15

Biostratigraphy of deep-water agglutinated Foraminifera in Scaglia Rossa­ type deposits of the Pieniny Klippen Belt, Carpathians, Poland

KRZYSZTOF BilK ;:1Stitute of Geography, Cracow Pedagogical University, Podchorqiych 2, 30-084 Krak6w, Poland

ABSTRACT A local biostratigraphical zonation based on agglutinated foraminifera, for Upper Cretaceous red deep-water pelagic deposits in the Polish part of the Pieniny Klippen Belt, is presented here. Studies were carried out based on 16 sections, to compare with results of earlier research. A standard zonal scheme of Geroch & Nowak (1984) was applied, with minor modifications. The Scaglia Rossa-type deposits in the Pieniny Klippen Belt represent the Plectorecurvoides alternalls (from Lower Cenomanian) through Goesella rugosa (through Upper Maastrichtian) zones. A correlation with the standard planktonic foraminiferal zones was established, enabling calibration of the OWAF to the standard chronostratigraphy.

~TRODUCTION Similar to the latter sections, red pelagic sedi­ C pper Cretaceous red marls and marly limestones ments occur in the Pieniny Klippen Belt (the often intercalated with thin-bedded greenish and Carpathians), representing facies deposited in a bluish, calcareous mudstones and sandstones are part of the Penninic Ocean - the northern part of the known from the Alps, Appenines and Penibetic Zone Western Tethys (Fourcade et aI., 1993). These facies as "Couches Rouge", "Scaglia Rossa" and "Capas are called the "Puchov beds" in the Ukrainian Rojas" facies. These sediments have a wide geo­ Carpathians (Glusko & Kruglov, 1971) or the graphic distribution in the Tethyan realm, charac­ "Kysuca beds" in the Slovak part of the Pieniny terizing pelagic deposition in the bathyal zones Klippen Belt (Scheibner & Scheibnerova, 1958). In above and/or near the CCO (calcite compensation the Polish part of the Pieniny Klippen Belt, they depth). The high content of calcium carbonate was have been distinguished as two formal lithostrati­ conducive to the preservation of planktonic graphic units, the Pustelnia Marl Member and the foraminifers and nannoplankton, which are used for Macelowa Marl Member (within the Jaworki biostratigraphic zonation of these facies. Deep­ Formation; Birkenmajer, 1977). Studies of the water agglutinated foraminifers (OWAF) are the planktonic foraminiferal, nannoplankton, and fossil group occuring in these sediments in large radiolarian assemblages from this area (e.g., numbers and in well diversified assemblages. The Alexandrowicz, 1966; Alexandrowicz et aI., 1968a,b; (:o-occurrence of different groups of microfauna Jednorowska, 1979; Bir kenmajer & J ednorowska, provides an opportunity to calibrate the strati­ 1983a,b, 1984; Bqk, 1994, 1995b; Dudziak, 1985; M. graphic ranges of agglutinated taxa with planktonic Bqk, 1995, 1996a,b) have provided evidence for foraminifers, and to propose biostratigraphic continuous sedimentation in the Pieniny Klippen schemes that are calibrated more accurately with Basin from the early Cenomanian through the late the standard chronostratigraphy. Campanian. Thus far there have been few contributions pre­ Red calcareous facies are the most widespread senting the calibration of OW AF with chrono­ Upper Cretaceous sediments in the Pieniny Klippen stratigraphy (Kaminski et ai., 1988; Kuhnt, 1990). Belt. The present author has carried out the Kaminski et al. (1988) presented the stratigraphic detailed biostratigraphic studies of these facies, ranges of Campanian-Maastrichtian agglutinated based on planktonic foraminifers (Bqk, 1998). foraminifers from the Trinidad area (the Caribbean Because of the abundance of OW AF in the studied Plate). Kuhnt (1990) calibrated the ranges of material, a precise calibration of their Turonian to Maastrichtian OWAF, using material stratigraphic ranges was possible. from sections at Gubbio (Umbrian Apeninnes, Italy) The present studies comprise, additionally, an and Hacho de Mantejaque (Betic Cordillera, analysis of agglutinated assemblages Southern Spain), representing the southern and the (Alexandrowicz & Birkenmajer, 1978; Jednorowska, westernmost part of the Western Tethys. 1980; Birkenmajer & Jednorowska, 1983b; Kostka,

III: Hart, M.B., Kaminski, M.A., & Smart, C.W. (eds) 2000. Proceedings of the Fifth International Workshop on Agglutinated Foraminifera. Grzybowski Foundation Special Publication, 7, 15-41. 16 Krzysztof Bqk

1993) from the Campanian-Maastrichtian pelagic the planktonic foraminiferal biozonation, using facies (partly red in colour), occurring in the papers by Robaszynski & Caron (1979) and by Maruszyna Scale (a tectonic unit incorporated into Robaszynski et al. (1984). the Pieniny Klippen Belt). These combined data Another kind of a synthesis was the presentation enable a comparison between a zonation based on of stages of development of the Pieniny Klippen agglutinated foraminifers (presented here) with Belt (Birkenmajer, 1986). According to Birkenmajer, other zonations developed earlier in the neigh­ sedimentation of the Macelowa Marl Member took bouring flysch areas (Geroch & Nowak, 1984; place during the stage of initial compression, when Olszewska, 1997) and from similar environments in deposition took place on an abyssal platform. other parts of the Western Tethys. This study is a Pelagic deposition was periodically interrupted by continuation of earlier research presented during the turbidity currents, cutting canyons, with their 4th International Workshop on Agglutinated deposits forming submarine fans. At the northern Foraminifera in Krak6w (Bqk et al., 1995). (Czorsztyn) ridge the sedimentation of pelagic Globotruncana marls took place. Outline of previous studies Because of recent advances in the biostrati­ The first description of Upper Cretaceous red marls graphical scheme for the Western Tethys, new came from research by Stur (1860) who distinguished information on the planktic foraminiferal ranges among others the "Puchov beds". Liebus & Schubert (Caron, 1985, Robaszynski et al., 1993, Gale et al., (1902) described foraminifera from these deposits 1996; Robaszynski & Caron, 1995), and new studied ("Gbelan inoceramid marls"). sections (Bqk, 1995b; 1998), it appeared that a fresh A new stage of research on the Upper Cretaceous look at the biostratigraphy of the Upper Cretaceous deposits in the Pieniny Klippen Belt (PKB) was of the Pieniny Klippen Belt was needed. started by Horwitz (e.g., 1938, 1963) and Andrusov (e.g., 1945). However, most of their biostratigraphi­ GEOLOGICAL SEITING cal analysis was determined basing on macrofauna The Pieniny Klippen Belt of Poland is part of a long and larger foraminifera. (approximately 600 km) and very narrow (maximum The next stage of research is connected with pub­ 20 km wide) structural unit, separating the Inner lications by Birkenmajer (1954, 1958), who dated the Carpathians from the Flysch Outer Carpathians red Cretaceous deposits as Cenomanian-Turonian (Figure 1A). During the Mesozoic, the PKB occupied ("Globotruncana marls"), Maastrichtian ("Puchov a separate basin within the northern part of the marls") and Palaeocene ("the variegated beds"). Western Tethys. In its present form, the PKB consists Later micropalaeontological studies based on of Klippen successions, and incorporated into the foraminifers (Birkenmajer & Geroch, 1961) enabled zone are elements of the Outer and Inner age determination of the red facies in the Magura Carpathians (e.g., the Maruszyna Scale; Succession as Cenomanian-Campanian. Successive Birkenmajer, 1986). Detailed studies of tectonic publications more precisely described the structures, litho- and biostratigraphy in that area, stratigraphy of the red deposits from the Czorsztyn allowed Birkenmajer to reconstruct several parallel Succession (Alexandrowicz et al., 1962) as Turonian facies zones, distinguished as successions. These are: to late Campanian. the Czorsztyn Succession corresponding to the north­ A milestone in the investigation of the Upper ern intra-oceanic ridge and its southern slope; the Cretaceous stratigraphy was the publication by Czertezik and the Niedzica Successions consisting of Alexandrowicz (1966). Foraminiferal and lithologi­ deposits sedimented on the slope of the basin; the cal studies were used for the correlation of these Branisko and the Pieniny Successions corresponding deposits with the surrounding areas (Alexandrowicz to the central furrow; the Haligovce Succession and et al., 1968a, 1968b). the Exotic (Andrusov) Ridge formed the southern A significant advance in the stratigraphy of the slope and ridge. Palaeotectonic position of Pieniny Klippen Belt was the publication by Maruszyna Succession was, according to Birkenmajer Birkenmajer (1977), which introduced a (1986), to the south of the Exotic (Andrusov) Ridge lithostratigraphic classification for that area. and to the north of the Central Carpathian Manin From that time, subsequent research was aimed at Basin and its Myjava cover. The sediments of this the document ion of the full micropalaeontological unit may have formed on a submerged ridge in a and lithological characteristics of particular back-arc basin position with respect to the Pieniny lithostratigraphic units of the Upper Cretaceous. Klippen Belt arc. Foraminiferal analysis by Jednorowska (1979; 1981), In this study, I examine the red Upper Cretaceous and Birkenmajer & Jednorowska (1983a,b; 1984) in deposits that accumulated on the northern the different sections enabled a partial revision of (Czorsztyn) ridge (the Pustelnia Marl Member; the the age of red deposits in the PKB. The consecutive Czorsztyn Succession), on the northern slope of the phase, encompassing micropalaeontological studies, basin (the Macelowa Marl Member; the Czorsztyn, has resulted in a new subdivision of the Upper the Czertezik and the Niedzica Successions), and in Cretaceous by Birkenmajer & Jednorowska (1987). the central furrow (the Macelowa Marl Member; the These authors established this subdivision based on Biostratigraphy of OWAF in Scaglia type deposits of the PKB, Poland 17

FOREDEEP FORELAND

INNER CARPATHIANS

50km • BratlalaV8

· .. ·d· h···· ::1·· ····F ·1:.···· ...... :h··· • Sz 1 . 0·::: a: :e::: ... : ··:y:·s·:c···:: P. .... :..... ":. ":.:":: : .. :.::: : .. .:.:.: " .. "

Figure 1. A. Location of the investigated sections in the Carpathians; Pieniny Klippen Belt (P.K.B.) in black. B. Locations of the investigated sections in the Pieniny Klippen Belt; 1 - profile symbol (see Figure 2); 2 - main faults; M.s. - Maruszyna Scale

Branisko and Pieniny successions}. Moreover, I have bedded marls occur. Horizontal or wavy lamination used the biostratigraphic data from the light green is often observed. Disintegrated Inoceramus shells, and variegated pelagic facies of the Maruszyna built of prismatic calcite crystals form thin (1-5 mm) Scale presented by Alexandrowicz & Birkenmajer intercalations. Thicker marls are often strongly (1978), Jednorowska (1980), Birkenmajer & bioturbated. Jednorowska (1983b), and Kostka (1993). Greyish red, usually structureless, calcareous mudstones (rarely marly limestones) make up the Pustelnia Marl Member second lithotype of the Macelowa Marl Member. The Pustelnia Marl Member (Birkenmajer, 1977) is Layers less than 8 cm and more than 14 cm thick represented by brick red marls devoid of clastic predominate. These rocks are frequent in the lower intercalations. Calcium carbonate content is high, part of this member. varying from 60 to 85%. The Lorencowe Chert Bed Grey to bluish sandy mudstones and sandstones (Birkenmajer, 1977) occurs within the upper part of occur frequently in the upper part of the Macelowa the Pustelnia Marl Member, corresponding to the Marl Member. Most layers are about 1-3 cm thick. Lower Campanian Oceanic Event (LCE). This unit The majority of mudstone layers show bioturbation. consists of very thin (1-4 cm) limestone layers and Horizontal and cross lamination is very rarely strongly calcareous marls, light green, partly red­ observed. Randomly distributed prismatic calcite dish in colour, and less than 3 m thick. Large fragments of Inoceramus shells occur as laminae 1-3 marginotruncanids are visible on weathered surfaces cm thick in some sandy mudstones.

of the limestone layers. The CaC03 content ranges from 72 to 95%. Pelagic facies of the Maruszyna Succession Sedimentary sequences described at two localities Macelowa Marl Member (Bialy Dunajec River at Szaflary, and Skrzypny The Macelowa Marl Member (Birkenmajer, 1977) is Stream at Maruszyna) represent continous represented by cherry red marls and calcareous Campanian to Middle Eocene pelagic successions mudstones intercalated by fine-bedded grey to grey­ (with the exception of the uppermost Maastrichtian ish blue calcareous mudstones and sandstones. and Lower Palaeocene). The Cretaceous part of the

The red marls (CaC03 contents from 16 to 75%) profile consists of hard, light marly limestones predominate in this unit, occurring in very thin followed by soft variegated marls (Alexandrowicz layers; their mean thickness is about 3 cm. In the & Birkenmajer, 1978). In the middle part of this stratigraphically lower part of the unit, medium- sequence, several layers of 4-50 cm thick, grey-green 18 Krzysztof Bqk

...; (ij c.: UlIS ~SSSSSSSSSS$. ssssssssssSS\sSS'iSSSSl: IV 0 t~""0 .. '. . . .. !j:; UJ 8.J! as ~ssssssssssssss~~ : = ~ . . ~~I !--:-~q: .. ~11111'- - ---~-I ,'----"'';'0 ~ • Iolll"t ~Ollll (III! 1- -.- -=:l. - ~ 1- -- liOHI -~. . ~"O'.. . c: IV mil I~ -- -:- ~d: ~N :s :~I I!! ~ LoJ "1I1lJ1V 2 ~ 01- roWs CI====:::1

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Figure 2. Age of the Scaglia Rossa-type facies in studied sections in the Pieniny Klippen Belt (summarised after Bqk, 1998, and Kostka, 1993). 1- red marls, marly limestones with intercalations of fine-bedded mudstones and sandstones, 2- light green and variegated marls and marly limestones, 3- black marly shales of CTBE, 4- light green limestones of the LCE. Analysed sections: (1) Pustelnia Marl Member: CSk- "Czerwona Skala Mt", MRog- "Maly Rogoinik Stream at Zaskale", Lor- "Lorencowe Skalki klippes", Rog- "Rogoinik Quarry and souroundings", Kiz- "Kizlinkowy Stream", Sz- "Szaflary­ ",:,apiennik Quarry''', Fl- "Falsztyn sourroundings", Smol- "Smolegowa Skala klippe". (2) Macelowa Marl Member: Zl­ "Zlobowy creek", Zam- "Czorsztyn Castle", Kap - "Kapusnica - Upszar area", Sos- "So snow Pass below Czertezik Mt.", Gr­ "Grodek Stream at Kroscienko", Kos- "Kosarzyska Valley", Bw- "Bukowiny Hill", BiW- "Biala Woda Stream", oBiW­ "tributary of Biala Woda Stream", CzW- "Czarna Woda stream", Bd- "Bukowiny Valley", Sk- "Skalski Stream", Tr- "Trawne Stream", Dr- "Dursztyn area", Zaw- "Zawiasy klippe and below Ociemny Wierch Mt", Kon- "Koniowski Stream", SW­ "Sromowce Wyine", Mar- Skrzypny Stream at Maruszyna", Mac- "Macelowa-Osice Mt", Or- "below Orlica hill", Nd- "Nie­ dziczanka Stream", Sob- "Sobczanski Wqwoz Gorge", BiD- "Bialy Dunajec River at Szaflary", PG- "Podskalnia Gora Mt", SzG- "Szewcow Gronik Hill", MrG- "Mardulowy Gronik hill", Dz- "Dzial Pass", "ps.fl.- "variegated flysch at Maruszyna. (3) Pelagic facies of the Maruszyna Scale: BD- "Bialy Dunajec River at Szaflary", Skrz- Skrzypny Stream at Maruszyna". Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 19 fine- to medium-grained calcareous sandstones, Santonian) Zones in the Niedzica Succession; the passing into laminated mudstones are observed. Fine Marginotruneana sigali (middle Turonian) through sedimentary breccia with fragments of green-grey Oieari nella eoneavata (latest Turonian/ early marls, quartz grains, and Inoceramus shells occurs at Santonian) Zones in the Branisko Succession; the the bases of some layers (Kostka, 1993). Praeglobotruneana delrioensis (latest Cenomanian­ earliest Turonian) through Globotruneanita elevata MATERIAL AND METHODS (early Campanian) Zones in the Pieniny Succession. Sixteen sections located near Jaworki, Szczawnica, According to Kostka (1993), the pelagic deposits Niedzica, Sromowce, Dursztyn, Krempachy, and of the Maruszyna Scale represent the Globotruneana Szaflary were examined (Figure 1 B, Table 1). area Interval Zone and Abathomphalus mayaro­ Samples were collected every 0.5-1.5 m depending on ensis Taxon Range Zone in their Cretaceous part. the state of the exposure and taking into account Comparison of foraminiferal biostratigraphy and lithological variations. calcareous nannoplankton stratigraphy from the Two hundred fifty samples were micropalaeonto­ same deposits (Dudziak, 1980, 1990, 1993) document logically examined. The samples (about 0.75 kg) the lower boundary of this pelagic sediementation were crushed into pieces 1-5 cm in diameter, then within the NC19/NC20 nannoplankton Zone, corre­ boiled in glauber salt. Samples taken from hard, sponding simultaneously to the Globotrunea strongly calcareous marls and marly limestones were ventrieosa Zone (middle Campanian). dried for 24 hours at 105°C, then dissolved in acetic acid (80%) for 6-8 hours at 75°C, and subsequently AGGLUTINATED FORAMINIFERAL ZONES washed through a 63 /lm screen and dried. The A local biostratigraphical zonation based on agglu­ C H 3COOH residues consist, in all cases, of tinated foraminifera, is proposed here for the Upper planktonic and benthic foraminifers of good Cretaceous deposits in the Polish part of the Pieniny preservation. Foraminifers (more than 300 specimens Klippen Belt. It takes into account the earlier if available) from the >63 /lm fraction were picked standard scheme for the Carpathians (Geroch & and mounted onto cardboard microscope slides. Nowak, 1984). The definition of foraminiferal zones The material is housed in the Institute of is based on vertical ranges of index taxa (Figure 4). Geography, Cracow Pedagogical University. The zones are interval zones: between the first Scanning electron microscope photomicrographs appearances of index taxa. A complete list of were prepared at the Electronic Microscopy Lab­ foraminifera with details about microfaunal assem­ oratory of the Department of Zoology, Jagiellonian blages and stratigraphy of the studied deposits is University. included in the paper by Bqk (1998).

AGE OF THE SCAGLIA ROSSA-TYPE FACIES IN Pleetoreeurvoides altemans Interval Zone THE PIENINY KLIPPEN BELT Definition: Lower boundary - first appearance Based on the examination of 16 sections of the datum (FAD) of Pleetoreeurvoides alternans Noth; Pustelnia Marl Member and the Macelowa Marl the boundary has not been identified in the sections Member, as well as taking into account results of ear­ examined; upper boundary - FAD of Bulbobaeulites lier microfaunal studies of these members (partly problematieus (Neagu). Identical to the P. alternmls revised by the present author), documented in 20 Zone of Geroch & Nowak (1984). sections and outcrops (mainly by Alexandrowicz, Occurrence: The zone has been recognised in the 1966, 1975; Birkenmajer & Jednorowska, 1976, 1983a, Pustelnia Marl Member and the Macelowa Marl 1983b, 1984; Jednorowska, 1979), a local planktonic Member (both members in the Czorsztyn Succession). foraminiferal biostratigraphy has been determined Agglutinated Foraminifera: The lowest part of this for the Pieniny Klippen Belt in Poland (Bqk, 1998). zone in the Macelowa Marl Member (Zlobowy Creek The calibration of these foraminiferal zones with section) is characterised by the dominance of benthic the chronostratigraphy is presented following foraminifers. Agglutinated forms prevail, com­ Robaszynski & Caron (1995). prising even up to 80% of the assemblage. The index The Pustelnia Marl Member represents the taxon dominates together with Recurvoides spp., Rotalipora reieheli (Middle Cenomanian) through siliceous ammodiscids (A. eretaeeus) and glomo­ Globotruneanella havanensis (Campanian) Zones spirids (G. eharoides (Jones & Parker), G. gordialis (Figs. 2, 3). The Macelowa Marl Member (Figs. 2, 3) (Jones & Parker) and G. irregularis (Grzybowski». represents the Rotalipora globotruneanoides (Early These species are accompanied by Troehammina Cenomanian) through Oiearinella asymetriea spp., Haplophragmoides spp., Arenobulimina sp. (Santonian) Zones in the Czorsztyn Succession; the and Oorothia oxyeona (Reuss). Moreover, forms Praeglobotruneana delrioensis (latest Cenomanian­ identical to Saeeammina d. placenta (Grzybowski), earliest Turonian) through Oiearinella eoneavata Spiroplectammina navarroana Cushman, and (latest Turonian-early Santonian) Zones in the Tritaxia gaultina (Moroz ova) also occur. This Czertezik Succession; the Helvetoglobotruneana assemblage characterises deposits of the Rotalipora helvetica (early-middle Turonian) through globotruncanoides Zone (Lower Cenomanian). Oiearinella eoneavata (latest Turonian/early 20 Krzysztof Bqk

r-r--- III UJ PLANKTONIC PIENINY KLIPPEN BELT III Cl UJ FORAMINIFERAL Klippen successions Cl ~ ZONES Maruszyna 111 ~ & Caron. 1119:1. Czorsztyn Czert. Nledz. Bran. Plen. Scale III en (Rabaaz)InaJrI I I I I ::l modified byK. Botlr. 18118) III Pustalnla M. M~ MaceIowa Marl Member pelagic facies , c ! Abatoomphalus .c mayaroemis :sU . \/I !II !II 70- == Ganssenna gansseri I- . Globotruncana aegyptiaca

C Globotruncanella navanensis .!!! C Globotruncanita co/carala !II ~ E !II Globotnmcana - U wntricosQ

80- Globotrunccmita elevala ,r-- ,.; Dicarirtella C aspnetn'ca en!II '--c- .!i ,~ Dican'nella concavata C 0 U U ------90- ,mC Dicarinella prinllUWJ - ~arginotruncana SJR.(1 i - c M e - lIel""toglobotnmcana ~ L INlvetica -.1-- ..., - Praeglobotnm. delrioensis CTBE c U Ro/alipora =hmani ..., - o 0 oR" • __"' •••• __ 'c" M oa a relC e' E r-- "0 Rotalipo'a ~ C L globotruncano/des ..., ~ .. '-'--

Figure 3. Upper Cretaceous biostratigraphy of the Scaglia Rossa-type facies in the analysed successions in the Polish part of the Pieniny KliEpen Belt; CTBE - anoxic deposits of die Cenomanian/Turonian boundary event; LCE - strongly calcareous deposits of the ower Campanian event

In the Pustelnia Marl Member the youngest part Occurrence: The zone has been recognised in the of the zone represents the older part of the Pustelnia Marl Member and the Macelowa Marl Rotalipora reicheli Zone (Middle Cenomanian). Member (both members in the Czorsztyn Succession). The benthic foraminifera make up less than 20% of Agglutinated Foraminifera: The deposits occupied the microfaunal assemblage. Agglutinated forms the Czorsztyn Ridge (Pustelnia Marl Member) in prevail among them, represented by only single outer shelf conditions (Bqk, 1995b) are characterised specimens of several taxa. by a high content of planktic foraminifers in the Age: This zone corresponds to the Rotalipora microfaunal assemblage (nearly 100%). Aggluti­ globotruncanoides Zone in the Scaglia Rossa-type nated foraminifers represent a subordinate compo­ facies (Bqk, 1998); Early Cenomanian. Its lower nent, and include: Arenobulimina preslii (Reuss), boundary was determined as lying within the Tritaxia gaultina (Morozova), T. subparisiensis Biticinella breggiensis Zone, late Albian (Bqk et al., (Grzybowski), Gaudryina carinata (Franke), 1995). Dorothia gradata (Berthelin), D. oxycona (Reuss), Textularia foeda (Reuss), Trochammina spp., Bulbobaculites problematicus Interval Zone Plectorecurvoides alternans Noth, Spiroplec­ Definition: Lower boundary - FAD of Bulbobaculites tammina tricarinata (d'Orbigny), S. cretosa, problematicus (Neagu); upper boundary - FAD of Ammodiscus cretaceus (Reuss), and Rhizammina sp. Uvigerinammina jankoi Majzon. Identical to the B. The index taxon appears as single specimens. problematicus Zone of Geroch & Nowak (1984). Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 21

PLANKTONIC DEEPWATER FORAMINIFERAL AGGLUTINATED ZONES FORAMINIFERAl ZONES I (R_~' CanwI, 1885, ~ ~CI) !!l CI) mo4l11"'''yl!..~ 1'"1 in P.K.B. ~ (this study) Abatho",phalus ·~T mayaroerul.J

... ~...... ~ ~o r------~ ,J :: .~ I ~ Garuserina gansseri ~- J 1------1 ~.,... l Globotnmcana aegyptiaca ~ Goese/J4 i c Globolnmcanella hawmeruu rllgosll .!! Globo'runcamta calcarata J i ~. E Globo,nmcana u" ventncosa U.jllllkoi -I 80 Globotnmcanila c. gigIInte!'l elevala - r------i 1-______--1 ~ Dicannella ~ asymetrico --c­ .!! u .!! Dicarinella concavata c f--,!r- Uvigerintunminll ex gr. jllllkoi 90 c U Dicarinella primirtva .1 ~ ~Atc=:"",'""I",=otnmc=a""na""''''''2'''',a'''''i-l

e~ Helveroglobotrwncana ~ L helvetIca - -- t-~-;:-r-ae-f(II~,obo;-rru-:--n-ck;-:Ir""'ioe-ru-'-is-t I------i U ._Ii __ Rotalipora CUJ'hma"i BlllbobfICulites C M ·~X···· ... problelflllticll5 !I 0 J ora n.c , ~-­ Rolalipora ; L globotnurcanoidet iplectonclITVoides u II/tem/IIU

~ _'-- L-______-...J

Figure 4. Calibration of stratigraphic ranges of selected agglutinated foraminifera and the zonal scheme based on DWAF in the Scaglia Rossa-type deposits of the Pieniny Klipppen Belt

The cherry red marls intercalated with thin-bedded from Lower-Middle Eocene of several locations in mudstones and fine-grained thin-bedded sandstones the Carpathians, Alps, and the North Atlantic (Macelowa Marl Member) are characterised by a (e.g., Kaminski et ai., 1990; Bqk et ai., 1997). The different microfauna. These facies represent the abundance of ammodiscids (up to 50%) accompanied edge of the Czorsztyn Ridge in outer shelf to upper with a lack of plankton and rare occurence of bathyal conditions (Bqk, 1995b). The benthic calcareous benthos was also noted from the Lower foraminiferal fauna comprises 55-80% of the total Cretaceous in the eastern Indian Ocean (Kuznetsova, assemblage, with dominating agglutinated forms. 1974), where it was interpreted as indicating Besides the index taxon, the most frequent deposition below the lysocline. The Glomospira foraminifers belong to the genera Plectorecurvoides, biofacies are interpreted here as deposition in low ReCllrvoides, Trochammina, Spiroplectammina, productivity and highly oxygenated conditions on Arenobulimina, Dorothia, Tritaxia, Saccammina, the sea floor with a low sedimentation rate. Glomospira, and Rlzizammina. Very characteristic During the youngest part of the Rotalipora is the high content of diverse glomospirids and cushmani Zone, the red facies are replaced by anoxic ammodiscids. Kuhnt & Kaminski (1989) described deposits (black, dark-grey marly shales and increased ammodiscids in the lower Campanian of siliceous shales; the Altana Shale Bed and the the North Atlantic, and termed this assemblage Magierowa Member; Birkenmajer, 1977; Birkenmajer "Biofacies B". According to these authors, it reflects & Jednorowska, 1984). They contain mainly pyri­ poorly oxygenated conditions at the sea floor. The tised radiolaria and numerous pyritised ostracods, most characteristic "Glomospira Event" was noted the significant benthic foraminifer Lenticulina 22 Krzysztof Bqk gaultina (Berthelin), and plankton represented by (Grzybowski), Trochammil1a umiatensis Tappan, single specimens of Praeglobotruncana delrioensis Uvigerinammina jankoi Majzon, H. d. walteri (PI ummer), and GlobigerineIloides uitramicra (Grzybowski), H. d. kirki Wickenden, Glomospira (Subbotina). Also occurring are single specimens of irregularis (Grzybowski), and Rhizammina sp. Less agglutinated forms belonging to the genera Nothia, frequent are: Spiroplectammina navarroana Rhabdammina, Rhizammina, Saccammina, Glomo­ Cushman, S. praelollga (Reuss), Gaudryina pyrami­ spira, Glomospirella, Hormosina, Bulbobaculites, data Cushman, Ammodiscus cretaceus (Reuss), Trochammina, and Tritaxia. These anoxic deposits Glomospira gordialis (Jones & Parker), Hormosina represent the local expression of the Cenomanian/ excelsa (Dylqzanka), Dorotlzia oxycona (Reuss), Turonian Boundary Event (CTBE) in the Pieniny Recurvoides primus Mjatliuk, Saccammina grzybow­ Klippen Belt. skii (Schubert), and S. placenta (Grzybowski). Age: This zone corresponds to the Rotalipora The following species have been observed as reicheli (Middle Cenomanian) through older part of single specimens: Hormosina velascoensis the Praeglobotruncana delrioensis zones (Cenoma­ (Cushman), Caudammina oVllla (Grzybowski), nian/Turonian boundary; Bqk, 1998). Ammodiscus tenuissi1l1us Grzybowski, Glomospira difundens Cushman & Renz, Pseudonodosinella Uvigerinam11lina ex gr. jankoi Interval Zone parvula (Huss), Aschemocella carpathica (Neagu), Definition: Lower boundary - FAD of Uvigerinam­ A. grandis (Grzybowski), Haplophragmoides d. mina ex gr. jankoi Majzon; upper boundary - FAD of eggeri Cushman, H. d. retroseptlls (Grzybowski), GoeseI/a rugosa (Hanzlikova). Identical to the U. Trochammina vocontiana Moullade, Paratrocham­ jankoi Zone of Geroch & Nowak (1984). milloides d. heteromorphus (Grzybowski), Tro­ Occurrence: The zone has been recognised in all chamminoides d. grzybowskii Kaminski & Geroch, Klippen successions of the Pustelnia Marl Member T. d. proteus (Karrer), T. coronatlls (Brady), T. and the Macelowa Marl Member. elegans Pokorny, Trochammilla d. boehmi Franke, T. Agglutinated Foraminifera: There is a significant d. nodosa, T. gyroidinaeformis Krasheninnikov, change in the microfaunal assemblage in comparison Gerochamina len is (Grzybowski), Verneuilinoides to the older zone. Some agglutinated taxa disap­ polystrophlls (Reuss), Spiroplectammina peared during the CTBE (Figure 4). They include lanceolata, S. costata (Huss), and S. tricarinata Haplophragmoides nonioninoides (Reuss), H. (d'Orbigny). concavus (Cha pm an), H. falcatosutllralis N eagu, The content of tubular forms, with prevailing Plectorecurvoides alternans N oth, Arenobulimina Rhizammina sp., less frequent Rhabdammina, and preslii (Reuss), Textularia foeda (Reuss). Several sporadic Nothia and Bathysiphon varies between other taxa appeared for the first time during the 10-40% (in extreme cases to 65%). These aggluti­ Zone, being represented by Uvigerinammina nated assemblages are very similar in all Klippen praejankoi Neagu, Hormosina excelsa (Dylqianka), successions of the PKB. Haploplzragmoides d. buI/oides (Beissel), H. eggeri Age: The lower boundary of the zone is diachronous, Cushman, H. kirki (Wickenden), H. d. walteri recorded by the top of CTBE anoxic facies (Figure 5). (Grzybowski), Recurvoides godulensis Hanzlikova, It represents the younger part of the Praeglobo­ Trochammina umiatensis Tappan, Karrerulina tnmcana delrioensis Zone (Early Turonian) within conifonnis (Grzybowski), Gerochammina conversa the slope facies of the Niedzica and the Czertezik (Grzybowski), G. tenuis (Grzybowski), Verneuilin­ successions; and the older part of the Margillo­ oides polystroplzus (Reuss), and Gaudryina truncana sigali Zone (middle part of Middle pyramidata Cushman. Turonian) within the Czorsztyn Ridge and the The deposits from the Czorsztyn Ridge (Pustelnia central furrow red facies. The upper boundary of this Marl Member) are characterised by a high content of Zone corresponds to the Late Santonian Dicarinella planktonic foraminifera (50-100%). However, in asymetrica Zone (Bqk, 1998). several samples, benthic foraminifera prevail. The benthos is very diverise. The content of agglutinated Goessella rugosa Interval Zone foraminifera varies from about 20% to 95% of the Definition: Lower boundary - FAD of Goessel/a benthic assemblage (mean 60%). rugosa (Hanzlikova); upper boundary - not defined Agglutinated foraminifers dominate the micro­ becouse of tectonic contact. faunal assemblages of the Macelowa Marl Member Occurrence: The zone has been recognised in the within all Klippen successions (besides the Macelowa Marl Member (Pieniny Succession) and Czorsztyn Succession). Planktonic forms are more pelagic deposits of the Maruszyna Scale. frequent only in single samples. These deposits cor­ Agglutinated Foraminifera: The assemblage of respond to lower-upper bathyal conditions (Bqk, agglutinated foraminifers in the lower part of the 1995a,b). Zone, is similar to the U. jankoi Zone. The prevail­ Agglutinated taxa are dominated by Recurvoides ing forms include Haplophragmoides d. bllIloides spp., Haplophragmoides d. bulloides ~Beissel), (Beissel), H. kirki (Wickenden), Recurvoides spp., Blllbobaculites problematicus Neagu, Geroclzam­ Bulbobaculites problematicus Neagu, Trochammi na mina conversa (Grzybowski), Karrerulina coniformis spp., Gerochammina conversa (Grzybowski), Karrer- Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 23 ulina coniformis (Grzybowski), and this Zone was described by Birkenmajer & Jednorow­ Uvigerinammina jankoi Majzon. ska (1984) from the Dzial pass section. In that sec­ Lower Campanian deposits contain a lower tion, the FAD of C. gigantea has been noted diversity and significantly less abundant DW AF ("sample 185"; op. cit.). The microfaunal assemblage assemblage. Its characteristic feature is a presence from these deposits consists of numerous tubular of Caudammina gigantea (Geroch). The first forms of Bathysiphon div. sp., Dendrophrya robllsta appearance of the index taxon was described by (Grzybowski) and ammodiscids. Moreover, there Alexandrowicz (1975) within the Pustelnia Marl are: Caudammina ovula (Grzybowski), Member, as a component of "assemblage with Globo­ Haplaphragmoides excavatus Cushman & Weters, truncana fornicata". This assemblage consists pre­ H. horridlls (Grzybowski), Cribrostomoides trini­ dominantly of planktonic foraminifers (78-86%) tatensis Cushman & Jarvis, Thalmannammina sub­ with rare agglutinated taxa (Arenoblllimilla sp., turbina Pokorny, Spiroplectammina boudouniana Gaudryina sp., Dorothia sp.). It may be correlated (d'Orbigny), 5. jarvisi Cushman, Gaudryina tricari­ with the Lower Campanian Event, characterised by nata Franke, Galldryina laevigata (Franke), very sparse benthic assemblages (e.g., Kuhnt et al., Goesella rugosa (Hanzlfkovii), Tritaxia amorpha 1992). (Cushman), T. subparisiensis (Grzybowski), T. capi­ The species Coudam11lina gigantea, used as an tosa Cushman, Dorothia crassa (Cushman), D. index taxon in most published zonations of trochoides (Mars son), Uvigerinammina jankoi Campanian-Maastrichtian (e.g., Geroch & Nowak, Majzon, and Gerochmnina lenis (Grzybowski). 1984; Moullade et al., 1988; Kuhnt et al., 1992), A significant change in the DW AF assemblage is occurs only within the Globotruncanita elevata­ recorded in this zone by the lack of numerous Globotruncana ventricosa Zones in the PKB (Figure Turonian-Santonian species (Figure 4), such as Recur­ 4). voides godlliensis, Troc/zammina umiatensis, Haplo­ The middle/late Campanian (from Globotrun­ phragmoides cf. blllloides, H. kirki, Gerochalllmilla canita calcarata Zone) through late Maastrichtian con versa and Karrerulina coniformis. (Abathomphailis mayaroensis Zone) DWAF Age: This zone represents the youngest part of the assemblages are characterised by a high abundance Globotruncanita elevata Zone through the older of tubular foraminifers and the frequent occurrence of part of the Globotruncana ventricosa Zone (early ammodiscids and Caudammina ovula (Alexandro­ Campanian). wicz & Birkenmajer, 1978; Jednorowska, 1980; Birkenmajer & Jednorowska, 1983b; Kostka, 1993). DISCUSSION ON BIOSTRATIGRAPHY Specimens belonging to the genera Spiroplectam­ The development of a reliable biostratigraphic mina, Tritaxia and Dorothia occur as single taxa. scheme is connected with the availability of conti­ The species Rzehakina epigona has its FO datum nous, stratigraphically well-calibrated sections. In within the Globotnmcnnita calcarata Zone (Kostka, strongly tectoni sed areas, such as the Pieniny 1993). This species becomes more abundant in the Klippen Belt, a biostratigraphic zonation is neces­ late Palaeocene wihin the variegated non­ sarily based on composite sections. The data from calcareous shales of the Maruszyna Scale, being the studied area come from 38 sections, comprising distinguished as the index taxon for the Rzehakina the Scaglia Rossa-type deposits of early epigona assemblage Local Zone (Kostka, 1993). Cenomanian through late Maastrichtian age. The Age: This zone represents the youngest part of the large number of sections and the occurrence of Dicarinella asymetrica Zone (late Santonian) planktonic foraminifers in these depOSits, which through the Abath011lphalus 11layaroensis Zone verify the continous sedimentation, constitute a very (late Maastrichtian). good databse for biostratigraphical study. Zonal schemes based on agglutinated foramin­ Uvigerinammina jankoi-Caudammina gigantea ifers have significant stratigraphical value in Concurrent Range Zone predominantly non-calcareous deep marine Definition: Lower boundary - FAD of Caudam11lina sediments. Biozonations based on this group of gigantea (Geroch); upper boundary - LAD of microfauna have been proposed by various authors, Uvigerinammina jankoi Majzon. during the last 15 years. The most useful of them and Occurrence: The zone has been recognised in the one of the first, simultaneously, was the zonal Macelowa Marl Member (Pieniny Succession). It is scheme by Geroch & Nowak (1984), prepared from proposed here as an additional zone within Scaglia the deep-water flysch deposits of the Outer Rosa-type deposits. Carpathians. This zonation has been tested and Agglutinated Foraminifera: The DWAF are repre­ modified in different areas including the North sented by a more diversified assemblage than in the Atlantic (Moullade et al., 1988; Kuhnt et az', 1989; lower part of Giobotrullcanita elevato Zone. Kuhnt & Collins, 1996; Kuhnt & Kaminski, 1997), However, the taxonomic composition of aggluti­ the South Atlantic (Volat et az', 1996), the nated foraminifers is different from the Turonian­ equatorial Atlantic (Kuhnt et az', 1998), the Santonian sediments. The assemblage representing Western Pacific (Wightman & Kuhnt, 1992), and 24 Krzysztof Bqk the other areas of the Western Tethys (Kuhnt & the late Cenomanian-early Turonian anoxic event. Kaminski, 1989; Kuhnt, 1990; Bubfk, 1995; Kaminski This is confirmed by the colour of deposits, intense of et aI., 1996; Olszewska, 1997). burrowing, trace fossil ichnofacies and diversified The stratigraphical value of the zonal schemes, agglutinated assemblage with tiny, smooth-walled based on agglutinated foraminifers is estimated species. from sections, where these forms co-occur with cal­ Trace fossils represent a low diversity assem­ careous microfossils. Only in small numbers of sec­ blage with prevailing Zoophycos in the red marls tions, investigated up to present day, this possibil­ and marly limestones, and tubular forms of ity exists. The calibration of Upper Cretaceous Planolites-type in the thin muddy or sandy interca­ DWAF ranges with chronostratigraphy (ranging in lations (Bqk, 1995a). The macrobenthos penetration age from Turonian), has been proposed by Kuhnt was controlled by a shortage of food on the well (1990) in the Gubbio sections (Umbrian Apennines, oxygenated sea floor. It could be confirmed by Italy) and the Hacho de Montejaque section reduced size of infaunal forms and by the presence of (Penibetic Zone, southern Spain). The deposits from organisms selectively reworking the sediments. these sections are very comparable with the Pieniny Oligotrophic conditions, connected with the high Klippen Belt in relation to the lithological features oxygentation level at the sea floor are reflected, and sedimentary conditions. The Zumaya section moreover, by a low density of benthic foraminiferal (North Iberian continental margin) studied by assemblages, dominated by shallow and deep Kuhnt & Kaminski (1997) is another complete sec­ infauna (average 55% of the foraminiferal benthos). tion, were an analysis of samples enabled the cal­ Sedimentation rate was very low during the ibration of the biostratigraphic ranges of the deposition of the Upper Cretaceous red facies. It was DWAF. calculated from 1-4 m/my in the shallowest part to The application of a zonal scheme based on 8-23 m/my in the deeper part of the Pieniny Klippen agglutinated taxa depends on its calibration with Basin. Very low sedimentation rate is emphasised chronostratigraphy, on the one hand, and is related by the high rate of sediment bioturbation. For to lithology and palaeogeographical setting, on the example, carbonate-rich marls of the Czorsztyn other hand. The palaeogeographic setting of the Succession (northern margin of the basin) are DW AF assemblages, their occurrence within certain completaly bioturbated. The rate of sediment types of lithologies and their taxonomic composition accretion changed during the deposition in the allowed the differentiation of six different deeper part of the basin, being reflected by a change foraminiferal biofacies in the Upper Cretaceous in the intensity of bioturbation, and trace fossil (Kuhnt et aI., 1989). Foraminifers from sections tiering (Bqk, 1995a). An intermittent fine clastic investigated in the western Mediterranean, the deposition by diluted turbidity currents, restricting Penibetic Zone, and the North Iberian areas the possibility of the sediment reworking by represent "Scaglia-type" deep-water assemblages. infauna, were more frequent during the Santonian. Their main feature is a high diversification of The middle Turonian and the uppermost agglutinated foraminifers with large numbers of Santonian/lower Campanian green and pink lime­ rhizamminids and tiny, finely agglutinating stones reflect extremaly low rate of sedimentation, species. These DW AF assemblages occurring in the calculated as about 1 m/my. "Scaglia Rossa" and grey limestone facies, indicate Palaeobathymetric information is given by slope sedimentation with only rare, fine-grained planktonic foraminifers (their total content and detrital inputs (Kuhnt, 1990). content of keeled forms), calcareous/agglutinated foraminifers ratio, trace fossil assemblage, and Environmental characteristics of the Scaglia Rossa calcium carbonate content. Planktonic foraminifers facies in the Pieniny Klippen Belt are represented predominantly (more than 90%) by A detailed analysis of the early Cenomanian large keeled morphotypes of the genera Rotalipora, through late Campanian palaeoenvironment of the Heivetogiobotrtlllcana, Marginotruncanl7, Globotrun­ Scaglia Rossa-type deposits in the PKB was pre­ calla, and Rosita. Only in the Czorsztyn Succession sented by the author in his PhD Thesis (Bqk, 1995b). (the shallowest part of the basin), the non-keeled The results of this were based on the lithological forms (Hedbergella, Globigerinelloides, Hetero­ features, analysis of trace fossil assemblages, helix) make up about 10-80% of the plankton, morphogroup diversity (calcareous and aggluti­ probably reflecting the sea level changes. nated), calcareous/ agglu tina ted foraminiferal Content of the calcareous benthic foraminifers is ratio, taxonomic diversity of certain groups of very small, ranging from sample to sample between 0 benthic microfossils, microfaunal density, and 20%. Their taxonomic diversity is low (1-5 plankton/benthos ratio, content of keeled planktonic species per sample). This confirms that deposition forms, and morphological fea tures of some the Scaglia Rossa facies took place in upper to lower agglutinated taxa. bathyal depths. Within the Czorszyn Succession, The sedimentation of the early Cenomanian to calcareous assemblages are more significant compo­ late Campanian red facies took place under highly nent, however, their content does not exceed 50% of oxygenated conditions at the sea floor, except during the whole benthos, and number of taxa range from 2- Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 25

12 taxa. These types of assemblages are interpreted Maastrichtian marls as fragments in fine-grained as indicating outer shelf-upper bathyal depths for sedimentary breccia and a few layers of fine-grained the Czorsztyn Ridge (northern margin of the Pieniny sandstone within the Upper Senonian complex was Klippen Basin) during the Late Cretaceous. The sug­ explained by Alexandrowicz & Birkenmajer (1978) gestion takes into account an observation, that opti­ as the effect of bottom erosion by episodic turbidity mal conditions for the calcareous benthos took place currents. Mean sedimentary rate for these deposits is in outer shelf environments (near the edge of shelf) calculated as 2 m/my. during the Late Cretaceous, as was concluded by The described sedimentary environment of the Kuhnt et al. (1989). Scaglia Rossa-type facies in the Pieniny Klippen An ichnofossil assemblage in the studied deposits Basin (including Klippen and Maruszyna succes­ (B q k, 1995a) is similar to other localities, sions) was very similar to that of the southern documented from deep-water Cretaceous and (Gubbio sections; Umbrian Apeninnes) and the west­ Cenozoic carbonate deposits (Ekdale & Bromley, ern (Hacho de Montejaque section; Penibetic Zone) 1984; Ekdale, 1985). The suggestion about the depths parts of the Western Tethys. However, the sedi­ and sedimentation rate is interpreted, among other, mentation in the Pieniny Klippen Basin was charac­ based on an ethological composition of ichnofauna in terised by more frequent turbiditic detrital inputs, the studied deposits. Pascichnia and Fodinichnin especially during the late Coniacian-Santonian. traces dominate there, being accompanied by rare Agrichnin and Repichnin traces. Comparison of index taxa ranges with different Outer shelf-upper bathyal through lower bathyal localities bathyal depths (near CCD) of the sea floor are also Plectorecllrvoides alternans suggested from the calcium carbonate content analy­ The species Plectorecurvoides alternans was used as

sis. More than 200 analyses of the CaC03 content in a zonal marker for the first time in the Flysch the marls and marly limestones (Bqk, 1995b), have Carpathians (Geroch, 1959, 1962; Hanzlikov;l, been used to support this interpretation, carried out 1966). Morgiel & Olszewska (1981) noted its strati­ in relation to the distinguished successions and the graphical ranges from Albian through Turonian, and

time scale. High values of CaC03 in the Middle­ emphasised its stratigraphical value within the Upper Turonian sediments (mean 40-60% in Albian and Turonian, as a part of "Assemblage of P. particular successions) decrease up section to about alternans". Later, its FO in the Middle Abian was 20-30% in the Santonian. This observation reflects a proposed as a base of the P. alternans Zone in Geroch remarkable change in the sedimentary processes, & Nowak's zonation (1984) and in Olszewska's from pelagic to hemipelagic, with more frequent zonation (1997). Similar data about the occurrence of turbiditic detrital inputs. this species were observed in the Romanian A palaeoecological interpretation of the Carpathians (Neagu, 1990). Campanian-Maastrichtian sediments in the In the PKB, P. alternans appeared within the Maruszyna Scale has been presented by Kostka Biticinella breggiensis Zone, corresponding to the (1993), based on taxonomic features of benthic and Middle Albian. It occurs in the red facies as frequent planktonic assemblages, lithology, and using the and common species within low to medium diversi­ planktic/benthic foraminifera ratio. Benthic fied assemblages, dominated by Glomospira spp, foraminifers are dominated by Reussella sznjnochae, Ammodiscus spp., Recurvoides spp., and Osnngulnria cordierinna, Gyroidinoides nitidus, rhizamminids. Anomalinoides affinis, Pleurostomella spp., The occurrence of P. alternans is restricted to the Gnvelinella beccnriiformis, Pullenin spp., Dorotlzia Western Tethys. Besides the Carpathian area, the trochoides, Tritaxia tricarinnta, T. amorpha and Alps (first time described by Noth, 1952), and the Spiroplectammina dentatn. The planktic/benthic Moroccan Numidian Flysch (Morgiel & Olszewska, foraminifera ratio is very high (about 0.9). The 1982), no data are known from the Atlantic and the planktic foraminiferal assemblages are dominated Indian oceans. It represents an element of typical by the genera Globigerinelloides, Hedbergella and deep-water assemblages from environments below Heterohelix. The content of deep-dwelling the CCD. However, it appeared within calcareous globotruncanids is consistent and varies between 10 flysch and hemipelagites, too. It seems that upper­ and 20% (Kostka, 1993). Taking into account the middle bathyal depths created an upper depth above features of microfaunal assemblages, Kostka limit for this taxon. concluded that Campanian-Maastrichtian sedi­ ments were deposited in off-shelf open marine con­ BlIlbobaclIlites problematiclIs ditions at middle bathyal depths. The lithological Stratigraphic ranges of the B. problematicus at dif­ character (about 20 m thick marls and marly lime­ ferent localities (including the abyssal oceanic, the stones) and lack of shallow water microfaunal marginal basins and the Carpathian trench) have markers record the location of this area at a dis­ been presented by Kuhnt & Kaminski (1990). The FO tance from shoreline on the order of 50-100 km, prob­ of this taxon was observed directly above the anoxic ably on the submerged ridge (Birkenmajer, 1986). deposits of CTBE in all localities, except in the The appearance of reworked Campanian- Carpathian area, where its FO occurs within 26 Krzysztof Bqk

Cenomanian strata. The above authors suggested, increase in the population could be linked with the that this fact correlates with the first occurrence of increase of oxygenation at the sea floor. This was the red oxic sedimentary environments, which took earlier suggested by Kuhnt & Kaminski (1990), in place significantly earlier in the Carpathian relation to the FO of this taxon in the similar type basins. Therefore, oxygen-depleted bottom waters of lithologies at different localities. Two of the B. constituted a faunal barrier for the colonisation of B. problematieLls "blooms" occurred in the PKB just problematiells. after large anoxia. They represent: 1) the Late Albian/Early Cenomanian episodic anoxia, recorded by black deep-water siliceous facies with Local 5ea lave Klippen successions curve opportunistic agglutinated assemblages of (K. Bilk. 1995/» Czor ~~~~ ~~~ __L-~ "Biofacies B", and 2) the Cenomanian/Turonian iii Boundary Event. The latter anoxia are expressed in o El !±l the PKB, by black shales, both from the shallow, as elrica and the deepest part of the basin, with rare and low-diverse agglutinated assemblages, and spe­ Dicarinella cially adapted other benthic communities, like concavaJa ostracods and calcareous foraminifers. The species B. i U problematieus, prefering probably the shallow .~ M I---=TF;:':'::;':'~ I infaunal habitats (comparable to Ammobaeulites - I see discussion by Tyszka & Kaminski, 1995), could be ~ L j t=~~mq more tolerant of dysoxia and low pH than other agglutinated taxa. Thus, during an increase in c oxygenation at the sea floor, this taxon could be an o~ c initial coloniser on the bottom, tolerating the oCP episodic anoxia occurring in the first phases of the environmental changes. Figure 5. Frequency of the Bulbobaculites problematiclls in On the other hand, it should be pointed out that the Scaglia Rossa-type facies, in relation the local sea-level an "increase" in the number of foraminiferal tests changes, the Pieniny Klippen Belt; p - present, r - rare, f - frequent, c - common can be caused by a low sedimentation rate, as took place during the sea level high-stands. The FO of B. problematieus in the PKB is well In the Carpathians, where B. problematieus documented near the base of the Rotalipora reieheli appeared earlier than in the rest of the oceanic Zone, corresponding to the base of the Middle realm, its FO datum is still studied. Neagu (1990) Cenomanian, independent of facies. A comparison of observed the FO of this species in the lower Albian frequency of this taxon in the Middle Cenomanian­ Haplaphragmoides nonioninoides Zone in the Lower Campanian sediments allowed to observe southern flysch zone of the Romanian Carpathians. three peaks of high abundance (Figure 5). They More recently, Olszewska (1997) presenting a com­ correspond to the Rotalipora reielzeli/R. posite zonation based on different foramininiferal greenhornensis, Helvetoglobotrllneana helvetiea/ groups for the Tithonian-Miocene in the Polish Marginotruneana sigaJi and Diearinella primitiva Flysch Carpathians, reported the FO datum of B. Zones, reflecting the sea level high-stands. These problematiells in the uppermost Albian (together high-stands were proposed on the basis of changes in with Planomalina buxtorfi and Rotalipora plankton morphotypes and mobile calcareous appenniniea). epifauna, observed in the deposits of the shallowest part of the Pieniny Klippen Basin (Bqk, 1995b). The changes of these two features of foraminiferal Uvigerinammina jankoi assemblages are linked with behaviour of A detailed description of U. jankoi and first report foraminifers. The increase of "deep-water" plank­ on its stratigraphical value originate from the tonic morpho types of genera Praeglobotrllneana, Polish Flysch Carpathians, presented by Geroch Helvetoglobotruneana, Rotalipora, Marginotrun­ (1957). From the same region, U. jankoi occurs as the eana, Contllsotruneana, and Globotrllneana correlates index taxon for the Upper Turonian-Santonian U. with increase of sea level, as was presented e.g., by jankoi Zone in the Nowak & Geroch's zonation Sliter (1975), Hart (1980), Leckie (1987), Hallock et (1984). Its FO is presented there immediately above al. (1991). A similar positive correlation can be green shales with radiolarians, correlated with the exemplified in relation to the calcareous mobile CTBE. epifauna (e.g., Fiirsich et al., 1991; Tyszka & After this presentation, U. jankoi has been used Kaminski, 1995). as stratigraphical marker species, both in the Thus, taking into account the positive correlation North Atlantic and the Tethan realm in every zonal between the high frequency of B. problematjells and scheme (e.g., Moullade et ai., 1988; Kuhnt et al., sea level high-stands, it can be concluded that the Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 27

en successions ieniny - Branisk Czertezik

lower-middle Planktonic foraminiferal bathyal depths zones (K. BlOlk. 1998) ~ r _!2i<:p!.i'!.e!!.a_c9.nE'!Yf!!a.. -- 90 L Dicarineila primitiva c: .!!! Marginotruncana siga/i c: -M ~FAD e r-- Helvetogiobotruncana t ;; .= FAD of ~ """" E helvetica ..... anoxic , deposlb . ... Praegiobotrunc. delrioensis I············ ...... ~jll!'~O~ "" ~'~"""""'I E L c~ ...... ~ Rotalipora cushmani 0c: - - II) 7foialiooro m,,'nhOrnemij • 0 M Rotaiipora reicheli '--

Figure 6. Diachronous lower boundary of the Uvigerinammina jankoi Zone in the Pieniny Klippen Belt.

1989a; Kuhnt & Moullade, 1991). Its FO datum was the lowermost part of U. jankoi Zone. In the PKB, noted at most localities just above or in the highest small specimens with pseudo-biserial arrangement part of anoxic deposits representing the CTBE. in the adult stage, classified as U. praejankoi occur However, at certain localities in bathyal within the H. helvetica and M. sigali zones (Bqk et environments, like in the Gubbio section (Umbrian al., 1995). However, its FO is the same as that of U. Apeninnes) and the Zumaya section (North Iberian jankoi. This fact can be explained by: 1) the later continental margin), it appeared in the Coniacian or migration of this taxon from the Romanian part of Santonian. Within the Scaglia Rossa facies at the the Carpathians, or 2) similar, like U. jankoi, Gubbio section (white to pink coloured siliceous requirements in relation to the oxygenation of the limestones), U. jankoi is practically absent (Kuhnt, bottom water, as well as 3) sedimentary conden­ 1990). Only single specimens have been found in the sation due to very low sedimentation rate during Santonian strata. This was explained by Kuhnt as this time (1 m/my). being due to the lack of the clay minerals used to The LO of U. jankoi is noted in the Scaglia Rossa­ agglutinate the wall. type deposits of the PKB within the Globotruncana This taxon, in all described localities, occurs ventricosa Zone (Alexandrowicz, 1975). A similar within highly diversified assemblages, with spec­ datum was reported from the Romanian Flysch imens that have a brownish siliceous agglutinating Carpathians, where this species has its LO within wall (Kuhnt et al., 1989a). The assemblages repre­ the Globotruncanita calcarata Zone (Neagu, 1990). sent the so-called "Biofacies A", corresponding to The LO in the middle/late Campanian was noted in the Upper Cretaceous oxygenated environments. ODP Hole 641A (abyssal part of the North In the PKB the first occurrence of U. jankoi is con­ Atlantic; Kuhnt et al., 1989a). In the Polish Flysch nected with changes of oxygenation of the bottom Carpathians (Geroch & Nowak, 1984), the Iberian water (Figure 6). Anoxic facies, representing by continental margin (Kuhnt & Kaminski, 1997) and at black shales and marly shales have been replaced most localities in the North Atlantic (e.g., by light-green, highly calcareous limestones, corre­ Moullade et al., 1988; Kuhnt et al., 1998), U. jankoi sponding to the high Eh level. The change of the last occurred during the early Campanian. In the facies took place earlier on the slope of the Pieniny Scaglia Rossa facies of the southern and western Klippen Basin - within the Praeglobotruncana part of the Western Tethys (Kuhnt, 1990), its LO delrioensis Zone through the Helvetoglobotrllncana was noted earlier, at the top of the Dicarinella helvetica Zone, corresponding respectively to the asymetrica Zone (near the Santonian/Campanian Cenomanian/Turonian boundary and the Early­ boundary). Middle Turonian. Simultaneously, a change in the agglutinated assemblages was observed in the stud­ Goesella rugosa ied sediments. A number of first occurrences of the Specimens of Goesella rugosa were described from agglutinated species are observed in the Turonian, only slope facies, representing the environments occuring within the highly diversified assemblage. above the CCD (Kuhnt & Kaminski, 1990). This In the Romanian Flysch Carpathians, Neagu restriction is linked with utilisation of calcareous (1990) described the species U. praejankoi, which cement by this taxon for agglutinating its test. The occurs in the Whiteinella archeocretacea through FO of G. rugosa was presented by Geroch & Nowak the Marginotruncana schneegansi Zones. Neagu sug­ (1984) at the base of the Campanian from the Polish gested to distinguish the U. praejankoi Zone within Flysch Carpathians. The same datum noted by 28 Krzysztof Bqk

Neagu (1990) from the Romanian Flysch PALAEOCEANOGRAPHIC EVENTS Carpathians, Kuhnt & Kaminski (1997) from the CenomanianfTuronian boundary event (CTBE) Zumaya section, and Kuhnt & Moullade (1991) from Beds corresponding to the CTBE are characterised by DSDP Hole 398D at the Vigo Seamount (the North anoxic facies with high level of organic carbon Atlantic). (Herbin et aI., 1986). Microfossil assemblages from Goessella rugosa has not been observed within these facies are dominated by radiolarians and the Scaglia Rossa facies at the Gubbio and devoid of benthic foraminifers, and directly over­ Montejaque sections (Kuhnt, 1990). In the PKB, this lying beds contain low diversified opportunistic taxon occurs as more frequent in deposits from the agglutinated taxa (e.g., Kuhnt, 1992; Lamolda & deepest part of the basin. This fact may be caused by Peryt, 1995). The event is accompanied by important restriction of the clay minerals used to agglutinate taxonomic changes in DWAF (Geroch & Nowak, the wall in an environment with extremely low 1984; Moullade et aI., 1988; Kuhnt, 1990; Neagu, sedimentation rate. 1990). The stratigraphic range of G. rugosa is restricted In the PKB the Cenomanian/Turonian boundary is to the late Maastrichtian (Geroch & Nowak, 1984)­ characterised by black shales and marly shales, ?early Palaeocene (Kuhnt & Kaminski, 1990). both in the Czorsztyn Ridge and in the deepest part However, at most localities it depends on the of the basin (Birkenmajer, 1977; Birkenmajer & location of the CCD in the basin. In Scaglia-type Jednorowska, 1984; Bqk, 1998). The microfossil assemblages within the Maruszyna Succession (the assemblage is represented by radiolarians and PKB), the LO of G. rugosa has been recorded in the ostracods (in the Czorsztyn Succession only), Abathomphalus mayaroensis Zone (Kostka, 1993). predominantly. Low diversity benthic foraminifers with single specimens of genera Haplophragmoides, Bulbobaculites, Gaudryina, Glomospira and Trochammina occur in the slope facies of CTBE (the Caudammina gigantea Niedzica Succession), where black marly shales are The species Caudammilla gigantea is used to define intercalated with muddy turbidities. They are the "Hormosina ovulum gigantea Zone" in the absent in the deep-sea successions, except of single Polish Flysch Carpathians (Geroch & Nowak, tubular forms. In the Czorsztyn Ridge facies, the 1984). The FO of this species marks in that area the agglutinated foraminifers are represented by single base of the mid-Campanian. In the Romanian opportunistic forms of genera Nothia, Rhab­ Flysch Carpathians, C. gigantea occurs within the dammina, Rhizammina, Saccammina, Ammodiscus, Globotruncanita elevata Zone (early Campanian), Glomospira, Glol1lospirella, Bulbobaculites (only in co-existing there together with U. jankoi (Neagu, lower part), and Trochammina. 1990). At some localities in the abyssal North The FO of Hormosina excels a was observed Atlantic, a similar coexisting took place (Moullade within the CTBE in the Szaflary section (Czorsztyn et aI., 1988), which formed the basis to define the Succession). This species has not been known from jankoi-gigantea concurrent range zone (Vigo this age, so far. Its earliest FO was described in the Seamount; Kuhnt & Moullade, 1991). Flysch Carpathians, from the Santonian/ In most localities, the FO of C. gigantea is Campanian boundary (Morgiel & Olszewska, 1981; observed above the benthic-free zone corresponding Geroch & Nowak, 1984). Kuhnt & Kaminski (1990) to the Lower Campanian Event. described H. excelsa from the Coniacian-Santonian Within the Scaglia-type assemblages this sediments in the Moroccan Rif. They speculated that species is rare. It is absent in the Gubbio material, some specimens of their assemblages could be and occurs as single specimens in the Campanian of intermediate forms to Hyperammina elongata and the Penibetic section (Kuhnt, 1990). In the PKB, it Hyperammina dilatata. In the PKB, above the was found as rare, in the Czorsztyn and the Pieniny CTBE, H. excelsa was found within the late successions, representing the shallowest and the Turonian through the late Santonian assemblages as deepest part of the basin, but only within single or few specimens in samples, exhibiting simi­ Globotruncanita elevata-Globotruncana ventricosa lar morphologic features like in the population from zones. The infrequent occurrence of C. gigantea in the Moroccan Rif. pelagic calcareous environments was linked with its Above the CTBE in the PKB, a change in the utilisation of siliceous cement and grains for agglutinated assemblages occurs, emphasised by agglutinating its test. Low concetration of silica and increase of diversity and appearance of new species. high pH value in the calcareous environments could The Turonian-Coniacian-Santonian agglu tina ted restrict the population of this species. Kuhnt et al. foraminifers are dominated by tiny smooth-walled (1998) suggested the lower bathal depths as the calcareous and siliceous specimens of the species upper depth limit for distribution of C. gigantea. It Uvigerinammina ex. gr. jankoi, Gerochammina seems to be realy true in most localities where C. con versa, Karrerulina coniformis, Haplophrag­ gigantea has been found. In the Pieniny Klippen moides d. bulloides, H. d. kirki, Recurvoides spp., Basin, this upper depth was- higher, corresponding Bulbobaculites problematicus, Trochammina spp. probably to the upper-middle bathyal. and rhizamminids. Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 29

r-r- .. t1 PLANKTONIC DWAF iJ'-d pellllic. hemipelagic facl .. CWAF ....o\Ion.ln tho baIt1yal rtrsch .nvlronments (Ibov. ceo) .. FORAMINIFERAL Ptm~.ticZon., ~~ogated day ZONES DSOP ~Ibrall... Aret North Iberian ! Umbr. Apennines belowCCD Pollah Flysch Poliah Flyaell ~ ZONES Carpathlana Carpathian. Hole 3880 -M,,·Yllan ConU".,..taI .. ; IR ....aqno/

Lower Campanian event (LCE) served calcified specimens of only several species An interval of biosiliceous sedimentation with (M. Bqk, 1996b). DW AF assemblages are represented abundant radiolarians and scarce, poorly preserved by single specimens of some taxa within this benthic foraminifers has been observed at many interval. Diversity of agglutinated assemblages is localities in the North Atlantic, South Atlantic and significantly lower than in the Santonian ones, and the Tethyan Realm (e.g., Butt, 1981; Hemleben & decreases above the calcareous horizon. The LO of Troester, 1984; Moullade ct aI., 1988; Kuhnt et aI., Bulbobaculites problematic us is observed within the 1989; Kuhnt et aI., 1998). The event was linked with LCE. the formation of warm saline bottom waters, influ­ encing changes in deep water circulation. These CONCLUSIONS resulted in changes among the DW AF assemblages. The Cenomanian through Upper Maastrichtian In some pelagic environments (the Umbrian Scaglia Rossa-type facies in the Pieniny Klippen Apennines and the Penibetic Zone; Kuhnt, 1990), constitute good material for calibration of DWAF biosiliceous deposits are not known. However, ranges with chronostratigraphy, because of the within the Lower Campanian deposits, a major occurrence of well diversified and abundant faunal change in agglutinated foraminifers was agglutinated taxa and presence of planktic foram­ observed. inifers and calcareous nannoplankton within the In the PKB, the LCE has a characteristic lithol­ microfossil assemblages. ogy, only within the shallowest succession (the The biostratigraphic succession of agglutinated Czorsztyn Succesion). The uppermost Santonian­ foraminifers in the analysed sections allows me to Lower Campanian deposits are represented by 2 m recognise the Upper Cretaceous zones oryginally thick thin-bedded light-green limestones, interca­ defined by Geroch & Nowak (1984) in the Polish lated with brick-red highly calcareous marls (the Flysch Carpathians. However, the ranges of certain Lorencowe Chert Bed in the Kietowy stream section; zones in Campanian-Maastrichtian are different Birkenmajer, 1977). Foraminifers are dominated by than in the latter zonation, being caused by specific planktic forms. Radiolarians occur as poorly pre- environmental conditions during sedimentation of 30 Krzysztof Bqk the Scaglia Rossa-type facies in this part of the helpful comments by Prof. K. Birkenmajer (Polish Western Tethys. The Goesella mgosa Zone, in Academy of Sciences) and Prof. S.W. Alexandrowicz Geroch & Nowak's and other zonal schemes (e.g., (Academy of Mining and Metallurgy). Michael A. Kuhnt & Kaminski, 1997; Figure 7), calibrated with Kaminski (University College London) and early Campanian, has in the PKB a longer range; Christoph Hemleben (University of Tiibingen) from the earliest Santonian (uppermost part of revieved an earlier draft of this paper and provided Diearinella asymetriea Zone) through the late useful comments on biostratigraphy. This study was Maastrichtian (Abathomplzalus mayaroensis Zone). supported by Cracow Pedagogical University grant The species Caudammina gigantea, another index BW-168/G/97. Thanks also to the Grzybowski marker in the Campanian and Maastrichtian in Foundation for a travel grant to attend the 5th many zonations (Geroch & Nowak, 1984; Moullade International Workshop on Agglutinated et aI., 1988; Kuhnt & Moullade, 1991; Kuhnt et aI., Foraminifera in Plymouth. 1992; Kuhnt & Kaminski, 1997; Olszewska, 1997), occurs here only within Globotruneanita elevata - Globotruneana ventrieosa zones. Thus it was used REFERENCES here as a marker in the concurrent range zone of U. Alexandrowicz, S.W. 1966. Stratigraphy of the Middle and jankoi - C. gigantea, considered as an additional Upper Cretaceous in the Polish part of the Pieniny zone (Figure 7). Klippen Belt. Zeszyty Nallkowe Akademii G6rniczo­ HlIl1ziczej, 157, (Rozprawy, 78), 1-142. Outer shelf - lower bathyal depths of the basins, low rate of pelagic sedimentation above CCD, oligo­ Alexandrowicz, S.W. 1975. Assemblages of Foraminifera and stratigraphy of the Puchov Marls in the Polish part of trophic conditions at the sea floor, high value of pH the Pieniny Klippen Belt. Bulletin de L'Acadhnie Polonaise and restriction of silica and siliceous grains at the des Sciences, Serie des Sciences Terre,23, (2), 123-132. sea floor, as well as periodic anoxia were the main Alexandrowicz, S.W. & Birkenmajer, K. 1978. 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Palaeoclimatology, Palaeoecology, 85, 149-159. Birkenmajer, K & Jednorowska, A. 1976. Lower Gale, AS., Kennedy, W.J., Burnett, J.A., Caron, M. & Kidd, Maastrichtian as upper age limit of pelagic foraminiferal B.E. 1996. The Albian to Early Cenomanian succession at marls in the Czorsztyn Succession, Pieniny Klippen Belt, Mont Risou near Rosans (Hautes-Alpes, SE France); an Carpathians. Rocznik Polskiego Towarzystwa integrated study (ammonites, inoceramids, planktonic Geologicznego, 46, (3), 297-307. foraminifera, nannofossils, oxygen and carbon isotopes). Birkenmajer, K. & Jednorowska, A. 1983a. Upper Cretaceous Research, 17, 5, 515-606. Cretaceous stratigraphy of the Branisko Nappe at Geroch, S. 1957. Uvigerinammina jank6i Majzon (Foramin­ Sromowce Wyine, Pieniny Klippen Belt of Poland. Studia ifera) in the Carpathian Flysch. Rocznik Polskiego Geologica Polonica, 77, 7-26. Towarzystwa Geologicznego, 25, (3), 231-244 (In Polish). Birkenmajer, K. & Jednorowska, A 1983b. Upper Cre­ Geroch, S. 1959. Stratigraphic significance of aranaceous taceous and Palaeogene deposits at Maruszyna, Pieniny foraminifera in the Carpathian flysch. Paliiontologische Klippen Belt of Poland. Studia Geologica Polonica, 77,27- Zeitschrift, 33, (1-2), 113-122. 53 (In Polish). Geroch, S. 1962. Tlwlmannammina and Plectorecurvoides Birkenmajer, K. & Jednorowska, A. 1984. Upper Cretaceous (Foraminifera) in the Lower Cretaceous of the Flysch stratigraphy in the Pieniny Nappe at Sromowce Niine, Carpathians. Rocznik Polskiego Towarzystwa Pieniny Klippen Belt, Carpathians, Poland. S tudia Geologicznego, 32,2,281-295. Geologica Polonica, 83, 25-50. Geroch, S. & Nowak, W. 1984. Proposal of zonation for the Birkenmajer, K. & Jednorowska, A. 1987. Late Cretaceous Late Tithonian-Late Eocene, based upon arenaceous foraminiferal biostratigraphy of the Pieniny Klippen Belt Foraminifera from the Outer Carpathians, Poland. In: H.J. (Carpathians, Poland). Studia Geologica Polonica, 92, 7-28. Oertli (ed.), BENTHOS '83: 2nd International Symposium Bubfk, M. 1995. Cretaceous to Paleogene agglutinated on Benthic Foramillifera (Pall, April 11-15, 1983), 225-239, foraminifera of the Bile Karpaty Unit (West Carpathians, Elf-Aquitane, ESO REP and TOTAL CFP, Pau & Czech Republik). In: M.A Kaminski, S. Geroch & M.A Bordeaux. Gasil1ski (eds), Proceedings of the Fourth International Glusko, V.V & Kruglov, S.s. (eds) et aI., 1971. Geologi­ Workshop on Agglutinated Foraminifera. Grzybowski ceskoje Stroenie i Gorjucie Iskopaemyje Ukra in skich Foundation Special Publication, 3, 71-116. Karpat. Trudy Ukrainskoj Nefl. Geoi. Razved Inst., 25, 1- 389 (In Russian). 32 Krzysztof Bqk

Hallock, P., Premoli-Silva, 1. & Boersma, A. 1991. Sim­ Kuhnt, W. 1992. Abyssal recolonization by benthic ilarities between planktonic and larger foraminiferal foraminifera after the Cenomanian-Turonian boundary evolutionary trends through Paleogene paleoceanographic anoxic event in the North Atlantic. Mar i n e changes. Palaeogeography, Palaeoclimatology, Micropaleontology, 19, 257-274. Palaeoecology, 83, 49-64. Kuhnt, W. & Collins, E.S. 1996. Cretaceous to Paleogene Hanzlikova, E. 1966. Die Foraminiferen der Lhoty­ benthic foraminifers from the Iberia Abyssal Plain. In: R.B. Schichten. Acta Musei Moraviae, Scientiae naturales, 60, Whitmarsh, D.s. Sawyer, A. Klaus & D.G. Masson (eds), 95-132. Proceedings of the OcellIl Drilling Program, Scientific Hart, M.B. 1980. A water depth model for the evolution of Results, 149, 203-216, College Station, TX (Ocean Drilling the planktonic Foraminiferida. Nature, 286, (5770), 252- Program), Washnigton (U.S. Goverment Printing Office). 254. Kuhnt, W. & Kaminski, M.A. 1989. Upper Cretaceous deep­ Herbin, J.P., Montadert, L., Mueller, C, Gomez, R, Thurow, J. water agglutinated benthic foraminiferal assemblages from the Western Mediterranean and adjacent areas. J. & Wiedmann, J. 1986. Organic-rich sedimentation at the In: Cenomanian-Turonian boundary in oceanic and costal Wiedmann (ed.), Cretaceous of the Western Tethys. basins in the North Atlantic and Tethys. In: e.P. Proceedings of 3rd International Cretaceous Symposium, pp. 93-120, Stuttgart (Schweizerbart). Summerhayes & N.J. Shakleton (eds), North Atlantic Palaeoceanography. Geological Society London Special Kuhnt, W. & Kaminski, M.A. 1990. Paleoecology of Late Publication, pp. 389-422. Cretaceous to Paleocene deep-water agglutinated Hemleben, e. & Troester, J. 1984. Campanian-Maestrichtian foraminifera from the North Atlantic and western Tethys. deep-water foraminifers from Hole 534A, Deep Sea In: e. Hemleben, M.A. Kaminski, W. Kuhnt & D.B. Scott Drilling Project. Ill: B. Biju-Duval, J.e. Moore et al. (eds), (eds), Paleoecology, Biostratigraphy, Paleoceanography and Initial Reports of Deep Sea Drilling Project, 78A, 509-532, Taxonomy of Aggilltinated Foraminifera, pp. 433-505, Washington (U.s. Goverment Printing Office). Dordrecht (Kluwer). Horwitz, L. 1938. Studia nad stratygrafiq oslony skalek Kuhnt, W. & Kaminski, M.A. 1997. Cenomanian to lower pieniriskich. Cz. 1 - Podzial oslony skalkowej i Eocene deep-water agglutinated Foraminifera from the rozmieszczenie jej ogniw. Sprawozdania Pa11stwowego Zumaya section, northern Spain. Annales Societatis Instytutu Geologicznego, 9, 177-205 (In Polish). Geologorum Poloniae, 67, (2-3), 257-270. Horwitz, L. 1963. Geology of the Pieniny Mts. Prace Kuhnt, W. & Moullade, M. 1991. Quantitative analysis of Illstytutu Geologiczrzego, 38, 1-152 (In Polish). Upper Cretaceous abyssal agglutinated foraminiferal dis­ tribution in the North Atlantic - paleoceanographic im­ Jednorowska, A. 1979. Microfauna and age of the plications. Revue de Micropaleontologie, 34, (4): 3l3-349. Malinowa Shale Formation, Upper Cretaceous, in the Pieniny Klippen Belt of Poland. Studia Geologica Polonica, Kuhnt, W., Kaminski, M.A. & Moullade, M. 1989a. Late 61, 37-76. Cretaceous deep-water agglutinated foraminiferal assem­ blages from the North Atlantic and its marginal seas. Jednorowska, A. 1980. Microfauna of the Maastrichtian Geologische Rlllldschau, 78, 1121-1140. and Paleocene deposits at Szaflary, Pieniny Klippen Belt, Carpathians. Stlldia Geologica Polan ira, 47, 23-44. Kuhnt, W., Morlotti, E., Winkler, W., & Kaminski, M.A. 1989b. Alpine Late Mesozoic and Early Cenozoic deep­ Jednorowska, A. 1981. Microfauna and age of the Upper water sequences and their agglutinated foraminifera. Cretaceous Sromowce Formations flysch in the type area, Third International Workshop on Agglutinated Pieniny Klippen Belt, Carpathians. Studia Geologica Foraminifera, Excursion Guidebook, Tiibingen 17-28 Polonica, 70, 37-50. Septem.ber 1989, 153 pp., NATO Advanced Study Kaminski, M.A., Gradstein, F.M., Berggren, W.A., Geroch, S. Institutes Program. & Beckmann, J.P. 1988. Flysch-type agglutinated foramini­ Kuhnt, W., Geroch, S., Kaminski, M.A., Moullade, M. & feral assemblages from Trinidad: taxonomy, stratigraphy Neagu, T. 1992. Upper Cretaceous abyssal claystones in and paleobathymetry. In: F. Rogl & F. Gradstein (eds), the North Atlantic and Western Tethys: current status of Proceedings of Second Workshop on Agglutinated biostratigraphical correlation using agglutinated Foraminifera Vienna 1986, Abhandlungen der foraminifers and palaeoceanographic events. Cretaceous Geologischen Bundesanstalt, 41,155-227. Research,13, 467-478. Kaminski, M.A., Gradstein, F.M, Goll, R. M. & Greig, D. Kuhnt, W., Kaminski, M.A. & Moullade, M. 1998. Upper 1990. Biostratigraphy and paleoecology of deep-water Cretaceous, KIT boundary, and Paleocene agglutinated agglutinated Foraminifera at ODP Site 643, Norwegian­ foraminifers from Hole 959D (Cote d'Ivoire-Ghana trans­ Greenland Sea. In: Ch. Hemleben et al. (eds), Paleoecology, form margin. In: J. Mascle, G.P. Lohmann & M. Moullade Biostratigraphy, Paleoceanography and Tllxonomy of (eds), Proceedings of the Ocean Drilling Program, Agglutinated Foraminifera. NATO ASI Series C, 327, pp. Scientific Results, 159, 389-411, College Station, TX 345-386, Kluwer Academic Publishers. (Oceanic Drilling Program). Kaminski, M.A., Kuhnt, W. & Radley, J. 1996. Paleocene­ Kuznetsova, K.I. 1974. Distribution of benthonic Eocene deep water agglutinated foraminifera from the foraminifera in Upper Jurassic and Lower Cretaceous at Numidian Flysch (Rif, Northern Morocco): their signifi­ Sites 261, DSDP Leg 27, in the eastern Indian Ocean. In: J.J. cance for the palaeoceanography of the Gibraltar Veevers, J.R Heirtzler et al. (eds), Initial Reports of the Gateway. Journal of Micropaleontology, 15,1-19. Deep Sea Drilling Project, 27, 673-68l. Kostka, A. 1993. The age and microfauna of the Maruszyna Lamolda, M.A. & Peryt, D. 1995. Benthonic foraminiferal Succession (Upper Cretaceous-Palaeogene), Pieniny response to the Cenomanian-Turonian boundary event in Klippen Belt, Carpathians, Poland. Studia Geologica the Ganuza section, northern Spain. Revista Espanola de Polonicll, 102, 7-l34. Paleontologia, No homenaje al Dr G. Colom, 101-118. Kuhnt, W. 1990. Agglutinated foraminifera of western Leckie, RM. 1987. Paleoecology of mid-Cretaceous plank­ Mediterranean Upper Cretaceous pelagic limestones tonic foraminifera: A comparison of open ocean and epi­ (Umbrian Apelmines, Italy, and Betic Cordillera, Southern continental sea assemblages. Micropaleontology, 33, (2), Spain). Micropaleontology, 36, (4), 297-330. 164-176. Biostratigraphy of DW AF in Scaglia-type deposits of the PKB, Poland 33

Liebus, A. & Schubert, R.J. 1902. Die Foraminiferen der Robaszynski, F., Caron, M., Gonzales Donoso, J.M. & karpatischen Inoceramen - mergelschichten von Gbellan in Wonders, A.A.H. 1984. Atlas of the Late Cretaceous Ungarn (Puchover Mergel). /ahrbuch der Geologischen globotruncanids. Revue de Microaleobiologie, 26, (3-4), Reichsanstalt,52, 285-310. 145-305. Morgiel, J. & Olszewska, B. 1981. Biostratigraphy of the Robaszynski, F., Caron, M., Amedro, F., Dupuis, c., Polish External Carpathians based on agglutinated Hardenbol, J., Gonzales Donoso, J.M. & Linares, D. 1993. foraminifera. Micropaleontology, 27, (1), 1-30. Le Cenomanien de la region de Kalaat Senan (Tunisie Morgiel, J. & Olszewska, B. 1982. Uniformity of the Tethyan Centrale): Litho-biostratigraphie et interpretation faunas from Cretaceous and Paleogene as shown by sequentielle. Revue de Paleobiologie, 12, (2),351-505. foraminifera from Morocco and Polish Flysch Scheibner, E. & Scheibnerova, V. 1958. Kysucke a sneznicke Carpathians. Cahiers de Micropaleontogie, 3, 45-53. vrstvy - nove cleny kriedy pieninskej serie v kysuckom Moullade, M., Kuhnt, W. & Thurow J. 1988. Agglutinated vyvine. Geologicky Sbornik, 9, (2), 178-181. benthic foraminifers from Upper Cretaceous variegated Sliter, W.V. 1975. Foraminiferal life and residue assem­ clays of the North Atlantic Ocean (DSDP Leg 93 and ODP blages from the Cretaceous slope deposits. Bulletin Leg 103). In: G. Boillot, E.L. Winterer et al. (eds), Geological of American Society, 86, 897-906. Proceedings of the Ocean Drilling Programm, Scientific Stur, D. 1860. Bericht tiber die geologische Ubersichts - Results, 103, 247-264, College Station, TX (Ocean Drilling Aufnahme d. Wassergebietes der Waag und Neutra. Program). /ahrbuch der Geologischen Reichsanstalt,11, 17-149. Neagu, T. 1990. Gerochammina n.g. and related genera from Tyszka, J. & Kaminski, M.A. 1995. Factors controlling the the Upper Cretaceous flysch-type benthic foraminiferal distribution of agglutinated foraminifera in Aalenian­ fauna, Eastern Carpathians - Romania. In: C. Hemleben, Bajocian dysoxic facies (Pieniny Klippen Belt, Poland). In: & M.A. Kaminski, W. Kuhnt, D.B. Scott (eds), M.A. Kaminski, S. Geroch & M.A. Gasinski (eds), Palaeoecology, Biostratigraphy, Paleoceanography and Proceedings of the Fourth International Workshop on taxonomy of Agglutinated Foraminifera, 245-256, Kluwer Agglutinated Foraminifera, Krakow Poland, September 12- Academic Publishers. 19,1993. Grzybowski Foundation SpeCial Publication, 3, Noth, R 1952. Plectorecurvoides, eine neue Foraminiferen­ 271-291. gattung. Verhandlzmgen der Geologischen Bundes{//zstalt, Volat, J.-L., Hugo, B. & Bignoumba-llogue, J. 1996. 3, 117-122. Foraminiferes arenaces du Cretace superieur du Gabon. Olszewska, B. 1997. Foraminiferal biostratigraphy of the Bulletin Centres Rech. Explor.-Prod. Elf Aquitaine, 20, Polish Outer Carpathians: a record of basin geohistory. 229-275. Annales Societatis Geologorum Poloniae, 67, (2-3), 325- Wightman, W.G. & Kuhnt, W. 1992. Biostratigraphy and pa­ 336. leoecology of Late Cretaceous abyssal agglutinated Robaszynski, F. & Caron, M. 1979. Atlas de Foraminifers foraminifers from the western Pacific Ocean (Deep Sea planctoniques du Cretace moyen (mer Boreale et Tethys). Drilling Project Holes 196A and 198A, and Ocean Cahiers Micropaleontologie, 1, 7-185 & 2, 9-181. Drilling Program Holes 800A and 801A). In: RL. Larson, Robaszynski, F. & Caron, M. 1995. Foraminiferes planc­ Y. Lancelot et a!. (eds), Proceedings of the Ocean Drilling toniques du Cretace: commentaire de la zonation Europe­ Program, Scientific Results, 129, 247-264, College Station, Mediterranee. Bulletin de la Societe geologique de France, TX (Ocean Drilling Program). 166, (6), 681-692.

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Plate 1. a. RhiwlIllllil1" illdivis(I Brady, Mac-44, x50. b. C(llldnllllllilln ovJt!a (Grzybowski), Or-5, x50. c. RI,iwlIIlI1illu sp., d-8, x60. d. Horlllosilla excelsn (Dylqzanka), Mac-38, x50. e. Honnosil1(/ exeelsa (Dylqianka), Mac-37, xSO. f. Honnosilln d. crnssn Geroch, SzG-l1, x75. g. Reoplwx I/ Odll!OSIIS Brady, SzG-6, x7S. h. $uc((I/IIl/Iillu grzybowskii (Schubert), Mac-61, xlOO. j. Sacc(llllminn grzybowskii (Schubert). Lor-1B. 75. j. $accallllllilla grzybowskii (Schubert), Mac-61, xl00. k. SncC(l1I1111illn plncen/a (Grzybowski), PG-20, x60. I. Ascllelllocelill gran dis (G(zybowski), Mac-42, x75. m. Aschemocelln gral1dis (Grzybowski), Mac-42, x75. n. Clo/llospim irregll/aris Grzybowski, Mac-37, x50. o. AllllllodisClis crc/acells (Reuss), Or-12, x50. p. A/!/lI/orlisClls ere/acells (Reu $), d-lO, x50. r. Ammodiscus sp., Bw-6, x50. s. Ammodisclls sp., Bw-5, x50. Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 35

Plate 2. a. Clolllospira cirnroides Oones & Parker), Bd-9, xl00. b . Clomospirn clznroides Oones & Parker), Nd- 11, x150. c. Clol/lospirn irregulnris (Grzybow ki), Mac-37, x75. d. Glomospirn irreglllnris (Grzybowski), SW-7, xlOO. e. Giolllospim irregulnris (Grzybowski), Bd-8, xl00. f. Glomospirn irregllinris (Grzybowski), Bd-8, x75. g. Buibobnwliles problemn/iells ( eagu), Bw-1 , xlOO. h. BlIlbobnwliles problell1nticus (Neagu), Bw-22, x7S. j.Spiropleetnmmilzn d. slIbJrnerillgellsis (Grzybowski), Mac-63, x75. k. Glolllospirn irregulnris (Grzybowski), Bd-S, x60 l. BlilbobnClllites problemnliClls (Neagu), Bw-24, x75. In. BufbobnclIliles pl"OblemnfiCIIs ( eaguL Kos-20, x75. 11. Spiroplectamminn p.; x75, 21-13, x7S. o. Dorolhia gradnta (Berthelin), CSk-ll, x75. p . Rewn,loides godlliellsis (Hanzlikova), Or-7, xSO r. ReClirvoides sp., Mac-66, x75. 36 Krzysztof Bqk

Plate 3. a.Spiropiectalllll/il1a carilln/a (d'Orbigny), CSk-ll, x7S. b. Spiropieclallllllilla llaVarrOalla Cu hman, Lor-6, x45. c. Spiroplectal1llllilla Ilnvarronrl!1 Cushman, Lor-6, x4S. d. Spiroplcctaml1lilla l1avnrroaJla Cu hman, Lor-6, x45. e. Texlllinria sp., Mac-9, x75. f. Verncllilil10ides p., CSk-18, x7S. g. Vel'llCllilinoides sp., CSk-18, x7S. h. Gerocilamminn cot/verSil (Grzybowski), Mac-33, xsO. i. Trilaxia ga llitilla (Morozova), CSk-ll , xsO. j. Karrerulilra coni/ormis (Grzybowski), Mac-14, x75. k. Gerocllnllllllina conversa (Grzybowski), Bw-18, x60. 1. Trilaxia gilliltinn (Morozova), CSk-ll, '50. m. Trilaxin galiltilln (Morozova), CSk-lO, xSO. n. Tri laxia gaultina (Morozova), Lor-3, x50. o. Tritnxin gal/ltina (Morozova), 21-13, xSO. p. Gal/dryillil pyramidala Cushman, Lor-5, x50. r. GaudnJina pyramidata Cushman, Lor-3, xIOO. s. Galldryilla pyramida ta Cushman, Lor-8, xIOO. t. Gal/dryilla pyramidata Cu hman, Lor-3, x75. u. Gal/dryilln pyramidala Cushman, Lor-8, x75. Biostratigraphy of DWAF in Scaglia-type depo its of the PKB, Poland 37

Plate 4. a. ReclIrvoides sp., Mac-72, x7S. b. Haplaphragmoides IIOlliollil1oides (Reuss), 21-19, x50. c. Haplophragmoides d. walteri (Grzybowski), Bd-6, xl00. d . Haplophragmoides d. kirki (Wickenden), Bw-S, xl00. e. Haplophragmoides llonionilloides (Reuss), PG-33, x7S. f. Haplophragmoides kirki (Wickenden), SW- 8, xl00. g. Haplophragmoides kirki (Wickenden), Kos-21, x7S. h. Haplophragmoides d. kirki (Wickenden), CSk-24, xl00. i. Haplaphragmoides kirk; (Wickenden), Mac-44, x7S. j. Haplophragmoides d. blil/oides (Beissel), d-l0, x75. k. Haplophragmoides cf. bul/aides (Beissel), SW-4, x7S. I. Haplaphragmoides d. bllllaides (Bei sel), d-9, xSO. m. Hnplopilraglllaides d. bill/aides (Beis el), Nd-6, xl00. n. Haplapilragmoides d. eggeri Cushman, Mac-42, x75. o. Haplophragmoides d. eggeri Cushman; x75, Mac-40, x75. p. Haplaphragmoides sp., Kos-9, x50. 38 Krzysztof Bqk

Plate 5. a. Ammosphaeroirlinn sp., 21-17, x50. b. Al!1/11osplzneroidilln sp., 2: 1-17, x75 . c. AlIllll()sp lweruidilljl sp., 21-17, x50. d. A1I1mosphneroidilln sp., 21-17, x75. e. Piectorecllrvoides niternnlls Nath, CSk-l0, x75. f. Trochnmminn sp., CSk-l0, x80. g. TroclwlIll1lil1a 1l1lliatensis Tappan, Mac-42, xl00. h. Plec.lorenlrvoides nlternans Noth, 21-13, x75. i. Piectoreclirvoides altemalls oth, CSk-ll, x75. j. lIvigerillnmmina jankoi Majzon, Nd-10, x75. k. Uvigerinamminn jnl1koi Majzon, Or-10, x75. I. Uvigerinnmlllina jankoi Majzon, Or-5, x50. m. Uvigerinammina jnl1koi Majzon, x50, Or-5, x50. n. Arel10UlIiilllilla sp., CSk-ll, x75. o. Dorotilia oxycona (Reuss), CSk-8, x75. p. Dorothia oxycona (Reuss), CSk-ll, xl00. r. Dorothin grndnta (Berthelin), CSk-l0, x40. s. Dorothin gradatn (Berthelin), 21-12, x50. t. Arenoul/limilln postcirapmnni Barnard & Banner, CSk-l0, x75. u. Arel1oimiil11ina postci1apl11nni Barnard & Banner, CSk-l0, x75. v. Arel10UII/imil1a preslii (Reuss), CSk-8, x60. w. Arenobu/il11illn preslii (Reuss), CSk-S, x75. Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 39

Appendix. Distribution of deep-water agglutinated foraminifers in the Scaglia Rossa-type facies in the Polish part of the Pieniny Klippen Belt; CTBE - Cenomanian/Turonian boundary event, LCE - Lower Campanian event.

Campanian­ w Age Cenomanian Turonian - Santonian g early MaBtricht. .!!?.. :Ii E Planktonic foraminiferal zones .r!! t, ~ .!,!e 12 13 14I 2 3 4 5 6 7 8 9 10 11 Nothia &p. p p p Bathysiphon &p. p p Dendrophrya maxima Dendrophrya robusta Rhabdammina cylindrica p Rhabdammina &p. p p c c p c c Rhizammina indivisa p p c Rhizammina sp. p p c c c p p c c Psammosphaera sp. 7 Saccammina grzybowskii p c c p Saccammina cf. placenta p p p p p p Saccammina sp. p p p Lituotuba lituifonnis p ? p Ammodiscus cretaceus p p p p Ammodiscus glabratus Ammodiscus tenuissimus p Ammodiscus &p. p p G/omospira charoides p p c c G/omospira difundens p G/omospira glomerata p G/omospira gorriialis p p p G/omospira irregularis p c c Glomospirella gauftina p p p Glomospirelfa gorayskii Labrospire pacifica p p Aschemocelfa carpathica p Aschemocelfa grandis p p p p Pseudonodosinella parvula p p c Reophax sp. p p c p p Hyperammina gauftina p p p Hyperammina sp. Honnosina excelsa p p Honnosina cf. velascoensis p p p Caudammina gigantea Caudammina ovulum p p p p Kalamopsis grzybowskii Nodelfum velfascoense p Rzehakina epigona p Haplophragmoides cf. bulfoides c c c c Haplophragmoides concavus 7 p Haplophragmoides ct. aggeri p p p p p Haplophragmoidas falcatosutura/is p Haplophragmoides kirki c c c c p Haplophragmoides cf. nonioninoides p Haplophragmoides cf. retroseptus p Haplophragmoides ct. waJteri p c c p p Haplophragmoides &p. A p p Haplophragmoides spp. p p c p Cribrostommoides trinitatensis Bulbobaculites Droblematicus ______r __ _r-c~r_~r_r~r_r~c~~c~~c~~c~r_~f_r~D~r_--r_----_+--_4 Recurvoides globulosus Recurvoides godulensis r c c c a Recurvoides primus p p p Rer;urvoides spp. r; r; p p p f r; r; f p p p p Pler;(orer;urvoides altemans c 40 Krzysztof Bqk

Appendix (continued):

1 2 I 3 4 5 6 7 8 9 10 11 12 13 14 Thalmanammina sp. r r p Spiropl8ctammina baudouniaria I p Spiroplectammina costata p p p p f Spiroplectammina dentata p p Spiroplectammina cretosa p p p r f Spiroplectammina jarvisi p I Spiroplectammina flexuosa I r Spiroplectammina lanceolata p p p f Spiroplectammina navarroana p p p p r c p p p p p Spiroplectammina praelonga p f p I j Spiroplectammina semicomplanata I r r Spiroplectammina spectabilis f f Spiroplectammina subhaerigensis p Spiroplectammina sp. p p p p p P f P P Trochammina cf. boehmi p p r Trochammina ct. globigeriformis p Trochammina cf. gyroidinaeformis f Trochammina cf. quadriloba p p Trochammina cf. quinqueloba p p 'fiOChammina ct. nodosa p Trochammina umiatensis p c f c f c r Trochammina vocontiana p Trochammina sp. f c r p p r r c c P Trochamminoides coronafus p p Trochamminoides elegans p Trochamminoides ct. grzybowski , p Trochamminoides irregularis p Trochamminoides ct. proteus p Trochamminoides spp. p f r r p Paratrochamminoides heteromorphus , p Paratrochamminoides spp. r r p Gerochammina conversa f c c c c Gerochammina tenuis p p p I KaJTBrulina coniformis f f c c c p Uvigerinammina praejankoi p p Uvigerinammina jankoi r c c c c p p Gaudryina carinata f r r Gaudryina cretacea f Gaudryina laevigata P Gaudryina cf. oblonga p Gaudryina cf. pyramidata p p r r p r p Gaudryina rugosa p Gaudryina sp. p p p Vemeuilina sp. p p r Vemeuilinoides polysfrophus p p r p p Textularia foeda p Textularia plummerae P Textularia sp. p p P ? Tn·taxia amorpha p p p P Tritaxia capitosa P c Tritaxia mitrata p r Tritaxia tricarinata p p r p p p f r Tritaxia trilatera f c Tritaxia gaultina p r p p p p r p p Tritaxia subparisiensis . p p p r p p f Arenobulimina postchapmani p p Arenobulimina preslii r p Arenobulimina sp. f P r P Ammosphaeroidina sp. f f P ? Goesella rugosa p p r c p Dorothia bulata r p Dorothia conula r Dorothia gradate p r p p p I Dorothia oxycona f f P P P r f f P P P Dorothia pupa p Dorothia refuse r Dorothia trochoides p f r Dorothia spp. p p p p p p