinuosa Porthault and Archaeglobigerinacretacea (d’Orbigny), known from the Coniacian (Caron,1985). The overlapping occurrence of the agglutinatedtaxa Uvigerinammina jankoi Majzon, Pseudoclavulinagaultina (Morozova) and P. subparisiensis (Grzybowski)also points to a Coniacian age (Geroch and Nowak,1984). Samples U4 and U5 contain mixed foraminiferaof different ages. Planomalina buxtorfi (Gandolfi) andP. praebuxtorfi Wonders are of Albian age. There arespecimens of AlbianeCenomanian Rotalipora appennin-ica (Renz) and Praeglobotruncana stephani (Gandolfi) aswell as Turonian Dicarinella hagni (Scheibnerova). Theyoungest planktonic foraminifera, such asGlobotruncanaarca (Cushman) and Contusotruncana fornicata (Plum-mer), represented by rare specimens, indicate that the as-semblage cannot be older than latest Santonian (Caron,1985). Some agglutinated taxa such as UvigerinamminajankoiMajzon, Gaudryina laevigata Franke, and Pseudo-clavulina amorpha (Cushman) are common componentsof TuronianeSantonian assemblages; Goesella rugosa(Hanzlikova) is very characteristic of the Campanian(Hanzlikova, 1972) but is known from deposits as old aslate Coniacian (Gawor-Biedowa et. al., 1984); thus all fitwell into a Santonian or younger assemblage.

4.2.3. Red and grey marls4.2.3.1. Calcareous nannofossils. Sample U11a yieldedpoorly preserved and strongly overgrown nannofossils.The presence of Broinsonia parca constricta, Reinhard-

tites laevis, Eiffellithus eximius and fragments of Predis-cosphaera grandis indicates a Campanian age. Extremelypoorly preserved nannofossils were found in sample U6where only one specimen of Broinsonia parca parca isevidence of a Campanian age. The taphocoenoses aremostly composed of reworked species from Coniacian,Albian and Jurassic strata. Furthermore, sample U6contains reworked species from Middle Jurassic andLower Cretaceous strata.

4.2.3.2. Foraminifera. An assemblage recovered fromsample U11A, homogeneous with regard to the age of itscomponents, is dominated by planktonic foraminifera.Very numerous Globotruncanita elevata (Brotzen) indi-cates an early Campanian age. Other planktonic taxa,represented by less frequent Heterohelix globulosa(Ehrenberg), H. pulchra (Brotzen), Globotruncana arca(Cushman), G. linneiana (d’Orbigny) and Contusotrun-cana fornicata (Plummer) also occur in the Campanian(Caron, 1985). Sample U6 yielded an assemblage thatdisplays mixed elements. There are some AlbianeCenomanian Rotalipora spp., TuronianeSantonianMarginotruncana spp., as well as Late SantonianeMaastrichtian Globotruncana arca (Cushman) and Con-tusotruncana fornicata (Plummer) and rare specimens ofCampanian Globotruncanita elevata (Brotzen). The over-lapping occurrence of the latter three species may indicatea Campanian age. The presence of a single specimen ofGlobotruncana sp. resembling G. falsostuarti Sigal, whoserange is from the upper part of the Campanian throughMaastrichtian (Premoli Silva and Sliter, 2002), suggests,however, that Maastrichtian cannot be excluded asa possible age for this assemblage. The assemblage alsocontains rare specimens of Lenticulina spp., which mayhave been reworked from some Jurassic deposits.

4.2.4. Eocene red marlsThe foraminiferal assemblage consists of abundant

agglutinated taxa indicating some reworking owingto their varied stratigraphic ranges. Glomospirella


Fig. 8. Cretaceous agglutinated and planktonic foraminifera of the Jaworki Formation, Udol section. A, Pseudoclavulina gaultina (Morozova),

s. U10. B, Goesella rugosa (Hanzlikova), s.U4. C, Gaudryina laevigata Franke, s.U4. D, Gaudryina cretacea (Karrer), s. U11A. E, Rotalipora

appenninica (Renz), s. U4. F, Rotalipora cushmani (Morrow), s. U4. G, H, Rotalipora montsalvensis Mornod, s U10. I, Rotalipora brotzeni (Sigal),

s. U4. JeL, Globotruncanita elevata (Brotzen), s. U11A. M, Globotruncana linneiana (d’Orbigny), s. U11A. N, O, Contusotruncana fornicata

(Plummer), s. U11A. P, Praeglobotruncana gibba Klaus s. U10. Q, Globotruncana arca (Cushman), s. U11A. R, S, Globotruncana linneiana

(d’Orbigny), s. U11A. T, Planomalina buxtorfi (Gandolfi), s. U4.


grzybowskii (Jurkiewicz) is very common in Paleoceneflysch assemblages (Olszewska et al., 1996). Reticulo-phragmoides jarvisi (Thalmann) emend. Gradstein andKaminski ranges from the late Paleocene to earlyOligocene (Gradstein and Kaminski, 1989). Thereare single specimens of Reticulophragmium amplectens(Grzybowski) and Praesphaerammina subgaleata(Vasicek) emend. Kaminski and Filipescu, representingthe common species of Middle Eocene assemblages(Olszewska et al., 1996; Kaminski and Filipescu,2000). Very rare planktonic foraminifera of Globigerinaex. gr. praebulloides Blow, whose first occurrence isknown from the Middle Eocene (Blow, 1969; Bolliand Saunders, 1985) confirms the Middle Eocene oryounger age.

4.3. Sztolnia section

In the Sztolnia Creek section 27 samples were pickedfrom the ‘‘black flysch’’ (Szlachtowa and Opaleniecformations), Hulina Formation, and Malinowa Forma-tion. Of these, 21 were chosen for nannofossil studies.The locations of the samples studied are shown in Figs.5e7 and the nannofossil contents in Tables 3 and 5; theforaminiferal distribution is given in Table 4. The mostimportant species are illustrated in Figs. 9e11.

Generally, the calcareous nannofossils proved to bepoorly preserved. Some specimens could not be identi-fied because of strong etching and mechanical damageof placoliths. Many placoliths were found in fragments.Relative abundances are usually low. Non-calcareous orslightly calcareous shales were barren of nannofossils.Specimens of Jurassic age are much better preservedthan those of the Cretaceous.

4.3.1. Black flysch (Szlachtowa Formation)4.3.1.1. Calcareous nannofossils. Samples 16 and 17yielded nearly monospecific assemblages of Lotharingiuscontractus accompanied by rare specimens of Ethmo-rhabdus gallicus,Tubirhabdus patulus,Discorhabdus stria-tus, transitional forms of LotharingiuseWatznaueria,and others. This nannofossil association documents anexclusively Jurassic age. Sample 18 contains rare nanno-fossils whose occurrence is known from both the Jurassic(Lotharingius) and the JurassiceCretaceous (generaWatznaueria and Discorhabdus).

4.3.1.2. Foraminifera. A characteristic feature of theforaminiferal assemblages (apart from that in sample15) is the presence of calcareous genera such as Lagena,Lenticulina, Marginulinopsis, Astacolus, Ramulina, andothers, which are usually long-ranging forms. Ostracods,spicules of Porifera and fragments of crinoids were alsofound in these samples. Their presence points to consider-able reworking. In sample 18 the following agglutinatedspecies, well known from the Early Cretaceous, were also

recorded: Trochammina abrupta Geroch, Verneuilinoidesneocomiensis (Mjatliuk) andAmmobaculoides carpathicusGeroch. They can also be regarded as reworked speciesderived from older, eroded deposits whose age, accordingto their occurrence in association, cannot be younger thanlatest Aptian (Geroch, 1966; Geroch and Nowak, 1984).Thus redeposition may have happened later, probably inthe Albian. The other foraminifera, commonly occurringin the flysch assemblages, are represented by long-ranging Rhizammina indivisa Brady, Nothia sp., Am-modiscus tenuissimus Guembel, Glomospira gordialis(Jones and Parker), Psammosphaera sp. and Hyper-ammina sp. Sample 15 yields an assemblage comprisinga few specimens of Saccammina placenta (Grzybowski),Plectorecurvoides alternans Noth, single examples ofPseudonosinella parvula (Huss), and Haplophragmoidescf. falcatosuturalis Neagu. The age of this assemblagemay be assumed to be Cenomanian according to therange of the last two species (Huss, 1966; Neagu,1990).

4.3.2. Opaleniec Formation4.3.2.1. Calcareous nannofossils. Sample 20 containsfairly well-preserved calcareous nannofossils. Watznaue-ria britannica and Lotharingius contractus occur in highnumbers accompanied by rare Cyclagelosphaera mar-gerelii. These indicate the upper part of the Bajocian.A nearly monogeneric assemblage of Watznaueria(W. barnesae: W. britannica=1:1) has been recordedfrom sample 26. Watznaueria manivitiae, Cyclagelos-phaera margerelii and Discorhabdus sp. are also present,but scarce. Watznaueria-dominated assemblages arecharacteristic of the Tithonian and Jurassic/Cretaceousboundary (Bown and Cooper, 1998).

4.3.2.2. Foraminifera. The foraminiferal assemblagefound in sample 30 is similar in character to those fromthe previous formation. Relatively most numerous arethe long-ranging Lenticulina species, which are accom-panied by less frequent agglutinated flysch forms(Bathysiphon sp., Rhizammina indivisa Brady, Hippo-creppina depressa Vasicek, Ammodiscus tenuissimusGuembel and Ammobaculites sp.). The age of thisassemblage can be assumed to be not younger thanCenomanian based on the last occurrence (LO) ofHippocrepina depressa Vasicek (Geroch and Nowak,1984). Poorly preserved Radiolaria have been alsonoted. The foraminiferal assemblage of sample 20contains relatively numerous calcareous specimens ofnodosarids, Involutina sp., as well as some ostracods.Scarce specimens of Early Cretaceous Ammobaculoidescarpathicus Geroch and a few examples of Bulbobacu-lites problematicus (Neagu) have also been found. Therange of the last species indicates Middle Cenoma-nianeTuronian as the possible age of this assem-blage (Geroch and Nowak, 1984; Neagu, 1990).

https://www.researchgate.net/publication/32899371_Taxonomy_and_Biostratigraphy_of_New_and_Emended_Species_of_Cenozoic_Deep-Water_Agglutinated_Foraminifera_from_the_Labrador_and_North_Seas?el=1_x_8&enrichId=rgreq-862d7391-1fa8-42d1-89dc-6234433ce4e5&enrichSource=Y292ZXJQYWdlOzIzMjM4ODA5NDtBUzo5ODk3NjYzNjM0MjI5MUAxNDAwNjA5MjgxNDk2


4.3.3. Hulina Formation and Cenomanian key horizon4.3.3.1. Nannofossils. The samples studied were barrenof nannofossils.

4.3.3.2. Foraminifera. Most of the samples yielded avery poor microfauna, and sample 4 was barren. Sample21 contains very abundant radiolaria, showing traces ofstrong recrystallization, accompanied by rare specimensof Bathysiphon sp. Sample 3 yielded a low diversityagglutinated assemblage with some specimens of Plec-torecurvoides alternans Noth and rare Uvigerinamminapraejankoi Neagu. The overlap occurrence of thesetaxa indicates a possible age of latest CenomanianeTuronian (Neagu, 1990).

4.3.4. Czerty limestoneIn sample 22 scarce Late Cretaceous nannofossils are

present, indicating an AlbianeCenomanian age. Theyare outnumbered by reworked species from TithonianeLower Cretaceous strata.

4.3.5. Variegated shales of theMalinowa Shale Formation4.3.5.1. Foraminifera. Sample 7 was barren of forami-nifera and samples 8 and 29 yielded poor assemblagessimilar in overall character to those from Szlachtowa andHulina formations. Sample 28 yielded an agglutinatedassemblage of medium diversity and abundance. Theco-occurrence of Pseudonodosinella parvula (Huss), Pseu-dobolivina variabilis Vasicek and Bulbobaculites pro-blematicus (Neagu) indicates a Cenomanian/Turonianboundary age (Gawor-Biedowa et al., 1984; Geroch andNowak, 1984). The most characteristic and rich assem-blage was recovered from sample 13. It consists exclu-sively of agglutinated taxa with relatively numerousUvigerinammina jankoi Majzon and Bulbobaculites pro-blematicus (Neagu), whose co-occurrence is commonlyattributed to the Turonian (Geroch and Nowak, 1984;Neagu, 1990). Sample 6 proved to contain a poor assem-

blage with single specimens of Caudammina gigantea(Geroch) and Globotruncana arca (Cushman) whose firstoccurrences in uppermost Santonian deposits (Gawor-Biedowa et al., 1984; Caron, 1985) indicate the older agelimit of this assemblage. Thus the studied part of theMali-nowa Formation ranges in age from the Cenomanian/Turonian transition up to the Santonian/Campanian.

4.3.6. Variegated marls of the Malinowa Formation4.3.6.1. Calcareous nannofossils. Sample 25 yieldedpoorly preserved nannofossils represented by taxawhose first occurrences are known from the Cretaceous:Eiffellithus turriseiffelii, Eprolithus floralis, Prediscos-phaera columnata, Radiolithus orbiculatus, and others(see Table 3). This association indicates an intervalfrom the Late Albian to the earliest Cenomanian.Furthermore, long-ranging JurassiceCretaceous speciesare also present (Helenea chiastia,Zeugrhabdotus noeliae,Watznaueria barnesae, Cretarhabdus conicus).

4.3.6.2. Foraminifera. Sample 25 contains a relativelyrich and mixed assemblage of foraminifera. Singlespecimens of Lenticulina, Astacolus and Pleurostomellaprobably represent the Jurassic element. There are somereworked specimens of AlbianeCenomanian planktonicRotalipora cushmani (Morrow), Praeglobotruncana ste-phani (Gandolfi) as well as TuronianeSantonian Dicar-inella sp. and Hedbergella spp. Among agglutinated taxacalcareous agglutinated Pseudoclavulina carinata (Nea-gu) and P. gaultina (Morozova) are the most numerous.The other more characteristic agglutinated foraminifersare represented by Bulbobaculites problematicus (Neagu),Trochammina globolaevigata Beckmann, Spiroplectinellasubhaeringensis (Grzybowski), and single specimens ofSpiroplectinella costata (Huss) and S. dentata (Alth).The overlapping occurrence of these species indicatesConiacian as the possible age for this assemblage(Geroch and Nowak, 1984; Gawor-Biedowa et. al.,1984; Beckmann, 1991).

Fig. 9. Stratigraphically significant Jurassic and Cretaceous calcareous nannofossils from Sztolnia and Udol sections. PPL, plane-polarized light;

XPL, cross-polarized light; scale on H. A, B, Lotharingius contractus Bown and Cooper. A, Sztolnia 17, Jurassic specimens reworked into the

Szlachtowa Formation. B, Udol 2, Jurassic specimen reworked into the ‘‘black flysch’’ of Albian age, XPL. C, D, plexus of LotharingiuseWatznaueria

transition, Sztolnia 17; Jurassic specimens reworked into the Szlachtowa Formation, XPL. E, F, Watznaueria britannica (Stradner) Reinhardt. E,

Sztolnia 20, Jurassic specimen reworked into the Opaleniec Formation. F, Sztolnia 30, Jurassic specimen reworked into the Opaleniec Formation,

XPL. G, H, Watznaueria barnesae (Black) Perch-Nielsen, Sztolnia 30, Jurassic specimens reworked into the Opaleniec Formation, XPL. I,

Carinolithus sp. (fragment), Udol 2, specimen reworked into the ‘‘black flysch’’ of the Albian age, XPL. J, Discorhabdus striatus Moshkovitz and

Ehrlich, Sztolnia 17, Jurassic specimen reworked into the Szlachtowa Formation, XPL. K, Crepidolithus sp., Sztolnia 17, Jurassic specimen reworked

into the Szlachtowa Formation, XPL. L, M, Watznaueria manivitiae Bukry, Sztolnia 30, Jurassic specimens reworked into the Opaleniec Formation,

XPL. N, O, Eprolithus floralis (Stradner) Stover, Udol 10, Late Cenomanian; Jaworki Formation, XPL. P, Corollithion kennedyi Crux, Udol 10, Late

Cenomanian, Jaworki Formation, XPL. Q, Broinsonia signata (Noel) Noel, Udol 10, Late Cenomanian, Jaworki Formation, XPL. R, Broinsonia

enormis (Shumenko) Manivit, Udol 8, Coniacian, Jaworki Formation, XPL. SeU, Prediscosphaera columnata (Stover) Perch-Nielsen, Udol 10, Late

Cenomanian, Jaworki Formation: S. PPL; T, U, XPL. V, Eiffellithus turriseiffelii (Deflandre) Reinhardt, Udol 5, Santonian, Jaworki Formation,

XPL. W, X, Eiffellithus eximius (Stover) Perch-Nielsen. W, Udol 5, Santonian; X, Udo l 11A; Campanian, Jaworki Formation, XPL.Y, Z,

Marthasterites furcatus (Deflandre) Deflandre, Udol 5, Santonian, Jaworki Formation, PPL. AA, ?Liliasterites sp., Udol 5, specimen reworked into

the Santonian of Jaworki Formation, PPL. BB, Micula decussata Vekshina, Udol 5, Santonian, Jaworki Formation, XPL. CC, Micula swastica

Stradner and Steinmetz, Udol 11A, Campanian, Jaworki Formation. DD, Manivitella pemmatoidea (Deflandre) Thierstein (fragments), Udol 10,

Late Cenomanian, Jaworki Formation, XPL. EE, FF, Rucinolithus sp., Udol 11A, Campanian, Jaworki Formation: EE, PPL; FF, XPL. GG,

Rucinolithus hayi Stover, Udol 11A, Campanian, Jaworki Formation, XPL. HH, Microrhabdulus attenuatus (Deflandre) Deflandre, Udol 11A,

Campanian, Jaworki Formation, XPL. II, JJ, Broinsonia parca constricta Hattner et al. Udol 11A, Campanian, Jaworki Formation, XPL.


Table 3

Calcareous nannofossil distribution at the locality of Sztolnia

Sztolnia Jurassic Cretaceous

Early BajocianBajocian

TithonianAlbiane

Cenom.Early Late

Cenom.


NJ8beNJ9 NJ9 NJ11

BC27

UC zones (Burnett, 1998) respect.

NJ zones (Bown and Cooper, 1998) UC0

Sample nos. 6Sz 7Sz 16 17 18 20 26 30 25 22

Sample abundance L L L M VL H M M M M

Preservation VP M VP M VP M P VP VP VP

Cretaceous nannofossil taxa

Braarudosphaera bigelowii VR

Eiffellithus turriseiffelii VR

Eprolithus floralis R

Haqius circumradiatus R

Prediscosphaera columnata F

Radiolithus orbiculatus F

Retacapsa crenulata R

Watznaueria biporta VR

Zeugrhabdotus diplogrammus R

JurassiceCretaceous nannofossil taxa

Conusphaera mexicana VR

Cretarhabdus conicus F R

Cyclagelosphaera margerelii F R VR R

Discorhabdus sp. VR VR R

Helenea chiastia R

Manivitella pemmatoidea f

Retacapca cf. octofenestrata VR

Watznaueria barnesae R VR F R A A A A

Watznaueria britannica ? ? R B A A R R

Zeugrhabdotus embergerii F

Zeugrhabdotus noeliae R


Crepidolithus pliensbachensis VR

Discorhabdus striatus VR R VR R VR

Ethmorhabdus gallicus VR VR VR

Lotharingius contractus F B B B F C VR

Lotharingius crucicentralis R VR R

Lotharingius-Watznaueria R F R F

Podorhabdus grassei VR

Polycostella beckmanii r

Tubirhabdus patulus VR R

Watznaueria manivitiae ? R R

For further details, see Table 1.

4.4. Black flysch in the Krupianka and Grajcarekcreeks, the Jaworki area

Only calcareous nannofossils, whose distribution ispresented in Table 5, were examined in the samples fromthese localities.

4.4.1. Krupianka CreekDeposits from this section yielded generally low

numbers (1e5 specimens per one field of view ofmicroscope) of poorly preserved nannofossils. Thespecimens are etched and mechanically damaged, andsome cannot be identified. The assemblages are charac-

terized by an abundance (bloom) of Lotharingiuscontractus accompanied by an evolutionary plexus ofthe LotharingiuseWatznaueria transition and by scarcespecimens of Watznaueria barnesae, Discorhabdusstriatus, Retacapsa incompta, Tubirhabdus patulus, Car-inolithus supertus and questionable specimens of Watz-naueria cf. manivitiae. The precise identification of W.britannica caused a problem because of poor preserva-tion. The nannofossils indicate Lower Bajocian zoneNJ9. The presence of AlbianeMaastrichtian Tranolithusorionatus was recorded from sample 2Kr. This mayindicate the real age of the deposits studied and re-deposition of the older Jurassic nannofossils.


Table 4

Distribution of foraminifera in the Sztolnia Creek

Sztolnia Lithostratigraphy Black flysch Opaleniec Fm Hul. Fm Malinowa Fm

Age ?Albiane

Cenomanian

Cenomanian M.Cen

Turon.

?U.Ce

Turon.

Cenomanian/

Turonian

Turonian Coniac. Sant/

Camp.

Samples 18 14 15 30 20 3 28 13 12 25 6

Agglutinated foraminifera

Bathysiphon sp. C F

Nothia excelsa C R vr

Rhizammina indivisa C F

Psammosphaera sp. vr

Saccammina sp. R

Hippocrepina depressa vr

Ammodiscus cretaceus vr

Ammodiscus tenuissimus vr vr vr

Glomospira choroides vr R vr

Glomospira gordialis R vr vr C R R

Glomospira irregularis vr R

Kalamopsis grzybowskii vr

Pseudonodosinella parvula vr F R vr

Caudammina crassa vr vr

Caudammina gigantea vr

Caudammina ovulum vr

Haplophragmoides cf. falcatosuturalis vr vr vr

Haplophragmoides cf. nonioninoides vr vr

Haplophragmoides cf. herbichi R

Haplophragmoides kirki R

Haplophragmoides sp. vr vr

Ammobaculites sp. R

Ammosphaeroidina pseudopauciloculata R vr vr

Recurvoides spp. vr F

Thalmannammina subturbinata R

Bulbobaculites problematicus vr F vr A F

Bulbobaculites cf. problematicus vr

Ammobaculoides carpathicus vr R

Spiroplectinella costata vr

Spiroplectinella dentata vr

Spiroplectinella subhaeringensis R

Plectorecurvoides alternans R F

Pseudobolivina variabilis vr

Trochammina abrupta F

Trochammina globolaevigata R

Trochammina gyroidinaeformis vr

Trochammina sp. vr R vr

Gerochammina lenis F vr

Gerochammina stanislavi vr F

Uvigerinammina jankoi A

Uvigerinammina praejankoi vr

Verneuilinoides neocomiensis F vr

Verneuilinoides sp. vr

Gaudryina bentonensis vr

Gaudryina cretacea vr

Remesella sp. R

Pseudoclavulina amorpha R

Pseudoclavulina carinata R F

Pseudoclavulina gaultina C

Benthonic calcareous

Involutina sp. vr

Lagena sp. vr vr

Lenticulina spp. C C A A vr

Marginulinopsis sp. R R

Astacolus sp. R R vr

Ramulina sp. vr

(continued on next page)



Sztolnia Lithostratigraphy Black flysch Opaleniec Fm Hul. Fm Malinowa Fm

Age ?Albiane

Cenomanian

Cenomanian M.Cen

Turon.

?U.Ce

Turon.

Cenomanian/

Turonian

Turonian Coniac. Sant/

Camp.

Samples 18 14 15 30 20 3 28 13 12 25 6

Pleurostomella sp. vr

Osangularia sp. vr

Gavelinella sp. vr

Gyroidinoides spp. R

Planktonic

Hedbergella spp. vr R

Praeglobotruncana stephani vr

Praeglobotruncana sp. vr

Rotalipora cushmani vr

Rotalipora sp. vr

Marginotruncana pseudolinneiana vr

Dicarinella imbricata vr

Globotruncana arca vr

Key: vr, very rare; R, rare; F, few; C, common; A, abundant.

4.4.2. Grajcarek CreekThe deposits at this locality contain a high number of

nannofossils with the specimens in a fair or poor state ofpreservation (samples: 1Gr, 2Gr and 6Gr). Nearlymonospecific assemblages of Lotharingius contratus areaccompanied by other Jurassic species such as Podo-rhabdus grassei, Lotharingius crucicentralis, Carinolithuscf. magharensis and Ethmorhabdus gallicus. Watznaueriabritannica and W. barnesae are rare. Samples 3Gr and4Gr yielded scarce calcareous nannofossils, and sample5Gr was devoid of them. Sample 7Gr provided a richnannofossil assemblage (30e40 specimens/one field ofview of microscope) with fairly well-preserved speci-mens. The assemblage is characterized by the dominanceof Lotharingius contractus (nearly 99%) and by rareoccurrences of Watznaueria barnesae, Lotharingiuscrucicentralis, Discorhabdus striatus, Tubirhabdus patulusand Triscutum tiziense. Only a few nannofossils wererecovered from sample 6Gr.

5. Discussion

The calcareous nannofossil assemblages indicate thefollowing ages (Tables 1, 3, 5): black flysch, AalenianeBajocian, mainly Early Bajocian; limestones and marlsat the top of black flysch, Tithonian (sample 26) andCenomanian (sample 22); variegated marls (JaworkiFormation), Albian and/or CenomanianeCampanian.

The foraminiferal assemblages indicate the followingages (Tables2, 4): blackflysch,AlbianeCenomanian;blackand green shales (Cenomanian key horizon sensu Sikora,1962; Hulina Formation sensu Birkenmajer, 1977),MiddleCenomanian/Turonian; variegatedmarls (Jaworki Forma-tion), Turoniane? Maastrichtian; variegated shales (Mali-nowa Formation), Cenomanian/TuronianeSantonian.

In the case of reworked, mixed assemblages theyoungest microfossil indications have been accepted asthe correct age assignment for specific lithostratigraphicunits. Mainly agglutinated foraminifera point to anAlbianeCenomanian age for the black flysch depositsstudied. This age is also confirmed by the dinocystsstudied by Gedl and Gedl (2001a,b). In the sectionswhere the black and green shales overlying black flyschare developed their age can be interpreted as LateCenomanian on the basis of foraminifera, supportedalso by the composition of the dinocyst assemblages.According to the foraminiferal and calcareous nanno-fossil data (sample U10, 11A; see Tables 1, 2) the redand grey marls of the Jaworki Formation were de-posited during the Late Cenomaniane?Maastrichtian.The agglutinated foraminiferal assemblages point toa Cenomanian/TuronianeSantonian age for the Mali-nowa Formation. The non-calcareous red shales of thisformation also yielded homogeneous but exclusivelyagglutinated foraminiferal assemblages, and these de-posits are usually barren of nannofossils.

Sample 25 collected from the variegated marls of theMalinowa Shale Formation in the Sztolnia section canserve as an example for explaining different foraminiferaland nannofossil age determinations. This sample yieldeda mixed foraminiferal assemblage with the youngest taxarepresented by agglutinated foraminifera whose rangespoint to a Coniacian age. Apart from the agglutinatedforms there are also redeposited AlbianeCenomanianplanktonic foraminifera and this explains the presence oftheAlbianeCenomanian calcareous nannofossils and thelack of younger species (see Tables 3, 4).

Calcareous nannofossil assemblages of Jurassic ageare characterized by the following: low species diversity;abundance (bloom) of Lotharingius contractus orWatznaueria britannica; presence of the evolutionaryplexus of the LotharingiuseWatznaueria transition; and


Fig. 10. Cretaceous agglutinated foraminifera of the ‘‘black flysch’’ (sample 18), Opaleniec Formation (samples 20 and 30) and Hulina Formation

(sample 3), Sztolnia section. A, Bathysiphon sp., s. 30. B, Rhizammina indivisa Brady, s. 18. CeE, Hippocrepina depressa Vasicek, s. 30. F, Glomospira

gordialis (Jones and Parker), s. 30. G, Plectorecurvoides alternans Noth, s. 3. H, I, Verneuilinoides neocomiensis (Mjatliuk), s. 18. J, Ammobaculoides

carpathicusGeroch, s. 20. K, Bulbobaculites cf. problematicus (Neagu), s. 30. LeO, Trochammina abruptaGeroch: L,- s. 30; MeO, s. 30.

rare occurrence of Watznaueria barnesae. According toBown and Cooper (1998) the AalenianeEarly Bajocianis characterized by an abundance of Lotharingius (L.contractus) and saw the evolutionary transition fromLotharingius to Watznaueria. This pattern correspondsto our observations of some of the samples studied.

The scarcity of Cretaceous nannofossil species or eventheir absence may have been caused by environmentalconditions that were adverse to the development ofnannoflora at that time or by their poor preservation inthe deposits that accumulated. Only reworked coccolithshad a chance of being preserved in an environment thatwas not conducive to the preservation of CaCO3, forinstance below or within fluctuating calcium compensa-tion depths (CCD). Nannofossils from older Jurassicstrata could have been covered by clay minerals, whichserved to protect them from dissolution.

It is necessary to point out that deposits containingthe Upper Cretaceous nannofossils usually do notcontain reworked Jurassic species. On the other hand,the exclusively Jurassic nannofossil taxa were found indeposits in which Cretaceous agglutinated or planktonicforaminifera were preserved (e.g., Udol sample U2:Jurassic nannofossils but scarce Cretaceous agglutinatedmicrofauna; and U3: Jurassic nannofossils but Creta-ceous agglutinated and planktonic foraminifera). Sam-ple 22, taken from the cherty limestone above the blackflysch in the Sztolnia section (Fig. 5; Table 3), is anexception because scarce Upper Cretaceous nannofossilsare present, though they are outnumbered by reworkedspecies from TithonianeLower Cretaceous strata.

The presence of Jurassic nannofossils in the LowereUpper Cretaceous deposits indicates that calcareousmaterial was derived from a Jurassic source area,


Fig. 11. Late Cretaceous agglutinated foraminifera of the Malinowa Shale Formation: variegated shales (samples 13 and 28) and variegated marls

(sample 25), Sztolnia section. A, Pseudonodosinella parvula (Huss), sample 13. B, Caudammina crassa (Geroch), s. 28. CeE, Bulbobaculites

problematicus (Neagu), s. 13. F, Spiroplectinella dentata (Alth) s. 25. G, Spiroplectinella subhaeringensis (Grzybowski), s. 25. H, I, Trochammina

globolaevigata Beckmann, s. 25. J, Gerochammina lenis (Grzybowski), s. 13. K, Gerochammina stanislavi Neagu, s.13. L, Uvigerinammina jankoi

Majzon, s. 13. M, Pseudoclavulina gaultina (Morozova), s.13. N, O, Pseudoclavulina carinata (Neagu), s. 25. P, Q, Remesella sp., s. 25.

probably the Czorsztyn Ridge. Rare occurrences ofCarinolithus magharensis in some samples may supportthe bioprovincial affiliation of the depositional areaduring the Jurassic, because according to Bown and

Cooper (1998) this species is thought to be a pre-dominantly Tethyan taxon.

Birkenmajer (2001) has recently repeated his earlierage assignment of the Szlachtowa Formation (black


Table 5

Calcareous nannofossil distribution in the Grajcarek and Krupianka creeks in the Jaworki area

GrajcarekeJaworki (1e8Gr)

KrupiankaeJaworki (1e5Kr)

Black flysch

Jurassic ?Cret.

Late AalenianeEarly Bajocian Early Bajocian AlbianeMaastr.

Calcareous nannofossil zones NJ8beNJ9 NJ9

NJ (Bown and Cooper, 1998)

Sample no. 1Gr 2Gr 3Gr 4Gr 6Gr 7Gr 8Gr 1Kr 3Kr 4Kr 5Kr 2Kr

Sample abundance H M VL L M H L L L VL L L

Preservation M M VP VP P M VP M VP VP P VP

Cret. Tranolithus orionatus R

Jur.e

Cret.

Watznaueria barnesae R R R R R

Watznaueria britannica R R


Axopodorhabdus cf. atavus f f

Carinolithus magharensis F f ?

Carinolithus superbus R

Carinolithus sp. f

Crepidolithus pliensbachensis ?r

Discorhabdus criotus VR R

Discorhabdus striatus F F R F VR R VR

Discorhabdus sp. VR VR

Ethmorhabdus gallicus R R VR

Lotharingius contractus B B R B B B B B A C C B

Lotharingius crucicentralis F R R R R

Lotharingius cf. sigillatus R

Lotharingius-Watznaueria F VR F VR R F

Podorhabdus grassei F F

Retacapsa incompta R R R

Schizosphaerella punctulata ?

Triscutum tiziense R VR

Tubirhabdus patulus F VR R

Watznaueria barnesae R R

Watznaueria britannica R

Watznaueria manivitiae ? ?

For further details, see Table 1.

flysch) to Toarcianeearliest Aalenian. In our analysisthe Jurassic nannofossil assemblages have indicateda different and wider age span (AalenianeBathonian)for this formation. It would also be very difficult toexplain the occurrence of crinoidal debris in turbidites ofthe age suggested by Birkenmajer (2001). The crinoidallimestones were developed on the Czorsztyn Ridge andits slopes during BajocianeBathonian time. They couldhave been redeposited in the flysch basin either then orlater. The presence of BajocianeBathonian fossils in the‘‘black flysch’’ also excludes a Toarcianeearliest Aale-nian age.

Mainly agglutinated foraminifera clearly indicate anAlbianeCenomanian age for the black flysch in both theUdol and Jaworki locations. Similar foraminifera weredescribed from the Trawne Beds of the western sector ofthe Polish PKB (Gasinski, 1983). Such an age is alsosupported by the geological position of the flyschdeposits. They occur together with variegated Creta-ceous shales or marls. In the Sztolnia section the ‘‘blackflysch’’ passes into black and green shales and then into

variegated shales, while in the Udol section it passesdirectly into variegated marls. These variegated marlsare equivalent in age to the variegated shales. They weredeposited above the CCD, probably on the slopewhereas the shales represent deep-water basinal faciesdeposited below the local CCD. The radiolarite keyhorizon is usually well marked only in the deep-waterfacies.

A similar position for the black flysch deposits iscommon along the entire margin of the Pieniny KlippenBelt and Magura Unit (Svabenicka et al., 1997) andtherefore cannot be coincidental or explained by localtectonic deformation. Nowhere are there Upper Jurassicand lowermost Cretaceous deposits between the blackflysch and the variegated Upper Cretaceous shales.

Redeposition of microfossils was also noted within theUpper Cretaceous deposits. Samples U4, U5 and U8from the Udol section contain mixed foraminifera ofdifferent ages. There are AlbianeCenomanian andTuronian components. The youngest planktonic forami-nifera indicate that these deposits cannot be older than


latest Santonian. That part of the section with mixedassemblages is followed by an olistostrome (sample U15taken from the matrix) with various Jurassic, Early andLate Cretaceous blocks derived from the different zonesof the Czorsztyn Ridge and surrounding slopes. Thisindicates continuous redeposition and olistrostrome-forming processes during the Late Cretaceous.

6. Conclusions

Our findings indicate significant redeposition of themicrofossils recovered from the black flysch sequencesin Poland and Slovakia. The enhanced recycling ofmicrofossils within the Carpathian realm was connectedwith tectonic pulses. The occurrence of redepositedfossils can lead to erroneous age determinations. Thebiostratigraphic analysis presented herein proves with-out doubt an AlbianeCenomanian age for the blackflysch deposits of the Pieniny Klippen Belt.

During the Early Cretaceous, prior to the Albian, theCzorsztyn Ridge area was uplifted and erosion reachedthe Middle Jurassic crinoidal limestones (Obermajer,1987). The slopes around the ridge and some parts of theridge itself were characterized by the deposition of marlsand limestones during the Albian. During the AptianeAlbian, complex tectonic movements began to takeplace in the zone of the future Alpine belt, betweensouthern Europe and North Africa/Arabia (Fig. 12).Continued closure of the western part of Neotethys wasrelated to subduction along the Neotethys margin. Inthe Eastern Carpathians compressional movement tookplace, the inner part of the Carpathians was folded andnapped, and coarse-grained sediments and olistostromesdeveloped in front of the moving nappes.

In the southern part of the Magura Basin black flyschdeposition followed the accumulation of the uppermostJurassiceEarly Cretaceous, extremely condensed, ba-sinal, deep-water sediments of Maiolica-type (Golonkaand Sikora, 1981). The erosion of the Czorsztyn pelagic

Organic-rich rock

Shale

MarlLand

Flysch

Subduction

Flysch Gault

Black Flysch

Coarse clastics

Biogenic siliceous rock

Hluk

Fig. 12. Palaeogeography of the Pieniny Klippen BelteMagura Basin and adjacent areas during Albian; plate positions at 112 Ma. Abbreviations of

names of oceans, basins, ridges and plates: CR, Czorsztyn Ridge; Du, Dukla Sub-basin; Hv, Helvetic shelf (European platform); In, Inacovce-

Kricevo Sub-basin; Mr, Marmarosh Massif (Bucovinian-Getic) terrane; Mg, Magura Sub-basin; Mn, Manin Basin; PKB, Pieniny Klippen Belt Sub-

basin; Ps, Sub-Silesian ridge; SC, Silesian Ridge (Cordillera); Sl, Silesian Sub-basin; Sk, Skole Sub-basin; Tr, Transylvanian Ocean. Abbreviations

of succession zones within the sub-basins of the Pieniny/Magura Basin: Bl, Bile Karpaty succession zone; Ct, Czorsztyn succession zone; Cz,

Czertezik succession zone; Gr, Grajcarek succession zone; Kl, Klapa succession zone; Ku, Kurovice succession zone; Nd, Niedzica succession zone;

Pi, Pieniny succession zone; Rc, Racza succession zone; Zn, Zldatna succession zone; Zw, Zawiasy succession zone.


swell supplied an enormous amount of redeposited rocks,including crinoidal limestones, a significant amount ofplanktonic microfossils, marine macrofossils and landplant remains. In the deepest and more distal part of theMagura Basin black-green and thin- to medium-beddedturbidites were deposited. In the Pieniny Klippen Belt,one of the global mid-Cretaceous oceanic anoxic events(OAE2) is reflected in the mixed green and blacksediments (Wojcik and Gasinski, 2000).

The orogenic process initiated during the time ofblack flysch deposition continued during the LateCretaceous and Paleogene (Golonka et al., 2000). Thepost-rift-collisional stage of the Outer Carpathians wascharacterized by further development of subductionzones along the active margin, by partial closing of theoceanic basin and development of the main flyschbasins. The planktonic microfossils originally depositedon the submarine plateaus or in marginal parts of thebasins were redeposited within turbiditic fans followinga new orogenic pulse (Bak and Oszczypko, 2000). Theseredepositional process accompanied by olistostrome-forming gravitational slides lasted until the final closureof the flysch basin.

Acknowledgements

This research has been financially supported by thePolish Committee for Scientific Research (KBN), grant6P04D 04019. We are grateful to Marta Oszczypko-Clowes for nannoplankton age determination of thePaleogene samples, discussion and for computer prep-aration of the illustrations, and to the referees andeditor, D. J. Batten, for their comments and help.

Appendix A

Jurassic calcareous nannofossil species cited in text

Axopodorhabdus atavus (Grun et al., 1974) Bown, 1987Carinolithus magharensis (Moshkovitz and Ehrlich,1976) Bown, 1987Carinolithus superbus (Deflandre, 1954) Prins in Grunet al., 1974Crepidolithus pliensbachensis Crux, 1985Cyclagelosphaera deflandrei (Manivit, 1966) Roth, 1973Discorhabdus criotus Bown, 1987Discorhabdus striatus Moshkovitz and Ehrlich, 1976Ethmorhabdus gallicus Noel, 1965Lotharingius contractus Bown and Cooper, 1989Lotharingius crucicentralis (Medd, 1971) Grun andZweili, 1980Lotharingius sigillatus (Stradner, 1961) Prins in Grunet al., 1974Podorhabdus grassei Noel, 1965Polycostella beckmanii Thierstein, 1971

Retacapsa incompta Bown, 1987Schizosphaerella punctulata Deflandre and Dangeard,1938Tubirhabdus patulus Rood et al., 1973Triscutum tiziense de Kaenel and Bergen, 1993Watznaueria manivitiae Bukry, 1973

Calcareous nannofossil taxa the first occurrences of

which are known in the Jurassic but with ranges that

continue into the Cretaceous

Cretarhabdus conicus Bramlette and Martini, 1964Cyclagelosphaera margerelii Noel, 1965Manivitella pemmatoidea (Deflandre in Manivit, 1965)Thierstein, 1971Watznaueria barnesae (Black, 1959) Perch-Nielsen, 1968Watznaueria britannica (Stradner, 1963) Reinhardt,1964Zeugrhabdotus embergerii (Noel, 1958) Perch-Nielsen, 1984Zeugrhabdotus noeliae Rood et al., 1971

Cretaceous calcareous nannofossil species cited in text

Amphizygus brooksii Bukry, 1969Axopodorhabdus albianus (Black, 1967) Wind and Wisein Wise and Wind, 1977Biscutum ellipticum (Gorka, 1957) Grun in Grun andAllemann, 1975Broinsonia parca constricta Hattner et al., 1980Broinsonia parca parca (Stradner, 1963) Bukry, 1969Broinsonia signata (Noel, 1969) Noel, 1970Chiastozygus litterarius (Gorka, 1957) Manivit, 1971Corollithion kennedyi Crux, 1981Cribrosphaerella ehrenbergii (Arkhangelsky, 1912)Deflandre in Piveteau, 1952Cylindralithus sculptus Bukry, 1969Eiffellithus eximius (Stover, 1966) Perch-Nielsen, 1968Eiffellithus turriseiffelii (Deflandre in Deflandre andFert, 1954) Reinhardt, 1965Eprolithus floralis (Stradner, 1962) Stover, 1966Eprolithus moratus (Stover, 1966) Burnett, 1998Gartnerago obliquum (Stradner, 1963) Noel, 1970Gartnerago theta (Black in Black and Barnes, 1959)Jakubowski, 1986Grantarhabdus coronadventis (Reinhardt, 1966) Grun inGrun and Allemann, 1975Haqius circumradiatus (Stover, 1966) Roth, 1978Helicolithus trabeculatus (Gorka, 1957) Verbeek, 1977Hexalithus gardetiae Bukry, 1969Lithastrinus grillii Stradner, 1962Lithastrinus septenarius Forchheimer, 1972Lithraphidites acutus Verbeek and Manivit in Manivitet al., 1977Lithraphidites carniolensis Deflandre, 1963Lucianorhabdus cayeuxii Deflandre, 1959Marthasterites furcatus (Deflandre in Deflandre andFert, 1954) Deflandre, 1959Micrantholithus obtusus Stradner, 1963


Microrhabdulus attenuatus (Deflandre, 1959) Deflandre,1963Microrhabdulus decoratus Deflandre, 1959Micula decussata Vekshina, 1959Micula praemurus (Bukry, 1973) Stradner and Steinmetz,1984Micula swastica Stradner and Steinmetz, 1984Nannoconus elongatus Bronnimann, 1955Placozygus fibuliformis (Reinhardt, 1964) Hoffmann,1970Prediscosphaera columnata (Stover, 1966) Perch-Nielsen,1984Prediscosphaera cretacea (Arkhangelsky, 1912) Gartner,1968Prediscosphaera grandis Perch-Nielsen, 1979Prediscosphaera ponticula (Bukry, 1969) Perch-Nielsen,1984Quadrum gartneri Prins and Perch-Nielsen in Manivitet al., 1977Retacapsa angustiforata Black, 1971Retacapsa crenulata (Bramlette and Martini, 1964) Grunin Grun and Allemann, 1975Rhagodiscus angustus (Stradner, 1963) Reinhardt, 1971Tegumentum stradneri Thierstein in Roth andThierstein, 1972Tranolithus phacelosus Stover, 1966Uniplanarius gothicus (Deflandre, 1959) Hattner andWise, 1980Watznaueria biporta Bukry, 1969Zeugrhabdotus bicrescenticus (Stover, 1966)Burnett in Gale et al., 1996Zeugrhabdotus diplogrammus (Deflandre in Deflandreand Fert, 1954) Burnett in Gale et al., 1996Zeugrhabdotus spiralis (Bramlette and Martini, 1964)Burnett, 1998

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Jurassic–Cretaceous controversies in the Western Carpathian Flysch: the “black flysch” case...

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