LITHOSTRATIGRAPHY AND BIOSTRATIGRAPHY OF THE UPPER … · LITHOSTRATIGRAPHY AND BIOSTRATIGRAPHY OF THE UPPER ALBIAN–LOWER/MIDDLE EOCENE FLYSCH DEPOSITS IN THE BYSTRICA AND RAÈA

Annales Societatis Geologorum Poloniae (2005), vol. 75: 27–69.

LITHOSTRATIGRAPHY AND BIOSTRATIGRAPHY OF THE UPPERALBIAN–LOWER/MIDDLE EOCENE FLYSCH DEPOSITS

IN THE BYSTRICA AND RAÈA SUBUNITS OF THE MAGURANAPPE; WESTERN FLYSCH CARPATHIANS (BESKID WYSPOWY

AND GORCE RANGES, POLAND)

Nestor OSZCZYPKO1, Ewa MALATA1, Krzysztof B¥K2, Mariusz KÊDZIERSKI1

& Marta OSZCZYPKO-CLOWES1

1Institute of Geological Sciences, Jagiellonian University, Oleandry St., 2a, 30-063 Kraków, Poland

2Institute of Geography, Cracow Pedagogical University, Podchor¹¿ych St., 2, 30-084, Kraków, Poland

Oszczypko, N., Malata, E., B¹k, K., Kêdzierski, M. & Oszczypko-Clowes, M., 2005. Lithostratigraphy andbiostratigraphy of the Upper Albian–Lower/Middle Eocene flysch deposits in the Bystrica and Raèa subunits of theMagura Nappe (Beskid Wyspowy and Gorce Ranges; Poland). Annales Societatis Geologorum Poloniae, 75: 27–69.

Abstract: Lithostratigraphy and biostratigraphy of the Bystrica and Raèa subunits of the Magura Nappe have beenstudied in the southern part of the Beskid Wyspowy Range and on the northern slopes of the Gorce Range (Polishpart of the Western Flysch Carpathians). Six new lithostratigraphic units (Jasieñ Formation, Bia³e Formation,Jaworzynka Formation, Szczawina Sandstone Formation, Krzysztonów Member, and Ropianka Formation) of theUpper Albian–Palaeocene age have been established, and five other units (Malinowa Shale Formation, Ha³uszowaFormation, £abowa Shale Formation, Beloveza Formation, Bystrica Formation) have been additionally described.

The newly created formations as well as the Malinowa Shale Formation and the Ha³uszowa Formation havebeen included to a new Mogielica Group of units (Upper Albian–Palaeocene). This group of units passes upwardsinto the Beskid Group (Eocene–Oligocene).The Mogielica Group, spanning over 40 myrs, represents the turbiditedepositional system, separated by highstand variegated clays which can be correlated with minor sequences interms of sequence stratigraphy.

The following biostratigraphic zones have been recognised in the Cretaceous–Lower/Middle Eocene deposits:Plectorecurvoides alternans, Bulbobaculites problematicus, 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 standardcalcareous 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 theMagura Nappe have been distinguished on the basis of theEocene deposit facies differentiation. These are from thenorth to the south: Siary (=northern Gorlice), Raèa (=south-ern Gorlice), Bystrica (=S¹cz), and Krynica subunits (Fig.1) (for references see Birkenmajer & Oszczypko, 1989).The present paper concerns deposits of the Raèa and By-strica subunits, which build the Beskid Wyspowy Rangeand 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 andthe 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 detailedstratigraphic work based on microfossil studies (foramini-fera and calacareous nannoplankton) by the other authors.The first results of these investigations were presented byMalata et al. (1996), B¹k and Oszczypko (2000), Osz-czypko et al. (1999), Oszczypko (2001), and Oszczypko-Clowes & Oszczypko (2004). Geology of this area was alsoa subject of P. Kruczek’s Msc thesis (1998). All these stud-

ies, supplemented by present investigations, enable us torecognize the stratigraphy and to propose a new litho- andbiostratigraphic subdivisions for the Upper Albian throughthe Lower/Middle Eocene deposits of the middle part of theMagura Nappe in Poland.

This paper presents five formal lithostratigraphic unitsin 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 theco-authors. The biostratigraphy is based mainly on deep-water agglutinated foraminifera (studied by E. Malata andK. B¹k), supplemented by planktonic foraminifera (studiedby K. B¹k) and calcareous nannoplankton (studied by M.Kêdzierski and M. Oszczypko-Clowes).

A part of the formal lithostratigraphic units (the Mali-nowa Shale, Ha³uszowa, £abowa Shale, Beloveza, andBystrica formations) corresponds to those already used inthe syntheses for the other facies-tectonic units of the Ma-gura Nappe (Birkenmajer & Oszczypko, 1989). Some of thegeographical names traditionally used for a long time havebeen left unchanged whenever it was possible. It refers tothe Kanina beds (Burtan et al., 1978; Oszczypko et al.,1991), the Jaworzynka beds (Burtan, 1973; Burtan et al.,1978), the Szczawina Sandstone (Sikora & ¯ytko, 1959;Oszczypko et al., 1991), and to the Ropianka beds. A newunit in the rank of a group comprises formations displayingsimilar lithology and corresponding to the same stage of theMagura Basin evolution. Most of the lithostratigraphic unitsin the studied area have diachronous boundaries. Some ofthe lithostratigraphic units, used in the presented division,occur also in other facies-tectonic units of the MaguraNappe. This paper has been prepared according to the PolishStratigraphical Code (Alexandrowicz et al., 1975, Racki etal., 2004).

STUDY AREA

The presented lithostratigraphic and biostratigraphicsubdivisions are based on detailed studies in two regions be-longing to the Raèa and Bystrica subunits, both located inthe Polish part of the Magura Nappe (Figs. 1, 2). The firstone is situated in the Beskid Wyspowy Range (Figs. 2, 3),including the area between the £ososina and KamienicaRivers, around the hills of Jasieñ (1062 m) and Mogielica(1171 m). The second one is located in the northern part ofthe Gorce Range (Figs 2, 4), in the vicinity of the Koninkiand Porêba Wielka villages.

The studied part of the Beskid Wyspowy Range is builtmainly of the Upper Cretaceous–Lower/Middle Eocenestrata of the Raèa subunit, extending eastwards from theMszana Dolna tectonic window and northwards from theSzczawa tectonic window (Fig. 2) (Œwiderski, 1953; Burtanet al., 1978). This part of the Raèa 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 WyspowyRange (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 (southof the Mszana Dolna tectonic window), the Bystrica subunitconsists of the Upper Cretaceous–Lower/Middle Eocenestrata, 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).

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 – Zg³obice Unit; 16 – Miocene of the Carpathian Fore-deep; 17 – andesite; 18 – studied area. Tectonic-facial subunits of the Magura Nappe: Su – Siary, Ru – Raèa, Bu – Bystrica, and Ku –Krynica

MATERIAL AND METHODS

About 90 samples were collected from the sections ofthe Raèa and Bystrica subunits for foraminiferal analyses(Figs 5, 11–14). The samples were processed by the stan-dard micropalaeontological method. They were boiled andfrozen using Na2CO3 solution, and then washed over a 63µm screen and dried out. In most of the samples, all micro-

fauna from the > 63 µm fraction were picked and mountedonto cardboard microscope slides. The material is hosted inthe Institute of Geological Sciences, Jagiellonian Universityand in the Institute of Geography, Cracow Pedagogical Uni-versity (the Pó³rzeczki and Bruski sections).

All samples for nannoplankton studies were preparedwith the standard smear slide technique for light microscope(LM) observations. The investigations were carried out un-

FLYSCH DEPOSITS IN THE BYSTRICA AND RAÈA SUBUNITS 29

Fig. 2. Geological sketch-map of the middle part of the Western Carpathians (Poland) (after Oszczypko et al., 1999b, supplemented)


Fig. 3. Geological map and geological cross-sections of the Pó³rzeczki-Bia³e-Szczawa area; Bystrica and Raèa subunits, MaguraNappe, Western Flysch Carpathians


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 Ha³uszowa Formation; 3 – Bia³e Formation; 4 – Szczawina Sandstone Formation; 5 – Ropianka Formation; 6 – JaworzynkaFormation, 7 – Grybów Beds, 8 – Krosno Beds

der LM at a magnification of 1000× using parallel andcrossed nicols. Several specimens photographed under LMare illustrated in Fig. 27. For the purpose of this work thestandard 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 rankof formation (Jasieñ Formation, Bia³e Formation, MalinowaShale Formation, Szczawina Sandstone Formation, Ropi-anka Formation, Jaworzynka Formation, £abowa ShaleFormation, Belove�a Formation, Bystrica Formation) havebeen 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 Œwi-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 sevenformations: the Jasieñ Formation, Malinowa Shale Forma-tion, Ha³uszowa Formation, Bia³e Formation, JaworzynkaFormation, 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 Raèa subunit.Dominant lithology. Spotty shales and variegated shalesare dominant in the basal part of the Group. Thin-beddedturbidites with intercalations of turbidite limestones andsubordinate, variegated shale horizons are predominant inthe 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 minorsequences in term of sequence stratigraphy.Boundaries. Lower boundary usually tectonic againstvarious lithostratigraphic units; upper boundary sharp assedimentary transition to the Beskid Group (cf. Oszczypko,1991).Geological age. Late Albian to Palaeocene.Equivalents. Grajcarek Group in the peri-Klippen Beltzone of the Magura Nappe (see Birkenmajer & Oszczypko,1989).

Jasieñ Formation (a new name)

History. The Albian–Cenomanian deposits of the MaguraNappe (Grajcarek Unit) of the Pieniny Klippen Belt (PKB)

have been described by Birkenmajer (1977) as the HulinaFormation. Furthermore, Birkenmajer & Oszczypko (1989)regarded the green spotty marls occurring in the southernmargin 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 investigatedarea, we have decided to use the name “Jasieñ Formation”for the Albian–Cenomanian deposits in the presented divi-sion.Name. After the Jasieñ Hill (1052 m), 5 km south of thePó³rzeczki village (Figs 3, 5A). Polish name: formacja z Ja-sienia.Type locality. The forest road-cut at an altitude of 840– 850m located about 1km NWN of the Jasieñ 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, noncalcareousshales with intercalations of black, green shales and spottyshales. Sometimes small manganese nodules are observed.The shales display fracture cleavage of the pencil type.Boundary. The bottom of the formation is tectonic. Upperboundary – at the bottom of the first red shale package, be-longing to the Malinowa Shale Formation.Distribution. This formation is known from two localitiesin the Koninki village (Figs 4, 5C), on the southern marginof the Mszana Dolna tectonic window. The deposits similarto the Jasieñ Formation are also known from the ObidowaIG-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 Švábenická et al.,1997).Equivalents. Hulina Formation of the Grajcarek Unit in thePieniny Klippen Belt (Birkenmajer, 1977; see also Osz-czypko et al., 2004) and green radiolarian shales (Barna-siówka Radiolarian Shale Formation, B¹k et al., 2001) inthe 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 etal., 1990). Later, this formation was described from the By-strica subunit (Malata & Oszczypko, 1990; Oszczypko etal., 1991; Malata et al., 1996). In the studied region, this for-mation occurs both in the Pó³rzeczki-Szczawa area, and inthe Koninki area (Figs 3, 4) (see also, Oszczypko et al.,1991, 1999; Malata & Oszczypko, 1990; Oszczypko-Clowes & Oszczypko, 2004).

In the Pó³rzeczki-Szczawa area, the Malinowa ShaleFormation crops out both on the northern and southern sidesof the Mogielica Range (Fig. 3). The best outcrops occur inthe Pó³rzeczki village and in the vicinity of Bruski hamlet,in the core of the Bia³e anticline (Malata & Oszczypko,1990; Oszczypko et al., 1991) and its continuation on thenorthern slope of Jasieñ and Kustrzyca hills.


The lower boundary of the Malinowa Shale Formationis sharp, located at the base of the first red shales. Thecherry-red (Fig. 6A), non-calcareous shales occur in 30–50cm layers, intercalated by grey-greenish shales, a few to 25cm thick. Partly, grey-green shales are thicker and containintercalations of thin-bedded (1–7 cm), single sandstonebeds, 30–65 cm thick. Northeast of the Pó³rzeczki village atthe Bruski hamlet, the Malinowa Shale Formation containsa few intercalations of thick-bedded, coarse to medium-

grained quartz-glauconite sandstones, laminated quartziticmudstones and hornstones. The thick-bedded sandstones re-vealed the palaeotransport from W and WNW. The fre-quency of grey-green shale intercalations increases in theupper portion of the formation, and deposits display some-times features of the Ha³uszowa-type facies (cf. Zasadnesection; Malata & Oszczypko, 1990). The upper boundary issharp, located at the top of the last, thick appearance of thered shales (Fig. 6B).


0 500 m 1 km SZCZAWA

BIA£E

BOKÓWKA

PÓ£RZECZKI

901

Kiczera

813

Kamienica

1051

Kustrzyca

0 500 m 1 km

£ososin

a

Kamienica

1062

Jasieñ

1171

Mogielica

BRUSKI

Mogie

licki

7/94

2-3/936/94, 33-39/94

31-33/945/944/94

27-30/94

12-13/94

10/941-3/94

1/93 35-36/9439/9440-41/94

42-43/94

1-4/878-10/87

43-44/8745/87

48/87

46/87

47/87

63/97

64/97

47-48/94

44-45/94

1-8Br

10/9514-26/94

6/97

3-4/93K2

49-53/87

54-55/87

JaF

RF

JF

BF

MG

SF

Thrust Faults Samples MG1-4/87

BF

SFSF

RF

LUBOMIERZ

0 500 m 1 km

Mszanka

9,63/98/N

45,46/00/N

Koninka

RFMF

RFJF

SF

BF

SF

PORÊBA WIELKA

KONIKI

PORÊBA G.

0 500 m 1 km

0 500 m 1 km

Konina

KONINA

SF

RF

A B

C D

Lithostratigraphic units: MG - Mogielica Group, JF - Jasieñ Formation, BF - Bia³eFormation,JaF - Jaworzynka Formation, SF - Szczawina Sandstones Formation, RF- Ropianka Formation

JaF

KMKRZYSZTONÓW

Fig. 5. Simplified geological map of the Pó³rzeczki-Bia³e-Szczawa area (Bystrica and Raèa subunits; Magura Nappe) with locality oftype sections and hypostratotypes of lithostratigraphic units and with position of micropalaeontological samples. 45, 46/00/N – GPS posi-tion of selected stratotype sections


Fig. 6. A – Red shales of the Malinowa Shale Formation; Koninki stream in Koninki; B – Boundary between the Malinowa Shale For-mation and the Bia³e Formation; Koninki stream in Koninki; C – Thin-bedded turbidites of the basal part of the Bia³e Formation, Ka-mienica River in Bia³e

Total thickness of the Malinowa Shale Formationreaches at least 100 m in the Bruski hamlet, ca. 50 m on theslopes of Jasieñ Hill and at the Zasadne section (Fig. 7; seealso Malata & Oszczypko, 1990; Cieszkowski et al., 1999),and at least 40–50 m in the area of Bia³e village (Malata &Oszczypko, 1990). Geological age of this formation rangesbetween Turonian and Late Santonian (Malata & Osz-czypko, 1990; Cieszkowski et al., 1999, Malata, 2001).Equivalents. Lower part of the Kaumberg Formation in theMoravia (Švábenická et al., 1997) and the lower part of theCebula Formation in the Pilsko area (Pivko, 2002, see alsoSikora & ¯ytko, 1959; Golonka & Wójcik, 1978a, b).

Ha³uszowa Formation

Remarks. The Ha³uszowa Formation represents a transi-tional unit between the variegated shales of the MalinowaShale Formation and thin-bedded turbidites of the Bia³eFormation (described below). This unit is composed of greyturbidite marls with intercalations of medium to thin-bedded turbidites and red marls. In the Zasadne and M³yñ-czyska sections (Malata & Oszczypko, 1990; Malata et al.,

1996), the Ha³uszowa Formation replaces laterally the Bia³eFormation. In the Porêba Górna and Koninki sections, thinintercalations of red marls occur in the upper part of the Ma-linowa Shale Formation. Thickness of the formation reaches100 m (Zasadne section: Malata & Oszczypko, 1990; Ciesz-kowski et al., 1999). Geological age – Late Santonian–Campanian (Malata & Oszczypko, 1990; Cieszkowski etal., 1999).Equivalents. Upper part of the Kaumberg Formation in theMoravia (Švábenická et al., 1997) and upper part of the Ce-bula Formation in the Pilsko area (Pivko, 2002, see also Si-kora & ¯ytko, 1959, Golonka & Wójcik, 1978a, b).

Bia³e Formation (a new name)

History. The Senonian–Palaeocene deposits of the MaguraNappe have been traditionally referred to the Inoceramianbeds (e.g., Bieda et al., 1963). In the investigated area thisunit has been sometimes divided into three divisions, knownas 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,


10

0m

Zasadne MogielicaHill

JasieñHill

Pó³rzeczki

£aF

BeF

RF

JWF

BF

MF

S S

ByF

S S

HF

JF

KM

KobylicaHill

SF

B Y S T R I C A S U B U N I T R A È AS U B U N I T

NS

Shales withthin-bedded turbidites

Thick to medium-bedded turbidites

Thick-beddedsandstones

Palaeotransportdirection

LithostratigraphicunitsMF

Turbiditemarls

Spottyshales

Variegatedshales

Turbiditelimestones & marls

Silicifiedmarls Siderites

S

S

S

Fig. 7. Lithostratigraphic logs of the Upper Albian–Lower/Middle Eocene deposits in the Raèa and Bystrica subunits in thePó³rzeczki-Bia³e-Szczawa area, Magura Nappe, Western Flysch Carpathians. Lithostratigraphic units: JF – Jasieñ Formation; MF – Mali-nowa Shale Formation; HF – Hulina Formation; BF – Bia³e Formation; JaF – Jaworzynka Formation; SF – Szczawina Sandstone; KM –Krzysztonów Member, RF – Ropianka Formation; £aF – £abowa Shale Formation; BeF – Beloveza Formation; ByF – Bystrica Formation

the name “Kanina Beds” was used by Kozikowski (1953) inthe marginal part of the Magura Nappe (Raèa subunit), NWof Nowy S¹cz. The subdivision of the Inoceramian beds wasalso used by the authors of the Detailed Geological Map ofPoland (e.g., Burtan et al., 1976, 1978; Paul, 1980a,b, Osz-czypko & Wójcik, 1992). However, it should be stressed outthat deposits included on these maps to the Kanina bedsvary considerably in their stratigraphic position, lithologyand thickness. Good exposures of the Kanina beds havebeen recently described from the Szczawa and M³yñczyskaareas by Cieszkowki et al. (1987, 1989), Oszczypko et al.(1991), Oszczypko (1992b), and Malata et al. (1996). Dueto the bad state of exposures in the Kanina area, the presentauthors 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 Bia³e hamlet, 5 km NW of the Szczawavillage (Figs 3, 5A). Polish name. Formacja z Bia³ego.Type locality. 500 m long exposure along the left bank ofthe Kamienica River (Figs. 3, 5A); about 1 km NNW of theBia³e hamlet (Bystrica subunit): GPS position – base of thesection: 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 theMagura Nappe; Lubomierz creek, beneath the bridge acrossthe road Mszana Dolna-Zabrze¿ (Figs. 4, 5D), GPS posi-

tion: N 49° 37, 140’, E 20° 09, 695’; section of PorêbaGórna – a basal part of the Magura Nappe overthrust,Porêba Górna creek (Figs. 4, 5C), GPS position: N 49° 35,886’, E 20° 03, 699’.Thickness. Variable, from 10 m in Porêba – Koninki thrustsheet (Raèa subunit) to ca. 50 m in the Konina – Lubomierzthrust-sheet (Bystrica subunit; see also Oszczypko-Clowes& Oszczypko, 2004). Thickness amounts to 100 m close tothe Mogielica Hill (Figs. 7, 8).Dominant lithology. Thin- to medium-bedded turbiditeswith intercalations of grey-bluish and grey-yellowish pelites(Fig. 6C). The formation is composed of 3–5 cm thick, veryfine, calcareous sandstones, displaying Tc and Tcd Boumaintervals. 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, afew to tens of centimetres thick, reveal very fine, parallellamination. In the middle and upper parts of the formation, acomplex (a few metres thick) of thin- to thick-bedded sand-stones and marls, with rare intercalations of red shales andred marls has been observed (Oszczypko et al., 1991). Theuppermost 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).


Fig. 8. Lithostratigraphical logs of the Upper Cretaceous–Eocene deposits in the Bystrica subunit in the southern margin of the MszanaDolna tectonic window. Lithostratigraphic units: MF – Malinowa Shale Formation; BF – Bia³e Formation; SF – Szczawina Sandstone For-mation; RF – Ropianka Formation; £aF – £abowa Shale Formation; BeF – Belove�a Formation; ByF – Bystrica Formation; ZF –¯eleŸnikowa Formation; MM – Maszkowice Member of the Magura Formation


Fig. 9. A – Typical development of the basal of the Bia³e Formation, Kamienica River at Bia³e; B – Cross-laminated, medium-beddedsandstone of the Bia³e Formation; Kamienica River at Bia³e; C – Thin-bedded turbidites of the Bia³e Formation at Pó³rzeczki; D – Thick-bedded sandstones of the Jaworzynka Formation; Pó³rzeczki section; E – Thick-bedded sandstones of the Szczawina Sandstone Formationin the Koninki section; F – Thick-bedded sandstones of the Szczawina Sandstone Formation in the Koninki section

In the Porêba section, the lower part of the formation(see Oszczypko-Clowes & Oszczypko, 2004) is composedof grey-green, non-calcareous shales, a few metres thick.The middle part of the sequence is dominated by dark-greymudstone/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 Porêba Górna section,the Bia³e Formation, including a few thin intercalations ofred shales, resembles the Ha³uszowa Formation from theZasadne section (Oszczypko-Clowes & Oszczypko, 2004).

The Bia³e Formation reveals a coarsening and thicken-ing upward sequence, which contains heavy minerals ofzircone-tourmaline-rutile, partly with chromite spinels (e.g.,Lubomierz section, see Oszczypko & Salata, submitted toprint). The sandstones of the Bia³e Formation reveal palaeo-transport from the SE.Boundaries. Lower boundary – at the top of the last thickintercalation of red shale package belonging to the Mali-nowa Shale Formation. Upper boundary – at the bottom ofthick-bedded sandstones of the Szczawina Sandstone For-mation (Figs 7, 8).Geological age. Early-middle Campanian in the studiedarea (B¹k & Oszczypko, 2000; Malata, 2001), and lateCampanian–early Maastrichtian in the M³yñczyska area(Malata et al., 1966).Distribution. The Bystrica and Raèa subunits in the Polishpart of the Magura Nappe.Equivalents. The Ha³uszowa Formation in the Krynicasubunit (Birkenmajer & Oszczypko, 1989) and the Bystricasubunit (Zasadne section).

Jaworzynka Formation (a new name)

History: Sikora and ¯ytko (1959) described the biotite-feldspar beds in the marginal part of the Magura Nappe, inthe Beskid Wysoki Range (Siary subunit). These beds arecharacterized by thick-bedded sandstones of grey (dirty)-green colour, medium to coarse-grained, with feldspars andadmixture of glauconite and biotite. The thick-bedded sand-stones are accompanied by thin intercalations of grey-greenand black argillaceous shales with siderite concretions. Ac-cording to Sikora and ¯ytko (1959), the age of the biotite-feldspar beds is the Late Cretaceous–Palaeocene, and theirthickness reaches 200 m.

Burtan (1973) named this unit as the Biotite beds fromJaworzynka. The name was given after the village Jawo-rzynka, which is located SW of ¯ywiec. In the stratotypearea (marginal part of the Magura Nappe SW of ¯ywiec),the Biotite beds are developed as thin to medium-bedded,flysch deposits. These beds were also described by Burtan etal. (1978) from the southern and eastern margins of theMszana Dolna tectonic window, close to the Pó³rzeczki vil-lage. Polish name: formacja z Jaworzynki.Type area. Marginal part of the Magura Nappe, SW of¯ywiec.Thickness. Variable, ca. 150–200 m.

Reference sections: Pó³rzeczki-Jurkowa creek (Figs 3, 5A)and Koninki creek.Dominant lithology. In the Pó³rzeczki area, the Ja-worzynka Formation is not homogenous in respect to lithol-ogy. Its lower part, ca. 50 m thick, is represented by thick-tovery thick-bedded, green-grey, non-calcareous sandstonesand fine-grained conglomerates, dominated by quartz andmetamorphic pebbles with subordinate admixture of biotiteand glauconite (Fig. 9D).The sandstones are intercalated bygrey-greenish, non-calcareous shales. This part of the for-mation displays flute casts showing palaeotransport fromWWN and W. The upper part of the formation, up to 150 mthick, is composed of thick-bedded, medium- to fine-grained muscovitic sandstones, which display palaeotrans-port from SE. These sandstones resemble the SzczawinaSandstone lithofacies (Fig. 7). In the Koninki area, this for-mation is represented by a 5–8 m thick, fining and thinningupward sequence. The lower part of this sequence, 3–4 mthick, is composed of thick-bedded sandstones (50–150cm), very coarse- to medium-grained, sometimes amalga-mated with Tab Bouma intervals. The thick-bedded sand-stones (partly glauconitic) from this section reveal somesimilarities 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 Bia³e Formation to thick-beddedsandstones. Upper boundary – sharp, thick-bedded sand-stones against the thin-bedded turbidites of the RopiankaFormation (Fig. 7).Distribution. The Raèa and Siary subunits of the MaguraNappe in Poland; Grybów Unit in the Polish part of theWestern Carpathians.Geological age. Middle Campanian to early Maastrichtian.Equivalents. Biotite-feldspar beds (Sikora & ¯ytko, 1959;Biotite beds from Jaworzynka (Burtan et al., 1978, proparte), partly Solan Formation in Moravia (Švábenická etal., 1997), Szczawina sandstones (Sikora & ¯ytko, 1959;Cieszkowski et al., 1989; Oszczypko, 1992a, b; Malata etal., 1996), Szczawina sandstones of the Raèa subunit(Pivko, 2002).

Szczawina Sandstone Formation (a new name)

History. The Szczawina sandstones have been described bySikora and ¯ytko (1959) in the Beskid Wysoki Range (Raèasubunit). This lithostratigraphic unit is commonly used inmany 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 etal., 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 ofthe Ropianka Formation in the Bystrica subunit, and as aformation between the Cebula and Ropianka formations inthe Raèa subunit.Name. After Szczawina Hill in the Beskid Wyspowy Range(see Fig. 2 in Sikora & ¯ytko, 1959). Polish name: for-macja piaskowców szczawiñskich.Type area. Central part of the Magura Nappe, south-west of


¯ywiec (Sikora & ¯ytko, 1959) and the southern part of theBeskid Wyspowy Range (Oszczypko et al., 1991; Malata etal., 1996).Reference section. In the Beskid Wysoki Range type area,the best exposures of the Szczawina Sandstone Formationare known from the nothern slope of the Pilsko Hill (1557m) and the top of the Szczawina Hill (1356 m) (see Fig. 2and Plate XXI in Sikora & ¯ytko, 1959). The following typeareas from the Beskid Wyspowy Range type are recom-mended: the section along the right bank of the KamienicaRiver, between Bia³e and Bukówka hamlets (Figs 3, 5A; seealso Oszczypko et al., 1991; Cieszkowski et al., 1989),Koninki and Porêba Górna (Figs 4, 5C; see also Oszczypkoet al., 1999; Oszczypko-Clowes & Oszczypko, 2004), GPSposition: N 49° 35, 920’, E 20° 04, 997’ and 49° 35, 688’, E20° 03, 416’ respectively. The very good exposures are alsoknown 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 Porêba Górna area(Raèa subunit), to 80–350 m in Zasadne, Mogielica Hill, Ja-sieñ 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-greensandstones with thin intercalations of shales. The thicknessof 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 bedsare 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 ofthe formation is a considerable content of mica flakes(mainly muscovite) and small admixture of glauconite. Thesandstones 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 tomedium-bedded sandstones. Its basal portion, ca. 25 mthick, is dominated by thin- to thick-bedded calcareoussandstones with intercalations of turbidite limestones, marlsand, locally, red shales. Flute-cast (Fig. 10A) measurementsdisplay palaeotransport from the south-east. This part of thesequence resembles the Kanina beds (see Cieszkowski etal., 1989). The Kanina-like flysch passes upwards intothick-bedded sandstones of the Krzysztonów Member (fordetails – see below).

In the Porêba Górna area (Raèa subunit), the SzczawinaSandstone Formation, at least 20 m thick, is dominated bythick and very thick-bedded (40–250 cm), medium to verycoarse 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 of mus-covite and coalified plants, are typical at the top of the beds.The muscovite sandstones display palaeotransport also fromSE.Boundaries. Lower boundary – transitional, from thin-bed-ded turbidites of the Bia³e Formation to thick-bedded sand-

stones. Upper boundary – sharp; thick-bedded sandstonesagainst the thin-bedded turbidites of the Ropianka Forma-tion.Distribution. The Bystrica and Raèa subunits in the Polishpart of the Magura Nappe.Geological age. Middle Campanian–early Palaeocene.

Krzysztonów Member (a new name)

Name. After Krzysztonów hamlet, between £ososina Riverand 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£ososina River) in the Krzysztonów hamlet (Bystrzycasubunit) (Fig. 5A).Reference section. Right tributary of the £ososina River,north of Jasieñ Hill (Figs 5A, 7).Thickness. Between 50–80 m (Fig. 7).Dominant lithology. Thick-bedded sandstones (1.0–2.0 mthick), which reveal the Tabc+conv Bouma divisions. Thesandstones are very coarse- to fine-grained, muscovitic,with carbonate cement, rich in shale clasts, up to 15 cm indiameter, occasionally armoured. The sandstone beds areintercalated by rare, dark-grey shales, up to a tens cm thick.The sandstones were deposited by palaeocurrents from theSE.Boundaries. Lower boundary – transitional, frommedium-bedded turbidites to thick-bedded sandstones. Up-per boundary – transitional; thick-bedded sandstonesagainst the medium and thin-bedded turbidites.Distribution. The Bystrica subunit in the Polish part of theMagura Nappe.Geological age. Maastrichtian.

Ropianka Formation

History. The name Ropianka beds, established more than130 years ago (Paul, 1869), has been very often used as anequivalent 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 wasstudied by Œl¹czka & Mizio³ek (1995). They documentedthat this section contains deposits of different age (from theLate Cretaceous to Oligocene) belonging to the Dukla andMagura nappes. According to Œl¹czka and Mizio³ek (1995),the name “Ropianka beds” should not be applied for therocks in the Magura Nappe, however, considering long tra-dition of this name, they suggested to use it only for thin-tomedium-bedded turbidites of the Upper Inoceramian beds.In this sense, the name of the Ropianka beds was used byMalata et al. (1996). We also support this point of view inthe present study.Reference sections. The Jurkowy creek (Figs 3, 5A) in thePó³rzeczki village (Raèa subunit), and the following sec-tions in the Bystrica subunit: the Jastrzêbia creek and uppercourse of the Je¿owa Woda creek in the M³yñczyska area(Malata et al., 1996), the lower course of the G³êbienieccreek in the Szczawa area, the Zasadne section (Malata etal., 1992), the Konina section (Figs 4, 5B), and the middlecourse of the Koninki creek (Fig. 5C), ca. 150 m higher upof the bridge (Oszczypko et al., 1999; Oszczypko-Clowes &



Fig. 10. A – Flute-casts at the base of the Szczawina Sandstone Formation in the Koninki section; B – Thick-bedded quartzitic sandstoneat 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 Pó³rzeczki section; E– Red shales of the £abowa Shale Forma-tion in the Lubomierz section; F – Variegated shales of the £abowa Shale Formation in the Pó³rzeczki section

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 Raèa subunit and80–100 m in the Bystrica subunit (Figs. 7, 8).Dominant lithology. Lithological features are different inthe Raèa and Bystrica subunits. The lower part of the Ro-pianka Formation is composed of thin- to medium-beddedturbidites with subordinate intercalations of thick-bedded(0.6–1.0 m), coarse- to medium-grained, parallel-laminatedsandstones (Fig. 10B–D). In this part of the sequence, a8-cm thick intercalation of red, calcareous shales has beenobserved. Thin- to medium-bedded sandstone beds (5–35cm) are mainly fine- to very fine-grained, calcareous, mus-covitic, with parallel, cross and convolute lamination. Grey-ish-green sandstones are intercalated with dark, muscoviticmudstones, coalified plant flakes, and dark-grey and blue,usually carbonate-free shales. Locally, in the upper part ofthe formation, intercalations of dark-grey, medium-beddedand very fine-grained, glauconite and biotite-rich, non-calcareous sandstones are observed. Single layers of tur-biditic limestones and siderites have also been found. Theuppermost 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 anddark-grey-coloured sandstones. The mudstones are oftenbioturbated.

In the Bystrica subunit (Figs 7, 8), this part of the for-mation contains locally frequent, thin intercalations of redshales (see M³yñczyska, Zasadne, Koninki, Konina). Flute-cast measurements display palaeotransport from WWN inthe lowermost portion of the formation (Pó³rzeczki area,Raèa subunit) and from to EES–SSE in the Bystrica subunit(and also in the upper part of the Pó³rzeczki area of the Raèasubunit). The Ropianka Formation contains zircone-tour-maline-rutile heavy minerals (Oszczypko & Salata, sub-mited to print).Boundaries. In the Raèa 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 SandstoneFormation to very thin-bedded turbidites with intercalationof red shales. The upper boundary is sharp in both subunits,against the first few metres thick layer of the variegatedshales belonging to the £abowa Shale Formation.Geological age. Maastrichtian–Palaeocene.Equivalents. Upper part of the Solan Formation in Moravia(Švábenická et al., 1997), Ropianka beds (Golonka &Wójcik, 1978a, b; Malata et al., 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 £abowa Shale For-mation (Oszczypko, 1991) occur in the Pó³rzeczki 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 betweenOlszówka and Lubomierz (Fig. 4). The lowermost portionof the formation is represented by red shales (Fig. 10E–F), afew metres thick, passing upwards into very fine-beddedturbidites. Very fine-grained, green, carbonate- free sand-stones (with Tc Bouma interval) pass upwards into greenshales, and finally to red shales, mainly soft and free of car-bonates, a few cm thick. In the Porêba Górna area, the low-ermost part of this formation contains two layers of thick-bedded sandstones (up to 2 m) and intercalations of greymarls. These sandstones reveal palaeotransport from ESE.Thick layers of the red shales are known from the middlepart of the Lubomierz village (Fig. 10E). In the PorêbaGórna and Lubomierz sections, the thickness of the forma-tion attains 50 m. In the Pó³rzeczki 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 redshales, passing upwards into very thin-bedded turbidites.The turbidite sequence usually begins with thin-bedded(1–6 cm), very fine-grained (Tc), green, carbonate-freesandstones, passing up to green shales, a few centimetresthick, and finally to thin package of red shales, also a fewcentimetres 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 shaleswith intercalations of thin-bedded sandstones are observed(Fig. 10F). Thickness of the formation varies from a fewdozen metres up to 200 m in the Pó³rzeczki section.Distribution. In all the facies-tectonic subunits of the Ma-gura Nappe, with exception of the Krynica subunit (seeBieda et al., 1963, Oszczypko, 1991, Leszczyñski & Uch-man, 1991).Geological age. Early Eocene.

Belove�a Formation

Remarks. The Belove�a Formation (Oszczypko, 1991) isvery well exposed along the southern margin of the MszanaDolna tectonic window (Oszczypko et al., 1999; Osz-czypko-Clowes & Oszczypko, 2004). This formation iscomposed 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 brownshales are usually calcareous, while the green ones are, as arule, 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 thePó³rzeczki area, the Belove�a Formation crops out along anarrow depression between Bania and Kiczora hills (Fig. 3),and in the £ososina River in the Pó³rzeczki village. In thebasal part of the formation, a sequence of alternating layersof various coloured shales occurs. A few intercalations ofred shales have also been observed in this part of the sec-tion. The accompanying muscovitic sandstones are veryfine-grained and thin-bedded (5–12 cm). The medium-bedded (20–40 cm), Tbc sandstones appear subordinately inthe Jurkowa creek. In the Pó³rzeczki area, the thickness ofthe Belove�a Formation reaches no more than 50 m.


Bystrica Formation

Remarks. The Bystrica Formation (Oszczypko, 1991) oc-curs in a narrow syncline between Bania and Kiczora hillsand SE of Kobylica Hill. This formation comprises thin- tomedium-bedded turbidites of the Belove�a-lithotype withintercalations of the £¹cko Marls. The marls are massive,sometimes silicified, brown or blue to grey and whitish asweathered. The thickness of individual beds of the £¹ckoMarls ranges from 2 to 5 m. The intercalations of the “Be-love�a-type” flysch are 0.5 to 2 m thick. The thickness ofthe formation can be roughly estimated at 50 m (Figs. 7, 8).

BIOSTRATIGRAPHY

FORAMINIFERA

Several stratigraphical zonal schemes, based on thedeep-water agglutinated foraminifera (DWAF) have beenproposed for the Cretaceous–Palaeogene deposits of theOuter (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 thebase 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 onthe 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, B¹k et al.,1997; Olszewska, 1997; B¹k, 2004), Northern Atlantic, andWestern Tethys (Kuhnt et al., 1992; Kuhnt & Kaminski,1997). However, definitions of these zones using the sameindex species are different in the particular zonal schemes(cf. summary in B¹k, 2004).

The chronostratigraphy is based on comparisons withthe stratigraphic ranges of identified species in the NorthAtlantic and the Western Tethys. The Cretaceous part of thestudied succession has been compared with the chronostra-tigraphy by Gradstein et al. (1994), and the Palaeogene witha time scale of Berggren et al. (1995).

Deep-water agglutinated foraminiferal zones

Plectorecurvoides alternans Interval ZoneDefinition: Lower boundary – first appearance of Plectore-curvoides alternans (Noth) – not observed in the studiedsuccession; upper boundary – the first occurrence (FO) ofBulbobaculites problematicus (Neagu).Remarks: index taxon accompanied by Hippocrepina de-pressa Vašièek, Pseudonodosinella troyeri (Tappan), Plec-torecurvoides irregularis Geroch, and Gerochammina stan-islavi Neagu.Age: late Albian–early/middle Cenomanian.

Bulbobaculites problematicus Interval ZoneDefinition: Lower boundary – the FO of Bulbobaculitesproblematicus (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 ZoneDefinition: Lower boundary – the FO of U. jankoi; upperboundary – the FO of Caudammina gigantea (Geroch).Remarks: in the lower part of the zone the index species isvery numerous. The species known from the abyssal oce-anic deposits such as ?Praecystammina globigeriniformisKrasheninnikov, Trochammina gyroidinaeformis Krashen-ninikov are relatively frequent in this part of the zone. Otherabyssal 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 abundantpresence of Gerochammina spp. with small amount of theindex taxon. Rzehakina inclusa (Grzybowski) has its FO inthe uppermost part of the zone.Age: Turonian–early Campanian.

Uvigernammina jankoi-Caudammina gigantea

Concurrent Range ZoneDefinition: 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 inthis zone by the disappearance of Gerochammina typical forthe red facies and more frequent occurrence of siliceous-walled taxa.

Caudammina gigantea Partial Range ZoneDefinition: 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 ZoneDefinition: Lower boundary – the FO of R. varians; upperboundary – the FO of Rzehakina fissistomata (Grzybowski).Remarks: Kuhnt and Moullade (1991) defined the lowerboundary of this zone as middle-late Maastrichtian in theNorth Atlantic. In the Zumaya section (Spain), Kuhnt andKaminski (1997) distinguished the R. varians subzone) inthe upper Maastrichtian. According to Olszewska (1997) R.varians has its FO in the early Maastrichtian.Age: middle-late Maastrichtian.


Rzehakina fissistomata Taxon Range ZoneDefinition: range of R. fissistomata.Remarks: Annectina grzybowskii (Jurkiewicz) is a verycharacteristic species of this zone and in case of absence ofRzehakina fissistomata may be regarded as an equivalent in-dex taxon.The FO of the Rzehakina fissistomata (Grzybowski) is closeto the Cretaceous /Tertiary boundary in the abyssal non-calcareous environments, as it was confirmed on the basisof 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 ZoneDefinition: 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 tubularforms; all of them have small dimensions, against underly-ing and overlying assemblages. This assemblage has beendistinguished by Morgiel & Olszewska (1981) in the OuterCarpathians, and since that time it has been in use in theNorth Atlantic and the Western Tethys zonal schemes.Age: early Eocene.

Saccamminoides carpathicus Interval ZoneDefinition: Lower boundary: the FO of Saccamminoidescarpathicus; upper boundary: the FO of Reticulophragmiumamplectens – 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) hasits FO.Age: late early Eocene.

CALCAREOUS NANNOFOSSILS

Recognised calcareous nannoplankton zones

UC 15 Nannofossil ZoneDefinition: Interval between the FO of Misceomarginatuspleniporus to the LO of Eiffellithus eximius.Author: Burnett (1998).Age: Upper early Campanian throughout upper part of lateCampanian.Remarks: The zone is dominated by the presence of genusWatznaueria and Micula. Occurrence of C. aculeus may in-dicate for at least second subzone of this Zone named byBurnett (1998) UC 15BTP. From among other taxa, the spe-cies of Broinsonia parca, Prediscosphaera ponticula, andthe genus Arkhangelskiella prevail. This subzone was dis-tinguished primarilyonly for the Tethyan-Intermediate

province for the Indian Ocean (Burnett, 1998).Locality: Pó³rzeczki, Jaworzynka Beds.

Markalius inversus Nannoplankton Zone (NP 1)Definition: Interval between the LO of Arkhangelskiellacymbiformis 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 NP1 Zone what may be compared with the base of the Cyclage-losphaera alta nannoplankton Zone (NNTp2) according toVarol (1998). It is worth to add that all NP 1 Zone lays be-low the FO of Coccolithus pelagicus which is very commonin the Paleocene sediments of the Ropianka Formation.Locality: Pó³rzeczki, 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 ofCoccolithus pelagicus are characteristic for this zone.Locality: Pó³rzeczki, 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 tothe lack of zone-marker species. The only occurrence of theSphenolithus cf. anarrophus which ranges from NP 6 to NP9 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 israther poor, the re-worked Cretaceous species are much bet-ter preserved.Locality: Pó³rzeczki, 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 thegenus Tribrachiatus, especially T. orthostylus is oftenfound, 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: Pó³rzeczki, the upper part of the Ropianka Forma-tion.



M-U.C. - Middle-Upper Cenomanian

UA-LC - Upper Albian - Lower Cenomanian

R.v. Remesella varians- Zone

B.p. - Bulbobaculites problematicus

Pl.a. - Plectorecurvoides alternans

Zone

Zone

Spotty shales

Variegated shales

Turbiditic marlsand limestones

Thin- bedded turbidites

Thick-bedded turbiditesand fluxoturbidites

Micropalaeontological samples

0

100

200

300

400

500

600

700

800

900

1000 m

93/3

93/4a72/99; 45/8710/85

46/8748/8747/87

63/978-10/8743/87

1-5/87

16/8827/87

33/8734/87

39/87

46b/9446a/9465/9744/94

42/8715/93

1,2/93/K

40/94; 47/94

41/94

42b/94E42a/94E

K2K1

JASIEÑ - BIA£E - G£ÊBIENIECT

uro

nia

n-

?Low

er

Cam

pania

n

R.v

.

Jasieñ ShaleFormation

M-U.C. B.p.

Pl.a.UA-LC

MalinowaShale

Formation

£abowaShale

Formation

BelovezaFormation

Szc

zaw

ina

Sandst

one

Form

atio

n

Ropia

nka

Form

atio

n

Bia³eFormation

Cam

pania

n-

Maast

rich

tian

U.

jankoi

Zone

Caudam

min

agig

ante

aZ

one

Rzehakin

afissis

tom

ata

Zone

Glo

mospira

Acm

eZ

one

S.car.

Zone

Pale

oce

ne

Low

er

Eoce

ne

Krz

yszt

ofo

nów

Mem

ber

35/87

1/87

U.

jan

ko

i-

C.g

iga

nte

aS

ub

zo

ne

93/4b

43/94*

39/94*

39/94* Micropalaeontological samplesbarren of Foraminifera

Fig. 11. Lithostratigraphic log of the Bystrica subunit in the Jasieñ – Bia³e – G³êbieniec area (Bystrica subunit; Magura Nappe) with po-sition of micropalaeontological samples

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. Thezone assignment is based on the presence of genus Nanno-tetrina. According to Perch-Nielsen, the species belongingto Nannotetrina are dificult to distinguish in the heavilyovergrown assemblages. In such case, the FO of Nanno-tetrina can be used to approximate theNP14/15 boundary inbadly preserved material. The assembage does not containthe species of Chiasmolithus gigas. The interval betweenthe FO and the LO of Chiasmolithus gigas defines Bukry’ssubzone CP13b (Bukry, 1973). Subzone CP13b is theequivalent 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 thesame time, no species indicating NP16 was observed.

Discoaster tani nodifer Nannoplankton Zone (NP16)

Definition: the base of the zone is defined by the LO ofRhabdolithus 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. Thezone assignment is based on the presence of Cyclicargo-lithus floridanus. At the same time, Discoaster tanii is notpresent. According to Aubry (1986), the FO of Cyclicargo-lithus floridanus takes place in zone NP16.

BIOSTRATIGRAPHY VERSUSLITHOSTRATIGRAPHY

Jasieñ Formation

The foraminiferal assemblages are composed entirelyof 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 lownumber of specimens and species diversity. However, thereare present a few stratigraphically important species such,as Hippocreppina depressa Vasièek (Fig. 19 A), Plectore-curvoides alternans Noth (Fig. 19 F, and P. irregularisGeroch. In the succeeding samples, apart from the alreadymentioned species, new taxa appear and species diversityand 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 ofthe mentioned taxa. The first occurrence (FO) of P. alter-nans and H. falcatosuturalis is in the Late Albian (Neagu1990), while the last occurrence (LO) of T. vocontiana hasbeen noticed at the Albian/Cenomanian boundary. Accord-ing to Geroch and Nowak (1984) and B¹k (2000), B. prob-lematicus has its FO in the Middle Cenomanian, whereasaccording to Olszew- ska (1997) it marks the Albian/Ceno-manian boundary. In the Jaworki Formation of the PieninyKlippen Belt, Plectorecurvoides alternans Zone is corre-lated with the planktonic zones of the Early Cenomanian(B¹k, 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 & Kamiñski, 1990).The data mentioned above suggest that this species had ap-peared first in the deep, flysch basins and then migrated intoother environments.

The top of the Jasieñ 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 irregularisGeroch, 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. Thisassemblage may be correlated with the B. problematicusZone representing the Middle-Upper Cenomanian (cf. B¹k,2000) and Uvigernammina jankoi Zone, whose base is closeto the Cenomanian/Turonian boundary (Geroch & Nowak,1984).Thus, the Jasieñ 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 Jasieñ-Bia³e-G³êbieniec and Koninki sections(Figs 11, 14), consists of exclusively agglutinated assem-blages of foraminifera displaying medium species diversityfrom about 20 to 25 species (Figs 16, 17). In the lower partof 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 Dyl¹-¿anka, Ammosphaeroidina pseudopauciloculata (Majtliuk),and Trochammina gyroidinaeformis Krashenninikov (Fig.19 M–O) are also numerous. The species Pseudobolivinacuneata Krashenninikov and P. munda Krashenninnikov(Fig. 19 G, H), though very rare, are also worth mentioning.These latter taxa as well as Trochammina gyroidinoideswere 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-


gests some similarities to the abyssal type of deep-water ag-glutinated foraminifera (Kuhnt & Kaminski, 1989).

The species Uvigerinammina jankoi Majzon was usedas a stratigraphic marker both in the North Atlantic and theTethyan realm within every zonal scheme (e.g., Geroch &Nowak, 1984; Moullade et al., 1988; Kuhnt et al., 1989;Kuhnt & Moullade, 1991; B¹k, 2000). Its FO datum wasnoted in most localities just above or in the highest part ofanoxic deposits representing the Cenomanian–Turonian

boundary event. The LO of U. jankoi was recorded from theearly Campanian through the middle/late Campanian (e.g.,Alexandrowicz, 1975; Geroch & Nowak, 1984; Moullade etal., 1988; Kuhnt et al., 1989; Neagu, 1990; Kuhnt & Kamin-ski, 1997; B¹k, 2000). Due to lack of planktonic foramini-fera and calcareous nannoplankton and taking into accountthe occurrence of U. jankoi, the age of the Malinowa ShaleFormation 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 Raèa subunit sequence, studied both in thePó³rzeczki and Koninki sections (Figs. 12, 13), the fora-miniferal assemblage is very similar to that from the Bytrica


10/8812/8854/97, 14/88*

1/95, 13, 15/89*0

20

40

60

80

100

120

15/95

12/95, 13/95*

19/95

4/95; 51/97

KONINKI (Raca subunit)

48/97*12/8949/97

?

?

?A-C

P.alt.

Zone

??

?

JasieñSh. Fm.

Szc

zaw

ina

Sd

s.F

m.

Ro

pia

nka

Fo

rma

tion

Bia³eFm.

Ca

mp

an

ian

-M

aa

strich

tian

Ca

ud

am

min

ag

iga

nte

aZ

on

e

Pa

leo

cen

e

R.

issis

tom

.f Z

one

Malin

ow

aS

hale

Form

atio

n140

U.

jan

ko

iZ

on

e

Tu

ron

.-L

.C

am

pa

nia

n

??

55/97*

16/89*

45/95*

46/97*

52/97*, 53/97*

2/95*, 3/95*

50/97*

Fig. 12. Lithostratigraphic log of the Raèa subunit in the Koninkiarea (Mogielica Range) with the position of samples. For lithologi-cal explanations – see Fig. 11

Pó³ 39 - Pó³ 33, Pó³-0

Pó³ 32

Pó³ 31, Pó³ 5

Pó³ 30

Pó³ 4

Pó³ 25Pó³ 26Pó³ 24Pó³ 21 - Pó³ 22

Pó³ 16, Pó³ 15Pó³ 3 - Pó³ 1Pó³ 20 - Pó³ 17

Pó³ 12 - Pó³ 13

Pó³ 10 - Pó³ 11

Pó³ 27 - Pó³ 29

Pó³ 6, Br-9

600

0

200

400

100

300

500

Br-6Br-5

Br-3, 4

Br-1

Br-7, 8

700

Turo

n.-

L.C

am

p.

U.

jankoiZ

one

Mid

dle

Cam

pania

n-M

iddle

Maast

rich

tian

Mid

dle

-Upper

Maast

rich

tian

Pale

oce

ne

Low

er

Eoce

ne

Caudam

min

agig

ante

aZ

one

Rem

esella

varians

Zone

R.fissis

t.Z

one

Glo

mospira

div

.sp

.Acm

eZ

one

£abow

aS

hale

Form

atio

nR

opia

nka

Form

atio

nJa

worz

ynka

Sandst

ones

Form

atio

n

Bia³eFm.

Mal. Fm.-

Ha³. Fm.

PÓ£RZECZKI

Fig. 13. Lithostratigraphic log of the Raèa subunit in the Pó³rzec-zki area (Mogielica Range), with the position of samples. Forlithological explanations – see Fig. 11

subunit (Figs. 15, 18). Deep-water agglutinated foramini-fera are the only component in these deposits, associated bymoulds of Radiolaria. DWAF are poorly and medium diver-sified (up to 26 taxa per sample), with dominance ofreddish-walled specimens of Recurvoides. The latter taxonmakes up to 65 percent of the whole assemblage (mean47%). Reddish-walled specimens of Gerochammina, Tro-chammina, Paratrochamminoides, Reophax and, tubularforms (mainly Rhabdammina) are frequent.

The index taxon, Uvigerinammina jankoi has beenfound only in the lower part of the Malinowa Shale Forma-tion, most probably because of the gradual change of faciesand environmental conditions up the section, which havebeen unfavourable for this taxon. Uvigerinammina jankoiwas recorded only from well oxygenated environments withlow input of terrigenous material in the Tethys and NorthAtlantic (Moullade et al., 1988; Kuhnt et al., 1989; Kuhnt &Moullade, 1991; B¹k, 2000). The uppermost part of the Ma-linowa Shale Formation consists of many sandstone andsiltstone intercalations, associated with grey-green shalesagainst the true cherry-red shales, practically devoid ofcoarser material in the lower part of the Malinowa Forma-tion.

The lack of planktonic foraminifera and calcareous nan-noplankton prevents precise age determination of the for-mation, which is stated broadly as Turonian–early/middleCampanian, similarly to the Bystrica subunit.

In the Koninki section (Fig. 12), the upper part of theMalinowa Formation consists of exclusively agglutinatedassemblages 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 ofUvigerinammina jankoi Majzon. These species enable tostate that the Malinowa Shale Formation represents the up-per part of the Uvigerinammina jankoi Zone, most probablycorrelated with the Santonian–early/middle Campanian (cf.Geroch & Nowak, 1984), on the basis of co-occurrence ofthese species. The FO of Rzehakina inclusa (Grzybowski)has been documented close to the Santonian/Campanianboundary in deep-water environments (Geroch & Nowak,1984), and the LO of U. jankoi is considered to occur closeto the early-middle Campanian (see discussion above).

Bia³e Formation

Foraminiferal assemblages of this formation, studied inthe Bystrica subunit of the Jasieñ-Bia³e-G³êbieniec andKoninki sections (Figs. 11, 14) and in the Raèa subunit ofthe Pó³rzeczki and Koninki sections (Figs. 12, 13), consistof exclusively agglutinated taxa showing some similaritiesto those from the Malinowa Shale Formation; displayinghowever, lower species diversity and abundance. The as-semblages are characterised by a presence of rare specimensof Uvigerinammina jankoi and Rzehakina inclusa (Grzy-bowski) (Figs. 15, 17). Tubular forms and Recurvoides are

almost permanent components of assemblages. The FO ofCaudammina gigantea (Geroch), which is the index taxonof the next foraminiferal zone, has been noticed in this for-mation. Single specimens of this taxon have been found atthe base of the formation (s. 63/97; Fig. 17), occurring to-gether with Uvigerinammina jankoi.

The foraminifera recovered from the Raèa subunit (Figs15, 18) represent similar assemblage in relation to its com-position and diversity, however, the base of the formation inthe Pó³rzeczki section is devoid of C. gigantea, against anoccurrence of U. jankoi (Fig. 15). On the other hand, thesample taken from the top of the formation (Koninki sec-tion; Fig. 18) does not include U. jankoi. This may suggestthat the base of the succeeding Caudammina gigantea Zoneoccurs in the upper part of the Bia³e Formation. Index taxonis accompanied there by tubular forms, Saccammina pla-centa (Grzybowski), Glomospirella diffundens (Cushman etRenz), Rzehakina inclusa (Grzybowski), Kalamopsis grzy-bowskii (Dyl¹¿anka), Caudammina ovulum (Grzybowski),Paratrochamminoides spp., and Gerochammina spp.

Consequently, the lower boundary of the Bia³e Forma-tion is diachronous. In the Raèa subunit, it represents the topof the U. jankoi Zone, and in the Bystrica subunit, it is at thebase of U. jankoi – C. gigantea concurrent range Zone (cor-related with the early Campanian; cf. Neagu, 1990; Kuhnt &Moullade, 1991; B¹k, 2000). The upper boundary is alsodiachronous. It is at the top of the U. jankoi – C. giganteaZone in the Bystrica subunit and at the base of C. giganteaZone in the Raèa 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-


0

100

200

300

58*, 59/97, 10/90

57/9760/9756/9717/95

9,10/93

11/93

13*, 14/93

KONINKI (Bystrica subunit)

Tur

on.-

Low

erC

ampa

nian

?

Szc

zaw

ina

Sds

.Fm

.R

opia

nka

For

mat

ion

MalinowaFm.

Bia³eFm.

£abowaSh. Fm.

Cam

pan.

-M

aast

richt

.

U.ja

nkoi

Zon

eC

.gig

.Z

one

Glo

mo

s.

div.

sp.

Zon

e

Pal

eoc.

Eoc

ene

12/93*

8/93*

61/97*

?

Fig. 14. Lithostratigraphic log of the Bystrica subunit in theKoninki area, with the position of samples. For lithological expla-nations – see Fig. 11


Lithostrat. units Mal-Ha³ Fm. B Jaworzynka Sd. Fm. Ropianka Formation £ab.Age Tur-L.Camp. Middle Camp. -Middle Maastr. Ma. Paleocene L.Eoc.

FORAMINIFERAL

AGGLUTINATED

ZONES

U. jankoi Caudammina gigantea

Rem

esella

varians

Rzehakina fissistomata

Glo

mospira

div

.sp

.

Samples (Br, Pó³)

Bathysiphon sp.

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

Br-

6/97

Br-

5/97

Br-

8/97

Br-

7/97

Br-

4/97

Br-

3/97

Br-

1/97

Pó³

-39/

94P

ó³-3

8/94

Pó³

-37/

94P

ó³-3

6/94

Pó³

-35/

94P

ó³-3

4/9

Pó³

-33/

94B

r-9/

97P

ó³-6

/93

Pó³

-32/

94P

ó³-5

/93

Pó³

-31/

94P

ó³-3

0/94

Pó³

-4/9

3P

ó³-2

9/94

Pó³

-28/

94P

ó³-2

7/94

Pó³

-25/

94P

ó³-2

6/94

Pó³

-24/

94P

ó³-2

2/94

Pó³

-21/

94P

ó³-2

0/94

Pó³

-19/

94P

ó³18

/94

Pó³

17/9

4P

ó³-3

/93

Pó³

-2/9

3P

ó³1/

93P

ó³-1

6/94

Pó³

-15/

94P

ó³13

/94

Pó³

-12/

94P

ó³-1

1/94

Pó³

-10/

94

Fig. 15. Occurrence range chart of the Turonian through early Eocene Foraminifera in the Raèa subunit in the Pó³rzeczki area. Mal Fm.– Malinowa Shale Formation; Ha³ Fm. – Ha³uszowa Formation; B – Bia³e Formation; Jaworzynka Sd. Fm – Jaworzynka Formation; £ab –£abowa Shale Formation; Ma – Maastrichtian


Lithostrat. units Mal-Ha³ Fm. B Jaworzynka Sd. Fm. Ropianka Formation £ab.Age Tur-L.Camp. Middle Camp. -Middle Maastr. Ma. Paleocene L.Eoc.

FORAMINIFERAL

AGGLUTINATED

ZONES

U. jankoi Caudammina gigantea

Re

me

se

llava

ria

ns

Rzehakina fissistomata

Glo

mo

sp

ira

div

.sp

.

Samples (Br, Pó³)

Haplophr. cf. eggeri

Haplophr. cf. herbichi

Haplophr. walteri

Haplophragm. sp.

Recurvoides spp.

Recurvoidella lamella ?

Cribrostommoides sp.

Praecystam. globiger.

Trochammina deformis

Trocham. gyroidinaef.

Trochammina sp.

Trochamm. variolarius

Trochamminoides sp.

Paratr. heteromorphus

Paratrochammin. spp.

Spiroplect. spectabilis

Spiroplectammina sp.

Spiroplectinella sp.

Uvigerinammina jankoi

Gerocham. conversa

Gerochammina tenuis

Karrerulina coniformis

Karrerulina sp.

Remesella varians

Dorothia oxycona

Dentalina sp.

Lagena sp.

Globotruncana sp. r

Eoglobigerina trivialis

Subb. triloculinoides

Parasubb. varianta

Parasubb. pseudobull.

Planorot. compressa

Subbotina sp.

Pleurostomella sp. ?

Gyroidinoides sp.

Cibicidoides sp.

Anomalina ekblomi

Echinoid spine

Radiolaria

Fish teeth

Number of specimens 1-4 5-9 10-19 20-49 >50

Br-

6/97

Br-

5/97

Br-

8/97

Br-

7/97

Br-

4/97

Br-

3/97

Br-

1/97

Pó³

-39/

94P

ó³-3

8/94

Pó³

-37/

94P

ó³36

/94

Pó³

-35/

94P

ó³34

/9P

ó³-3

3/94

Br-

9/97

Pó³

6/93

Pó³

-32/

94P

ó³-5

/93

Pó³

-31/

94P

ó³-3

0/94

Pó³

-4/9

3P

ó³-2

9/94

Pó³

-28/

94P

ó³-2

7/94

Pó³

-25/

94P

ó³-2

6/94

Pó³

-24/

94P

ó³-2

2/94

Pó³

-21/

94P

ó³-2

0/94

Pó³

19/9

4P

ó³18

/94

Pó³

17/9

4P

ó³-3

/93

Pó³

-2/9

3P

ó³1/

93P

ó³-1

6/94

Pó³

-15/

94P

ó³13

/94

Pó³

-12/

94P

ó³-1

1/94

Pó³

-10/

94

perfamily Astrorhizacea (Fig. 15). Moreover, there are nu-merous specimens of the following genera: Paratrocham-minoides, Trochamminoides, Reophax, Trochammina, Re-curvoides, and of such species as: Saccammina placenta(Grzybowski) (Fig. 20C), S. grzybowskii (Shubert), Cau-

dammina ovulum (Grzybowski) and, C. gigantea (Geroch).Other foraminifera of predominantly siliceous-walled spe-cies occur occasionally.

Caudammina gigantea (Geroch) is the biostratigraphicmarker of these deposits. The first occurrence (FO) of thisspecies was noted by many authors from the early-late Cam-panian. Geroch & Nowak (1984) have reported its FO dur-ing the early Campanian in the Polish Flysch Carpathians,co-occurring with Uvigerinammina jankoi Majzon. In theRomanian Flysch Carpathians (Neagu, 1990) C. giganteahas been reported to appear within the Globotruncanita ele-vata planktonic foraminiferal Zone (early Campanian),similarly to the Pieniny Klippen Belt, where it was docu-mented from the lower part of this zone (B¹k, 2000). Ac-cepting stratigraphic significance of Caudammina gigantea(and lack of U. jankoi in the assemblage), the JaworzynkaFormation represents the lower part the Caudammina gi-gantea Zone sensu Geroch & Nowak (1984), which maybroadly correspond with the middle-Upper Campanianthrough ?early Maastrichtian.

An unusual assemblage of microfauna, described in de-tails by B¹k & Oszczypko (2000), has been found in the lo-west part of the Jaworzynka Formation. Sample Pó³-0/93(Fig. 13), taken from 10 cm thick chert layer (silicified mud-stone) contains very well preserved, rich assemblage ofplanktonic and benthic (calcareous and agglutinated) fora-minifera. Silicified (most recrystallised), small radiolariaare also numerous in this assemblage. This microfauna is atypical assemblage of Planomalina buxtorfi-Rotalipora ap-penninica Zone corresponding to Late Albian, known frompelagic environments (e.g., the Pieniny Klippen Belt; Ga-siñski, 1988; B¹k, 1992; M.B¹k, 1999).This unusual assem-blage of microfauna has been interpreted (B¹k & Osz-czypko, 2000) as an example of redeposition of microfaunain the clay clasts derived from the shallower part of the ba-sin with pelagic sedimentation in the submarine plateau en-vironment.

Other samples from dark and black shales taken at thebase of this formation are practically devoid of foramini-fera. Only tubular, pyritized forms have been found there.The studied black shales and siliceous mudstones could rep-resent the older part of the C. gigantea Zone sensu Geroch& Nowak (1984). Their tectonic position, the occurrence ofsiliceous facies, and scarcity of benthic foraminifera maysuggest their correspondence to the upper part of the lower-middle Campanian event (LMCE). Kuhnt (1987) describedsimilar benthic-free deposits representing the LMCE in theflysch units of the Gibraltar Arch area between U. jankoiand C. gigantea zones. Kuhnt et al. (1992) documented de-posits in the North Atlantic devoid of benthic foraminiferathat are directly overlain by the beds characterised by low-diversity agglutinated tubular forms and ammodiscids. Inthe Tethyan pelagic realm, the LMCE is characterised by anoccurrence of biosiliceous facies (e.g., Neagu, 1968; Butt;1981). It coincides with a taxonomic change in agglutinatedforaminifers – the U. jankoi assemblage is replaced by theC. gigantea assemblage in the flysch series (Kuhnt et al.,1992). The LMCE deposits have not yet been noted fromthe Carpathian flysch, however, the changes in agglutinatedassemblages are well documented (Jurkiewicz, 1961; Ge-


Lithostratigraphic Units Mal. Sh. Fm. B Ropian. £

Age Turon.-E.Camp. C-M. ?P

E1

FORAMINIFERAL

AGGLUTINATED ZONES

U.

jan

ko

i

C.

gig

an

tea

? Glo

mo

sp

ira

acm

e

Samples5

9/9

7

10

/90

57

/97

60

/97

56

/97

17

/95

9/9

3

10

/93

11/9

3

14

/93

Bathysiphon sp.

Nothia excelsa

Rhabdammina cylindrica

Rhabdammina robusta

Rhizammina sp.Saccammina placenta

Hyperammina elongata

Hyperammina sp.Ammodiscus cretaceus

Ammodiscus sp.Glomospira charoides

Glomospira gordialis

Glomospira irregularis

Glomospirella sp.Kalamopsis grzybowskii

Reophax duplex

Caudammina gigantea

Caudammina ovulum

Hormosina excelsa

Hormosina velascoensis

Pseudonodosinella parvula

Buzasina sp.Cribrostomoides sp.Haplophr. suborbiculariscf.Haplophragmoides sp.Paratrochamminoides spp.Ammosph. pseudopauciloculata

Recurvoides spp.Thalmannammina sp.Spiroplectinella dentata

Pseudobolivina cuneata

Trochammina altiformis

Trochammina globigeriniformis

Trochammina gyroidinaeformis

Trochammina sp.Gerochammina spp.Gerochammina conversa

Gerochammina lenis

Gerochammina obesa

Gerochammina stanislavi

Gerochammina sp.Karrerulina sp.Uvigerinammina jankoi

Fig. 16. Occurrence range chart of the Turonian through earlyEocene Foraminifera in the Bystrica subunit in the Koninki area.Mal. Sh. Fm. – Malinowa Shale Formation; B – Bia³e Formation;Ropian – Ropianka Formation; £ – £abowa Shale Formation;C–M – Campanian–Maastrichtian; P – Palaeocene; E1 – Early Eo-cene

roch & Nowak, 1984; Geroch & Koszarski, 1988; Neagu,1990).

Sample 7/94 (Fig. 13), located in the basal portion ofthe Jaworzynka Formation, contains a poorly to moderatelypreserved nannofossils assemblage dominated by the Creta-ceous forms, such as Watznaueria barnesae or Micula stau-rophora. It yielded also Broinsonia parca parca and Cera-tolithoides aculeus which indicate early Campanian (UC15Zone), according to Burnett (1998).

Szczawina Sandstone Formation

Due to its lithological character, this formation is gener-ally devoid of foraminifera. Only in the upper part of theformation, in the Jasieñ-Bia³e-G³êbieniec section, a poor as-semblage was recovered (Fig. 18). In sample 16/88, apartfrom a few agglutinated taxa, some poorly preserved speci-mens of Cretaceous planktonic foraminifera of the Margi-notruncana- or Globotrunacana-type have been noticed,while in sample 27/87 there have been numerous flysch-type forms, including mainly Rhabdammina spp. and Para-trochamminoides spp., accompanied by rare specimens ofAschemocella carpathica (Neagu), Caudammina gigantea(Geroch), C. ovulum (Grzybowski), Recurvoides spp., andGerochammina obesa Neagu. This assemblage belongs tothe Caudammina gigantea Zone, correlated with the middleCampanian–early (?middle) Maastrichtian. The upper limitof this zone is diachronous in deep-water environments; theindex species disappeared at different times during theMaastrichtian (Geroch & Nowak, 1984; Kuhnt et al., 1992;Olszewska, 1997, B¹k, 2004).

This formation was studied earlier in the other area ofthe Bystrica subunit (Beskid Wyspowy Range: M³yñczyskasection; Malata et al., 1996), where the foraminiferal assem-blage was also poorly diversified with non-characteristicdeep-water agglutinated forms. However, the upper part ofthis formation in that region represents the lowermost Pa-laeocene, documented by the occurrence of planktonic fora-minifera.

Ropianka Formation

Foraminiferal assemblages occurring in the RopiankaFormation vary in the state of preservation, abundance, andspecies diversity from section to section. The richest andstratigraphically significant assemblages have been recov-ered in the Pó³rzeczki area of the Raèa subunit (Fig. 15),whereas only the uppermost part of the formation is pre-served in the Koninki area. Most samples include well pre-served and highly diversified DWAF. Moreover, relativelynumerous Palaeocene planktonic foraminifera have beenfound at the top of the formation.

The lower part of this formation is characterised by nu-merous occurrences of tubular astrorhizids (Fig. 20A, B),Paratrochamminoides spp. (Fig. 22D), Trochamminoidesspp. (Fig. 22C), and Saccammina placenta (Grzybowski),accompanied by ammodiscids (Fig. 21A, D–H, Hormosinaexcelsa (Dyl¹¿anka) (Fig. 20E), Recurvoides spp. (Fig.22E–J) Recurvoidella lamella (Fig. 22K), and Trocham-mina spp. (Fig. 22N, O). A distinctive feature of this assem-

blage is the presence of the index taxon, Caudammina gi-gantea. The presence of this species and simultaneous lackof other short-ranging agglutinated species, suggest that thelower boundary of this formation is within the C. giganteaZone, corresponding, most probably, to the early-middleMaastrichtian. The described foraminifera could be corre-lated with the Saccammina-Bathysiphon Assemblage fromthe Dukla Nappe (B¹k, 2004), and to the similar in taxo-nomic compositition, Aschemocella-Saccammina placentaAssemblage from the Numidian Flysch of Northern Mo-rocco (Kaminski et al., 1996). Both of them are character-ised by abundant presence of the index taxa and the com-mon occurrence of Rhabdammina and Paratrochamminoi-des.

The younger part of the formation (about 100 m aboveits lower boundary), including intercalations of calca

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