Annales Societatis Geologorum Poloniae (2005), vol. 75: 27-69. LITHOSTRATIGRAPHY AND BIOSTRATIGRAPHY OF THE UPPER ALBIAN-LOWER/MIDDLE EOCENE FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS OF THE MAGURA NAPPE; WESTERN FLYSCH CARPATHIANS (BESKID WYSPOWY AND GORCE RANGES, POLAND) Nestor OSZCZYPKO1, Ewa MALATA1, Krzysztof BĄK2, Mariusz KĘDZIERSKI1 & Marta OSZCZYPKO-CLOWES1 11nstitute of Geological Sciences, Jagiellonian University, Oleandry St., 2a, 30-063 Kraków, Poland 2 Institute of Geography, Cracow Pedagogical University, Podchorążych St., 2, 30-084, Kraków, Poland Oszczypko, N., Malata, E., Bąk, K., Kędzierski, M. & Oszczypko-Clowes, M., 2005. Lithostratigraphy and biostratigraphy of the Upper Albian-Lower/Middle Eocene flysch deposits in the Bystrica and Raca subunits of the MaguraNappe (Beskid Wyspowy and Gorce Ranges; Poland). Annales Societatis Geologorum Poloniae, 75:27-69. Abstract: Lithostratigraphy and biostratigraphy of the Bystrica and Raca subunits of the Magura Nappe have been studied in the southern part of the Beskid Wyspowy Range and on the northern slopes of the Gorce Range (Polish part of the Western Flysch Carpathians). Six new lithostratigraphic units (Jasień Formation, Białe Formation, Jaworzynka Formation, Szczawina Sandstone Formation, Krzysztonów Member, and Ropianka Formation) of the Upper Albian-Palaeocene age have been established, and five other units (Malinowa Shale Formation, Hałuszowa Formation, Łabowa Shale Formation, Beloveza Formation, Bystrica Formation) have been additionally described. The newly created formations as well as the Malinowa Shale Formation and the Hałuszowa Formation have been included to a new Mogielica Group of units (Upper Albian-Palaeocene). This group of units passes upwards into the Beskid Group (Eocene-Oligocene).The Mogielica Group, spanning over 40 myrs, represents the turbidite depositional system, separated by highstand variegated clays which can be correlated with minor sequences in terms of sequence stratigraphy. The following biostratigraphic zones have been recognised in the Cretaceous-Lower/Middle Eocene deposits: Plectorecurvoides alternans, Bulbobaculitesproblematicus, Uvigerinammina jankoi, U. jankoi-C. gigantea, Cau- dammina gigantea, Remesella varians, Rzehakina fisistomata, Glomospira div. sp., and Saccamminoides carpa- thicus. A few lithostratigraphic units consisting of calcareous sediments have been correlated with the standard calcareous nannoplankton zonation and the chronostratigraphy. Key words: lithostratigraphy, biostratigraphy, deep-water agglutinated foraminifera, calcareous nannoplankton, Early Cretaceous-Palaeogene, Magura Nappe, Western Flysch Carpathians. Manuscript received 29 July 2004, accepted 13 January 2005 INTRODUCTION Four facies-tectonic subunits in the Polish sector of the Magura Nappe have been distinguished on the basis of the Eocene deposit facies differentiation. These are from the north to the south: Siary (=northern Gorlice), Raca (=south- ern Gorlice), Bystrica (=Sącz), and Krynica subunits (Fig. 1) (for references see Birkenmajer & Oszczypko, 1989). The present paper concerns deposits of the Raca and By- strica subunits, which build the Beskid Wyspowy Range and the northern part of the Gorce Range. During the last decade of detailed mapping (1992- 2003), the stratigraphic standards of the Upper Cretaceous and Paleogene deposits of the Beskid Wyspowy Range and the northern part of the Gorce Range underwent consider- able changes. This was due to sedimentological investiga- tions and tectonic analyses by the first author, and detailed stratigraphic work based on microfossil studies (foramini- fera and calacareous nannoplankton) by the other authors. The first results of these investigations were presented by Malata et al. (1996), Bąk and Oszczypko (2000), Osz- czypko et al. (1999), Oszczypko (2001), and Oszczypko- Clowes & Oszczypko (2004). Geology of this area was also a subject of P. Kruczek’s Msc thesis (1998). All these stud- 28 N. OSZCZYPKO ET AL. Fig. 1. Tectonic map of the Western Carpathians (compiled by Oszczypko-Clowes, 2001). 1 - crystalline core of the Tatra Mountains; 2 - High Tatric and Sub-Tatric units; 3 - Podhale flysch; 4 - Pieniny Klippen Belt; 5 - Magura Nappe; 5a - Malcov Formation; 6 - Grybów Unit; 7 - Dukla Unit; 8 - Fore-Magura Unit; 9 - Silesian Nappe; 10 - Sub-Silesian Nappe; 11 - Skole Nappe; 12 - Lower Mio- cene; 13 - Miocene deposits upon the Carpathians; 14 - Stebnik (Sambir) Unit; 15 - Zgłobice Unit; 16 - Miocene of the Carpathian Fore- deep; 17 - andesite; 18 - studied area. Tectonic-facial subunits of the Magura Nappe: Su - Siary, Ru - Raca, Bu - Bystrica, and Ku - Krynica ies, supplemented by present investigations, enable us to recognize the stratigraphy and to propose a new litho- and biostratigraphic subdivisions for the Upper Albian through the Lower/Middle Eocene deposits of the middle part of the Magura Nappe in Poland. This paper presents five formal lithostratigraphic units in a rank of formation and one in a rank of member pro- posed by the first author (N. Oszczypko), and a biostra- tigraphic division of the studied sequence presented by the co-authors. The biostratigraphy is based mainly on deep- water agglutinated foraminifera (studied by E. Malata and K. Bąk), supplemented by planktonie foraminifera (studied by K. Bąk) and calcareous nannoplankton (studied by M. Kędzierski and M. Oszczypko-Clowes). A part of the formal lithostratigraphic units (the Mali- nowa Shale, Hałuszowa, Łabowa Shale, Beloveza, and Bystrica formations) corresponds to those already used in the syntheses for the other facies-tectonic units of the Ma- gura Nappe (Birkenmajer & Oszczypko, 1989). Some of the geographical names traditionally used for a long time have been left unchanged whenever it was possible. It refers to the Kanina beds (Burtan et al., 1978; Oszczypko et al., 1991), the Jaworzynka beds (Burtan, 1973; Burtan et al., 1978), the Szczawina Sandstone (Sikora & Żytko, 1959; Oszczypko et al., 1991), and to the Ropianka beds. A new unit in the rank of a group comprises formations displaying similar lithology and corresponding to the same stage of the Magura Basin evolution. Most of the lithostratigraphic units in the studied area have diachronous boundaries. Some of the lithostratigraphic units, used in the presented division, occur also in other facies-tectonic units of the Magura Nappe. This paper has been prepared according to the Polish Stratigraphical Code (Alexandrowicz et al., 1975, Racki et al., 2004). STUDY AREA The presented lithostratigraphic and biostratigraphic subdivisions are based on detailed studies in two regions be- longing to the Raca and Bystrica subunits, both located in the Polish part of the Magura Nappe (Figs. 1, 2). The first one is situated in the Beskid Wyspowy Range (Figs. 2, 3), including the area between the Łososina and Kamienica Rivers, around the hills of Jasień (1062 m) and Mogielica (1171 m). The second one is located in the northern part of the Gorce Range (Figs 2, 4), in the vicinity of the Koninki and Poręba Wielka villages. The studied part of the Beskid Wyspowy Range is built mainly of the Upper Cretaceous-Lower/Middle Eocene strata of the Raca subunit, extending eastwards from the Mszana Dolna tectonic window and northwards from the Szczawa tectonic window (Fig. 2) (Swiderski, 1953; Burtan et al., 1978). This part of the Raca subunit is built up of sev- eral synclines, filled with the Magura Formation, and under- lain by the older formations (Beskid Wyspowy thrust-sheet; see Mastella, 1988). The SE branch of the Beskid Wyspowy Range (with Mogielica Hill), studied by the authors, is lo- cated in the area built up of the Bystrica subunit, which in- cludes several thrust-sheets (Fig. 3). In the studied, northern part of the Gorce Range (south of the Mszana Dolna tectonic window), the Bystrica subunit consists of the Upper Cretaceous-Lower/Middle Eocene strata, and builds up the frontal thrust of the Magura Nappe (Fig. 4) (Burtan et al., 1976, 1978; Oszczypko-Clowes & Oszczypko, 2004). This unit is visible very well in morphol- ogy forming W-E trending belt of round-of hills (Osz- czypko et al., 1999). FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 29 Fig. 2. Geological sketch-map of the middle part of the Western Carpathians (Poland) (after Oszczypko et al., 1999b, supplemented) MATERIAL AND METHODS About 90 samples were collected from the sections of the Raca and Bystrica subunits for foraminiferal analyses (Figs 5, 11-14). The samples were processed by the stan- dard micropalaeontological method. They were boiled and frozen using Na2CO3 solution, and then washed over a 63 p.m screen and dried out. In most of the samples, all micro- fauna from the > 63 p.m fraction were picked and mounted onto cardboard microscope slides. The material is hosted in the Institute of Geological Sciences, Jagiellonian University and in the Institute of Geography, Cracow Pedagogical Uni- versity (the Półrzeczki and Bruski sections). All samples for nannoplankton studies were prepared with the standard smear slide technique for light microscope (LM) observations. The investigations were carried out un- 30 N. OSZCZYPKO ET AL. Fig. 3. Geological map and geological cross-sections of the Półrzeczki-Białe-Szczawa area; Bystrica and Raca subunits, Magura Nappe, Western Flysch Carpathians FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 31 Fig. 4. Geological map of the southern margin of the Mszana Dolna tectonic window, Western Flysch Carpathians (after Burtan et al., 1976; Oszczypko et al., 1999b, supplemented) and geological cross-section along the Koninki stream (after Oszczypko-Clowes & Oszc- zypko, 2004, supplemented). Lithostratigraphic units marked on geological cross-section: 1 - Hulina Formation; 2 - Malinowa Shale For- mation and Hałuszowa Formation; 3 - Białe Formation; 4 - Szczawina Sandstone Formation; 5 - Ropianka Formation; 6 - Jaworzynka Formation, 7 - Grybów Beds, 8 - Krosno Beds 32 N. OSZCZYPKO ET AL. der LM at a magnification of 1000* using parallel and crossed nicols. Several specimens photographed under LM are illustrated in Fig. 27. For the purpose of this work the standard nannofossil zonation of Martini (1971), Varol (1998), and Burnett (1998) were used. LITHOSTRATIGRAPHY The study area is built up of the Upper Albian-Lower/ Middle Eocene rocks. Nine lithostratigraphic units in a rank of formation (Jasień Formation, Białe Formation, Malinowa Shale Formation, Szczawina Sandstone Formation, Ropi- anka Formation, Jaworzynka Formation, Łabowa Shale Formation, Beloveza Formation, Bystrica Formation) have been distinguished here. They were included to the Mo- gielica Group and to the Beskid Group. MOGIELICA GROUP (a new group) Name. After Mogielica Hill (1171 m) in the Beskid Wys- powy Range of the Polish part of the Western Carpathians. The name “Mogielica” was for the first time used by Swi- derski (1953) in a tectonic sense (Mogielica thrust-sheet), and then by Wójcik et al. (1996) as the name of the forma- tion embracing the Senonian-Palaeocene deposits (Mo- gielica Fm.). This formation has not been formalized so far. Polish name: Grupa mogielicka. Subdivision. The Mogielica Group is subdivided into seven formations: the Jasień Formation, Malinowa Shale Forma- tion, Hałuszowa Formation, Białe Formation, Jaworzynka Formation, Szczawina Formation, and Ropianka Formation, spanning the time from Albian through Palaeocene. Thickness. Variable, maximum 600 m in the Bystrica sub- unit and up to 500 m in the Raca subunit. Dominant lithology. Spotty shales and variegated shales are dominant in the basal part of the Group. Thin-bedded turbidites with intercalations of turbidite limestones and subordinate, variegated shale horizons are predominant in the lower part of the Group. Massive, thick-bedded turbid- ites dominate in the middle part of the Group and thin- bedded turbidites with subordinate intercalations of varie- gated shale occur in the upper part of Group. The Mogielica Group, spanning over 40 myrs, repre- sents the turbidite depositional system, separated by high- stand variegated clays, which can be correlated with minor sequences in term of sequence stratigraphy. Boundaries. Lower boundary usually tectonic against various lithostratigraphic units; upper boundary sharp as sedimentary transition to the Beskid Group (cf. Oszczypko, 1991). Geological age. Late Albian to Palaeocene. Equivalents. Grajcarek Group in the peri-Klippen Belt zone of the Magura Nappe (see Birkenmajer & Oszczypko, 1989). Jasień Formation (a new name) History. The Albian-Cenomanian deposits of the Magura Nappe (Grajcarek Unit) of the Pieniny Klippen Belt (PKB) have been described by Birkenmajer (1977) as the Hulina Formation. Furthermore, Birkenmajer & Oszczypko (1989) regarded the green spotty marls occurring in the southern margin of the Mszana Dolna tectonic window (the Koninki- Kustrzyca thrust-sheet, see Burtan et al. 1978, Burtan et al. 1992) as an equivalent of the Hulina Formation. Taking into account differences in lithological develop- ment between the Hulina Formation in the stratotype sec- tion in the PKB and observed lithology in the investigated area, we have decided to use the name “Jasień Formation” for the Albian-Cenomanian deposits in the presented divi- sion. Name. After the Jasień Hill (1052 m), 5 km south of the Półrzeczki village (Figs 3, 5A). Polish name: formacja z Ja- sienia. Type locality. The forest road-cut at an altitude of 840- 850 m located about 1km NWN of the Jasień Hill (Fig. 3, 5A) Reference section. Koninki creek (Figs 4, 5C) (Osz- czypko et al., 1999; Oszczypko-Clowes & Oszczypko, 2004), GPS position: N 49° 35, 930’, E 20° 04, 257’. Thickness. At least 15 m. Dominant lithology. Green and olive green, noncalcareous shales with intercalations of black, green shales and spotty shales. Sometimes small manganese nodules are observed. The shales display fracture cleavage of the pencil type. Boundary. The bottom of the formation is tectonic. Upper boundary - at the bottom of the first red shale package, be- longing to the Malinowa Shale Formation. Distribution. This formation is known from two localities in the Koninki village (Figs 4, 5C), on the southern margin of the Mszana Dolna tectonic window. The deposits similar to the Jasień Formation are also known from the Obidowa IG-1 deep borehole (Cieszkowski & Sikora, 1976; Fig. 2) and from the uppermost part of the Gault Formation (Ma- gura Nappe) in Moravia (for details - see Svabenicka et al., 1997). Equivalents. Hulina Formation of the Grajcarek Unit in the Pieniny Klippen Belt (Birkenmajer, 1977; see also Osz- czypko et al., 2004) and green radiolarian shales (Barna- siówka Radiolarian Shale Formation, Bąk et al., 2001) in the Silesian-Subsilesian and Skole units (Bieda et al., 1963). Malinowa Shale Formation Remarks. The Malinowa Shale Formation has been distin- guished by Birkenmajer and Oszczypko (1989) in the Kry- nica subunit of the Magura Nappe (see also Oszczypko et al., 1990). Later, this formation was described from the By- strica subunit (Malata & Oszczypko, 1990; Oszczypko et al., 1991; Malata etal., 1996). In the studied region, this for- mation occurs both in the Półrzeczki-Szczawa area, and in the Koninki area (Figs 3, 4) (see also, Oszczypko et al., 1991, 1999; Malata & Oszczypko, 1990; Oszczypko- Clowes & Oszczypko, 2004). In the Półrzeczki-Szczawa area, the Malinowa Shale Formation crops out both on the northern and southern sides of the Mogielica Range (Fig. 3). The best outcrops occur in the Półrzeczki village and in the vicinity of Bruski hamlet, in the core of the Białe anticline (Malata & Oszczypko, 1990; Oszczypko et al., 1991) and its continuation on the northern slope of Jasień and Kustrzyca hills. FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 33 Fig. 5. Simplified geological map of the Półrzeczki-Białe-Szczawa area (Bystrica and Raca subunits; Magura Nappe) with locality of type sections and hypostratotypes of lithostratigraphic units and with position of micropalaeontological samples. 45, 46/00/N - GPS posi- tion of selected stratotype sections The lower boundary of the Malinowa Shale Formation is sharp, located at the base of the first red shales. The cherry-red (Fig. 6A), non-calcareous shales occur in 30-50 cm layers, intercalated by grey-greenish shales, a few to 25 cm thick. Partly, grey-green shales are thicker and contain intercalations of thin-bedded (1-7 cm), single sandstone beds, 30-65 cm thick. Northeast of the Półrzeczki village at the Bruski hamlet, the Malinowa Shale Formation contains a few intercalations of thick-bedded, coarse to medium- grained quartz-glauconite sandstones, laminated quartzitic mudstones and hornstones. The thick-bedded sandstones re- vealed the palaeotransport from W and WNW. The fre- quency of grey-green shale intercalations increases in the upper portion of the formation, and deposits display some- times features of the Hałuszowa-type facies (cf. Zasadne section; Malata & Oszczypko, 1990). The upper boundary is sharp, located at the top of the last, thick appearance of the red shales (Fig. 6B). 34 N. OSZCZYPKO ET AL. Fig. 6. A - Red shales of the Malinowa Shale Formation; Koninki stream in Koninki; B - Boundary between the Malinowa Shale For- mation and the Białe Formation; Koninki stream in Koninki; C - Thin-bedded turbidites of the basal part of the Białe Formation, Ka- mienica River in Białe FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 35 Fig. 7. Lithostratigraphic logs of the Upper Albian-Lower/Middle Eocene deposits in the Raca and Bystrica subunits in the Półrzeczki-Białe-Szczawa area, Magura Nappe, Western Flysch Carpathians. Lithostratigraphic units: JF - Jasień Formation; MF - Mali- nowa Shale Formation; HF - Hulina Formation; BF - Białe Formation; JaF - Jaworzynka Formation; SF - Szczawina Sandstone; KM - Krzysztonów Member, RF - Ropianka Formation; ŁaF - Łabowa Shale Formation; BeF - Beloveza Formation; ByF - Bystrica Formation Total thickness of the Malinowa Shale Formation reaches at least 100 m in the Bruski hamlet, ca. 50 m on the slopes of Jasień Hill and at the Zasadne section (Fig. 7; see also Malata & Oszczypko, 1990; Cieszkowski et al., 1999), and at least 40-50 m in the area of Białe village (Malata & Oszczypko, 1990). Geological age of this formation ranges between Turonian and Late Santonian (Malata & Osz- czypko, 1990; Cieszkowski et al., 1999, Malata, 2001). Equivalents. Lower part of the Kaumberg Formation in the Moravia (Svabenicka et al., 1997) and the lower part of the Cebula Formation in the Pilsko area (Pivko, 2002, see also Sikora & Żytko, 1959; Golonka & Wójcik, 1978a, b). Hałuszowa Formation Remarks. The Hałuszowa Formation represents a transi- tional unit between the variegated shales of the Malinowa Shale Formation and thin-bedded turbidites of the Białe Formation (described below). This unit is composed of grey turbidite marls with intercalations of medium to thin- bedded turbidites and red marls. In the Zasadne and Młyń- czyska sections (Malata & Oszczypko, 1990; Malata et al., 1996), the Hałuszowa Formation replaces laterally the Białe Formation. In the Poręba Górna and Koninki sections, thin intercalations of red marls occur in the upper part of the Ma- linowa Shale Formation. Thickness of the formation reaches 100 m (Zasadne section: Malata & Oszczypko, 1990; Ciesz- kowski et al., 1999). Geological age - Late Santonian- Campanian (Malata & Oszczypko, 1990; Cieszkowski et al., 1999). Equivalents. Upper part of the Kaumberg Formation in the Moravia (Svabenicka et al., 1997) and upper part of the Ce- bula Formation in the Pilsko area (Pivko, 2002, see also Si- kora & Żytko, 1959, Golonka & Wójcik, 1978a, b). Białe Formation (a new name) History. The Senonian-Palaeocene deposits of the Magura Nappe have been traditionally referred to the Inoceramian beds (e.g., Bieda et al., 1963). In the investigated area this unit has been sometimes divided into three divisions, known as the lower, middle, and upper Inoceramian beds (Ciesz- kowski et al., 1987, 1989). The lower part of the Inoce- ramian beds is known as the Kanina beds. For the first time, 36 N. OSZCZYPKO ET AL. Fig. 8. Lithostratigraphical logs of the Upper Cretaceous-Eocene deposits in the Bystrica subunit in the southern margin of the Mszana Dolna tectonic window. Lithostratigraphic units: MF - Malinowa Shale Formation; BF - Białe Formation; SF - Szczawina Sandstone For- mation; RF - Ropianka Formation; ŁaF - Łabowa Shale Formation; BeF - Beloveża Formation; ByF - Bystrica Formation; ZF - Żeleźnikowa Formation; MM - Maszkowice Member of the Magura Formation the name “Kanina Beds” was used by Kozikowski (1953) in the marginal part of the Magura Nappe (Raca subunit), NW of Nowy Sącz. The subdivision of the Inoceramian beds was also used by the authors of the Detailed Geological Map of Poland (e.g., Burtan et al., 1976, 1978; Paul, 1980a,b, Osz- czypko & Wójcik, 1992). However, it should be stressed out that deposits included on these maps to the Kanina beds vary considerably in their stratigraphic position, lithology and thickness. Good exposures of the Kanina beds have been recently described from the Szczawa and Młyńczyska areas by Cieszkowki et al. (1987, 1989), Oszczypko et al. (1991), Oszczypko (1992b), and Malata et al. (1996). Due to the bad state of exposures in the Kanina area, the present authors have decided to propose a new formal lithostra- tigraphic unit for those deposits, which were previously de- scribed as the Kanina Beds. Name. After the Białe hamlet, 5 km NW of the Szczawa village (Figs 3, 5A). Polish name. Formacja z Białego. Type locality. 500 m long exposure along the left bank of the Kamienica River (Figs. 3, 5A); about 1 km NNW of the Białe hamlet (Bystrica subunit): GPS position - base of the section: N 49° 37, 480’, E 20° 15, 060’; top of section: 49° 37, 057’, E 20° 14,536’. Reference sections. Lubomierz section - a basal part of the Magura Nappe; Lubomierz creek, beneath the bridge across the road Mszana Dolna-Zabrzeż (Figs. 4, 5D), GPS posi- tion: N 49° 37, 140’, E 20° 09, 695’; section of Poręba Górna - a basal part of the Magura Nappe overthrust, Poręba Górna creek (Figs. 4, 5C), GPS position: N 49° 35, 886’, E 20° 03,699’. Thickness. Variable, from 10 m in Poręba - Koninki thrust sheet (Raca subunit) to ca. 50 m in the Konina - Lubomierz thrust-sheet (Bystrica subunit; see also Oszczypko-Clowes & Oszczypko, 2004). Thickness amounts to 100 m close to the Mogielica Hill (Figs. 7, 8). Dominant lithology. Thin- to medium-bedded turbidites with intercalations of grey-bluish and grey-yellowish pelites (Fig. 6C). The formation is composed of 3-5 cm thick, very fine, calcareous sandstones, displaying Tc and Tcd Bouma intervals. Sporadically, 10-15 cm thick, fine-grained sand- stones with Tbc+conv intervals are observed (Fig. 9A-C). Greenish and yellowish marly shales, usually bioturbated, a few to tens of centimetres thick, reveal very fine, parallel lamination. In the middle and upper parts of the formation, a complex (a few metres thick) of thin- to thick-bedded sand- stones and marls, with rare intercalations of red shales and red marls has been observed (Oszczypko et al., 1991). The uppermost portion of the formation displays thin-to me- dium-bedded turbidites with numerous, 5-7 to 30 cm thick, intercalations of turbiditic limestones (Cieszkowski et al., 1989). The marls are rich in Helminthoida ichnosp. (= Nere- ites irregularis (Schafhautl). FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 37 Fig. 9. A - Typical development of the basal of the Białe Formation, Kamienica River at Białe; B - Cross-laminated, medium-bedded sandstone of the Białe Formation; Kamienica River at Białe; C - Thin-bedded turbidites of the Białe Formation at Półrzeczki; D - Thick- bedded sandstones of the Jaworzynka Formation; Półrzeczki section; E - Thick-bedded sandstones of the Szczawina Sandstone Formation in the Koninki section; F - Thick-bedded sandstones of the Szczawina Sandstone Formation in the Koninki section 38 N. OSZCZYPKO ET AL. In the Poręba section, the lower part of the formation (see Oszczypko-Clowes & Oszczypko, 2004) is composed of grey-green, non-calcareous shales, a few metres thick. The middle part of the sequence is dominated by dark-grey mudstone/siltstone couplets and very fine-grained, thin- bedded, muscovite sandstones. The upper part of this se- quence is composed of thin- to medium-bedded sandstones, intercalated by dark-grey silty/shaly couplets (green/yel- lowish if weathered). The yellowish siltstones are often cal- careous and strongly bioturbated (Helminthoida ichnofa- cies; Cieszkowski et al., 1999). In the Poręba Górna section, the Białe Formation, including a few thin intercalations of red shales, resembles the Hałuszowa Formation from the Zasadne section (Oszczypko-Clowes & Oszczypko, 2004). The Białe Formation reveals a coarsening and thicken- ing upward sequence, which contains heavy minerals of zircone-tourmaline-rutile, partly with chromite spinels (e.g., Lubomierz section, see Oszczypko & Salata, submitted to print). The sandstones of the Białe Formation reveal palaeo- transport from the SE. Boundaries. Lower boundary - at the top of the last thick intercalation of red shale package belonging to the Mali- nowa Shale Formation. Upper boundary - at the bottom of thick-bedded sandstones of the Szczawina Sandstone For- mation (Figs 7, 8). Geological age. Early-middle Campanian in the studied area (Bąk & Oszczypko, 2000; Malata, 2001), and late Campanian-early Maastrichtian in the Młyńczyska area (Malata et al., 1966). Distribution. The Bystrica and Raca subunits in the Polish part of the Magura Nappe. Equivalents. The Hałuszowa Formation in the Krynica subunit (Birkenmajer & Oszczypko, 1989) and the Bystrica subunit (Zasadne section). Jaworzynka Formation (a new name) History: Sikora and Żytko (1959) described the biotite- feldspar beds in the marginal part of the Magura Nappe, in the Beskid Wysoki Range (Siary subunit). These beds are characterized by thick-bedded sandstones of grey (dirty)- green colour, medium to coarse-grained, with feldspars and admixture of glauconite and biotite. The thick-bedded sand- stones are accompanied by thin intercalations of grey-green and black argillaceous shales with siderite concretions. Ac- cording to Sikora and Żytko (1959), the age of the biotite- feldspar beds is the Late Cretaceous-Palaeocene, and their thickness reaches 200 m. Burtan (1973) named this unit as the Biotite beds from Jaworzynka. The name was given after the village Jawo- rzynka, which is located SW of Żywiec. In the stratotype area (marginal part of the Magura Nappe SW of Żywiec), the Biotite beds are developed as thin to medium-bedded, flysch deposits. These beds were also described by Burtan et al. (1978) from the southern and eastern margins of the Mszana Dolna tectonic window, close to the Półrzeczki vil- lage. Polish name: formacja z Jaworzynki. Type area. Marginal part of the Magura Nappe, SW of Żywiec. Thickness. Variable, ca. 150-200 m. Reference sections: Półrzeczki-Jurkowa creek (Figs 3, 5A) and Koninki creek. Dominant lithology. In the Półrzeczki area, the Ja- worzynka Formation is not homogenous in respect to lithol- ogy. Its lower part, ca. 50 m thick, is represented by thick-to very thick-bedded, green-grey, non-calcareous sandstones and fine-grained conglomerates, dominated by quartz and metamorphic pebbles with subordinate admixture of biotite and glauconite (Fig. 9D).The sandstones are intercalated by grey-greenish, non-calcareous shales. This part of the for- mation displays flute casts showing palaeotransport from WWN and W. The upper part of the formation, up to 150 m thick, is composed of thick-bedded, medium- to fine- grained muscovitic sandstones, which display palaeotrans- port from SE. These sandstones resemble the Szczawina Sandstone lithofacies (Fig. 7). In the Koninki area, this for- mation is represented by a 5-8 m thick, fining and thinning upward sequence. The lower part of this sequence, 3-4 m thick, is composed of thick-bedded sandstones (50-150 cm), very coarse- to medium-grained, sometimes amalga- mated with Tab Bouma intervals. The thick-bedded sand- stones (partly glauconitic) from this section reveal some similarities to those from the Jaworzynka beds of the Gry- bów Unit, displaying similar palaeotransport directions, from the NW and SE. Boundaries. Lower boundary - transitional, from thin- bedded turbidites of the Białe Formation to thick-bedded sandstones. Upper boundary - sharp, thick-bedded sand- stones against the thin-bedded turbidites of the Ropianka Formation (Fig. 7). Distribution. The Raca and Siary subunits of the Magura Nappe in Poland; Grybów Unit in the Polish part of the Western Carpathians. Geological age. Middle Campanian to early Maastrichtian. Equivalents. Biotite-feldspar beds (Sikora & Żytko, 1959; Biotite beds from Jaworzynka (Burtan et al., 1978, pro parte), partly Solan Formation in Moravia (Svabenicka et al., 1997), Szczawina sandstones (Sikora & Żytko, 1959; Cieszkowski et al., 1989; Oszczypko, 1992a, b; Malata et al., 1996), Szczawina sandstones of the Raca subunit (Pivko, 2002). Szczawina Sandstone Formation (a new name) History. The Szczawina sandstones have been described by Sikora and Żytko (1959) in the Beskid Wysoki Range (Raca subunit). This lithostratigraphic unit is commonly used in many publications for the description of the Upper Seno- nian-Palaeocene, thick-bedded, muscovite sandstones (Bieda et al., 1963; Geroch et al., 1967; Sikora, 1971; Cieszkowski et al., 1989; Oszczypko, 1992a, b; Malata et al., 1996). Recently, in the northern part of the Orava area (W Slovakia), Pivko (2002) has distinguished the Szcza- wina sandstones in two different positions: as a member of the Ropianka Formation in the Bystrica subunit, and as a formation between the Cebula and Ropianka formations in the Raca subunit. Name. After Szczawina Hill in the Beskid Wyspowy Range (see Fig. 2 in Sikora & Żytko, 1959). Polish name: for- macja piaskowców szczawińskich. Type area. Central part of the Magura Nappe, south-west of FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 39 Żywiec (Sikora & Żytko, 1959) and the southern part of the Beskid Wyspowy Range (Oszczypko et al., 1991; Malata et al., 1996). Reference section. In the Beskid Wysoki Range type area, the best exposures of the Szczawina Sandstone Formation are known from the nothern slope of the Pilsko Hill (1557 m) and the top of the Szczawina Hill (1356 m) (see Fig. 2 and Plate XXI in Sikora & Żytko, 1959). The following type areas from the Beskid Wyspowy Range type are recom- mended: the section along the right bank of the Kamienica River, between Białe and Bukówka hamlets (Figs 3, 5A; see also Oszczypko et al., 1991; Cieszkowski et al., 1989), Koninki and Poręba Górna (Figs 4, 5C; see also Oszczypko et al., 1999; Oszczypko-Clowes & Oszczypko, 2004), GPS position: N 49° 35, 920’, E 20° 04, 997’ and 49° 35, 688’, E 20° 03, 416’ respectively. The very good exposures are also known from the Konina (Figs 4, 5B), Zasadne (Malata & Oszczypko, 1990; Cieszkowski et al., 1992, Malata et al., 1992), and Lubomierz sections (Cieszkowski et al., 1992). Thickness. Variable, from 20 m in the Poręba Górna area (Raca subunit), to 80-350 m in Zasadne, Mogielica Hill, Ja- sień Hill, and Kobylica Hill (Bystrica subunit) (Figs 5, 6). Subdivision. In the Mogielica and Krzysztonów sections (Figs 3, 5A, 7), within the Szczawina Sandstone Formation, the Krzysztonów Member can be distinguished. This Mem- ber, 50-80 m thick; is composed of thin-bedded turbidites. Dominant lithology. Mainly thick-bedded, grey-green sandstones with thin intercalations of shales. The thickness of sandstone beds varies from 0.5-0.6 m to a few metres (Figs 9E, F). The sandstones are coarse- to fine-grained, lo- cally with small pebble admixture. The conglomerate beds are locally frequent in the uppermost portion of the forma- tion. The sandstones are composed of quartz, clasts of meta- morphic rocks, and feldspars. The characteristic feature of the formation is a considerable content of mica flakes (mainly muscovite) and small admixture of glauconite. The sandstones are carbonate-cemented. The sandstone and con- glomerate beds are separated by layers of green, black, lo- cally red, argillaceous shales with intercalations of thin to medium-bedded sandstones. Its basal portion, ca. 25 m thick, is dominated by thin- to thick-bedded calcareous sandstones with intercalations of turbidite limestones, marls and, locally, red shales. Flute-cast (Fig. 10A) measurements display palaeotransport from the south-east. This part of the sequence resembles the Kanina beds (see Cieszkowski et al., 1989). The Kanina-like flysch passes upwards into thick-bedded sandstones of the Krzysztonów Member (for details - see below). In the Poręba Górna area (Raca subunit), the Szczawina Sandstone Formation, at least 20 m thick, is dominated by thick and very thick-bedded (40-250 cm), medium to very coarse grained sandstones with slightly carbonate cement. The basal parts of the beds are composed of light-grey, quartz-glauconitic, coarse-grained sandstones, while grey, calcareous sandstones and mudstones, rich in flakes ofmus- covite and coalified plants, are typical at the top of the beds. The muscovite sandstones display palaeotransport also from SE. Boundaries. Lower boundary - transitional, from thin-bed- ded turbidites of the Białe Formation to thick-bedded sand- stones. Upper boundary - sharp; thick-bedded sandstones against the thin-bedded turbidites of the Ropianka Forma- tion. Distribution. The Bystrica and Raca subunits in the Polish part of the Magura Nappe. Geological age. Middle Campanian-early Palaeocene. Krzysztonów Member (a new name) Name. After Krzysztonów hamlet, between Łososina River and Mogielica Hill in the Beskid Wyspowy Range (see Fig. 5). Polish name: ogniwo z Krzysztonowa. Type area. Exposures along a creek (right tributary of the Łososina River) in the Krzysztonów hamlet (Bystrzyca subunit) (Fig. 5A). Reference section. Right tributary of the Łososina River, north of Jasień Hill (Figs 5A, 7). Thickness. Between 50-80 m (Fig. 7). Dominant lithology. Thick-bedded sandstones (1.0-2.0 m thick), which reveal the Tabc+conv Bouma divisions. The sandstones are very coarse- to fine-grained, muscovitic, with carbonate cement, rich in shale clasts, up to 15 cm in diameter, occasionally armoured. The sandstone beds are intercalated by rare, dark-grey shales, up to a tens cm thick. The sandstones were deposited by palaeocurrents from the SE. Boundaries. Lower boundary - transitional, from medium-bedded turbidites to thick-bedded sandstones. Up- per boundary - transitional; thick-bedded sandstones against the medium and thin-bedded turbidites. Distribution. The Bystrica subunit in the Polish part of the Magura Nappe. Geological age. Maastrichtian. Ropianka Formation History. The name Ropianka beds, established more than 130 years ago (Paul, 1869), has been very often used as an equivalent of the Inoceramian beds. Furthermore, the Ro- pianka Formation was established as a formal lithostrati- graphic unit in the Skole nappe (Kotlarczyk, 1978). The sec- tion regarded as the stratotype of the Ropianka beds was studied by Ślączka & Miziołek (1995). They documented that this section contains deposits of different age (from the Late Cretaceous to Oligocene) belonging to the Dukla and Magura nappes. According to Ślączka and Miziołek (1995), the name “Ropianka beds” should not be applied for the rocks in the Magura Nappe, however, considering long tra- dition of this name, they suggested to use it only for thin-to medium-bedded turbidites of the Upper Inoceramian beds. In this sense, the name of the Ropianka beds was used by Malata et al. (1996). We also support this point of view in the present study. Reference sections. The Jurkowy creek (Figs 3, 5A) in the Półrzeczki village (Raca subunit), and the following sec- tions in the Bystrica subunit: the Jastrzębia creek and upper course of the Jeżowa Woda creek in the Młyńczyska area (Malata et al., 1996), the lower course of the Głębieniec creek in the Szczawa area, the Zasadne section (Malata et al., 1992), the Konina section (Figs 4, 5B), and the middle course of the Koninki creek (Fig. 5C), ca. 150 m higher up of the bridge (Oszczypko et al., 1999; Oszczypko-Clowes & 40 N. OSZCZYPKO ET AL. Fig. 10. A - Flute-casts at the base of the Szczawina Sandstone Formation in the Koninki section; B - Thick-bedded quartzitic sandstone at the bottom of the Ropianka Formation in the Koninki section; C - Thin-bedded turbidites of the Ropianka Formation in the Koninki sec- tion; D - Turbiditic limestone at the top of the Ropianka Formation in the Półrzeczki section; E- Red shales of the Łabowa Shale Forma- tion in the Lubomierz section; F - Variegated shales of the Łabowa Shale Formation in the Półrzeczki section FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 41 Oszczypko, 2004), GPS position:N 49° 35, 746’, E 20° 04, 786’; top of the section: 49° 37, 057’, E 20° 14, 536’. Thickness. Variable, up to 250 m in the Raca subunit and 80-100 m in the Bystrica subunit (Figs. 7, 8). Dominant lithology. Lithological features are different in the Raca and Bystrica subunits. The lower part of the Ro- pianka Formation is composed of thin- to medium-bedded turbidites with subordinate intercalations of thick-bedded (0.6-1.0 m), coarse- to medium-grained, parallel-laminated sandstones (Fig. 10B-D). In this part of the sequence, a 8-cm thick intercalation of red, calcareous shales has been observed. Thin- to medium-bedded sandstone beds (5-35 cm) are mainly fine- to very fine-grained, calcareous, mus- covitic, with parallel, cross and convolute lamination. Grey- ish-green sandstones are intercalated with dark, muscovitic mudstones, coalified plant flakes, and dark-grey and blue, usually carbonate-free shales. Locally, in the upper part of the formation, intercalations of dark-grey, medium-bedded and very fine-grained, glauconite and biotite-rich, non- calcareous sandstones are observed. Single layers of tur- biditic limestones and siderites have also been found. The uppermost part of the formation (ca. 50-70 m thick) dis- plays a sequence of zebra-like, thin-bedded turbidites (Tcd,Td Bouma intervals), with light-grey mudstones and dark-grey-coloured sandstones. The mudstones are often bioturbated. In the Bystrica subunit (Figs 7, 8), this part of the for- mation contains locally frequent, thin intercalations of red shales (see Młyńczyska, Zasadne, Koninki, Konina). Flute- cast measurements display palaeotransport from WWN in the lowermost portion of the formation (Półrzeczki area, Raca subunit) and from to EES-SSE in the Bystrica subunit (and also in the upper part of the Półrzeczki area of the Raca subunit). The Ropianka Formation contains zircone-tour- maline-rutile heavy minerals (Oszczypko & Salata, sub- mited to print). Boundaries. In the Raca subunit, lower boundary is transi- tional from thick-bedded (60-80 cm) sandstones of the Ja- worzynka Formation to medium-thin-bedded turbidites, whereas in the Bystrica subunit, this boundary is sharp, from thick-bedded sandstones of the Szczawina Sandstone Formation to very thin-bedded turbidites with intercalation of red shales. The upper boundary is sharp in both subunits, against the first few metres thick layer of the variegated shales belonging to the Łabowa Shale Formation. Geological age. Maastrichtian-Palaeocene. Equivalents. Upper part of the Solan Formation in Moravia (Svabenicka et al., 1997), Ropianka beds (Golonka & Wójcik, 1978a, b; Malata etal., 1996), Ropianka Formation (Pivko, 2002). BESKID GROUP This group was distinguished in the Krynica subunit (for details - see Birkenmajer & Oszczypko, 1989). £abowa Shale Formation Remarks. The deposits belonging to the Łabowa Shale For- mation (Oszczypko, 1991) occur in the Półrzeczki area (Fig. 3) as well as at the southern margin of the Mszana Dolna tectonic window (Oszczypko et al., 1999; Oszczypko- Clowes & Oszczypko, 2004), in a narrow belt between Olszówka and Lubomierz (Fig. 4). The lowermost portion of the formation is represented by red shales (Fig. 10E-F), a few metres thick, passing upwards into very fine-bedded turbidites. Very fine-grained, green, carbonate- free sand- stones (with Tc Bouma interval) pass upwards into green shales, and finally to red shales, mainly soft and free of car- bonates, a few cm thick. In the Poręba Górna area, the low- ermost part of this formation contains two layers of thick- bedded sandstones (up to 2 m) and intercalations of grey marls. These sandstones reveal palaeotransport from ESE. Thick layers of the red shales are known from the middle part of the Lubomierz village (Fig. 10E). In the Poręba Górna and Lubomierz sections, the thickness of the forma- tion attains 50 m. In the Półrzeczki area, the formation oc- curs in a broad synclinal zone, in the centre of the village, and in a narrow belt on the southern slope of Kobylica hill. In the Jurkowa creek, the lowermost portion of the forma- tion is represented by a few metres thick sequence of red shales, passing upwards into very thin-bedded turbidites. The turbidite sequence usually begins with thin-bedded (1-6 cm), very fine-grained (Tc), green, carbonate-free sandstones, passing up to green shales, a few centimetres thick, and finally to thin package of red shales, also a few centimetres thick. The shales are mainly soft and carbonate- free. In the middle part of the formation, 2-3 m thick pack- age of red shales occurs. Subordinately, green or blue shales with intercalations of thin-bedded sandstones are observed (Fig. 10F). Thickness of the formation varies from a few dozen metres up to 200 m in the Półrzeczki section. Distribution. In all the facies-tectonic subunits of the Ma- gura Nappe, with exception of the Krynica subunit (see Bieda et al., 1963, Oszczypko, 1991, Leszczyński & Uch- man, 1991). Geological age. Early Eocene. Beloveza Formation Remarks. The Beloveza Formation (Oszczypko, 1991) is very well exposed along the southern margin of the Mszana Dolna tectonic window (Oszczypko et al., 1999; Osz- czypko-Clowes & Oszczypko, 2004). This formation is composed of thin- to medium-bedded turbidites (Tc+conv. and Tcd Bouma intervals). The shales, which vary in colour, distinctly prevail over sandstones. The yellowish and brown shales are usually calcareous, while the green ones are, as a rule, carbonate-free. The accompanying medium-bedded (20-40 cm), Tbc sandstones occur less frequently. Thick- ness of this formation reaches 50-120 m (Figs 7, 8). In the Półrzeczki area, the Beloveza Formation crops out along a narrow depression between Bania and Kiczora hills (Fig. 3), and in the Łososina River in the Półrzeczki village. In the basal part of the formation, a sequence of alternating layers of various coloured shales occurs. A few intercalations of red shales have also been observed in this part of the sec- tion. The accompanying muscovitic sandstones are very fine-grained and thin-bedded (5-12 cm). The medium- bedded (20-40 cm), Tbc sandstones appear subordinately in the Jurkowa creek. In the Półrzeczki area, the thickness of the Beloveza Formation reaches no more than 50 m. 42 N. OSZCZYPKO ET AL. Bystrica Formation Remarks. The Bystrica Formation (Oszczypko, 1991) oc- curs in a narrow syncline between Bania and Kiczora hills and SE of Kobylica Hill. This formation comprises thin- to medium-bedded turbidites of the Beloveza-lithotype with intercalations of the Łącko Marls. The marls are massive, sometimes silicified, brown or blue to grey and whitish as weathered. The thickness of individual beds of the Łącko Marls ranges from 2 to 5 m. The intercalations of the “Be- loveza-type” flysch are 0.5 to 2 m thick. The thickness of the formation can be roughly estimated at 50 m (Figs. 7, 8). BIOSTRATIGRAPHY FORAMINIFERA Several stratigraphical zonal schemes, based on the deep-water agglutinated foraminifera (DWAF) have been proposed for the Cretaceous-Palaeogene deposits of the Outer (Flysch) Carpathians (e.g., Morgiel & Olszewska, 1981, Geroch & Nowak, 1984; Olszewska, 1997). Unfortu- nately, the distinguished zones coincide poorly with chro- nostratigraphic scale due to scarcity of calcareous nanno- plankton and planktonic foraminifera in the Upper Creta- ceous-Palaeocene sediments. The studied succession includes practically only non- calcareous deep-water sediments; thus, the DWAF are the base for the local biostratigraphy. Planktonic foraminifera, in most cases redeposited within diluted gravitational flows, occur only as single specimens. The distinguished biostratigraphical zones are based on the cosmopolitan DWAF species, used also in the other zo- nal schemes, both for the Outer Carpathians (Geroch & Nowak, 1984; Bubik, 1995; Malata et al., 1996, Bąk et al., 1997; Olszewska, 1997; Bąk, 2004), Northern Atlantic, and Western Tethys (Kuhnt et al., 1992; Kuhnt & Kaminski, 1997). However, definitions of these zones using the same index species are different in the particular zonal schemes (cf. summary in Bąk, 2004). The chronostratigraphy is based on comparisons with the stratigraphic ranges of identified species in the North Atlantic and the Western Tethys. The Cretaceous part of the studied succession has been compared with the chronostra- tigraphy by Gradstein et al. (1994), and the Palaeogene with a time scale of Berggren et al. (1995). Deep-water agglutinated foraminiferal zones Plectorecurvoides alternans Interval Zone Definition: Lower boundary - first appearance of Plectore- curvoides alternans (Noth) - not observed in the studied succession; upper boundary - the first occurrence (FO) of Bulbobaculitesproblematicus (Neagu). Remarks: index taxon accompanied by Hippocrepina de- pressa Vasicek, Pseudonodosinella troyeri (Tappan), Plec- torecurvoides irregularis Geroch, and Gerochammina stan- islavi Neagu. Age: late Albian-early/middle Cenomanian. Bulbobaculites problematicus Interval Zone Definition: Lower boundary - the FO of Bulbobaculites problematicus (Neagu); upper boundary - the FO of Uvi- gerinammina jankoi Majzon. Remarks: index taxon accompanied by Caudammina crassa (Geroch), Recurvoides imperfectus Hanzlikova, Thalman- nammina neocomiensis Geroch, Plectorecurvoides alter- nans (Alth), P. irregularis Geroch and Gerochammina stan- islavi Neagu. Age: Middle Cenomanian-Cenomanian/Turonian bound- ary. Uvigerinammina jankoi Interval Zone Definition: Lower boundary - the FO of U. jankoi; upper boundary - the FO of Caudammina gigantea (Geroch). Remarks: in the lower part of the zone the index species is very numerous. The species known from the abyssal oce- anic deposits such as ?Praecystammina globigeriniformis Krasheninnikov, Trochammina gyroidinaeformis Krashen- ninikov are relatively frequent in this part of the zone. Other abyssal species, such as Pseudobolivina cuneata Krashen- ninikov and P. munda Krashenninikov may be also present. The upper part of the zone is characterized by the abundant presence of Gerochammina spp. with small amount of the index taxon. Rzehakina inclusa (Grzybowski) has its FO in the uppermost part of the zone. Age: Turonian-early Campanian. Uvigernammina jankoi-Caudammina gigantea Concurrent Range Zone Definition: Lower boundary - FO of Caudammina gigantea (Geroch); upper boundary - last occurrence (LO) of Uviger- nammina jankoi Majzon. Remarks: A change in the DWAF assemblage is recorded in this zone by the disappearance of Gerochammina typical for the red facies and more frequent occurrence of siliceous- walled taxa. Caudammina gigantea Partial Range Zone Definition: Lower boundary - the LO of U. jankoi Majzon; upper boundary - the FO of Remesella varians (Glaessner). Remarks: the appearance of the index taxon may be con- nected with the lower-middle Campanian event (LMCE). The index taxon is often accompanied by frequent Caudam- mina ovulum (Grzybowski). In the Maastrichtian C. gigan- tea is less frequent. Age: Campanian-early-?middle Maastrichtian. Remesella varians Interval Zone Definition: Lower boundary - the FO of R. varians; upper boundary - the FO of Rzehakinafissistomata (Grzybowski). Remarks: Kuhnt and Moullade (1991) defined the lower boundary of this zone as middle-late Maastrichtian in the North Atlantic. In the Zumaya section (Spain), Kuhnt and Kaminski (1997) distinguished the R. varians subzone) in the upper Maastrichtian. According to Olszewska (1997) R. varians has its FO in the early Maastrichtian. Age: middle-late Maastrichtian. FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 43 Rzehakina fissistomata Taxon Range Zone Definition: range of R. fissistomata. Remarks: Annectina grzybowskii (Jurkiewicz) is a very characteristic species of this zone and in case of absence of Rzehakina fissistomata may be regarded as an equivalent in- dex taxon. The FO of the Rzehakina fissistomata (Grzybowski) is close to the Cretaceous /Tertiary boundary in the abyssal non- calcareous environments, as it was confirmed on the basis of integrated biostratigraphical studies in the Magura Nappe (Czech part of the Outer Carpathians: Bubik et al., 1999).The LO of this taxon is within the late Palaeocene, however it has not been precisely defined. Age: Palaeocene. Glomospira div. sp. Acme Zone Definition: This zone corresponds to the numerous occur- rence of Glomospira spp. Remarks: Numerous occurrence of small specimens of G. charoides (Jones & Parker) and G. gordialis (Jones & Parker), accompanied by numerous Paratrochamminoides, Trochamminoides, Recurvoides, Karrerulina and tubular forms; all of them have small dimensions, against underly- ing and overlying assemblages. This assemblage has been distinguished by Morgiel & Olszewska (1981) in the Outer Carpathians, and since that time it has been in use in the North Atlantic and the Western Tethys zonal schemes. Age: early Eocene. Saccamminoides carpathicus Interval Zone Definition: Lower boundary: the FO of Saccamminoides carpathicus; upper boundary: the FO ofReticulophragmium amplectens - not observed in the studied succession. Remarks: Index taxon is rare, accompanied by relatively nu- merous Recurvoides spp., Paratrochamminoides spp., Glo- mospira spp., and Karrerulina conversa (Grzybowski). Cal- careous benthic species Nuttallides truempyi (Nuttall) has its FO. Age: late early Eocene. CALCAREOUS NANNOFOSSILS Recognised calcareous nannoplankton zones UC 15 Nannofossil Zone Definition: Interval between the FO of Misceomarginatus pleniporus to the LO of Eiffellithus eximius. Author: Burnett (1998). Age: Upper early Campanian throughout upper part of late Campanian. Remarks: The zone is dominated by the presence of genus Watznaueria and Micula. Occurrence of C. aculeus may in- dicate for at least second subzone of this Zone named by TP ** Burnett (1998) UC 15B . From among other taxa, the spe- cies of Broinsonia parca, Prediscosphaera ponticula, and the genus Arkhangelskiella prevail. This subzone was dis- tinguished primarilyonly for the Tethyan-Intermediate province for the Indian Ocean (Burnett, 1998). Locality: Półrzeczki, Jaworzynka Beds. Markalius inversus Nannoplankton Zone (NP 1) Definition: Interval between the LO of Arkhangelskiella cymbiformis and the FO of Cruciplacolithus tenuis. Author: Hay and Mohler (1967) emended by Martini (1971). Age: early Danian. Remarks: The species of B. sparsus is common in this Zone. Placozygus sigmoides first occurs within this Zone. Cruci- placolithus primus has its first entry in the upper part of NP 1 Zone what may be compared with the base of the Cyclage- losphaera alta nannoplankton Zone (NNTp2) according to Varol (1998). It is worth to add that all NP 1 Zone lays be- low the FO of Coccolithuspelagicus which is very common in the Paleocene sediments of the Ropianka Formation. Locality: Półrzeczki, the upper part of the Ropianka Forma- tion. Chiasmolithus danicus Nannoplankton Zone (NP 3) Definition: Interval between the FO of Chiasmolithus dani- cus and the FO of Ellipsolithus macellus. Author: Martini (1970). Age: middle Danian. Remarks: Although the index species has not been found, the presence of genera Chiasmolithus and the occurrence of Coccolithus pelagicus are characteristic for this zone. Locality: Półrzeczki, the upper part of the Ropianka Forma- tion. Heliolithus kleinpellii Nannoplankton Zone (NP 6) Definition: Interval between the FO of Heliolithus kleinpel- lii and the FO Discoaster mohleri. Author: Mohler & Hay in Hay et al. (1967). Age: late Palaeocene (Thanetian). Remarks: This zone is tentatively introduced herein, due to the lack of zone-marker species. The only occurrence of the Sphenolithus cf. anarrophus which ranges from NP 6 to NP 9 may indicate at least that age. This zone is also character- ised by the occurrence of the C. pelagicus and genus Cycla- gelospahera or Elipsogelosphaera. State of preservation is rather poor, the re-worked Cretaceous species are much bet- ter preserved. Locality: Półrzeczki, the upper part of the Ropianka Forma- tion. Tribrachiatus contortus Nannoplankton Zone (NP 10) Definition: Interval between the FO of Tribrachiatus bram- lettei and LO of Tribrachiatus contortus. Author: Hay (1964). Age: earliest Eocene (early Ypresian). Remarks: This zone is characterised by an occurrence of the genus Tribrachiatus, especially T. orthostylus is often found, what corresponds with upper part of NP 10 Zone (Martini, 1971). FO of this species is used by Varol (1998) for defining the base of the NNTe1 Zone. Locality: Półrzeczki, the upper part of the Ropianka Forma- tion. 44 N. OSZCZYPKO ET AL. Fig. 11. Lithostratigraphic log of the Bystrica subunit in the Jasień - Białe - sition of micropalaeontological samples Głębieniec area (Bystrica subunit; Magura Nappe) with po- Thick-bedded turbidites and fluxoturbidites Turbiditic marls and limestones Thin- bedded turbidites Variegated shales Spotty shales Micropalaeontological samples Micropalaeontological samples barren of Foraminifera M-U.C. - Middle-Upper Cenomanian UA-LC - Upper Albian - Lower Cenomanian R.v. - Remesella varians Zone B.p. - Bulbobaculites problematicus Zone Pl.a. - Plectorecurvoides alternans Zone FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 45 Nannotetrina fulgens Nannoplankton Zone (NP15) Definition: the base of the zone is defined by FO of Nanno- tetrina fulgens, and the top by the FO of Rhabdolithus gla- dius. Author: Hay in Hay et al. (1967), emend. Martini (1970), Bukry (1973). Age: middle Eocene. Remarks: This zone was identified in sample 46/00/N. The zone assignment is based on the presence of genus Nanno- tetrina. According to Perch-Nielsen, the species belonging to Nannotetrina are dificult to distinguish in the heavily overgrown assemblages. In such case, the FO of Nanno- tetrina can be used to approximate theNP14/15 boundary in badly preserved material. The assembage does not contain the species of Chiasmolithus gigas. The interval between the FO and the LO of Chiasmolithus gigas defines Bukry’s subzone CP13b (Bukry, 1973). Subzone CP13b is the equivalent of middle part Martini’s NP15 zone (Martini, 1970). Thus, it can be concluded that the assemblage repre- sents either the lowest or highest part of NP15 zone. At the same time, no species indicating NP16 was observed. Discoaster tani nodifer Nannoplankton Zone (NP16) Definition: the base of the zone is defined by the LO of Rhabdolithus gladius, and the top by the LO of Chiasmo- lithus solitus. Author: Hay et al. (1967), emend. Martini (1970). Age: middle Eocene. Remarks: This zone was identified in samples 63/98/N, 9/98/N, 45/00/N, Lubomierz, Beloveza Formation. The zone assignment is based on the presence of Cyclicargo- lithus floridanus. At the same time, Discoaster tanii is not present. According to Aubry (1986), the FO of Cyclicargo- lithus floridanus takes place in zone NP16. BIOSTRATIGRAPHY VERSUS LITHOSTRATIGRAPHY Jasień Formation The foraminiferal assemblages are composed entirely of agglutinated taxa, varying in abundance and state of pres- ervation (Fig. 17: samples: 93/3, K1, K2, 93/4). The oldest assemblage is relatively poor and of low number of specimens and species diversity. However, there are present a few stratigraphically important species such, as Hippocreppina depressa Vasicek (Fig. 19 A), Plectore- curvoides alternans Noth (Fig. 19 F, and P. irregularis Geroch. In the succeeding samples, apart from the already mentioned species, new taxa appear and species diversity and number of specimens grow. Pseudonodosinella troyeri (Tappan) (Fig. 19 C) is relatively numerous, the other spe- cies, such as Haplophragmoides falcatosuturalis Neagu, Buzasina pacifica (Krasheninnikov), Trochammina vocon- tiana Moullade, and Gerochammina stanislavi Neagu (Fig. 19 J) are less numerous but also important for age determi- nation. A single specimen of Bulbobaculites problematicus (Neagu) has also been noticed. The age of these assem- blages may be included within the late Albian-middle Ce- nomanian interval due to the ranges and co-occurrence of the mentioned taxa. The first occurrence (FO) of P. alter- nans and H. falcatosuturalis is in the Late Albian (Neagu 1990), while the last occurrence (LO) of T. vocontiana has been noticed at the Albian/Cenomanian boundary. Accord- ing to Geroch and Nowak (1984) and Bąk (2000), B. prob- lematicus has its FO in the Middle Cenomanian, whereas according to Olszew- ska (1997) it marks the Albian/Ceno- manian boundary. In the Jaworki Formation of the Pieniny Klippen Belt, Plectorecurvoides alternans Zone is corre- lated with the planktonic zones of the Early Cenomanian (Bąk, 1998). Outside the Polish Carpathians, the FO of B. problematicus varies; in the Romanian Carpathians it is no- ticed at the Albian/Cenomanian boundary, while in the mar- ginal and oceanic basins it is regarded as a marker of the Ce- nomanian/Turonian boundary (Kuhnt & Kamiński, 1990). The data mentioned above suggest that this species had ap- peared first in the deep, flysch basins and then migrated into other environments. The top of the Jasień Formation (Fig. 11, s. 93/4a) yielded an assemblage with relatively numerous B. prob- lematicus (Fig. 19 D, E), accompanied by Thalmannam- mina neocomiensis Geroch, Plectorecurvoides irregularis Geroch, and less abundant Caudammina crassa (Geroch) (Fig. 19 B), Recurvoides imperfectus Hanzlikova, Plectore- curvoides alternans Noth, and Trochammina gyroidinae- formis Krashenninikov. A few juvenile specimens of Uvi- gerinammina jankoi Majzon have also been recorded. This assemblage may be correlated with the B. problematicus Zone representing the Middle-Upper Cenomanian (cf. Bąk, 2000) and Uvigernammina jankoi Zone, whose base is close to the Cenomanian/Turonian boundary (Geroch & Nowak, 1984).Thus, the Jasień Formation belongs to the P. alter- nans, B. problematicus and the base of U. jankoi zones, cor- related with the later Albian-early Turonian interval. Malinowa Shale Formation The Malinowa Shale Formation of the Bystrica subunit, studied in the Jasień-Białe-Głębieniec and Koninki sections (Figs 11, 14), consists of exclusively agglutinated assem- blages of foraminifera displaying medium species diversity from about 20 to 25 species (Figs 16, 17). In the lower part of the unit, specimens are relatively small in size. Uvigeri- nammina jankoi Majzon (Fig. 19 K, L) is the most charac- teristic species, usually represented by numerous speci- mens, and the other two genera Gerochammina (Fig. 19 I, J) and Recurvoides are generally also abundant. In some sam- ples (Fig. 11, s. 72/99, 45/87), Hormosina excelsa Dylą- żanka, Ammosphaeroidinapseudopauciloculata (Majtliuk), and Trochammina gyroidinaeformis Krashenninikov (Fig. 19 M-O) are also numerous. The species Pseudobolivina cuneata Krashenninikov and P. munda Krashenninnikov (Fig. 19 G, H), though very rare, are also worth mentioning. These latter taxa as well as Trochammina gyroidinoides were described from the oceanic abyssal clays (Krashen- ninikov, 1973, 1974), and in the Magura Nappe were no- ticed for the first time in the Zasadne section (Malata & Oszczypko, 1990). Thus, the presence of these species sug- 46 N. OSZCZYPKO ET AL. Fig. 13. Lithostratigraphic log of the Raca subunit in the Półrzec- zki area (Mogielica Range), with the position of samples. For lithological explanations - see Fig. 11 Fig. 12. Lithostratigraphic log of the Raca subunit in the Koninki area (Mogielica Range) with the position of samples. For lithologi- cal explanations - see Fig. 11 gests some similarities to the abyssal type of deep-water ag- glutinated foraminifera (Kuhnt & Kaminski, 1989). The species Uvigerinammina jankoi Majzon was used as a stratigraphic marker both in the North Atlantic and the Tethyan realm within every zonal scheme (e.g., Geroch & Nowak, 1984; Moullade et al., 1988; Kuhnt et al., 1989; Kuhnt & Moullade, 1991; Bąk, 2000). Its FO datum was noted in most localities just above or in the highest part of anoxic deposits representing the Cenomanian-Turonian boundary event. The LO of U. jankoi was recorded from the early Campanian through the middle/late Campanian (e.g., Alexandrowicz, 1975; Geroch & Nowak, 1984; Moullade et al., 1988; Kuhnt et al., 1989; Neagu, 1990; Kuhnt & Kamin- ski, 1997; Bąk, 2000). Due to lack of planktonic foramini- fera and calcareous nannoplankton and taking into account the occurrence of U. jankoi, the age of the Malinowa Shale Formation is stated here broadly within the Uvigerinam- mina jankoi Zone sensu Geroch & Nowak (1984), corre- lated with the Turonian through the early Campanian. In the Raca subunit sequence, studied both in the Półrzeczki and Koninki sections (Figs. 12, 13), the fora- miniferal assemblage is very similar to that from the Bytrica FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 47 subunit (Figs. 15, 18). Deep-water agglutinated foramini- fera are the only component in these deposits, associated by moulds of Radiolaria. DWAF are poorly and medium diver- sified (up to 26 taxa per sample), with dominance of reddish-walled specimens of Recurvoides. The latter taxon makes up to 65 percent of the whole assemblage (mean 47%). Reddish-walled specimens of Gerochammina, Tro- chammina, Paratrochamminoides, Reophax and, tubular forms (mainly Rhabdammina) are frequent. The index taxon, Uvigerinammina jankoi has been found only in the lower part of the Malinowa Shale Forma- tion, most probably because of the gradual change of facies and environmental conditions up the section, which have been unfavourable for this taxon. Uvigerinammina jankoi was recorded only from well oxygenated environments with low input of terrigenous material in the Tethys and North Atlantic (Moullade et al., 1988; Kuhnt et al., 1989; Kuhnt & Moullade, 1991; Bąk, 2000). The uppermost part of the Ma- linowa Shale Formation consists of many sandstone and siltstone intercalations, associated with grey-green shales against the true cherry-red shales, practically devoid of coarser material in the lower part of the Malinowa Forma- tion. The lack ofplanktonic foraminifera and calcareous nan- noplankton prevents precise age determination of the for- mation, which is stated broadly as Turonian-early/middle Campanian, similarly to the Bystrica subunit. In the Koninki section (Fig. 12), the upper part of the Malinowa Formation consists of exclusively agglutinated assemblages of foraminifera, displaying medium species di- versity (Fig. 18). The assemblages contain more numerous, in comparison with the underlying Malinowa Shale Forma- tion, siliceous-walled forms (Ammodiscus, Glomospira, Caudammina) with first representatives of rzehakinids. The most characteristic taxa of this assemblage are Rze- hakina epigona (Rzehak), Rzehakina inclusa (Grzybowski), Spiroplectinella dentata (Alth), and single specimens of Uvigerinammina jankoi Majzon. These species enable to state that the Malinowa Shale Formation represents the up- per part of the Uvigerinammina jankoi Zone, most probably correlated with the Santonian-early/middle Campanian (cf. Geroch & Nowak, 1984), on the basis of co-occurrence of these species. The FO of Rzehakina inclusa (Grzybowski) has been documented close to the Santonian/Campanian boundary in deep-water environments (Geroch & Nowak, 1984), and the LO of U. jankoi is considered to occur close to the early-middle Campanian (see discussion above). Białe Formation Foraminiferal assemblages of this formation, studied in the Bystrica subunit of the Jasień-Białe-Głębieniec and Koninki sections (Figs. 11, 14) and in the Raca subunit of the Półrzeczki and Koninki sections (Figs. 12, 13), consist of exclusively agglutinated taxa showing some similarities to those from the Malinowa Shale Formation; displaying however, lower species diversity and abundance. The as- semblages are characterised by a presence of rare specimens of Uvigerinammina jankoi and Rzehakina inclusa (Grzy- bowski) (Figs. 15, 17). Tubular forms and Recurvoides are Fig. 14. Lithostratigraphic log of the Bystrica subunit in the Koninki area, with the position of samples. For lithological expla- nations - see Fig. 11 almost permanent components of assemblages. The FO of Caudammina gigantea (Geroch), which is the index taxon of the next foraminiferal zone, has been noticed in this for- mation. Single specimens of this taxon have been found at the base of the formation (s. 63/97; Fig. 17), occurring to- gether with Uvigerinammina jankoi. The foraminifera recovered from the Raca subunit (Figs 15, 18) represent similar assemblage in relation to its com- position and diversity, however, the base of the formation in the Półrzeczki section is devoid of C. gigantea, against an occurrence of U. jankoi (Fig. 15). On the other hand, the sample taken from the top of the formation (Koninki sec- tion; Fig. 18) does not include U. jankoi. This may suggest that the base of the succeeding Caudammina gigantea Zone occurs in the upper part of the Białe Formation. Index taxon is accompanied there by tubular forms, Saccammina pla- centa (Grzybowski), Glomospirella diffundens (Cushman et Renz), Rzehakina inclusa (Grzybowski), Kalamopsis grzy- bowskii (Dylążanka), Caudammina ovulum (Grzybowski), Paratrochamminoides spp., and Gerochammina spp. Consequently, the lower boundary of the Białe Forma- tion is diachronous. In the Raca subunit, it represents the top of the U. jankoi Zone, and in the Bystrica subunit, it is at the base of U. jankoi - C. gigantea concurrent range Zone (cor- related with the early Campanian; cf. Neagu, 1990; Kuhnt & Moullade, 1991; Bąk, 2000). The upper boundary is also diachronous. It is at the top of the U. jankoi - C. gigantea Zone in the Bystrica subunit and at the base of C. gigantea Zone in the Raca subunit (correlated broadly with the mid- dle Campanian). Jaworzynka Formation Only agglutinated foraminifera have been found in de- posits of the Jaworzynka Formation. Samples are character- ised by the common occurrence of tubular forms of the su- 48 N. OSZCZYPKO ET AL. Fig. 15. Occurrence range chart of the Turonian through early Eocene Foraminifera in the Raca subunit in the Półrzeczki area. Mal Fm. - Malinowa Shale Formation; Hał Fm. - Hałuszowa Formation; B - Białe Formation; Jaworzynka Sd. Fm - Jaworzynka Formation; Łab - Łabowa Shale Formation; Ma - Maastrichtian Lithostrat. units Mal-Hał Fm. B Jaworzynka Sd. Fm. Ropianka Formation Łab. Age Tur-L.Camp. Middle Camp. -Middle Maastr. Ma. Paleocene L.Eoc. FORAMINIFERAL U. jankoi Caudammina gigantea Remesella Rzehakina fissistomata Glomospira AGGLUTINATED varians div. sp. ZONES 03 03 03 03 03 03 CO 03 CO 03 03 CO 'sT 03 03 "vT 03 03 03 03 03 03 03 CO CO CO 03 "śT 'vT "v!- 'nT h- h- h- 03 h- 03 CO CO CO U3 03 CO h- 03 CN 03 CO Ö 03 03 CO c\| 03 CO op CN op Ö 03 CO 03 03 03 03 CD 03 03 03 03 03 Samples (Br, Pół) 03 03 03 03 03 CO 03 CO CO <3 CO CO CO CO 03 CD CO up <3 CO <3 03 CN <3 u5 op <3 op <3 op <3 5 CL CO Op <3 <3 u5 CO CNJ <3 O CO up CO CL <3 CL <3 <3 CL <3 03 CL <3 <3 CL CL CL CVI CL CL op <3 CL <3 CL CL CL CL <3 <3 CL CL CL CL <3 CL <3 CQ CL CL CL CL CQ CL CL CL CL CL CL CL CL CL CL Bathysiphon sp. 1 Nothia excelsa Nothia sp. ■ ■ Hyperammina sp. Hyperam. cf. dilatata Hyperammina gaultina Kalamop. grzybowski Rhabdam. cylindrica Rhabdammina sp. ■ Rhizammina sp. Saccam. grzybowskii Saccammina placenta Saccammina sp. Ammodis. cretaceus Ammodis. tenuissimus Ammodiscus sp. Glomospira charoides Glomospira glomerata Glomospira gordialis Glomospira irregularis Glomospira serpens Glomospirella gaultina Aschemocella grandis Reophax ovuloides Reophax sp. Subr. cf. splendidus Subr. cf. guttifer Pseudonodos. parvula Hormosina crassa Hormosina excelsa Horm. cf. velascoen. Hormosina sp. Caudammina ovulum Caudammina gigantea Rzehakina epigona Rzehak. fissistomata Rzehakina sp. Bulbob. problematicus Haplophr. bulloides Haplophragm. cf. kirki FLYSCH DEPOSITS IN THE BYSTRICA AND RACA SUBUNITS 49 Lithostrat. units Mal-Hał Fm. B Jaworzynka Sd. Fm. Ropianka Formation Łab. Age Tur-L.Camp. Middle Camp. -Middle Maastr. Ma. Paleocene L.Eoc. FORAMINIFERAL U. jankoi Caudammina gigantea Remesella Rzehakina fissistomata Glomospira AGGLUTINATED varians div. sp. ZONES O" O" O" o- o- O- O" o- O- O" O" O" O- CO O" O" O" r- 05 05 h- 05 05 05 O" 05 05 05 h~ CO 05 CO o- 05 05 05 O" 05 05 O- 05 o- 05 O- O" 05 CO O" 05 05 05 0¬ O" Samples (Br, Pół) 05 LO 00 05 05 CO 05 co 05 CD LO 05 CO 05 05 CN 05 05 O CO 05 co 05 LO s 05 eg 05 O 05 05 O" CO 05 CO 05 LO CO eg 05 05 CD Pp 05 CO CO CO CO CO CO CO 05 CD CO up CO CO 05 eg eg eg eg eg eg eg eg eg 05 co 05 '■5 eg 05 CD i ‘"5 i i O m m m CL CL CL CL CL CL CL m CL CL CL CL CL CL CL CL CL CL CL CL CL CL CL CL CL CL CL CL _CL _CL_ CL Q_ _cl _CL_ CL Haplophr. cf. eggeri Haplophr. cf. herbichi Haplophr. walteri 1 Haplophragm. sp. 1 r Recurvoides spp. --- Recurvoidella lamella ? Cribrostommoides sp. Praecystam. globiger. Trochammina deformis Trocham. gyroidinaef. Trochammina sp. - _ --- H Trochamm. variolarius Trochamminoides sp. - _ 1 _ n Paratr. heteromorphus Paratrochammin. spp. _ - _ --- - --- r I --- Spiroplect. spectabilis _ Spiroplectammina sp. Spiroplectinella sp. Uvigerinammina jankoi Gerocham. conversa ■ ■ --- _ Gerochammina tenuis _ Karrerulina coniformis ELL Karrerulina sp. _ --- _ --- Remesella varians Dorothia oxycona Dentalina sp. Lagena sp. Globotruncana sp. r Eoglobigerina trivialis 1 Subb. triloculinoides 1 Parasubb. varianta Parasubb. pseudobull. Planorot. compressa Subbotina sp. Pleurostomella sp. ? Gyroidinoides sp. Cibicidoides sp. Anomalina ekblomi Echinoid spine Radiolaria I □ I m ■ Fish teeth □ Number of specimens 50 N. OSZCZYPKO ET AL. Lithostratigraphic Units Mal. Sh. Fm. B Ropian. £ Age Turon.-E.Camp. C-M. CL LLJ FORAMINIFERAL U. jankoi 1 C. gigantea | 0" 1 Glomospira acme | AGGLUTINATED ZONES Is- Is- LO CO CO CO Samples 5? 03 03 CO 03 03 5? 03 Ö 03 Ö to 106/01 1 57/971