15

Biostratigraphy of deep-water agglutinated Foraminifera in Scaglia Rossa­type 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

C pper Cretaceous red marls and marly limestones often intercalated with thin-bedded greenish and bluish, calcareous mudstones and sandstones are known from the Alps, Appenines and Penibetic Zone as "Couches Rouge", "Scaglia Rossa" and "Capas Rojas" facies. These sediments have a wide geo­graphic distribution in the Tethyan realm, charac­terizing pelagic deposition in the bathyal zones above and/or near the CCO (calcite compensation depth). The high content of calcium carbonate was conducive to the preservation of planktonic foraminifers and nannoplankton, which are used for biostratigraphic zonation of these facies. Deep­water agglutinated foraminifers (OWAF) are the fossil group occuring in these sediments in large numbers and in well diversified assemblages. The (:o-occurrence of different groups of microfauna provides an opportunity to calibrate the strati­graphic ranges of agglutinated taxa with planktonic foraminifers, and to propose biostratigraphic schemes that are calibrated more accurately with the standard chronostratigraphy.

Thus far there have been few contributions pre­senting the calibration of OW AF with chrono­stratigraphy (Kaminski et ai., 1988; Kuhnt, 1990). Kaminski et al. (1988) presented the stratigraphic ranges of Campanian-Maastrichtian agglutinated foraminifers from the Trinidad area (the Caribbean Plate). Kuhnt (1990) calibrated the ranges of Turonian to Maastrichtian OWAF, using material from sections at Gubbio (Umbrian Apeninnes, Italy) and Hacho de Mantejaque (Betic Cordillera, Southern Spain), representing the southern and the westernmost part of the Western Tethys.

Similar to the latter sections, red pelagic sedi­ments occur in the Pieniny Klippen Belt (the Carpathians), representing facies deposited in a part of the Penninic Ocean - the northern part of the Western Tethys (Fourcade et aI., 1993). These facies are called the "Puchov beds" in the Ukrainian Carpathians (Glusko & Kruglov, 1971) or the "Kysuca beds" in the Slovak part of the Pieniny Klippen Belt (Scheibner & Scheibnerova, 1958). In the Polish part of the Pieniny Klippen Belt, they have been distinguished as two formal lithostrati­graphic units, the Pustelnia Marl Member and the Macelowa Marl Member (within the Jaworki Formation; Birkenmajer, 1977). Studies of the planktonic foraminiferal, nannoplankton, and radiolarian assemblages from this area (e.g., Alexandrowicz, 1966; Alexandrowicz et aI., 1968a,b; J ednorowska, 1979; Bir kenmajer & J ednorowska, 1983a,b, 1984; Bqk, 1994, 1995b; Dudziak, 1985; M. Bqk, 1995, 1996a,b) have provided evidence for continuous sedimentation in the Pieniny Klippen Basin from the early Cenomanian through the late Campanian.

Red calcareous facies are the most widespread Upper Cretaceous sediments in the Pieniny Klippen Belt. The present author has carried out the detailed biostratigraphic studies of these facies, based on planktonic foraminifers (Bqk, 1998). Because of the abundance of OW AF in the studied material, a precise calibration of their stratigraphic ranges was possible.

The present studies comprise, additionally, an analysis of agglutinated assemblages (Alexandrowicz & Birkenmajer, 1978; Jednorowska, 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

1993) from the Campanian-Maastrichtian pelagic facies (partly red in colour), occurring in the Maruszyna Scale (a tectonic unit incorporated into the Pieniny Klippen Belt). These combined data enable a comparison between a zonation based on agglutinated foraminifers (presented here) with other zonations developed earlier in the neigh­bouring flysch areas (Geroch & Nowak, 1984; Olszewska, 1997) and from similar environments in other parts of the Western Tethys. This study is a continuation of earlier research presented during the 4th International Workshop on Agglutinated Foraminifera in Krak6w (Bqk et al., 1995).

Outline of previous studies The first description of Upper Cretaceous red marls came from research by Stur (1860) who distinguished among others the "Puchov beds". Liebus & Schubert (1902) described foraminifera from these deposits ("Gbelan inoceramid marls").

A new stage of research on the Upper Cretaceous deposits in the Pieniny Klippen Belt (PKB) was started by Horwitz (e.g., 1938, 1963) and Andrusov (e.g., 1945). However, most of their biostratigraphi­cal analysis was determined basing on macrofauna and larger foraminifera.

The next stage of research is connected with pub­lications by Birkenmajer (1954, 1958), who dated the red Cretaceous deposits as Cenomanian-Turonian ("Globotruncana marls"), Maastrichtian ("Puchov marls") and Palaeocene ("the variegated beds"). Later micropalaeontological studies based on foraminifers (Birkenmajer & Geroch, 1961) enabled age determination of the red facies in the Magura Succession as Cenomanian-Campanian. Successive publications more precisely described the stratigraphy of the red deposits from the Czorsztyn Succession (Alexandrowicz et al., 1962) as Turonian to late Campanian.

A milestone in the investigation of the Upper Cretaceous stratigraphy was the publication by Alexandrowicz (1966). Foraminiferal and lithologi­cal studies were used for the correlation of these deposits with the surrounding areas (Alexandrowicz et al., 1968a, 1968b).

A significant advance in the stratigraphy of the Pieniny Klippen Belt was the publication by Birkenmajer (1977), which introduced a lithostratigraphic classification for that area. From that time, subsequent research was aimed at the document ion of the full micropalaeontological and lithological characteristics of particular lithostratigraphic units of the Upper Cretaceous. Foraminiferal analysis by Jednorowska (1979; 1981), and Birkenmajer & Jednorowska (1983a,b; 1984) in the different sections enabled a partial revision of the age of red deposits in the PKB. The consecutive phase, encompassing micropalaeontological studies, has resulted in a new subdivision of the Upper Cretaceous by Birkenmajer & Jednorowska (1987). These authors established this subdivision based on

Krzysztof Bqk

the planktonic foraminiferal biozonation, using papers by Robaszynski & Caron (1979) and by Robaszynski et al. (1984).

Another kind of a synthesis was the presentation of stages of development of the Pieniny Klippen Belt (Birkenmajer, 1986). According to Birkenmajer, sedimentation of the Macelowa Marl Member took place during the stage of initial compression, when deposition took place on an abyssal platform. Pelagic deposition was periodically interrupted by turbidity currents, cutting canyons, with their deposits forming submarine fans. At the northern (Czorsztyn) ridge the sedimentation of pelagic Globotruncana marls took place.

Because of recent advances in the biostrati­graphical scheme for the Western Tethys, new information on the planktic foraminiferal ranges (Caron, 1985, Robaszynski et al., 1993, Gale et al., 1996; Robaszynski & Caron, 1995), and new studied sections (Bqk, 1995b; 1998), it appeared that a fresh look at the biostratigraphy of the Upper Cretaceous of the Pieniny Klippen Belt was needed.

GEOLOGICAL SEITING The Pieniny Klippen Belt of Poland is part of a long (approximately 600 km) and very narrow (maximum 20 km wide) structural unit, separating the Inner Carpathians from the Flysch Outer Carpathians (Figure 1A). During the Mesozoic, the PKB occupied a separate basin within the northern part of the Western Tethys. In its present form, the PKB consists of Klippen successions, and incorporated into the zone are elements of the Outer and Inner Carpathians (e.g., the Maruszyna Scale; Birkenmajer, 1986). Detailed studies of tectonic structures, litho- and biostratigraphy in that area, allowed Birkenmajer to reconstruct several parallel facies zones, distinguished as successions. These are: the Czorsztyn Succession corresponding to the north­ern intra-oceanic ridge and its southern slope; the Czertezik and the Niedzica Successions consisting of deposits sedimented on the slope of the basin; the Branisko and the Pieniny Successions corresponding to the central furrow; the Haligovce Succession and the Exotic (Andrusov) Ridge formed the southern slope and ridge. Palaeotectonic position of Maruszyna Succession was, according to Birkenmajer (1986), to the south of the Exotic (Andrusov) Ridge and to the north of the Central Carpathian Manin Basin and its My java cover. The sediments of this unit may have formed on a submerged ridge in a back-arc basin position with respect to the Pieniny Klippen Belt arc.

In this study, I examine the red Upper Cretaceous deposits that accumulated on the northern (Czorsztyn) ridge (the Pustelnia Marl Member; the Czorsztyn Succession), on the northern slope of the basin (the Macelowa Marl Member; the Czorsztyn, the Czertezik and the Niedzica Successions), and in the central furrow (the Macelowa Marl Member; the

Biostratigraphy of OW AF in Scaglia type deposits of the PKB, Poland 17

FORELAND

• BratlalaV8

• Sz 1

FOREDEEP

INNER CARPATHIANS

50km

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.... : ..... ":. ":.:":: : .. :.::: : .. .:.:.: " .. "

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 used the biostratigraphic data from the light green and variegated pelagic facies of the Maruszyna Scale presented by Alexandrowicz & Birkenmajer (1978), Jednorowska (1980), Birkenmajer & Jednorowska (1983b), and Kostka (1993).

Pustelnia Marl Member The Pustelnia Marl Member (Birkenmajer, 1977) is represented by brick red marls devoid of clastic intercalations. Calcium carbonate content is high, varying from 60 to 85%. The Lorencowe Chert Bed (Birkenmajer, 1977) occurs within the upper part of the Pustelnia Marl Member, corresponding to the Lower Campanian Oceanic Event (LCE). This unit consists of very thin (1-4 cm) limestone layers and strongly calcareous marls, light green, partly red­dish in colour, and less than 3 m thick. Large marginotruncanids are visible on weathered surfaces of the limestone layers. The CaC03 content ranges from 72 to 95%.

Macelowa Marl Member The Macelowa Marl Member (Birkenmajer, 1977) is represented by cherry red marls and calcareous mudstones intercalated by fine-bedded grey to grey­ish blue calcareous mudstones and sandstones.

The red marls (CaC03 contents from 16 to 75%) predominate in this unit, occurring in very thin layers; their mean thickness is about 3 cm. In the stratigraphically lower part of the unit, medium-

bedded marls occur. Horizontal or wavy lamination is often observed. Disintegrated Inoceramus shells, built of prismatic calcite crystals form thin (1-5 mm) intercalations. Thicker marls are often strongly bioturbated.

Greyish red, usually structureless, calcareous mudstones (rarely marly limestones) make up the second lithotype of the Macelowa Marl Member. Layers less than 8 cm and more than 14 cm thick predominate. These rocks are frequent in the lower part of this member.

Grey to bluish sandy mudstones and sandstones occur frequently in the upper part of the Macelowa Marl Member. Most layers are about 1-3 cm thick. The majority of mudstone layers show bioturbation. Horizontal and cross lamination is very rarely observed. Randomly distributed prismatic calcite fragments of Inoceramus shells occur as laminae 1-3 cm thick in some sandy mudstones.

Pelagic facies of the Maruszyna Succession Sedimentary sequences described at two localities (Bialy Dunajec River at Szaflary, and Skrzypny Stream at Maruszyna) represent continous Campanian to Middle Eocene pelagic successions (with the exception of the uppermost Maastrichtian and Lower Palaeocene). The Cretaceous part of the profile consists of hard, light marly limestones followed by soft variegated marls (Alexandrowicz & Birkenmajer, 1978). In the middle part of this sequence, several layers of 4-50 cm thick, grey-green

18

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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- "Nie­dziczanka 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, passing into laminated mudstones are observed. Fine sedimentary breccia with fragments of green-grey marls, quartz grains, and Inoceramus shells occurs at the bases of some layers (Kostka, 1993).

MATERIAL AND METHODS Sixteen sections located near Jaworki, Szczawnica, Niedzica, Sromowce, Dursztyn, Krempachy, and Szaflary were examined (Figure 1 B, Table 1). Samples were collected every 0.5-1.5 m depending on the state of the exposure and taking into account lithological variations.

Two hundred fifty samples were micropalaeonto­logically examined. The samples (about 0.75 kg) were crushed into pieces 1-5 cm in diameter, then boiled in glauber salt. Samples taken from hard, strongly calcareous marls and marly limestones were dried for 24 hours at 105°C, then dissolved in acetic acid (80%) for 6-8 hours at 75°C, and subsequently washed through a 63 /lm screen and dried. The C H 3COOH residues consist, in all cases, of planktonic and benthic foraminifers of good preservation. Foraminifers (more than 300 specimens if available) from the >63 /lm fraction were picked and mounted onto cardboard microscope slides.

The material is housed in the Institute of Geography, Cracow Pedagogical University. Scanning electron microscope photomicrographs were prepared at the Electronic Microscopy Lab­oratory of the Department of Zoology, Jagiellonian University.

AGE OF THE SCAGLIA ROSSA-TYPE FACIES IN THE PIENINY KLIPPEN BELT Based on the examination of 16 sections of the Pustelnia Marl Member and the Macelowa Marl Member, as well as taking into account results of ear­lier microfaunal studies of these members (partly revised by the present author), documented in 20 sections and outcrops (mainly by Alexandrowicz, 1966, 1975; Birkenmajer & Jednorowska, 1976, 1983a, 1983b, 1984; Jednorowska, 1979), a local planktonic foraminiferal biostratigraphy has been determined for the Pieniny Klippen Belt in Poland (Bqk, 1998). The calibration of these foraminiferal zones with the chronostratigraphy is presented following Robaszynski & Caron (1995).

The Pustelnia Marl Member represents the Rotalipora reieheli (Middle Cenomanian) through Globotruneanella havanensis (Campanian) Zones (Figs. 2, 3). The Macelowa Marl Member (Figs. 2, 3) represents the Rotalipora globotruneanoides (Early Cenomanian) through Oiearinella asymetriea (Santonian) Zones in the Czorsztyn Succession; the Praeglobotruneana delrioensis (latest Cenomanian­earliest Turonian) through Oiearinella eoneavata (latest Turonian-early Santonian) Zones in the Czertezik Succession; the Helvetoglobotruneana helvetica (early-middle Turonian) through Oiearinella eoneavata (latest Turonian/early

Santonian) Zones in the Niedzica Succession; the Marginotruneana sigali (middle Turonian) through Oieari nella eoneavata (latest Turonian/ early Santonian) Zones in the Branisko Succession; the Praeglobotruneana delrioensis (latest Cenomanian­earliest Turonian) through Globotruneanita elevata (early Campanian) Zones in the Pieniny Succession.

According to Kostka (1993), the pelagic deposits of the Maruszyna Scale represent the Globotruneana area Interval Zone and Abathomphalus mayaro­ensis Taxon Range Zone in their Cretaceous part. Comparison of foraminiferal biostratigraphy and calcareous nannoplankton stratigraphy from the same deposits (Dudziak, 1980, 1990, 1993) document the lower boundary of this pelagic sediementation within the NC19/NC20 nannoplankton Zone, corre­sponding simultaneously to the Globotrunea ventrieosa Zone (middle Campanian).

AGGLUTINATED FORAMINIFERAL ZONES A local biostratigraphical zonation based on agglu­tinated foraminifera, is proposed here for the Upper Cretaceous deposits in the Polish part of the Pieniny Klippen Belt. It takes into account the earlier standard scheme for the Carpathians (Geroch & Nowak, 1984). The definition of foraminiferal zones is based on vertical ranges of index taxa (Figure 4). The zones are interval zones: between the first appearances of index taxa. A complete list of foraminifera with details about microfaunal assem­blages and stratigraphy of the studied deposits is included in the paper by Bqk (1998).

Pleetoreeurvoides altemans Interval Zone Definition: Lower boundary - first appearance datum (FAD) of Pleetoreeurvoides alternans Noth; the boundary has not been identified in the sections examined; upper boundary - FAD of Bulbobaeulites problematieus (Neagu). Identical to the P. alternmls Zone of Geroch & Nowak (1984). Occurrence: The zone has been recognised in the Pustelnia Marl Member and the Macelowa Marl Member (both members in the Czorsztyn Succession). Agglutinated Foraminifera: The lowest part of this zone in the Macelowa Marl Member (Zlobowy Creek section) is characterised by the dominance of benthic foraminifers. Agglutinated forms prevail, com­prising even up to 80% of the assemblage. The index taxon dominates together with Recurvoides spp., siliceous ammodiscids (A. eretaeeus) and glomo­spirids (G. eharoides (Jones & Parker), G. gordialis (Jones & Parker) and G. irregularis (Grzybowski». These species are accompanied by Troehammina spp., Haplophragmoides spp., Arenobulimina sp. and Oorothia oxyeona (Reuss). Moreover, forms identical to Saeeammina d. placenta (Grzybowski), Spiroplectammina navarroana Cushman, and Tritaxia gaultina (Moroz ova) also occur. This assemblage characterises deposits of the Rotalipora globotruncanoides Zone (Lower Cenomanian).

20 Krzysztof Bqk

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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 of the zone represents the older part of the Rotalipora reicheli Zone (Middle Cenomanian). The benthic foraminifera make up less than 20% of the microfaunal assemblage. Agglutinated forms prevail among them, represented by only single specimens of several taxa. Age: This zone corresponds to the Rotalipora globotruncanoides Zone in the Scaglia Rossa-type facies (Bqk, 1998); Early Cenomanian. Its lower boundary was determined as lying within the Biticinella breggiensis Zone, late Albian (Bqk et al., 1995).

Bulbobaculites problematicus Interval Zone Definition: Lower boundary - FAD of Bulbobaculites problematicus (Neagu); upper boundary - FAD of Uvigerinammina jankoi Majzon. Identical to the B. problematicus Zone of Geroch & Nowak (1984).

Occurrence: The zone has been recognised in the Pustelnia Marl Member and the Macelowa Marl Member (both members in the Czorsztyn Succession). Agglutinated Foraminifera: The deposits occupied the Czorsztyn Ridge (Pustelnia Marl Member) in outer shelf conditions (Bqk, 1995b) are characterised by a high content of planktic foraminifers in the microfaunal assemblage (nearly 100%). Aggluti­nated foraminifers represent a subordinate compo­nent, and include: Arenobulimina preslii (Reuss), Tritaxia gaultina (Morozova), T. subparisiensis (Grzybowski), Gaudryina carinata (Franke), Dorothia gradata (Berthelin), D. oxycona (Reuss), Textularia foeda (Reuss), Trochammina spp., Plectorecurvoides alternans Noth, Spiroplec­tammina tricarinata (d'Orbigny), S. cretosa, Ammodiscus cretaceus (Reuss), and Rhizammina sp. The index taxon appears as single specimens.

Biostratigraphy of DW AF in Scaglia-type deposits of the PKB, Poland 21

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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 mudstones and fine-grained thin-bedded sandstones (Macelowa Marl Member) are characterised by a different microfauna. These facies represent the edge of the Czorsztyn Ridge in outer shelf to upper bathyal conditions (Bqk, 1995b). The benthic foraminiferal fauna comprises 55-80% of the total assemblage, with dominating agglutinated forms. Besides the index taxon, the most frequent foraminifers belong to the genera Plectorecurvoides, ReCllrvoides, Trochammina, Spiroplectammina, Arenobulimina, Dorothia, Tritaxia, Saccammina, Glomospira, and Rlzizammina. Very characteristic is the high content of diverse glomospirids and ammodiscids. Kuhnt & Kaminski (1989) described increased ammodiscids in the lower Campanian of the North Atlantic, and termed this assemblage "Biofacies B". According to these authors, it reflects poorly oxygenated conditions at the sea floor. The most characteristic "Glomospira Event" was noted

from Lower-Middle Eocene of several locations in the Carpathians, Alps, and the North Atlantic (e.g., Kaminski et ai., 1990; Bqk et ai., 1997). The abundance of ammodiscids (up to 50%) accompanied with a lack of plankton and rare occurence of calcareous benthos was also noted from the Lower Cretaceous in the eastern Indian Ocean (Kuznetsova, 1974), where it was interpreted as indicating deposition below the lysocline. The Glomospira biofacies are interpreted here as deposition in low productivity and highly oxygenated conditions on the sea floor with a low sedimentation rate.

During the youngest part of the Rotalipora cushmani Zone, the red facies are replaced by anoxic deposits (black, dark-grey marly shales and siliceous shales; the Altana Shale Bed and the Magierowa Member; Birkenmajer, 1977; Birkenmajer & Jednorowska, 1984). They contain mainly pyri­tised radiolaria and numerous pyritised ostracods, the significant benthic foraminifer Lenticulina

22

gaultina (Berthelin), and plankton represented by single specimens of Praeglobotruncana delrioensis (PI ummer), and GlobigerineIloides uitramicra (Subbotina). Also occurring are single specimens of agglutinated forms belonging to the genera Nothia, Rhabdammina, Rhizammina, Saccammina, Glomo­spira, Glomospirella, Hormosina, Bulbobaculites, Trochammina, and Tritaxia. These anoxic deposits represent the local expression of the Cenomanian/ Turonian Boundary Event (CTBE) in the Pieniny Klippen Belt. Age: This zone corresponds to the Rotalipora reicheli (Middle Cenomanian) through older part of the Praeglobotruncana delrioensis zones (Cenoma­nian/Turonian boundary; Bqk, 1998).

Uvigerinam11lina ex gr. jankoi Interval Zone Definition: Lower boundary - FAD of Uvigerinam­mina ex gr. jankoi Majzon; upper boundary - FAD of GoeseI/a rugosa (Hanzlikova). Identical to the U. jankoi Zone of Geroch & Nowak (1984). Occurrence: The zone has been recognised in all Klippen successions of the Pustelnia Marl Member and the Macelowa Marl Member. Agglutinated Foraminifera: There is a significant change in the microfaunal assemblage in comparison to the older zone. Some agglutinated taxa disap­peared during the CTBE (Figure 4). They include Haplophragmoides nonioninoides (Reuss), H. concavus (Cha pm an), H. falcatosutllralis N eagu, Plectorecurvoides alternans N oth, Arenobulimina preslii (Reuss), Textularia foeda (Reuss). Several other taxa appeared for the first time during the Zone, being represented by Uvigerinammina praejankoi Neagu, Hormosina excelsa (Dylqianka), Haploplzragmoides d. buI/oides (Beissel), H. eggeri Cushman, H. kirki (Wickenden), H. d. walteri (Grzybowski), Recurvoides godulensis Hanzlikova, Trochammina umiatensis Tappan, Karrerulina conifonnis (Grzybowski), Gerochammina conversa (Grzybowski), G. tenuis (Grzybowski), Verneuilin­oides polystroplzus (Reuss), and Gaudryina pyramidata Cushman.

The deposits from the Czorsztyn Ridge (Pustelnia Marl Member) are characterised by a high content of planktonic foraminifera (50-100%). However, in several samples, benthic foraminifera prevail. The benthos is very diverise. The content of agglutinated foraminifera varies from about 20% to 95% of the benthic assemblage (mean 60%).

Agglutinated foraminifers dominate the micro­faunal assemblages of the Macelowa Marl Member within all Klippen successions (besides the Czorsztyn Succession). Planktonic forms are more frequent only in single samples. These deposits cor­respond to lower-upper bathyal conditions (Bqk, 1995a,b).

Agglutinated taxa are dominated by Recurvoides spp., Haplophragmoides d. bulloides ~Beissel),

Blllbobaculites problematicus Neagu, Geroclzam­mina conversa (Grzybowski), Karrerulina coniformis

Krzysztof Bqk

(Grzybowski), Trochammil1a umiatensis Tappan, Uvigerinammina jankoi Majzon, H. d. walteri (Grzybowski), H. d. kirki Wickenden, Glomospira irregularis (Grzybowski), and Rhizammina sp. Less frequent are: Spiroplectammina navarroana Cushman, S. praelollga (Reuss), Gaudryina pyrami­data Cushman, Ammodiscus cretaceus (Reuss), Glomospira gordialis (Jones & Parker), Hormosina excelsa (Dylqzanka), Dorotlzia oxycona (Reuss), Recurvoides primus Mjatliuk, Saccammina grzybow­skii (Schubert), and S. placenta (Grzybowski).

The following species have been observed as single specimens: Hormosina velascoensis (Cushman), Caudammina oVllla (Grzybowski), Ammodiscus tenuissi1l1us Grzybowski, Glomospira difundens Cushman & Renz, Pseudonodosinella parvula (Huss), Aschemocella carpathica (Neagu), A. grandis (Grzybowski), Haplophragmoides d. eggeri Cushman, H. d. retroseptlls (Grzybowski), Trochammina vocontiana Moullade, Paratrocham­milloides d. heteromorphus (Grzybowski), Tro­chamminoides d. grzybowskii Kaminski & Geroch, T. d. proteus (Karrer), T. coronatlls (Brady), T. elegans Pokorny, Trochammilla d. boehmi Franke, T. d. nodosa, T. gyroidinaeformis Krasheninnikov, Gerochamina len is (Grzybowski), Verneuilinoides polystrophlls (Reuss), Spiroplectammina lanceolata, S. costata (Huss), and S. tricarinata (d'Orbigny).

The content of tubular forms, with prevailing Rhizammina sp., less frequent Rhabdammina, and sporadic Nothia and Bathysiphon varies between 10-40% (in extreme cases to 65%). These aggluti­nated assemblages are very similar in all Klippen successions of the PKB. Age: The lower boundary of the zone is diachronous, recorded by the top of CTBE anoxic facies (Figure 5). It represents the younger part of the Praeglobo­tnmcana delrioensis Zone (Early Turonian) within the slope facies of the Niedzica and the Czertezik successions; and the older part of the Margillo­truncana sigali Zone (middle part of Middle Turonian) within the Czorsztyn Ridge and the central furrow red facies. The upper boundary of this Zone corresponds to the Late Santonian Dicarinella asymetrica Zone (Bqk, 1998).

Goessella rugosa Interval Zone Definition: Lower boundary - FAD of Goessel/a rugosa (Hanzlikova); upper boundary - not defined becouse of tectonic contact. Occurrence: The zone has been recognised in the Macelowa Marl Member (Pieniny Succession) and pelagic deposits of the Maruszyna Scale. Agglutinated Foraminifera: The assemblage of agglutinated foraminifers in the lower part of the Zone, is similar to the U. jankoi Zone. The prevail­ing forms include Haplophragmoides d. bllIloides (Beissel), H. kirki (Wickenden), Recurvoides spp., Bulbobaculites problematicus Neagu, Trochammi na spp., Gerochammina conversa (Grzybowski), Karrer-

Biostratigraphy of DWAF in Scaglia-type deposits of the PKB, Poland 23

ulina coniformis (Grzybowski), and Uvigerinammina jankoi Majzon.

Lower Campanian deposits contain a lower diversity and significantly less abundant DW AF assemblage. Its characteristic feature is a presence of Caudammina gigantea (Geroch). The first appearance of the index taxon was described by Alexandrowicz (1975) within the Pustelnia Marl Member, as a component of "assemblage with Globo­truncana fornicata". This assemblage consists pre­dominantly of planktonic foraminifers (78-86%) with rare agglutinated taxa (Arenoblllimilla sp., Gaudryina sp., Dorothia sp.). It may be correlated with the Lower Campanian Event, characterised by very sparse benthic assemblages (e.g., Kuhnt et al., 1992).

The species Coudam11lina gigantea, used as an index taxon in most published zonations of Campanian-Maastrichtian (e.g., Geroch & Nowak, 1984; Moullade et al., 1988; Kuhnt et al., 1992), occurs only within the Globotruncanita elevata­Globotruncana ventricosa Zones in the PKB (Figure 4).

The middle/late Campanian (from Globotrun­canita calcarata Zone) through late Maastrichtian (Abathomphailis mayaroensis Zone) DWAF assemblages are characterised by a high abundance of tubular foraminifers and the frequent occurrence of ammodiscids and Caudammina ovula (Alexandro­wicz & Birkenmajer, 1978; Jednorowska, 1980; Birkenmajer & Jednorowska, 1983b; Kostka, 1993). Specimens belonging to the genera Spiroplectam­mina, Tritaxia and Dorothia occur as single taxa.

The species Rzehakina epigona has its FO datum within the Globotnmcnnita calcarata Zone (Kostka, 1993). This species becomes more abundant in the late Palaeocene wihin the variegated non­calcareous shales of the Maruszyna Scale, being distinguished as the index taxon for the Rzehakina epigona assemblage Local Zone (Kostka, 1993). Age: This zone represents the youngest part of the Dicarinella asymetrica Zone (late Santonian) through the Abath011lphalus 11layaroensis Zone (late Maastrichtian).

Uvigerinammina jankoi-Caudammina gigantea Concurrent Range Zone Definition: Lower boundary - FAD of Caudam11lina gigantea (Geroch); upper boundary - LAD of Uvigerinammina jankoi Majzon. Occurrence: The zone has been recognised in the Macelowa Marl Member (Pieniny Succession). It is proposed here as an additional zone within Scaglia Rosa-type deposits. Agglutinated Foraminifera: The DWAF are repre­sented by a more diversified assemblage than in the lower part of Giobotrullcanita elevato Zone. However, the taxonomic composition of aggluti­nated foraminifers is different from the Turonian­Santonian sediments. The assemblage representing

this Zone was described by Birkenmajer & Jednorow­ska (1984) from the Dzial pass section. In that sec­tion, the FAD of C. gigantea has been noted ("sample 185"; op. cit.). The microfaunal assemblage from these deposits consists of numerous tubular forms of Bathysiphon div. sp., Dendrophrya robllsta (Grzybowski) and ammodiscids. Moreover, there are: Caudammina ovula (Grzybowski), Haplaphragmoides excavatus Cushman & Weters, H. horridlls (Grzybowski), Cribrostomoides trini­tatensis Cushman & Jarvis, Thalmannammina sub­turbina Pokorny, Spiroplectammina boudouniana (d'Orbigny), 5. jarvisi Cushman, Gaudryina tricari­nata Franke, Galldryina laevigata (Franke), Goesella rugosa (Hanzlfkovii), Tritaxia amorpha (Cushman), T. subparisiensis (Grzybowski), T. capi­tosa Cushman, Dorothia crassa (Cushman), D. trochoides (Mars son), Uvigerinammina jankoi Majzon, and Gerochmnina lenis (Grzybowski).

A significant change in the DW AF assemblage is recorded in this zone by the lack of numerous Turonian-Santonian species (Figure 4), such as Recur­voides godlliensis, Troc/zammina umiatensis, Haplo­phragmoides cf. blllloides, H. kirki, Gerochalllmilla con versa and Karrerulina coniformis. Age: This zone represents the youngest part of the Globotruncanita elevata Zone through the older part of the Globotruncana ventricosa Zone (early Campanian).

DISCUSSION ON BIOSTRATIGRAPHY The development of a reliable biostratigraphic scheme is connected with the availability of conti­nous, stratigraphically well-calibrated sections. In strongly tectoni sed areas, such as the Pieniny Klippen Belt, a biostratigraphic zonation is neces­sarily based on composite sections. The data from the studied area come from 38 sections, comprising the Scaglia Rossa-type deposits of early Cenomanian through late Maastrichtian age. The large number of sections and the occurrence of planktonic foraminifers in these depOSits, which verify the continous sedimentation, constitute a very good databse for biostratigraphical study.

Zonal schemes based on agglutinated foramin­ifers have significant stratigraphical value in predominantly non-calcareous deep marine sediments. Biozonations based on this group of microfauna have been proposed by various authors, during the last 15 years. The most useful of them and one of the first, simultaneously, was the zonal scheme by Geroch & Nowak (1984), prepared from the deep-water flysch deposits of the Outer Carpathians. This zonation has been tested and modified in different areas including the North Atlantic (Moullade et al., 1988; Kuhnt et az', 1989; Kuhnt & Collins, 1996; Kuhnt & Kaminski, 1997), the South Atlantic (Volat et az', 1996), the equatorial Atlantic (Kuhnt et az', 1998), the Western Pacific (Wightman & Kuhnt, 1992), and

24

the other areas of the Western Tethys (Kuhnt & Kaminski, 1989; Kuhnt, 1990; Bubfk, 1995; Kaminski et aI., 1996; Olszewska, 1997).

The stratigraphical value of the zonal schemes, based on agglutinated foraminifers is estimated from sections, where these forms co-occur with cal­careous microfossils. Only in small numbers of sec­tions, investigated up to present day, this possibil­ity exists. The calibration of Upper Cretaceous DWAF ranges with chronostratigraphy (ranging in age from Turonian), has been proposed by Kuhnt (1990) in the Gubbio sections (Umbrian Apennines, Italy) and the Hacho de Montejaque section (Penibetic Zone, southern Spain). The deposits from these sections are very comparable with the Pieniny Klippen Belt in relation to the lithological features and sedimentary conditions. The Zumaya section (North Iberian continental margin) studied by Kuhnt & Kaminski (1997) is another complete sec­tion, were an analysis of samples enabled the cal­ibration of the biostratigraphic ranges of the DWAF.

The application of a zonal scheme based on agglutinated taxa depends on its calibration with chronostratigraphy, on the one hand, and is related to lithology and palaeogeographical setting, on the other hand. The palaeogeographic setting of the DW AF assemblages, their occurrence within certain types of lithologies and their taxonomic composition allowed the differentiation of six different foraminiferal biofacies in the Upper Cretaceous (Kuhnt et aI., 1989). Foraminifers from sections investigated in the western Mediterranean, the Penibetic Zone, and the North Iberian areas represent "Scaglia-type" deep-water assemblages. Their main feature is a high diversification of agglutinated foraminifers with large numbers of rhizamminids and tiny, finely agglutinating species. These DW AF assemblages occurring in the "Scaglia Rossa" and grey limestone facies, indicate slope sedimentation with only rare, fine-grained detrital inputs (Kuhnt, 1990).

Environmental characteristics of the Scaglia Rossa facies in the Pieniny Klippen Belt A detailed analysis of the early Cenomanian through late Campanian palaeoenvironment of the Scaglia Rossa-type deposits in the PKB was pre­sented by the author in his PhD Thesis (Bqk, 1995b). The results of this were based on the lithological features, analysis of trace fossil assemblages, morphogroup diversity (calcareous and aggluti­nated), calcareous/ agglu tina ted foraminiferal ratio, taxonomic diversity of certain groups of benthic microfossils, microfaunal density, plankton/benthos ratio, content of keeled planktonic forms, and morphological fea tures of some agglutinated taxa.

The sedimentation of the early Cenomanian to late Campanian red facies took place under highly oxygenated conditions at the sea floor, except during

Krzysztof Bqk

the late Cenomanian-early Turonian anoxic event. This is confirmed by the colour of deposits, intense of burrowing, trace fossil ichnofacies and diversified agglutinated assemblage with tiny, smooth-walled species.

Trace fossils represent a low diversity assem­blage with prevailing Zoophycos in the red marls and marly limestones, and tubular forms of Planolites-type in the thin muddy or sandy interca­lations (Bqk, 1995a). The macrobenthos penetration was controlled by a shortage of food on the well oxygenated sea floor. It could be confirmed by reduced size of infaunal forms and by the presence of organisms selectively reworking the sediments. Oligotrophic conditions, connected with the high oxygentation level at the sea floor are reflected, moreover, by a low density of benthic foraminiferal assemblages, dominated by shallow and deep infauna (average 55% of the foraminiferal benthos).

Sedimentation rate was very low during the deposition of the Upper Cretaceous red facies. It was calculated from 1-4 m/my in the shallowest part to 8-23 m/my in the deeper part of the Pieniny Klippen Basin. Very low sedimentation rate is emphasised by the high rate of sediment bioturbation. For example, carbonate-rich marls of the Czorsztyn Succession (northern margin of the basin) are completaly bioturbated. The rate of sediment accretion changed during the deposition in the deeper part of the basin, being reflected by a change in the intensity of bioturbation, and trace fossil tiering (Bqk, 1995a). An intermittent fine clastic deposition by diluted turbidity currents, restricting the possibility of the sediment reworking by infauna, were more frequent during the Santonian.

The middle Turonian and the uppermost Santonian/lower Campanian green and pink lime­stones reflect extremaly low rate of sedimentation, calculated as about 1 m/my.

Palaeobathymetric information is given by planktonic foraminifers (their total content and content of keeled forms), calcareous/agglutinated foraminifers ratio, trace fossil assemblage, and calcium carbonate content. Planktonic foraminifers are represented predominantly (more than 90%) by large keeled morphotypes of the genera Rotalipora, Heivetogiobotrtlllcana, Marginotruncanl7, Globotrun­calla, and Rosita. Only in the Czorsztyn Succession (the shallowest part of the basin), the non-keeled forms (Hedbergella, Globigerinelloides, Hetero­helix) make up about 10-80% of the plankton, probably reflecting the sea level changes.

Content of the calcareous benthic foraminifers is very small, ranging from sample to sample between 0 and 20%. Their taxonomic diversity is low (1-5 species per sample). This confirms that deposition the Scaglia Rossa facies took place in upper to lower bathyal depths. Within the Czorszyn Succession, calcareous assemblages are more significant compo­nent, however, their content does not exceed 50% of 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 as indicating outer shelf-upper bathyal depths for the Czorsztyn Ridge (northern margin of the Pieniny Klippen Basin) during the Late Cretaceous. The sug­gestion takes into account an observation, that opti­mal conditions for the calcareous benthos took place in outer shelf environments (near the edge of shelf) during the Late Cretaceous, as was concluded by Kuhnt et al. (1989).

An ichnofossil assemblage in the studied deposits (B q k, 1995a) is similar to other localities, documented from deep-water Cretaceous and Cenozoic carbonate deposits (Ekdale & Bromley, 1984; Ekdale, 1985). The suggestion about the depths and sedimentation rate is interpreted, among other, based on an ethological composition of ichnofauna in the studied deposits. Pascichnia and Fodinichnin traces dominate there, being accompanied by rare Agrichnin and Repichnin traces.

Outer shelf-upper bathyal through lower bathyal depths (near CCD) of the sea floor are also suggested from the calcium carbonate content analy­sis. More than 200 analyses of the CaC03 content in the marls and marly limestones (Bqk, 1995b), have been used to support this interpretation, carried out in relation to the distinguished successions and the time scale. High values of CaC03 in the Middle­Upper Turonian sediments (mean 40-60% in particular successions) decrease up section to about 20-30% in the Santonian. This observation reflects a remarkable change in the sedimentary processes, from pelagic to hemipelagic, with more frequent turbiditic detrital inputs.

A palaeoecological interpretation of the Campanian-Maastrichtian sediments in the Maruszyna Scale has been presented by Kostka (1993), based on taxonomic features of benthic and planktonic assemblages, lithology, and using the planktic/benthic foraminifera ratio. Benthic foraminifers are dominated by Reussella sznjnochae, Osnngulnria cordierinna, Gyroidinoides nitidus, Anomalinoides affinis, Pleurostomella spp., Gnvelinella beccnriiformis, Pullenin spp., Dorotlzia trochoides, Tritaxia tricarinnta, T. amorpha and Spiroplectammina dentatn. The planktic/benthic foraminifera ratio is very high (about 0.9). The planktic foraminiferal assemblages are dominated by the genera Globigerinelloides, Hedbergella and Heterohelix. The content of deep-dwelling globotruncanids is consistent and varies between 10 and 20% (Kostka, 1993). Taking into account the above features of microfaunal assemblages, Kostka concluded that Campanian-Maastrichtian sedi­ments were deposited in off-shelf open marine con­ditions at middle bathyal depths. The lithological character (about 20 m thick marls and marly lime­stones) and lack of shallow water microfaunal markers record the location of this area at a dis­tance from shoreline on the order of 50-100 km, prob­ably on the submerged ridge (Birkenmajer, 1986). The appearance of reworked Campanian-

Maastrichtian marls as fragments in fine-grained sedimentary breccia and a few layers of fine-grained sandstone within the Upper Senonian complex was explained by Alexandrowicz & Birkenmajer (1978) as the effect of bottom erosion by episodic turbidity currents. Mean sedimentary rate for these deposits is calculated as 2 m/my.

The described sedimentary environment of the Scaglia Rossa-type facies in the Pieniny Klippen Basin (including Klippen and Maruszyna succes­sions) was very similar to that of the southern (Gubbio sections; Umbrian Apeninnes) and the west­ern (Hacho de Montejaque section; Penibetic Zone) parts of the Western Tethys. However, the sedi­mentation in the Pieniny Klippen Basin was charac­terised by more frequent turbiditic detrital inputs, especially during the late Coniacian-Santonian.

Comparison of index taxa ranges with different bathyal localities Plectorecllrvoides alternans The species Plectorecurvoides alternans was used as a zonal marker for the first time in the Flysch Carpathians (Geroch, 1959, 1962; Hanzlikov;l, 1966). Morgiel & Olszewska (1981) noted its strati­graphical ranges from Albian through Turonian, and emphasised its stratigraphical value within the Albian and Turonian, as a part of "Assemblage of P. alternans". Later, its FO in the Middle Abian was proposed as a base of the P. alternans Zone in Geroch & Nowak's zonation (1984) and in Olszewska's zonation (1997). Similar data about the occurrence of this species were observed in the Romanian Carpathians (Neagu, 1990).

In the PKB, P. alternans appeared within the Biticinella breggiensis Zone, corresponding to the Middle Albian. It occurs in the red facies as frequent and common species within low to medium diversi­fied assemblages, dominated by Glomospira spp, Ammodiscus spp., Recurvoides spp., and rhizamminids.

The occurrence of P. alternans is restricted to the Western Tethys. Besides the Carpathian area, the Alps (first time described by Noth, 1952), and the Moroccan Numidian Flysch (Morgiel & Olszewska, 1982), no data are known from the Atlantic and the Indian oceans. It represents an element of typical deep-water assemblages from environments below the CCD. However, it appeared within calcareous flysch and hemipelagites, too. It seems that upper­middle bathyal depths created an upper depth limit for this taxon.

BlIlbobaclIlites problematiclIs Stratigraphic ranges of the B. problematicus at dif­ferent localities (including the abyssal oceanic, the marginal basins and the Carpathian trench) have been presented by Kuhnt & Kaminski (1990). The FO of this taxon was observed directly above the anoxic deposits of CTBE in all localities, except in the Carpathian area, where its FO occurs within

26

Cenomanian strata. The above authors suggested, that this fact correlates with the first occurrence of the red oxic sedimentary environments, which took place significantly earlier in the Carpathian basins. Therefore, oxygen-depleted bottom waters constituted a faunal barrier for the colonisation of B. problematiells.

Local 5ea lave Klippen successions curve

(K. Bilk. 1995/» Czor ~~~~ ~~~ __ L-~

El !±l iii o

as elrica

Dicarinella concavaJa

i U .~ M I---=TF;:':'::;':'~

~ L

j t=~~mq c

~ o c CP o

I I

Figure 5. Frequency of the Bulbobaculites problematiclls in the Scaglia Rossa-type facies, in relation the local sea-level changes, the Pieniny Klippen Belt; p - present, r - rare, f -frequent, c - common

The FO of B. problematieus in the PKB is well documented near the base of the Rotalipora reieheli Zone, corresponding to the base of the Middle Cenomanian, independent of facies. A comparison of frequency of this taxon in the Middle Cenomanian­Lower Campanian sediments allowed to observe three peaks of high abundance (Figure 5). They correspond to the Rotalipora reielzeli/R. greenhornensis, Helvetoglobotrllneana helvetiea/ Marginotruneana sigaJi and Diearinella primitiva Zones, reflecting the sea level high-stands. These high-stands were proposed on the basis of changes in plankton morphotypes and mobile calcareous epifauna, observed in the deposits of the shallowest part of the Pieniny Klippen Basin (Bqk, 1995b). The changes of these two features of foraminiferal assemblages are linked with behaviour of foraminifers. The increase of "deep-water" plank­tonic morpho types of genera Praeglobotrllneana, Helvetoglobotruneana, Rotalipora, Marginotrun­eana, Contllsotruneana, and Globotrllneana correlates with increase of sea level, as was presented e.g., by Sliter (1975), Hart (1980), Leckie (1987), Hallock et al. (1991). A similar positive correlation can be exemplified in relation to the calcareous mobile epifauna (e.g., Fiirsich et al., 1991; Tyszka & Kaminski, 1995).

Thus, taking into account the positive correlation between the high frequency of B. problematjells and sea level high-stands, it can be concluded that the

Krzysztof Bqk

increase in the population could be linked with the increase of oxygenation at the sea floor. This was earlier suggested by Kuhnt & Kaminski (1990), in relation to the FO of this taxon in the similar type of lithologies at different localities. Two of the B. problematieLls "blooms" occurred in the PKB just after large anoxia. They represent: 1) the Late Albian/Early Cenomanian episodic anoxia, recorded by black deep-water siliceous facies with opportunistic agglutinated assemblages of "Biofacies B", and 2) the Cenomanian/Turonian Boundary Event. The latter anoxia are expressed in the PKB, by black shales, both from the shallow, and the deepest part of the basin, with rare and low-diverse agglutinated assemblages, and spe­cially adapted other benthic communities, like ostracods and calcareous foraminifers. The species B. problematieus, prefering probably the shallow infaunal habitats (comparable to Ammobaeulites -see discussion by Tyszka & Kaminski, 1995), could be more tolerant of dysoxia and low pH than other agglutinated taxa. Thus, during an increase in oxygenation at the sea floor, this taxon could be an initial coloniser on the bottom, tolerating the episodic anoxia occurring in the first phases of the environmental changes.

On the other hand, it should be pointed out that an "increase" in the number of foraminiferal tests can be caused by a low sedimentation rate, as took place during the sea level high-stands.

In the Carpathians, where B. problematieus appeared earlier than in the rest of the oceanic realm, its FO datum is still studied. Neagu (1990) observed the FO of this species in the lower Albian Haplaphragmoides nonioninoides Zone in the southern flysch zone of the Romanian Carpathians. More recently, Olszewska (1997) presenting a com­posite zonation based on different foramininiferal groups for the Tithonian-Miocene in the Polish Flysch Carpathians, reported the FO datum of B. problematiells in the uppermost Albian (together with Planomalina buxtorfi and Rotalipora appenniniea).

Uvigerinammina jankoi A detailed description of U. jankoi and first report on its stratigraphical value originate from the Polish Flysch Carpathians, presented by Geroch (1957). From the same region, U. jankoi occurs as the index taxon for the Upper Turonian-Santonian U. jankoi Zone in the Nowak & Geroch's zonation (1984). Its FO is presented there immediately above green shales with radiolarians, correlated with the CTBE.

After this presentation, U. jankoi has been used as stratigraphical marker species, both in the North Atlantic and the Tethan realm in every zonal scheme (e.g., Moullade et ai., 1988; Kuhnt et al.,

Biostratigraphy of DW AF in Scaglia-type deposits of the PKB, Poland 27

~ 90 L

c: -.!!! c: M e r--.=

E

Planktonic foraminiferal zones (K. BlOlk. 1998)

r _!2i<:p!.i'!.e!!.a_c9.nE'!Yf!!a.. - -Dicarineila primitiva

Marginotruncana siga/i

Helvetogiobotruncana helvetica

ieniny - Branisk

lower-middle bathyal depths

en successions Czertezik

t ;; FAD of ~ """"

..... anoxic , ~

~FAD

~jll!'~O~ "" ~'~"""""'I deposlb I············ .. . c~ ............. .

Praegiobotrunc. delrioensis E L Rotalipora cushmani

.............. . ... ..................................... 0

- c: - 7foialiooro m,,'nhOrnemij • II)

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 noted at most localities just above or in the highest part of anoxic deposits representing the CTBE. However, at certain localities in bathyal environments, like in the Gubbio section (Umbrian Apeninnes) and the Zumaya section (North Iberian continental margin), it appeared in the Coniacian or Santonian. Within the Scaglia Rossa facies at the Gubbio section (white to pink coloured siliceous limestones), U. jankoi is practically absent (Kuhnt, 1990). Only single specimens have been found in the Santonian strata. This was explained by Kuhnt as being due to the lack of the clay minerals used to agglutinate the wall.

This taxon, in all described localities, occurs within highly diversified assemblages, with spec­imens that have a brownish siliceous agglutinating wall (Kuhnt et al., 1989a). The assemblages repre­sent the so-called "Biofacies A", corresponding to the Upper Cretaceous oxygenated environments.

In the PKB the first occurrence of U. jankoi is con­nected with changes of oxygenation of the bottom water (Figure 6). Anoxic facies, representing by black shales and marly shales have been replaced by light-green, highly calcareous limestones, corre­sponding to the high Eh level. The change of the facies took place earlier on the slope of the Pieniny Klippen Basin - within the Praeglobotruncana delrioensis Zone through the Helvetoglobotrllncana helvetica Zone, corresponding respectively to the Cenomanian/Turonian boundary and the Early­Middle Turonian. Simultaneously, a change in the agglutinated assemblages was observed in the stud­ied sediments. A number of first occurrences of the agglutinated species are observed in the Turonian, occuring within the highly diversified assemblage.

In the Romanian Flysch Carpathians, Neagu (1990) described the species U. praejankoi, which occurs in the Whiteinella archeocretacea through the Marginotruncana schneegansi Zones. Neagu sug­gested to distinguish the U. praejankoi Zone within

the lowermost part of U. jankoi Zone. In the PKB, small specimens with pseudo-biserial arrangement in the adult stage, classified as U. praejankoi occur within the H. helvetica and M. sigali zones (Bqk et al., 1995). However, its FO is the same as that of U. jankoi. This fact can be explained by: 1) the later migration of this taxon from the Romanian part of the Carpathians, or 2) similar, like U. jankoi, requirements in relation to the oxygenation of the bottom water, as well as 3) sedimentary conden­sation due to very low sedimentation rate during this time (1 m/my).

The LO of U. jankoi is noted in the Scaglia Rossa­type deposits of the PKB within the Globotruncana ventricosa Zone (Alexandrowicz, 1975). A similar datum was reported from the Romanian Flysch Carpathians, where this species has its LO within the Globotruncanita calcarata Zone (Neagu, 1990). The LO in the middle/late Campanian was noted in ODP Hole 641A (abyssal part of the North Atlantic; Kuhnt et al., 1989a). In the Polish Flysch Carpathians (Geroch & Nowak, 1984), the Iberian continental margin (Kuhnt & Kaminski, 1997) and at most localities in the North Atlantic (e.g., Moullade et al., 1988; Kuhnt et al., 1998), U. jankoi last occurred during the early Campanian. In the Scaglia Rossa facies of the southern and western part of the Western Tethys (Kuhnt, 1990), its LO was noted earlier, at the top of the Dicarinella asymetrica Zone (near the Santonian/Campanian boundary).

Goesella rugosa Specimens of Goesella rugosa were described from only slope facies, representing the environments above the CCD (Kuhnt & Kaminski, 1990). This restriction is linked with utilisation of calcareous cement by this taxon for agglutinating its test. The FO of G. rugosa was presented by Geroch & Nowak (1984) at the base of the Campanian from the Polish Flysch Carpathians. The same datum noted by

28

Neagu (1990) from the Romanian Flysch Carpathians, Kuhnt & Kaminski (1997) from the Zumaya section, and Kuhnt & Moullade (1991) from DSDP Hole 398D at the Vigo Seamount (the North Atlantic).

Goessella rugosa has not been observed within the Scaglia Rossa facies at the Gubbio and Montejaque sections (Kuhnt, 1990). In the PKB, this taxon occurs as more frequent in deposits from the deepest part of the basin. This fact may be caused by restriction of the clay minerals used to agglutinate the wall in an environment with extremely low sedimentation rate.

The stratigraphic range of G. rugosa is restricted to the late Maastrichtian (Geroch & Nowak, 1984)­?early Palaeocene (Kuhnt & Kaminski, 1990). However, at most localities it depends on the location of the CCD in the basin. In Scaglia-type assemblages within the Maruszyna Succession (the PKB), the LO of G. rugosa has been recorded in the Abathomphalus mayaroensis Zone (Kostka, 1993).

Caudammina gigantea The species Caudammilla gigantea is used to define the "Hormosina ovulum gigantea Zone" in the Polish Flysch Carpathians (Geroch & Nowak, 1984). The FO of this species marks in that area the base of the mid-Campanian. In the Romanian Flysch Carpathians, C. gigantea occurs within the Globotruncanita elevata Zone (early Campanian), co-existing there together with U. jankoi (Neagu, 1990). At some localities in the abyssal North Atlantic, a similar coexisting took place (Moullade et aI., 1988), which formed the basis to define the jankoi-gigantea concurrent range zone (Vigo Seamount; Kuhnt & Moullade, 1991).

In most localities, the FO of C. gigantea is observed above the benthic-free zone corresponding to the Lower Campanian Event.

Within the Scaglia-type assemblages this species is rare. It is absent in the Gubbio material, and occurs as single specimens in the Campanian of the Penibetic section (Kuhnt, 1990). In the PKB, it was found as rare, in the Czorsztyn and the Pieniny successions, representing the shallowest and the deepest part of the basin, but only within Globotruncanita elevata-Globotruncana ventricosa zones. The infrequent occurrence of C. gigantea in pelagic calcareous environments was linked with its utilisation of siliceous cement and grains for agglutinating its test. Low concetration of silica and high pH value in the calcareous environments could restrict the population of this species. Kuhnt et al. (1998) suggested the lower bathal depths as the upper depth limit for distribution of C. gigantea. It seems to be realy true in most localities where C. gigantea has been found. In the Pieniny Klippen Basin, this upper depth was- higher, corresponding probably to the upper-middle bathyal.

Krzysztof Bqk

PALAEOCEANOGRAPHIC EVENTS CenomanianfTuronian boundary event (CTBE) Beds corresponding to the CTBE are characterised by anoxic facies with high level of organic carbon (Herbin et aI., 1986). Microfossil assemblages from these facies are dominated by radiolarians and devoid of benthic foraminifers, and directly over­lying beds contain low diversified opportunistic agglutinated taxa (e.g., Kuhnt, 1992; Lamolda & Peryt, 1995). The event is accompanied by important taxonomic changes in DW AF (Geroch & Nowak, 1984; Moullade et aI., 1988; Kuhnt, 1990; Neagu, 1990).

In the PKB the Cenomanian/Turonian boundary is characterised by black shales and marly shales, both in the Czorsztyn Ridge and in the deepest part of the basin (Birkenmajer, 1977; Birkenmajer & Jednorowska, 1984; Bqk, 1998). The microfossil assemblage is represented by radiolarians and ostracods (in the Czorsztyn Succession only), predominantly. Low diversity benthic foraminifers with single specimens of genera Haplophragmoides, Bulbobaculites, Gaudryina, Glomospira and Trochammina occur in the slope facies of CTBE (the Niedzica Succession), where black marly shales are intercalated with muddy turbidities. They are absent in the deep-sea successions, except of single tubular forms. In the Czorsztyn Ridge facies, the agglutinated foraminifers are represented by single opportunistic forms of genera Nothia, Rhab­dammina, Rhizammina, Saccammina, Ammodiscus, Glomospira, Glol1lospirella, Bulbobaculites (only in lower part), and Trochammina.

The FO of Hormosina excels a was observed within the CTBE in the Szaflary section (Czorsztyn Succession). This species has not been known from this age, so far. Its earliest FO was described in the Flysch Carpathians, from the Santonian/ Campanian boundary (Morgiel & Olszewska, 1981; Geroch & Nowak, 1984). Kuhnt & Kaminski (1990) described H. excelsa from the Coniacian-Santonian sediments in the Moroccan Rif. They speculated that some specimens of their assemblages could be intermediate forms to Hyperammina elongata and Hyperammina dilatata. In the PKB, above the CTBE, H. excelsa was found within the late Turonian through the late Santonian assemblages as single or few specimens in samples, exhibiting simi­lar morphologic features like in the population from the Moroccan Rif.

Above the CTBE in the PKB, a change in the agglutinated assemblages occurs, emphasised by increase of diversity and appearance of new species. The Turonian-Coniacian-Santonian agglu tina ted foraminifers are dominated by tiny smooth-walled calcareous and siliceous specimens of the species Uvigerinammina ex. gr. jankoi, Gerochammina con versa, Karrerulina coniformis, Haplophrag­moides d. bulloides, H. d. kirki, Recurvoides spp., Bulbobaculites problematicus, Trochammina spp. 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 ZONES ..

~ ; ZONES Ptm~.ticZon., ~~ogated day

Umbr. Apennines belowCCD Pollah Flysch Poliah Flyaell DSOP ~Ibrall ... Aret North Iberian Hole 3880 -M,,·Yllan ConU".,..taI InP.K.B. .. IR .... aqno/<t' Coron,li115, RangHof North AaanUc

Carpathlana Carpathian. (Ol""'h .. (0_1<1, Vlgolilmoun! Flysch Margin .. mod/WN by K. /14k. feel) (this study)

r==-==-Important r:J!NAF IMOU~~:l. II .• (Kuhn~ 1980) NOWIk,1IM) 1917) (Kuhnl" IKuhnl'''4 IKuhnl"

Mounld •. 1H1 1112) Kaminski 19$7 ------c -------" Abalhompholus :p .c. mayaroensls .!.! -=

RemeseJIa RemeseJIa varians

varian.s Honnosina

I ------ ovuJum

::IE Gansserlno gansseri ,---~

.. 'i ~

Honnosina -----_. Hormosina Rzehakina gigantea

C. avuJai ovuJum inc/usa ----_. G. aegyp/iaca Goesel/a ill Hormosina gigantea

gigantea

.!i G. havallensis rugosa

! G. calcara/a

5 Glooo/rulicalla <.J venlricOSQ

U. jlUlkoi -J Globotruncalu/a ~giganJea

eleva/a

~ Dicarillel/a

~ asymelrica

gigantea

., ~ 'i ., r " Ie ~ J § ~ :t ...., .~ 2

n " '5 U./ankoi .S .~

G. rugosa Hormosina H. gigantea gigantea

acme

GoeseJIa

Go;s;ijd Hormosina U.J·;nJc;;i -:: rugosa

------_r:u59.sE_

gigantea ~gigantea benthic-free

r-;-- ! ~ " ~ .! ------

~ Dicarillella C iUvigerinam 0 co/Jcavala <.J ex gr. r--r-

u --------- jankoi c Dlcan'nella primir;va

J 17,,«p/_ gwbit/erilo.

S. costala V.Jankoi V./ankoi

V./anko; UJankoi

B. probJe-III r; r---M sifl:ali-'E IiI"l'wph,"I"" maticus B.probJe-V.Jankoi e t- Helve/oglobo/l1l71Calla "",k';

UApenlnnes -----------_. malicus

~ L helvetica IPenibelic Z ------ ------- - P. delrioens/s

C U Ro/alipora cushmani B. proh/e-. !!I M -.i1..- ,,",,- mat;cus

~ _x. reicileli_ -g L Ro/ol/pora Plectorec. G.I globo/runcallOities aiJernans <.J

A. probJe- benthic-free rnaticus -----_ . ------ B. probJe-

IPJectorecur. maticus PJectorecur. aiternan.!

aJternans ----- ------- ------ ,

Figure 7. A comparison between the succession of DWAF zones observed in the Pieniny Klippen Belt, with other zonations

Lower Campanian event (LCE) An interval of biosiliceous sedimentation with abundant radiolarians and scarce, poorly preserved benthic foraminifers has been observed at many localities in the North Atlantic, South Atlantic and the Tethyan Realm (e.g., Butt, 1981; Hemleben & Troester, 1984; Moullade ct aI., 1988; Kuhnt et aI., 1989; Kuhnt et aI., 1998). The event was linked with the formation of warm saline bottom waters, influ­encing changes in deep water circulation. These resulted in changes among the DW AF assemblages. In some pelagic environments (the Umbrian Apennines and the Penibetic Zone; Kuhnt, 1990), biosiliceous deposits are not known. However, within the Lower Campanian deposits, a major faunal change in agglutinated foraminifers was observed.

In the PKB, the LCE has a characteristic lithol­ogy, only within the shallowest succession (the Czorsztyn Succesion). The uppermost Santonian­Lower Campanian deposits are represented by 2 m thick thin-bedded light-green limestones, interca­lated with brick-red highly calcareous marls (the Lorencowe Chert Bed in the Kietowy stream section; Birkenmajer, 1977). Foraminifers are dominated by planktic forms. Radiolarians occur as poorly pre-

served calcified specimens of only several species (M. Bqk, 1996b). DW AF assemblages are represented by single specimens of some taxa within this interval. Diversity of agglutinated assemblages is significantly lower than in the Santonian ones, and decreases above the calcareous horizon. The LO of Bulbobaculites problematic us is observed within the LCE.

CONCLUSIONS The Cenomanian through Upper Maastrichtian Scaglia Rossa-type facies in the Pieniny Klippen constitute good material for calibration of DWAF ranges with chronostratigraphy, because of the occurrence of well diversified and abundant agglutinated taxa and presence of planktic foram­inifers and calcareous nannoplankton within the microfossil assemblages.

The biostratigraphic succession of agglutinated foraminifers in the analysed sections allows me to recognise the Upper Cretaceous zones oryginally defined by Geroch & Nowak (1984) in the Polish Flysch Carpathians. However, the ranges of certain zones in Campanian-Maastrichtian are different than in the latter zonation, being caused by specific environmental conditions during sedimentation of

30

the Scaglia Rossa-type facies in this part of the Western Tethys. The Goesella mgosa Zone, in Geroch & Nowak's and other zonal schemes (e.g., Kuhnt & Kaminski, 1997; Figure 7), calibrated with early Campanian, has in the PKB a longer range; from the earliest Santonian (uppermost part of Diearinella asymetriea Zone) through the late Maastrichtian (Abathomplzalus mayaroensis Zone). The species Caudammina gigantea, another index marker in the Campanian and Maastrichtian in many zonations (Geroch & Nowak, 1984; Moullade et aI., 1988; Kuhnt & Moullade, 1991; Kuhnt et aI., 1992; Kuhnt & Kaminski, 1997; Olszewska, 1997), occurs here only within Globotruneanita elevata -Globotruneana ventrieosa zones. Thus it was used here as a marker in the concurrent range zone of U. jankoi - C. gigantea, considered as an additional zone (Figure 7).

Outer shelf - lower bathyal depths of the basins, low rate of pelagic sedimentation above CCD, oligo­trophic conditions at the sea floor, high value of pH and restriction of silica and siliceous grains at the sea floor, as well as periodic anoxia were the main factors that stimulated the occurrence of some deep­water foraminifers in the Scaglia Rossa-type deposits of the PKB. Such conditions were conducive to large B. problematieus, U. jankoi and G. rugosa populations on the one side, and restricted the life habiatats of C. gigantea, on the other.

It is interesting that the ranges of the above men­tioned taxa differ significantly from the same species occurring in the similar facies of the southern and the western parts of the Western Tethys (Umbrian Apeninnes and Penibetic Zone; Kuhnt, 1990; Figure 7). It seems that the timing of local anoxia, the basin depths, and the frequency of detri­tal inputs could be responsible for these differences. On the other hand, the ranges of stratigraphically important taxa are more similar to the slope assem­blages with flysch or hemipelagic sedimentation above CCD (compare with the Flysch Carpathian and North Iberian continental margin zonal schemes; Figure 7), with the exception of the late Campanian - Maastrichtian assemblages, which were quite different because of different lithofacies, reflecting the depth of the sea floor and CCD during that time.

For several species of DWAF, their stratigraphic distribution is correlated to certain palae­oceanographic events, including the Cenomanian/ Turonian Boundary Event and the Lower Campanian Event. During these phases, significant taxonomic changes within DWAF took place. Local sea-level changes could similarly affect the populations of some taxa (e.g., B. problematieus).

AKCNOWLEDGMENTS The study of agglutinated foraminifera in the Pieniny Klippen Belt is based on the author's PhD thesis, supervised by Prof. A. Radomski Gagiellonian University) and reviewed with many

Krzysztof Bqk

helpful comments by Prof. K. Birkenmajer (Polish Academy of Sciences) and Prof. S.W. Alexandrowicz (Academy of Mining and Metallurgy). Michael A. Kaminski (University College London) and Christoph Hemleben (University of Tiibingen) revieved an earlier draft of this paper and provided useful comments on biostratigraphy. This study was supported by Cracow Pedagogical University grant BW-168/G/97. Thanks also to the Grzybowski Foundation for a travel grant to attend the 5th

International Workshop on Agglutinated Foraminifera in Plymouth.

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Kuhnt, W. 1990. Agglutinated foraminifera of western Mediterranean Upper Cretaceous pelagic limestones (Umbrian Apelmines, Italy, and Betic Cordillera, Southern Spain). Micropaleontology, 36, (4), 297-330.

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------~,~~-------

34 Krzysztof Bqk

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 (Dylqzan ka), Mac-38, x50. e. Honnosil1(/ exeelsa (Dylqianka), Mac-37, xSO. f. Honnosilln d. crnssn Geroch, SzG-l1, x75. g. Reoplwx I/ Od ll!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 llit illa (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()splweruidilljl 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

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.

Age

Planktonic foraminiferal zones

Nothia &p.

Bathysiphon &p.

Dendrophrya maxima

Dendrophrya robusta

Rhabdammina cylindrica Rhabdammina &p.

Rhizammina indivisa Rhizammina sp. Psammosphaera sp. Saccammina grzybowskii Saccammina cf. placenta

Saccammina sp. Lituotuba lituifonnis

Ammodiscus cretaceus

Ammodiscus glabratus

Ammodiscus tenuissimus Ammodiscus &p.

G/omospira charoides

G/omospira difundens

G/omospira glomerata G/omospira gorriialis

G/omospira irregularis

Glomospirella gauftina

Glomospirelfa gorayskii

Labrospire pacifica

Aschemocelfa carpathica Aschemocelfa grandis

Pseudonodosinella parvula Reophax sp.

Hyperammina gauftina Hyperammina sp.

Honnosina excelsa

Honnosina cf. velascoensis

Caudammina gigantea

Caudammina ovulum

Kalamopsis grzybowskii Nodelfum velfascoense Rzehakina epigona Haplophragmoides cf. bulfoides

Haplophragmoides concavus Haplophragmoides ct. aggeri

Haplophragmoidas falcatosutura/is

Haplophragmoides kirki

Haplophragmoides cf. nonioninoides Haplophragmoides cf. retroseptus Haplophragmoides ct. waJteri

Haplophragmoides &p. A Haplophragmoides spp.

Cribrostommoides trinitatensis

Cenomanian

2

p

p

p

p

.!!? .. :Ii E

t ,

~ .!,! e 3

p

p

p

p

7

p

p

4

p

p

p

p

p p

p

p

5 p

p p

p p

p

p p p

p

p

Turonian - Santonian

6 7 8 9 10 p p

p

p c c p p c

c c c p 7

p c c p p p

p ? p

p p

p c c p

p p

c c p

p p p p p

p c c p

p

p p

p p p p

c c c c

p p p

c c c c

p p c c

p p c p

w g

11

p

p p

p

p

Campanian­early

MaBtricht.

12 13

p

c c

c c

p

p

p

p

p

p

p

.r!!

I 14

p

p

p

p

p

p

p

Bulbobaculites Droblematicus Recurvoides globulosus

________ r __ _r-c~r_~r_r~r_r~c~~c~~c~~c~r_~f_r~D~r_--r_----_+--_4

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

39

40 Krzysztof Bqk

Appendix (continued):

1 2 I 3 4 5 6 7 8 9 10 11 12 13 14 Thalmanammina sp. I r r p Spiropl8ctammina baudouniaria 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 I

j

Spiroplectammina semicomplanata 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 T rochamminoides coronafus p p T rochamminoides 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 T ritaxia capitosa P c Tritaxia mitrata p r

Tritaxia tricarinata p p r p p p f r T ritaxia trilatera f c

Tritaxia gaultina p r p p p p r p p T ritaxia 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