The tectonics and stratigraphy of the transitional zone between the Pieniny Klippen Belt and Magura Nappe ( Szczawnica area , Poland )

The Pieniny Klippen Belt is a narrow, complex structure stretching along a tectonic boundary between the Central and Outer Carpathians. Its formation involved two main evolutionary stages, the first, related to Late Cretaceous-Paleocene folding and thrusting, and the second, associated with Miocene orogenic events in the Outer Carpathians. Interactions between the Pieniny Klippen Belt and Outer Carpathians during both the sedimentation and deformation stages have resulted in the establishment of a peri-klippen transitional zone (named the Šariš Transitional Zone), in which the tectonic deformation effects gradually decrease towards the north. The stratigraphy and tectonic position of this zone have been controversial for decades. The key stratigraphic problems concern 1) the lithologic identity and position of the Szlachtowa (“black flysch”), Opaleniec and Pieniny formations and 2) the relation of the Jarmuta Formation, associated mainly with the Šariš Transitional Zone, to the Szczawnica and Zarzecze formations of the Magura Nappe. We provide an early Paleogene dinoflagellate cyst stratigraphic record of deposits that, according to some recent reinterpretations, represent the Neogene “Kremna Formation”. The legitimacy of new lithostratigraphic assignments of the “Kremna Formation” at Jaworki is put into question upon the basis of the primacy of units introduced for the same strata earlier.


TECTONIC EVOLUTION OF THE PIENINY KLIPPEN BELT
The Pieniny Klippen Belt (PKB) represents a ca.600-700 km long trace of a major suture located between the Central and Outer Carpathians (Figs. 1, 2).It involves Jurassic (locally Triassic) to Paleogene deposits of very variable lithology (e.g.Andrusov 1965, Birkenmajer 1986, Plašienka et al. 2012).In the Polish/Slovakian borderland, the structure of the PKB includes the so called Klippen tectonostratigaphic units of Czorsztyn, Niedzica, Czertezik, Branisko, Pieniny and Haligovce (e.g.Birkenmajer 1986, Mišík 1997).In the lithostratigraphical sense, the PKB sedimentary sequences can be divided into two main complexes: a "rigid" carbonate rocks -dominated complex of Middle Jurassic-Late Cretaceous age, and a ductile complex of shales, marls and flysch rocks of Late Cretaceous age.The third rock complex, in most cases less significant than the other two because of its smaller thickness, consists of ductile Lower-to-Middle Jurassic marls, shales and mudstones.This contrasting lithology of sedimentary sequences was responsible for the PKB disintegration into isolated klippen during a complex tectonic evolution (Birkenmajer 1959).
https://journals.agh.edu.pl/geolJurewicz E., Segit T.   Birkenmajer 1979, Jurewicz 1994, 2018, Plašienka 2012, simplified and modified) During the deposition of the PKB sedimentary succession, a separate Grajcarek Basin was located to the north.Both the basins have been isolated by the Czorsztyn Ridge since the latest Aalenian-Early Bajocian.From the Albian onward, the Grajcarek Basin lost its individuality and became part of the Magura depositional basin.The recent structure of the PKB developed in two main stages of tectonic evolution (e.g.Froitzheim et al. 2008).The first stage was related to Late Cretaceous-Paleocene folding and thrusting.Simultaneously with the folding events, in the Magura Basin located to the north, the so called Jarmuta Fm. originated, composed mainly of wildflysch sediments, containing clasts of the klippen rocks (Birkenmajer 1970).Due to a favorable paleotopography, the northernmost tectonostratigraphic units of the PKB (the Czorsztyn and Niedzica units) were transported through gravity sliding, defragmented into slices and thrust onto sediments of the Magura Basin, forming numerous olistoliths and olistostromes (Jurewicz 1994, 1997, Plašienka et al. 2017).One of the largest olistoliths can be observed in the Małe Pieniny.It defines the Homole-Biała Woda Block, composed of the flat-laying Czorsztyn Unit and of the thrust-faulted and strongly folded Niedzica Unit.The Biała Woda Block has gravitationally slid onto sediments which used to be considered part of the so called Grajcarek Unit by Birkenmajer (1970).According to Birkenmajer (1970), the Grajcarek Unit was back-thrust to the south over the nappes of the Klippen Belt, to later form tectonic remnants.Plašienka (2012), in turn, called this unit the Šariš Unit which -in his opinion -formed the tectonically lowermost tectonic body of the PKB.This unit was interpreted by this author as having formed due to repeated gravity sliding which episodically continued until the early Eocene.However, both the Grajcarek Unit in Poland (Birkenmajer 1979(Birkenmajer , 1986) ) and the Šariš Unit in Slovakia (Plašienka et al. 2012) do not fulfill the necessary criteria to constitute a separate tectonic unit, since representing such a unit would require: (1) coherent tectonosedimentary evolution, (2) a precise timing of its tectonic deformation and (3) an unambiguous definition of its borders (Jurewicz 2018).Instead of defining the Grajcarek or Šariš Unit, it is a better idea to distinguish a transitional zone at the Magura-directed front of the Klippen Belt, and to name it the Šariš Transitional Zone.The latter must have originated due to polygenetic and polyphase tectono-sedimentary processes.Such a transitional zone does not require a northern limit, which is also expected to separate the Central from the Outer Carpathians and which is difficult to be found in the field.

S L O V A K I A T H I
During the Paleocene-Eocene Thermal Maximum (Storey et al. 2007) and global sea-level changes, the PKB collapsed and was buried under a blanket of flysch deposits.The latter represented the fill of the then forming Central Carpathian Paleogene Basin (Jacko & Janoko 2000) in the northern part of the Tatricum realm.
The second stage of the deformation of the PKB was related to the Miocene orogenic processes in the Outer Carpathians (e.g.Oszczypko 2006 and references therein).Consequently, the original structure of the PKB was obliterated by local thrust-and strike-slip faulting, tectonic slicing and formation of out-of-sequence faults.The PKB became further fragmented into isolated klippen.In the opinion of Oszczypko & Oszczypko-Clowes (2014), who documented an occurrence of Miocene sediments (Kremna Fm.) in the Magura Nappe and within the PKB, the nappes of the PKB, together with the Grajcarek sheets, overode on a shallow dipping thrust the Miocene sediments of the Magura Nappe.In their conception, the PKB in the Małe Pieniny Mts.does not represent a sub-vertical and deep-rooted structure and it is only a zone of tectonic remnants floating on the rear rim of the Magura Nappe.The age of the folding and thrusting is ascribed by the latter authors to the Early Miocene, i.e. it must have occurred after the deposition of the Kremna Fm.

INFLUENCE OF THE PLATFORM BASEMENT ON THE PKB STRUCTURE
During the Miocene formation of the Outer Carpathians accretionary prism, the North-European platform was underthrust below the nascent orogen, undercutting and underplating the PKB and the Tatricum massifs located in the south.This underplated platform basement, with a number of deep fracture zones, must have influenced the overlying geological structure of the PKB.The fault pattern within the North-European Platform mostly dates back to the Variscan orogeny and earlier events.Important major faults are generally subparallel to the Teisseyre-Tornquist Zone (e.g.Pożaryski 1991, Guterch & Grad 2006), that is they are oriented NNW-SSE.A regional-size major fault, of a deep fracture zone nature, is the Kraków-Myszków Fault Zone, defining a contact between the Małopolska and Upper Silesian blocks and representing a Paleozoic terrane boundary (Żaba 1996(Żaba , Buła & Żaba 2008)).A southeastern extension of this fault is likely the Dunajec Fault, which (Figs. 2,3), at its eastern side, offsets the PKB by 700 m to the south (Birkenmajer 1979).
The Dunajec fault thus seems to represent a mantle rooted fracture in the basement of the Outer Carpathians (Jurewicz 2005, Jurewicz et al. 2007, Nejbert et al. 2012).Along the course of this fault, the platform basement under the Outer Carpathians occurs 3000 m deeper on its eastern than on the western side (Zuchiewicz & Oszczypko 2008).The Dunajec Fault has repeatedly been activated as a dextral strike-slip fault (see Buła & Żaba 2008).
During one of its latest activation stages in the Miocene, andesitic rocks were emplaced along an "en échelon" system of second-order faults adjacent to the Dunajec Fault.The isotopic K-Ar dating of Birkenmajer & Pécskay (1999) indicated two phases of volcanic activity there in the interval of 12.5-10.8Ma (see Anczkiewicz & Anczkiewicz 2016).A parental magmatic chamber of the andesites may have been located at a depth of ca 10-12 km.The chemical composition of the andesites from the area in question is not typical of andesites from subduction zones, and its formation may rather be linked with a deep fault zone (Pin et al. 2004, Jurewicz & Nejbert 2005).In the vicinity of Szczawnica, Leśniak et al. (1997) documented a strong mantle helium signal related to andesites.
Pieniny andesites must have been generated in a metasomatised lithosphere of the European plate.Its partial melting may have been triggered by a local rise of asthenospheric material, related to reactivation of dextral motion on the Dunajec Fault.It might have also been connected with zones of adhesion originating as a result of fault-related shearing processes.The youngest stage of the Dunajec Fault activity is documented by extensional fractures in andesites, filled with flowstone-like calcite.The U-Th age of this calcite is ~2.5-6.5 ka (Jurewicz et al. 2007).Along the southern prolongation of the Dunajec Fault, near Ružbachy, travertine occurrences can be observed.

THE GRAJCAREK SUCCESSION AND SOME CONTROVERSIES CONCERNING ITS STRATIGRAPHY
The Šariš Transitional Zone involves some Jurassic-Lower Cretaceous deposits of the Grajcarek Succession which are strongly folded due to two reasons: their frontal position during the late Cretaceous-Paleogene nappe-stacking and their mechanically weak dominant lithology.The Grajcarek Succession represents a facies-bathymetric zone of a basin installed to the north of the submarine Czorsztyn Swell (pre-Late Albian Magura Basin of Barski et al. 2012).Dark micaceous mudstones with sandy-crinoidal turbidite beds, ascribed to the Szlachtowa Fm. (Birkenmajer 1977), are typical of the lowermost part of the Grajcarek Succession.According to Birkenmajer (1977) and Birkenmajer & Gedl (2017), deposition of the Szlachtowa Fm. also stretched over the Branisko Czertezik and Niedzica successions on the southern slope of the Czorsztyn Swell (ridge).However, the stratigraphic interval of the Szlachtowa Fm. is occupied by the Harcygrund and Podzamcze fms.

Fig. 4. Chrono-and lithostratigraphic assignments made for the same deposits of the Grajcarek or flysch Magura successions by different authors
Disparate opinions in favour of the Jurassic age involve two overlapping stratigraphic ranges: upper Lower to lower Middle Jurassic, with some hiatuses (Gedl 2008) and exclusively lower Middle Jurassic (Barski et al. 2012, Segit et al. 2015).
Regarding the source of Cretaceous stratigraphic record ascribed to the Szlachtowa Fm., it may have come from: (1) tectonic slices of some Cretaceous strata mistaken for the Szlachtowa Fm., (2) uncertain lithostratigraphic attribution and misinterpreted location of archived samples (e.g.samples collected by E. Blaicher in the 1960-70s in Oszczypko et al. 2012), (3) incorrect taxonomic determination of foraminifera in typically impoverished, poorly preserved or consisting of not age-diagnostic species assemblages in the true Szlachtowa Fm. (see also Tyszka 1995, Gedl & Jozsa 2015).
The Szlachtowa Fm. is overlain by the spotted-marly Opaleniec Fm., which yielded rich and well preserved palynomorph assemblages of the lowermost Upper Bajocian to Lower Bathonian (with no data on the uppermost part of the formation; Segit et al. 2015) or the uppermost Lower Bajocian to Callovian interval (Gedl 2008(Gedl , 2013)).Oszczypko et al. (2012) referred the Opaleniec Fm. at Jaworki/Szlachtowa to the Sprzycne beds from the Spisz sector of the Pieniny Klippen Belt (Sikora 1962(Sikora , 1971) ) of alleged Cenomanian age.The Sprzycne beds, however, proved to comprise tectonically amalgamated Jurassic and Cretaceous strata, erroneously attributed entirely to the Cretaceous by Sikora (1972) (Segit et al. 2015).
The tectonics and stratigraphy of the transitional zone between the Pieniny Klippen Belt and Magura Nappe (Szczawnica area, Poland) Calcareous nannoplankton recovered from the Jarmuta Fm. in Czarna Woda north of Jaworki, indicated Maastrichtian to Middle Paleocene interval (Birkenmajer et al. 1987), whereas the overlying Szczawnica Fm. yielded Middle Paleocene to possibly Early Eocene species (Birkenmajer & Jednorowska 1979).Although the chronostratigraphy of the boundary of the Szczawnica and Zarzecze fms. is not well constrained (see Waśkowska & Golonka 2016) it has been widely accepted that both units represent lower Paleogene.
A completely different interpretation of the stratigraphy and tectonics of the Szczawnica -Jaworki area was given by Oszczypko & Oszczypko-Clowes (2014).They attributed the whole flysch succession exposed between (and partially including) the Jarmuta Fm. in the south and the Magura Fm. in the north to the Kremna Fm. (Oszczypko et al. 2005) of supposedly latest Oligocene to Early Miocene age, as based on calcareous nannoplankton (zones NN1 and NN2) (Fig. 4).
The stratigraphic and taxonomic documentation of the Kremna Fm. at Jaworki in Oszczypko & Oszczypko-Clowes (2014) suffer, however, from some imperfections.First, figures showing detail position of sampled beds in the sections studied are lacking; exemplary outcrops of typical lithofacies and small-scale cross sections were illustrated instead.The situation of the exotic pebbly mudstones of the Jarmuta Fm. in the middle course of the Czarna Woda Creek as proposed by Oszczypko & Oszczypko-Clowes (2014) is confusing; the area and lithology described therein were attributed elsewhere in the same paper to the Kremna Fm.
It should be stressed that partial or total substitution of the Jarmuta, Szczawnica and/or Zarzecze fms.(see Birkenmajer & Jednorowska 1979, Golonka & Rączkowski 1984, Birkenmajer et al. 1987) for the Kremna Fm. (as in Oszczypko & Oszczypko-Clowes 2014) in the area to the north of Szlachtowa and Jaworki was intrinsically illegitimate.This interpretation was invalidly founded upon the priority of chronostratigraphic equivalence over the lithologic/facies identity of lithostratigraphic units.On the premise that the considered deposits (i.e.Jarmuta, Szczawnica and Zarzecze fms.) were age-equivalent to the Kremna Fm., but had significantly different lithology, the individual lithostratigraphic assignments should have been retained.According to Oszczypko & Oszczypko-Clowes (2014), the Kremna Fm. can be characterized by the presence of thin to medium-bedded carbonate flysch with intercalations of thick to very thick-bedded sandstones and conglomerates, as well as exotic paraconglomerates and thick marly beds and laminated sandy limestones and dark grey marl mudstones with Chondrites ichnofacies.Regarding the Jarmuta Fm., it is represented by thick-bedded turbidites, conglomerates and sandstones with subordinate intercalations of grey marly shale and locally contains debris flow paraconglomerates, whereas the Szczawnica and Zarzecze fms are composed of sandstone-dominated turbidites (see Oszczypko & Oszczypko-Clowes 2014).These characteristics are not sufficient to unambiguously infer a lithological distinction or identity of the deposits in question with regard to the Kremna Fm.If, in terms of chronostratigraphic and lithologic/facies features, the Kremna Fm. were to be equivalent to the considered deposits, then the "Kremna Formation" would have been a junior synonym of the lithostratigraphic units representing these deposits and should have been discarded.

SELECTED KEY PROBLEMS OF THE PKB GEOLOGY: THREE FIELD EXAMPLES
The primary aim of presenting the three localities described below is to clarify the issue of the northern limit of the PKB, which, at the same time, also defines the boundary between the Outer and Central Carpathians (see Birkenmajer 1986, Jurewicz 2018 and references therein).The secondary aim is to highlight the currently underestimated impact of heterogeneity of the underplated North European platform on the tectonic evolution and present-day structure of the PKB.Yet another aim is to show the type area and exposures of the Grajcarek Succession and lowermost flysch Magura Succession which were involved to a large extent into the accretionary prism during the Late Cretaceous-Paleocene formation of the PKB.The context of major stratigraphic misconceptions related to these deposits are also to be presented and discussed in light of the newly acquired stratigraphic evidence.

Zawiasy 49°26'00"N; 20°26'18"E (see Figs. 1, 2 for location) Role of the Dunajec Fault in the tectonic evolution of the PKB Edyta Jurewicz
The Dunajec Valley is a good spot to highlight the impact of the heterogeneity of the underplated North European Platform on the tectonic evolution and present-day structure of the PKB.The Dunajec Fault which can be correlated with the deep rooted Kraków-Myszków Fault Zone (Żaba 1996, Jurewicz 2005, Nejbert et al. 2012) has divided the PKB into two different segments: the Pieniny Mts. to the west and the Małe Pieniny Mts. to the east of it.Towards the east, the PKB becomes consecutively more fragmented into isolated klippen and its northern limit becomes progressively more difficult to delineate.
The main differences between both areas are presented in Table 1.

Table 1
The main geological differences between the Pieniny and Małe Pieniny Mts.

Pieniny Mts.
Małe Pieniny Mts.The arguments in favor of the Dunajec Fault's (DF) connection with the Kraków-Myszków Fault Zone (KMFZ) are listed below: − DF is one of the NNW-SSE fault zones sub-parallel to the TTZ; − DF shows the same trend and it occurs at a direct continuation of the KMFZ; − the same dextral strike slip movement is observed on DF at the PKB offset, connected with Miocene transpression (Birkenmajer 1977(Birkenmajer , 1986)); − the platform basement is in 3000 m deeper on the DF' s eastern side (Zuchiewicz & Oszczypko 2008); − andesite dykes are in "en echelon" position with respect to the DF (Jurewicz et al. 2007); − chemical composition of andesites is typical of a deep fault zone associated by adiabatic decompression of upper mantle, related to shearing processes and a pull-apart displacement (Pin et al. 2004, Nejbert et al. 2012); − magmatic chamber of andesites could have been located at a depth of 10-12 km (Nejbert et al. 2012); − there is a strong mantle helium signal connected with andesites (Leśniak et al. 1997); − there is neotectonic activity (6000 k) along DF indicating the same dextral shearing as that on KMFZ (Jurewicz et al. 2007); − there is a travertine occurrence along the DF near Ružbachy.

Krupianka Creek and Baba Rock 49°24'15"N; 20°32'25"E (see Figs. 1, 2 for location) The Šariš Transitional Zone Edyta Jurewicz
At the base of the Baba Rock one can ask: Where are we?In the PKB or in the Outer Carpathians?
The answer is not easy because of displacements and other interactions between the PKB and Outer Carpathians during the sedimentation and deformation stages of their development which have resulted in a difficult-to-delimit, transitional zone.Until now, in the structural sense, this zone had the rank of a tectonic unit.It was termed the Grajcarek (in Poland) or Šariš Unit (in Slovakia) but the northern boundary of this "unit" was difficult to recognize in the field.The tectonic deformations in this area gradually vanish towards the north, and therefore one could not know if the boundary should be put along the "last thrust-fault" or on the "last olistolith" (?).In the opinion of this author, the sediments in the Krupianka Creek near the Baba Rock (Fig. 5) should not be ascribed to a separate tectonic unit, but considered only as occurring in a distinct zone of deformation (Jurewicz 1994(Jurewicz , 1997)).This zone, transitional in its nature, consists of strongly deformed slices composed of Jurassic-Cretaceous sediments originated in the peri-klippen Grajcarek (pre-Albian Magura) Basin and synorogenic wild-flysch rocks, breccia type sediments and numerous olistoliths composed of klippen units.This zone can therefore be defined as a peri-klippen part of the Magura Nappe which lacks a distinct northern tectonic limit.To discriminate it with the Grajcarek Basin, it is named the Šariš Transitional Zone (because it is not only the sediments from the Grajcarek Basin that are included to this zone).The name "Grajcarek" will be reserved to the lithostratigraphic succesion of the Grajcarek Basin (Birkenmajer & Gedl 2017), which existed during Jurassic to Early Cretaceous times in the southernmost (peri-klippen) part of the Magura (pre-Albian Magura) Basin.

The Czorsztyn Succession in Krupianka Creek Tomasz Segit
The Krupianka Creek, as well as the adjacent Homole Gorge, are unique along the Pieniny Klip-pen Belt in that they show the fairly complete mid-Jurassic-Cretaceous strata of the Czorsztyn Succession lying almost flat.The lowermost beds in the sequence are grey and black shales of the Skrzypny Fm. (Fig. 6A).These deposits differ from the Szlachtowa Fm. in their lack of turbidites, paucity of mica flakes, more clayey composition and common presence of siderite nodules.Unlike the Krempachy Marl Fm., which underlies the Skrzypny Fm. elsewhere, the dark shales of the latter formation are not distinctively bioturbated (spotted) and therefore should not be associated with the Fleckenkalk/Fleckenmergel facies (cf.Krobicki & Golonka 2008).Exposures of the Skrzypny Fm. in the Krupianka Creek yielded rich ammonite fauna (mainly Brasilia spp.) indicative of the Bradfordensis zone (Middle Aalenian) (see Myczyński 2004).Gedl (2008), on the basis of the impoverished dinoflagellate cyst assemblages, argued for a Lower and Middle Aalenian position of the same strata.The extensive ammonite collection from the Skrzypny Fm. (Myczyński 2004) clearly indicates that the basal part of this unit represents the Middle Aalenian (Murchisonae Zone).The sequence of the Skrzypny Fm. currently exposed in Krupianka Creek is probably not complete (partly covered) and lacks the Upper Aalenian component.
The Pieniny Klippen Basin witnessed a major facies changeover in the Early Bajocian (see Krobicki & Wierzbowski 2004).The rising of the Czorsztyn Ridge led to the formation of individualized bathymetric zones -the successions.The position of the Czorsztyn Succession was the shallowest and thus prone to emersion, winnowing and condensation.The Lower Bajocian hiatus, which involved some shallow parts of the basin, is recorded in the lowermost part of the massive crinoidal limestones (Smolegowa Fm.), directly above the Aalenian shales.These beds yielded phosphatic nodules, lithoclasts of green micritic limestones and ammonites diagnostic of the uppermost Lower Bajocian (see Krobicki & Wierzbowski 2004, Wierzbowski et al. 2004).Birkenmajer 1970, 1977, Wierzbowski 1994, Wierzbowski et al. 1999, Krobicki & Wierzbowski 2004, Barski et al. 2012, Plašienka et al. 2012, Segit et al. 2015, modified)

A B C
The tectonics and stratigraphy of the transitional zone between the Pieniny Klippen Belt and Magura Nappe (Szczawnica area, Poland) The contact of the Skrzypny and Smolegowa fms. is not exposed, except for the base of the limestone blocks that slid down the slope of the ravine (see Krobicki & Wierzbowski 2004).Abundant lithoclasts and concretions probably constitute the residue of green phosphatic shales, analogous to these recognized at base of the Smolegowa Fm. in Slovakia (Segit 2010).The thickness of the crinoidal limestone in Krupianka Creek, reportedly amounting to ca. ?20 m (see Birkenmajer 1979) (the bottom not exposed), contrasts with 100 m in neighboring Homole Gorge and 150 m in Biała Woda Creek (Smolegowa Klippe), indicating intensive synsedimentary faulting (see Krobicki & Wierzbowski 2004).White crinoidal limestones pass upward (following an omission surface) into the 1 m thick, thin bedded, fine-grained, reddish crinoidal limestones of the Krupianka Fm., attributed to the middle Upper Bajocian (Wierzbowski et al. 1999).Higher up in the sequence, above another hiatal interval, there occur red to violet-brown Amonitico Rosso limestones (Czorsztyn Fm.) with horizons of ferro-manganese nodules and encrustations (see Wierzbowski et al. 1999) of a total thickness ca. 15 m.These nodular limestones embrace a wide stratigraphic range up to the Tithonian (see Wierzbowski 1994, Hudson et al. 2005) (Birkenmajer 1979).

Tomasz Segit
The incised ravine of the Krupianka Creek cuts off the western margin of the Homole-Biała Woda Block (Czorsztyn Succession).The creek bed erosion reached the base of the block and exposed deposits of the Grajcarek Succession, represented predominantly by the Szlachtowa Fm. ("black flysch") (Fig. 6B).The Opaleniec Fm. is just a few meters thick.The overlying, tectonically reduced sequence of the Sokolica, Czajakowa and Pieniny fms.(Birkenmajer 1979, Gedl 2008) was erroneously attributed by Oszczypko et al. (2012) to the Hulina Fm. and their "Cenomanian Key Horizon" (see the discussion in Birkenmajer & Gedl 2017).
The absence of the Palenica Mb. (Czorsztyn Fm.), a unit typical of the Grajcarek Succession (Birkenmajer 1977), is probably a tectonic perturbation.The Pieniny Fm. is capped by marlstones of the Kapuśnica Fm., best exposed in a section of a large waterfall in the upper part of the ravine (Fig. 5).

Edyta Jurewicz
In the Czarna Woda Stream, located less than 2 km to the north-east of the earlier stop, we are a little further from the PKB units.In this locality one can observe synorogenic sediments of the Jarmuta Fm. (Maastricht-Paleocene), chaotic in nature, originating from gravitational slumping and mass movement.We can find material coming from the folded klippen units as well as exotic fragments of crystalline rocks, e.g.basalts or gneisses.In one place we can see a convolute fold apparently developed in an uconsolidated layer of sandstone, in a gravity-driven debris flow (Fig. 7).
It consists mainly of mudstone with numerous rounded pebbles.Middle Paleocene foraminifera and coccoliths (NP 5 zone) have been found by Birkenmajer & Dudziak (1991)

Fig. 1 .Fig. 2 .
Fig. 1.Approximate location of field session stops on a generalized geological map showing the tectonic setting of the Pieniny Klippen Belt in Poland (based onBirkenmajer 1979 and Jurewicz 2005, simplified)

Fig. 3 .
Fig. 3. Schematic diagram of the relationships between the North-European Platform, Central Carpathian Block and the PKB trapped between the two (not to scale).Note the differences between two segments of the PKB: the Pieniny and Małe Pieniny Mts.
Dominant units: Pieniny, Branisko (in the south additionally Haligovce Unit) Dominant units: Czorsztyn, Niedzica, Branisko (lack of Pieniny Unit) The structure is coherent The structure is composed of isolated klippen Layers are mostly steeply dipping Layers are shallowly dipping Platform basement is shallower (−4000 m) Platform basement is deeper (−7000 m) There is rigid block of Tatra Mts. in the south There is no rigid block in the south Transitional zone along northern boundary of the PKB is narrower Transitional zone along northern boundary of the PKB is wider

Fig. 5 .
Fig. 5. Šariš Transitional Zone: outcrop of the Jurassic-Lower Cretaceous sediments of the Grajcarek Succession, resting at the base of the Baba Rock

Fig. 7 .
Fig. 7. Šariš Transitional zone: convolute fold formed by a gravity-driven slump incorporated into mudstone with numerous rounded pebbles of different lithologies and size