The Geology of the External Carpathians: The classic localities revisited

Andrzej Slqczka Instytut Nauk Geologicznych Uniwersytet Jagiellonski ul. Oleand 2a 30-063 ~ra%w,

INTRODU(X1ON The Carpathians consist of two mountain in the development of the flysch facies. From ranges: an inner, older one known as the Inner south to north, these are the Magura basin, Carpathians (which include the Tatra Moun- the Fore-Magura Dukla Basins, the Silesian tains) and a northern, younger one known as Basin, and the Skole Basin. The Silesian and the Outer Carpathians. The contact between Skole Basins were separated by a submarine these two ranges consists of a tectonically ridge (Subsilesian) where during the Late disturbed zone known as the Pieniny Klippen Cretaceous and early Paleogene variegated Belt. marls predominated. During the Miocene The work of Grzybowski and his col- orogeny nappes were formed which developed leagues were connected with the faunas of the from the former basins. These are (1) The Outer Carpathians. The sedimentary se- Magura Nappe bordered from the south by the quences in this part of the Carpathians range Pieniny Klippen Belt, (2) the Pre-Magura in age from Tithonian to early Miocene. Dur- nappes, (3) the Silesian Nappe, (4) the Sub- ing this period, flysch sedimentation predom- silesian nappe, (5) the Skole nappe. Along the inated in the Carpathian basins, and there- outer margin of the Carpathians a narrow belt fore the range is also known as the "Flysch of folded Miocene deposits was formed. Zone". Several basins formed which differed

Figure 1. Tectonic sketch map of the Polish Carpathians, showing the extent of major structural units and localities of Gn bowski, Friedberg, and DylqiPnka. 1- Miocene Molasse, 2- Skole Na pe, 3- Subsilesian Unit, 4 - Andrychow dPp5- Silesian Na pe, 6- PreMapm units, 7- Magn Nappe, fC Pieniny Klippen Belt, 10 Podhale flyxh, Tatra units. D &kla; C Szyrnbark; Z- Friedberg s localities.

From: Karninski, M.A., Geroch, S., & Karninski, D.G., (eds.) 1993. The Origins of A lied Micropalaeontolo - The School of JhfGrrybowski. Grzybowski Foundation Special Publication no. 1. Eden Press. pp. 2252% 226 Andrzej Slqczka

The whole stack of nappes has been over- GRZYBOWSKI'S LOCALITIES: thrusted onto the Northern European Plat- form. The platform itself is built of Paleozoic 1. The Dukla Unit and Mesozoic rocks covered by the Miocene The sediments that Grzybowski (1894) col- molasse of the Carpathian Foredeep. The lected for his first monograph on the extent of thrusting exceeds 60 km. Carpathian Microfauna are today classified The purpose of this paper is to provide a as belong to a distinct tectonic-stratigraphic detailed description of the lithological units unit the Dukla Nappe. Grzybowski sampled that comprise the classic outcrops described by the Oligocene, which constitutes the upper Grzybowski, Friedberg, and Dylazanka, and part of the sediment column of the unit. The discuss their mutual relations in terms of the Oligocene of the Dukla Unit is represented by tectonic framework of the Carpathians. The the Menilite beds, which are in turn overlain localities discussed are shown in Figure 1. by the beds.

Figure 2. Geological sketch map of the area south o Dukla, from Teisseyre (1930). Map symbols are as follows: 1. Krosno Formation, 2. Transitional beds between t f, Krosno Fm. and tkMenilite beds, 3-6. Menilite beds (3. Menilite shales, 4. sandstones, 5. ckrts and Iawornik marls, 6. Msznna sandstones), 7. variegated shales, 8. line of main overthrust, 9. line of secondary overthrust, 10. tectonic contact, 11. landslips. Geology of classic localities 227

The Menilite beds in the western part of LITHOSTRATIGRAPHY - DUKLA UNIT the Dukla Unit begin with a unit of thickly E bedded, coarse-grained sandstones that dis- lower play graded bedding, known as the Mszanka Krosno Sandstones (Teisseyre, 1930). These lie 2 Y beds directly upon the upper Eocene Globigerina .... marls (Figure 3). The Mszanka sandstones at- tain a maximum thickness of 250 m. The sand- + stones are interbedded with dark brown Menilite -- -- - shales and marls. shales --- - - Above these two lithologic units, a hori- --- - 200 zon consisting of dark brown bedded cherts is developed which is several tens of meters thick. Higher in the stratigraphic column is a ca. 100 meter thick unit of hard, dark brown, partly silicified marls known as the Subcer- .. . 100 gowa marls or Jawomik marls. Recent studies h ...... indicate that these deposits have been 6 _.... deposited by density currents (Radomski and 0 -.-a, .... . Slaczka, 1985). The Subcergowa Marls contain O_ Cergowa . - . 0 foraminiferal assemblages with Globigerina sandstones . officinalis Subbotina, G. angustiumbilicata Bolli, G. ouachitaensis Howe & Wallace, . . -::-.. al .... -. Subbotina ampliapertura (Bolli) (Olszewska .-- .._-- - in slaczka, 1985). C .. ..a. .---.-.. ... Above the Jawornik marls lies a ca. 300- 3 .. - ..--. meter complex of thickly bedded turbidite sandstones called the Cergowa sandstones after the prominent mountain peak southeast of Dukla. The sandstones are calcareous, . . - medium to fine grained, and are interbedded with gray calcareous shales and thin-bedded sandstones. The shaly horizons contain a planktonic foraminiferal assemblage with Chiloguembelina gracillima (And.), Turboro- Figure 3. Composite stratigraphic section o the upper talia liverovskae (Bykova), Pa rag lo boro- Eocene to Oligocene deposlts of the Dukla 6nit in the vicinit of Dukla. Arrow indicates the position of the talia opima nana (Bolli), Subbotina amplia- ~kalnillimestone,sampled by Grzybowski (1890. pert ura (Bolli), Cibicides amphylisensis (Andr.), C. lopjanicus (Mjatliuk), Uviger- The microfauna Grzybowski described is inella majcopica Kraeva, Bolivina fastiga from the so-called "sandy limestone layer". Cushman, Trifarina tenuistriata (Reuss) Detailed geological mapping in the area has (Olszewska in slaczka, 1985). revealed that this bed lies within the Above the sandstone complex, a ca. 350- Menilite beds, not within the "red shales" as meter series of dark brown, fissile shales with Grzybowski noted in his paper. The "sandy minor thinly-bedded sandstones is developed. limestone layer" can be seen today in a number These are known as the Menilite shales. In of small abandoned quarries, the most notable the lower and middle portions of this series, of which is situated northwest of the her- bedded cherts layers are found. Accompanying mitage of Blessed John of Dukla (Figure 2). the upper bedded chert horizon, a several- 228 Andrzej Slqczka meter-thick layer of calcareous sandstones low area at the western edge of the Dukla and conglomerate is found in the area of Basin. Away from the source region, the Dukla, which is locally known as the Skalnik thickness of the Skalnik limestone diminishes limestones. This layer consists of fragments of to ca. 2 m toward the southeast and the pro- marly limestones, bryozoans, Lithothamnia, portion of calcareous clasts declreases. Toward foraminifera, and grains of quartz. Less com- the top of the sedimentary column, the monly, mica flakes, dasts of green and gray Menilite shales are gradually replaced by a shales, and fragments of Calpionella lime- ca. 500-meter complex of gray shales and thin- stones are found. A rich assemblage of fossil bedded, laminated, fine-grained turbidite bryozoans has been described from this layer sandstones belonging to the Krosno beds. at its type locality in Skalnik (Pazdro, 1929, Malecki, 1963) and from the old quarry south 2. The Wadowice Region of Dukla (near the hermitage of Blessed John Detailed geological investigations in the area of Dukla) Grzybowski (1894) and Gmigielska of Wadowice undertaken by Ksiazkiewicz (1961) described a rich foraminifera1 fauna. (1951, 1966) have revealed that the red and Subsequent investigations have found that this limestone horizon extends in a finer- green marls analyzed by Grzybowski (1'896) were derived from the Subsilesian Unit. The grained facies throughout a significant part of exact locality where Grzybowski's samples the Dukla Unit (Glaczka, 1971). Glaczka and were collected no longer exists, because a Walton (1992) have suggested the limestone church and parish school now stands on that was deposited by a turbidity current that was spot. However, very similar lithologies can be probably generated by a seismic event (a seis- found in small outcrops in streams in the area moturbidite). The clastic material was surrounding Wadowice (figure 4). derived from a paleobathymetrically shal-

Fi re 4. Geological map of the area south of &owice, redrawn after Kaiazkiewicz (1951). @ - Krosno Beds, OEm - Menilite beds, Kms- Senonian varie ated shales, I(' - Szydlowiec bryozoan - ~itfothamniasand- stones, Ek- Gorzen glauconitic sandstones. Qt - Quaternary terraces. A - Grzybowski's locality, B - Neotype locality in Zawadka. Geology of classic localities 229

The Subsilesian unit, which is situated green marls or variegates marly shales, and between the Silesian and Skole tectonic units, the upper Eocene consists of green shales. As in is characterised by sediments dominated by the other parts of the Carpathian basin, envi- marls and claystones. These marly sediments ronmental conditions changed markedly at are interpreted as having been deposited on a the Eocene/Oligocene boundary, and the submarine high that bordered the Silesian Oligocene is developed as dark Menilite basin to the north. In the area of Wadowice, shales. Tectonic disturbance does not allow us the Subsilesian sediments are highly dis- to determine whether younger deposits (i.e. turbed tectonically. The presence of numerous the lateral equivalent of the Krosno beds) small tectonic slices and the poor state of the occur in this profile of the Subsilesian Unit. outcrops do not allow the luxury of a complete However, these beds are known from other stratigraphic profile where the succession of units to the south and to the north of the sediment fades can be reconstructed by super- Wadowice region. We cannot exclude that a position. A further complication is the part of the Krosno beds placed in the external presence of submarine slumps and debris flows flysch in fact belong in this profile. in which blocks of marls and clays of various ages occur (Gwizdowska, 1992). 3. The Krosno Region In the Wadowice region, Ksiqzkiewicz The Paleogene deposits from which Grzy- was able to distinguish various lithological bowski (1898) described his "Foraminifera horizons within the Subsilesian Unit Senon- from the oil-bearing deposits of the Krosno ian variegated marls, green Paleocene and region" mainly belong to the northern part of lower Eocene clays, middle Eocene greenish the Silesian nappe: the Potok - Turaszbwka - clays, light green upper Eocene Globigerina Krosaenko Anticline (figure 5). Additional marls, Oligocene brown Menilite clays, as material (Bobrka, Wietrzno, Rbwne, Iwonicz) well as Oligocene gray marly clays and sand- was collected from the B6brka - Rogi and stones (corresponding to the Krosno beds). To- Iwonicz Folds, which are located in the wards the south, Ksiqzkiewicz recognised the southern part of the Silesian nappe. Szydlowiec bryozoan-Lithothamnia sand- Grzybowski's samples were collected from stones, as well as the Gorzen glauconitic sand- boreholes that no longer exist. Fortunately, stones, both of which are now placed in the the outcrop Grzybowski described on the "external flysch", interpreted as the western Wislok River near the confluence of the extension of the Skole Nappe (Koszarski, Smierdziqczka Stream in the northern suburbs 1985). of Krosno may still be sampled, and serves as Recent detailed investigations southwest a neotype locality for many of Grzybowski's of Wadowice (Gwizdowska, 1992; Balcer, species (Kaminski and Geroch, this volume). 1990) have resulted in a more detailed under- The only locality outside the Silesian nappe standing of the sedimentary profile of the was the area of (the Suszycki Subsilesian Unit. This profile commences with well), which is situated in the marginal part Turonian noncalcareous red shales. These of the Magura nappe. grade into lower Senonian red shales and The Paleogene deposits of the northern marly shales or red shales with thin streaks part of the Silesian nappe begin with lower of green shales. The Campanian is present as Eocene thickly bedded, coarse grained con- red marls with green streaks or as variegated glomeratic Ciezkowice Sandstones. These marls. The Maastrichtian is developed as comprise several lenses that are separated by green and light green marls, and the Paleocene thin red shale horizons. Above the sandstones as greenish marls or as variegated marls and is a middle Eocene red shale complex with shales. The lower Eocene is present as red intercalations of green clays (layer 5 of marls, variegated marly shales, and green Grzybowski) that attains a thickness of 200 m. shales. The middle Eocene is represented by The presence of exclusively deep-water Andrzej Slqczka

Figure 5. Geological map of the Krosno Area. ok- Krosno beds; Om - Menilite beds (sandstones); E~ - Hieroglyphic Beds; EC- Ciekowice Sandstones; OmU-Menilite beds - Kliwa Sandstones. agglutinated foraminifera1 assemblages clays. This sedimentary change marks the points to a deep sea environment that is com- beginning of the Oligocene Menilite beds, and parable to the lower Marssonella facies or is linked to Eocene/Oligocene tectonic Recurvoides facies of Haig (1979). Toward the movements which isolated the Carpathian north, the Ciezkowice sandstones are replaced basin from the Atlantic. These "sub-hornstone laterally by the red shale complex. Locally, shales" reach a thickness of ca. 20 m, and are especially in the southern part of the Silesian almost totally devoid of foraminifera and nappe, a unit of medium- to thin-bedded sand- trace fossils. Within these sub-hornstone stones with intercalated green shales lies shales local lenses of sandstones or directly upon the Ciezkowice sandstones. conglomerates can be found (up to 50 m thick), These are called the Hieroglyphic beds which contain a redeposited shallow-water because of their abundant trace fossils. In the fauna. Above the dark claystones, a horizon of upper Eocene, the variegated shales give way brown bedded cherts and silicified marls to green and greenish gray shales several tens (hornstones) overlain by a several tens of of meters thick (layer 4 of Grzybowski), meters thick unit of dark Menilite shales is which are overlain in turn by a several-meter- observed. This corresponds to Grzybowski's thick unit of yellowish green marls containing layer 2. Above the Menilite shales lies the abundant globigeriniform planktonic complex known as the Krosno beds, which is foraminifera. These are the so-called over two thousand meters thick. These beds "Globigerina marls" (layer 3 of Grzybowski), begin with a thickly bedded gray, rnicaceous which represent the latest Eocene (Van sandstones (layer 1 of Grzybowski) that grade Couvering et al., 1981). Subsequent to the upwards into a complex of medium-bedded, deposition of the Globigerina marls a drastic fine-grained, micaceous sandstones and gray paleoenvironmental change took place in the clays and marly clays. In the upper part of Carpathian Basin, represented by the onset of this profile, the shales and mudstones are the deposition of dark brown clays and marly dominant lithology. Geology of classic localities

Region 4. The Gdce dred years, and the sampled sedimentary Grzybowski devoted his last palaeonto- horizons sometimes outcrop in other places. logical monograph to the foraminifera1 The Carpathian flysch deposits in the assemblages of the Magura Unit in the vicin- area of Gorlice are comprised of two major tec- ity of Gorlice, Siary, %kowa, and Ropica tonic units: the Magura Unit and the Silesian (figure 6). In nearby Szymbark there was an Unit. In small tectonic windows within the exposure of the Inoceramus beds desaibed by Magura nappe, evidence of third unit tectonic his student M. Dyl~ankain 1923 (figure 7). unit is found. This is locally termed the The deposits are today classified as belonging 'Window Series", which constitutes the west- to the Magura tectonic-stratigraphic Unit. em extension of the Dukla Unit. The Magura The exact localities that Grzybowski and Unit comprises sediments of Turonian to later Dylaianka can only be identified in Oligocene age (Figure 8). In the Gorlice region, general terms, because the majority of wells the Magura Unit is developed in its northern and buildings these authors desaibed has facies, which has been variously termed the been destroyed during the two world wars. Racza-Gorlice facies (Kozikowski, 1%3), the The quarry described by Dylaianka has dis- Gorlice facies (Weclawik, 1%9), or the Siary appeared without a trace. In addition, the sub-unit. condition of the stream outaops described by both authors has changed over the last hun

Figure 6. Geological map of the Siary - Spkowa area, after Widz (1985). EC- Cigikowice sandstones, Ki - Inoce- ramian beds with lenses of red shales, Kk - thick-bedded sandstones of the Inoceramian beds, K - Inoceramian beds (undifferenti-ated),d: - Krosno beds, OEm - Magura Formation, SM - Sub-Magura shales. Scale bar is 1 km. Andrzej Slqczka

Figure 7. Geological map of the Szymbark area, after Sznicm (1991). EC - Ciezkowice sandstones, EPs - Variegated shales, Eh - Hieroglyphic beds, Ki - Inoceramian beds with lenses of red shales, @ - thick-bedded sandstones of the Inocelamian beds, OEm - Magum Formation, SM - Sub- Magura shales.

The oldest sediments exposed in the area the Szczawina beds (Sikora, 1970). The mid- are represented by a unit of strongly lithified dle part of the Inoceramus beds consists of a red shales with sporadic thin beds of sand- lenticular complex comprised primarily of stones and fucoid marls. The thickness of this coarse, thickly-bedded, feldspathic, graded basal complex reaches several tens of meters. sandstones which are commonly noncalcareous Above the basal complex occurs a unit of and contain redeposited plant fragments. The thin- to medium-bedded, fine- to medium- thickness of this complex reaches 180 m. In the grained laminated, micaceous, calcareous valley of the Ropa River, sporadic layers of sandstones that are interbedded with dark red shales appear in the upper portion of the gray, clayey or calcareous shales known as the Inoceramus beds. In this region, the transition Inoceramus beds. This lithological unit is also between the Inweramus beds and the overly- called the Ropianka Beds after the nearby ing variegated shale series has been described village. This unit also contains layers of light by Sznicer (1991). By contrast, near the town of gray fucoid marls as well as sporadic medium- Siary, between the Inweramus beds and the to thick-bedded sandstones. The latter variegated shales it is possible to recognise a display graded bedding. The layers of fucoid several tens of meters thick complex of dark marls gradually disappear toward the top of gray, sometimes greenish, usually noncalcare- the unit. ous shales and mudstones. These are interbed- The lower part of the Inoceramus beds is ded with thinly bedded, fine-grained, lami- characterised by the presence of abundant nated, micaceous-calcareous sandstones as muscovite mica flakes, and have been called well as with greenish, fine - grained sand Geology of classic localities 2 3 3

stones that are noncalcareous. This complex correlates with the Swia tkowa beds (Kozikowski, 1956). The total thickness of the hoceramus beds is difficult to determine be- cause of the high degree of folding. However, structural relationships suggest their thick- ness reaches 800 m. Above the Inoceramus (or Swiatkowa) beds, a complex of red and green shales is found. The lower part of the variegated shale unit consists of almost pure shales, with rare I intercalations of thinly-bedded, green-gray, sometimes glauconitic, noncalcareous sand- stones. The number of sandstone layers in- aeases towards the top of that portion of the variegated shales, where a ca. 170 m thick lense of thick-bedded glauconitic sandstones and conglomerates appears. The sandstones display graded bedding, and slump deposits are occasionally developed. h one of these slump deposits, a block of red claystones with tuffaceous layers was found (Sznicer, 19911. Because of their lithologic similarity to co- eval sandstones of the Silesian Unit, these sandstones have also been referred to the Cieikowice sandstones. Similarly in the mid- dle part of the variegated shale unit, a ca. 30 m-thick sandstone unit is found. The sand- stones are greenish, thin- to medium-bedded, laminated, fine-grained, noncalcareous, and are characterised by abundant trace fossils. The sandstones are interbedded with red, green, and dark brown shales. This unit corre- sponds to the Hieroglyphic beds in other parts of the Polish Carpathians. In the marginal thrust sheets of the Magura nappe, both sandstone units disappear (Sznicer, 1991, Widz; 1985). The uppermost part of the variegated shales, which is nearly 200 m thick, is nearly devoid of sand- stone layers. Locally, the variegated shales are overlain by a ca. 30 m-thick complex of olive-green, noncalcareous shales. h other places, layers of green marls with planktonic foraminifera are found (Sikora, 1970). The latter correspond to the Globigerina marls of ~igure8. Composite stratigraphic column of the 0th- tectonic units. This complex is overlain Mngura Unit in the Siary-SrymbPrk area. by a unit of dark brown claystones that is sev- eral meters thick. The local absence of the 234 Andrzej Slqczka green and brown claystones may be explained are developed here mainly as light gray or by tectonic shearing, or by synsedimentary yellowish, thick-bedded, coarse- to medium- erosion during the deposition of the overlying grained noncalcareous sandstones and micro- Magura beds. conglomerates. The sandstones are of the flux- The Magura beds are represented above oturbidite type and are homogeneous. Spo- all by thickly bedded, coarse- to medium- radic interbeds of fucoid marls and clayey con- grained, graded calcareous sandstones and glomerates with abundant crystalline clasts conglomerates. In addition to quartz, the are also found. The sandstone series is over- Magura sandstones contain clasts of feldspar, lain by a ca. 50 cm-thick unit of red and green glauconite, and muskovite. The sandstones are shales, which is in turn overlain by a complex interbedded with gray, green, and black mud- of thick-bedded Cigzkowice sandstones. These stones and shales. The mudstones sometimes are yellowish, thickly-bedded, noncalcare- contain abundant plant detritus and thin to ous, fluxoturbiditic sandstones and microcon- medium sandstone beds. Debris flow deposits glomerates, with individual beds several me- are also found. This series of shales and sand- ters thick. A several-centimeter-thick band of stones sometimes attains a thickness of tens of red shale divides the Cieikowice sandstones meters, and most commonly comprises the into two horizons: Horizon 1 (upper) and lower part of the Magura beds. The total Horizon 2 (lower). In the western part of the thickness of the Magura beds in the Gorlice study area, the Ciezkowice sandstones are ca. area is estimated at 600 m. 200 m thick, whereas towards the east their The Magura Unit in the Gorlice area is thickness diminishes to ca. 100 m. strongly disturbed by tectonics. It is developed Above the Ciezkowice sandstones is as a series of imbricated folds, with dis- another unit of red shales (about 10 m thick), placements between the beds. These folds are which is overlain in turn by the Hieroglyphic broken into blocks by transverse faults, which beds. The latter unit consists of red, green, and are particularly well-developed in the Ropa brown shales with thinly-bedded, laminated, River valley. fine-grained, glauconitic, noncalcareous sand- stones. Toward the top of the unit the sand- The Window Series stones are replaced by brown shales. Sediments of the "Window Series" are present The overlying Menilite beds in this por- as small blocks that have been ripped up and tion of the Silesian nappe are developed incorporated into the Magura nappe. These in somewhat atypically. They are present as a turn, have been overthrusted onto the Silesian thick-bedded, coarse-grained, glauconitic nappe. The sediments consist of gray, thick- sandstones with lenses of conglomerate, known bedded marls with occasional thinly-bedded collectively as the Magdalena sandstones. In laminated sandstones such as those found in the upper part of the stratigraphic column, the Siarka Stream (Widz, 1985), or by dark white quartz sandstones appear. The dark gray noncalcareous shales and mudstones with brown claystones that typically comprise ihe gray, thinnly-bedded, muscovite-bearing, cal- Menilite beds are only a subsidiary component careous sandstones (Sznicer, 1991). in this profile. Their total thickness is esti- mated as ca. 200 m. The Silesian Unit Generally, the Magdalena sandstones are In the area of Gorlice, the southern part of the directly overlain by gray, micaceous, thickly- Silesian Unit is present as the strongly imbri- bedded, medium-grained, calcareous sand- cated Gorlice Fold. The unit is comprised of stones. These comprise the lower part of the sediments of late Senonian to Oligocene age Krosno beds. The upper Krosno beds are pre- (Swidzihski, 1973). sent as laminated, medium-bedded, fine- The oldest sediments known from surface grained, micaceous, calcareous sandstones exposures belong to the Istebna beds, which with intercalations of gray calcareous shales. Geology of classic localities 235

Thickly-bedded sandstones occur only sporad- are in turn overlain by a unit of calcareous tur- ically. Near the top of the profile, the thick- bidites that is largely silicified (the siliceous ness of shaly interbeds increases and finally marls, or Holwina marls), and contains Z-lel- shales predominate. In this part of the upper vetoglobotruncana helvetica (Bolli), D i- Krosno beds, the thin, laminated, Jaslo lime- carinella imbricata (Mornod), Globotruncana stones have been found (Swidzifiski, 1973). angusticarinata (Gandolfi), Marginotruncana The thickness of the Krosno beds exceeds 2000 tricarinata (Quereau), M. marginata (Reuss), m. In the Gorlice area they are predominantly Uvigerinammina jankoi Majzon, Stensioina covered by the overthrust of the Magura praeexculpta (Keller) among other species nappe. (Kotlarczyk, 1988). This assemblages indi- cates that the siliceous marls continue to the 5. The Rzesz6w - Debice Region Coniacian. These are covered by a several- The area sampled by Friedberg (1901) is hundred-meter thick turbidite series belong- located in the northern marginal part of the ing to the upper part of the Inoceramus beds. Skole Unit. This unit is the most external Thickly bedded sandstones are found in the nappe of the Carpathians in Poland (figure 9). middle part of this unit. Beds of fucoid marls The deposits that Friedberg sampled belong to occur sporadically. In the lower part of the various horizons in the Upper Cretaceous unit, and in the upper part, lenses of light- Inoceramian beds, a unit that is also known as coloured limestones are found. The latter rep- the Ropianka beds. These beds have now been resent sediments that were deposited by mud subdivided into individual formations, mem- flows or submarine slumps (the Wegierka bers, and beds (Kotlarczyk, 1978). marls, or Baculites marls). This part of the In this part of the Skole Unit, subsequent Inoceramus beds is early Campanian to Pale- studies have demonstrated that the Upper ocene in age. Cretaceous consists of Turonian variegated The lack of detailed geographical infor- clays overlain by (and partially interfinger- mation in Friedberg's paper makes it difficult ing with) the Inoceramian beds (Wdowiarz, to determine which lithological horizons he 1949; Jurkiewicz and WoiAski, 1981). The lat- sampled. Based on his descriptions, it is prob- ter are comprised of siliciclastic turbidites able that the "dark clays from E;opuchowa" and marls and are known as the Pisarzowice were collected from the upper part of the beds (Jurkiewicz and Woihski, 1981). These Inoceramian beds close to the Wegierka marls.

km ((. - Skole Nappe tbrust margin O- O-

Figure 9. Geological map of the Skole Nappe in the Debica region. M - Miocene; P - Eocene variegated shales, KP - Upper Cretaceous - Paleocene Inoceramian beds; Wk - Upper Senonian Wegierka (Baculites)Marls; K - Upper Cretaceous Inoceramian sandstones; Pk - Turonian Pisa~zowicebeds (after Jurkiewicz and Woihski, 1981). 236 Andrzej Slqczka

Gumniska were collected from claystones within the thickly bedded sandstones in the middle part of this unit. The sample from Slocina east of Rzeszow is derived from red claystone layers within the Inoceramian beds.

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