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... Cieszkowski (1992) de fined these strata as the Malcov For ma tion and Waksmund Beds (Up per most Eocene-Lower Mio cene). A, B -pack ets of the thin-bed ded flysch de pos its; C -bro ken pack ets of the £¹cko type marls; D -over turned, NE dip ping se quence of the thick-bed ded sand stones, "£¹cko Marls" and thin-bed ded turbidites; E, F -de tail of the Figure 11D Waksmund (N49°29.418' E20°04.520'). ...
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Citations
... The younger Karpatian terrestrial, lagoonal, and deltaic sedimentation took place in the central and southern parts of the basin and was characterized by depositional systems prograding from the south towards the basin depocenters in the north (Jiříček & Seifert 1990;Fodor 1995;Decker 1996;Kováč et al. 2004;Strauss et al. 2006;Harzhauser et al. 2020). The present shape of the Lower Miocene basin fill is a result of the tearing apart and disintegration of a significantly larger accommodation domain (e.g., Kováč et al. 2016Kováč et al. , 2017aOszczypko-Clowes et al. 2018). The rapid erosion which accompanied the inversion of the northern margin of the basin at the beginning of the Middle Miocene is displayed in the present-day geological settings (Kováč et al. 2004). ...
... The basal clastics pass into pelites with calcareous nannoplankton of an NN2 Zone (Salaj & Zlinská 1991;Andrejeva-Grigorovič & Halásová 2000). These sediments, however, were deposited over a much larger basin system that spread towards the east (as Čausa Fm. ;Vass 2002), up to the front of the Eastern Carpathians (e.g., Kováč et al. 2017a;Oszczypko-Clowes et al. 2018;Pelech et al. 2020). The Chropov Mb., formed by unsorted conglomerates derived from the Flysh Belt, was covered by coarse-grained sandstones and the fine conglomerates to rubbles of the Veterník Mb. (which is the geographically correct term for Winterberg ;Buday 1955;Gaža 1983;Jiříček 1988a,b;Vass 2002) followed by marine transgression with calcareous nannoplankton of the NN3 Zone. ...
Long-term research of the Vienna Basin (Central Europe) has resulted in multiple stratigraphic concepts, though these are at least in part mutually exclusive. This contribution aims to reconsider the available information on the northeastern Vienna Basin, located in Slovakia, to create a consistent stratigraphic model. Lithostratigraphic correlations based on benthic taxa - widely used elsewhere - are omitted, since these include inherently diachronous paleoecological zones. This presumption of diachroneity is further supported by the evidence of shelf-slope scale clinoforms. The following sequences were identified: (1) the Early Miocene wedge-top basin, genetically unrelated to the subsequently formed Vienna Basin; Eggenburgian-Ottnangian cycles are still obscured, and the Karpatian includes two transgressive-regressive cycles; (2) Middle Miocene early Badenian rifting including the Kúty Fm. lowstand and Lanžhot Fm., together with the Devínska Nová Ves Fm., comprising transgression and a highstand; (3) Middle Miocene late Badenian rifting including lowstand offshore Jakubov Mb. and transgressive littoral Stupava Fm., followed by the highstand offshore Studienka Mb. passing to normal regressive Matzen delta; (4) Middle Miocene Sarmatian rifting including the basal Kopčany and Radimov mbs., the offshore transgressive to regressive Holíč Fm. and the highstand normal regressive deltaic Skalica Fm.; (5) supposed Late Miocene rifting with Lake Pannon transgression resulting in the lacustrine Bzenec Fm., followed by the highstand normal regressive deltaic Čáry and alluvial Gbely fms.
... Its Early Miocene age was documented by Paul and Poprawa (1992). Calcareous nannoplankton (Oszczypko-Clowes et al., 2018) and the study of foraminifera from sample Knurów 17 point to the Early Miocene age of the Malcov Fm. ...
... The deposits of the Szczawnica Fm (Birkenmajer and Oszczypko, 1989;Chrustek et al., 2005) are not sufficiently different from the Ropianka Fm in the Bystrica or Rača subunits and they do not constitute an independent lithosome, so the "Szczawnica Formation" term was abandoned. Furthermore, some deposits assigned to the Szczawnica Fm (Cretaceous-Paleocene; Birkenmajer and Oszczypko, 1989) east of the study area in the region of Krościenko and Szczawnica were considered to be Oligocene-Miocene in age (Oszczypko et al., 2018). This weakens the usefulness of this division. ...
The south-western part of the Gorce Mts (Outer Carpathians) is composed of flysch deposits of the Krynica and Bystrica subunits of the Magura Nappe. The Krynica Subunit includes the Late Cretaceous–Paleocene Ropianka Fm, the Early Eocene Beloveža Fm, the Early Eocene–Oligocene Magura Fm and the Oligocene–Early Miocene Malcov Fm, while the Bystrica Subunit includes the Middle Eocene–?Oligocene Magura Fm, represented mainly by the thick-bedded Magura Sandstone. Thin- and medium-bedded sandstone-shale turbidites predominate in the other formations. The lithostratigraphic units are dated on the basis of foraminifers. The studied deposits accumulated in the southern part of the Magura Basin. Their detrital material was derived from a ridge, bounding the basin in the south. In the study area, the Krynica Subunit overthrusts the Bystrica Subunit. The studied deposits are folded, thrust and cut by numerous faults. The Turbacz Thrust Sheet and the newly identified Kudłoń Thrust Sheet were distinguished in the Krynica Subunit. Faults of different lengths and throws are transverse or oblique. Some of them form complex dislocation zones with lengths of up to several km. In general, the high-resolution digital elevation model DEM contributed significantly to progress in the geological and geomorphological research.
... The youngest deposits of the Magura Nappe in the area are represented by the Malcov Formation the Oligocene-Early Miocene in age (Cieszkowski & Olszewska, 1986;Cieszkowski, 1992Cieszkowski, , 1995Oszczypko-Clowes et al., 2018) (Fig. 5C-F). The main facies of this formation consists of thin-and medium-bedded sandstone-shale turbidites ( Fig. 5D-F). ...
The area in the vicinity of Nowy Targ is located within the northern part of the Orawa-Nowy Targ Basin and the southern slopes of the Gorce Mountains in the Polish sector of the Outer Carpathians. Geologically, the region is built of the Upper Cretaceous–Palaeogene turbiditic deposits representing sedimentary successions of the Krynica Subunit of the Magura Nappe and the Neogene–Quaternary fresh-water deposits filling the Orawa-Nowy Targ Basin. The Magura Nappe in the described area is represented by the thick-bedded sandstones of the Magura Formation and thin-and medium-bedded sandstone-shale deposits of the Malcov Formation, which are well-exposed in numerous outcrops, especially in the Łopuszna stream valley. The Magura Nappe deposits were folded and cut by a fault system in the Miocene. The presented area displays varied geomorphological relief and picturesque landscapes. Moreover, rare species of fauna and flora occurring here, as well as the still-alive culture of the Podhale Highlanders and continuously improving tourist infrastructure additionally contribute to the development of geotourism in this area. In addition, this area is an increasingly popular place among cyclists, thanks to the development of a network of bicycle paths, therefore the proposed geotourist bicycle path will extend the offer for this group of tourists.
... The age of the Kremna Fm. remains controversial since Jurewicz (2018) and Jurewicz and Segit (2018) recently supported the concept of the Szczawnica Fm. (Kremna Fm. in this paper), documenting its early Eocene age, based on dinoflagellates. Nonetheless, the present authors sustain their opinion on the late Oligocene/early Miocene age of the Kremna Fm., which is firmly based on planktonic foraminifera and calcareous nannoplankton identified in several sections (see Oszczypko et al. 2005b;Oszczypko-Clowes 2010;Oszczypko-Clowes et al. 2018). ...
... The prolongation of the Kremna Fm. to the west of the Dunajec River is a kind of flower structure located between the Magura Nappe and the PKB (Oszczypko-Clowes et al. 2018). These deposits occupy the morphological deflection between the Gorce and the PKB in the north and south, respectively (Text- fig. ...
... East of the Stary Stream, flysch deposits of the Kremna Fm. contain thick layers of exotic conglomerates, formerly regarded as the Jarmuta Fm. (Birkenmajer 1979;Birkenmajer et al. 1987;Krobicki and Olszewska 2005). From the south, the Kremna Fm. is overthrust by the Grajcarek (Šariš) Unit of the PKB Oszczypko-Clowes 2014, 2017;Oszczypko-Clowes et al. 2018). This unit is composed of Jurassic-Upper Cretaceous/?Paleocene pelagic and flysch formations, which were deposited in the southernmost part of the Magura Basin, and then during the Paleocene incorporated into the PKB. ...
During the late Oligocene to early Miocene the residual Magura Basin was located along the front of the Pieniny Klippen Belt (PKB). This basin was supplied with clastic material derived from a south-eastern direction. In the Małe (Little) Pieniny Mts. in Poland, the late Oligocene/ early Miocene Kremna Fm. of the Magura Nappe (Krynica subunit) occurs both in front of the PKB as well as in the tectonic windows within the PKB. Lenses of exotic conglomerates in the Kremna Fm. contain frequent clasts of Mesozoic limestones (e.g. limestones with “filaments” microfacies and Urgonian limestones) and Eocene shallow-water limestones. Fragments of crystalline and volcanic rocks occur subordinately. The provenance of these exotic rocks could be probably connected with Eocene exhumation and erosion of the SE part of the Dacia and Tisza Mega-Units.
... However, the cartographic determination of these transitional elements is problematic. The situation is even more complicated by the presence of the Lower Miocene deepwater flysch deposits occurring just next to the northern PKB limit in the Pieniny Mts (Oszczypko et al. 2005;Oszczypko-Clowes et al. 2018). Consequently, our interpretation of the presence of the Biele Karpaty (Strihovce Unit, Fig. 2x-z) in the underlier of the Oravic nappes in the eastern PKB branch should be taken as tentative only and ought to be verified by the future research. ...
... Residual latest Oligocene-earliest Miocene (late Egerian, ca 25-22 Ma) depressions with accumulation of deep-water flysch deposits terminated evolution of the CCPB forearc basin. The depocentres are rimming the PKB from the north (Kremná Fm in the Pieniny Mts- Oszczypko et al. 2005;Oszczypko-Clowes et al. 2018), as well as from the south in the eastern part of the CCPB Podhale Basin (Środoń et al. 2006) and south of the ŠKZ (Soták et al. 2001). Supposedly, these depressions developed on the inner side of the EWC accretionary wedge in a retroarc position, i.e., in a broad basinal zone in front of S-verging backthrust of the wedge rear, which was subsequently segmented into synclinal depressions by large-scale folding. ...
The Pieniny Klippen Belt (PKB) and adjoining zones form a narrow, but lengthy belt that separates the Cretaceous nappe stack of the Central (Austroalpine) and the Cenozoic accretionary wedge of the External Western Carpathians (Flysch Belt). The PKB shares units and structures of both, in addition to the distinctive Oravic units, derived from a continental fragment in the Middle Penninic position. In map view, the northward-convex PKB consists of two branches—the western one striking roughly SW–NE and the eastern one oriented in the NW–SE direction. The western branch experienced a continuous NW–SE convergence and forward accretion of units derived from the foreland plate during the Late Cretaceous up to Oligocene. The developing accretionary wedge was supported by the backstop of the Central Carpathians. In contrast, the eastern branch originated by separation of PKB units and their dextral translation along the NE margin of the Central Carpathian block in the Late Eocene. During the Miocene reorganization of plate movements in the Carpathian area, the situation reversed. The eastern, formerly dextral transform margin was converted to the frontal backstop of the eastern part of the accretionary wedge. In contrast, the western, previously orthogonally convergent branch was affected by along-strike sinistral movements. Despite these considerable kinematic changes, the PKB remained fixed to both backstop edges and records deformation structures and associated sediments differentiated into several evolutionary stages.
... The last basinal stages are connected with sedimentation during the formation of the Lower Miocene nappe structure. That condition developed a piggy-back basin with mixed marly and clastic sedimentation (Zawada, Stare Bystre, Kopaczyska, Kochanów and Kremna formations; Cieszkowski 1992; Oszczypko et al. 1999Oszczypko et al. , 2015Ryłko 2004;Oszczypko-Clowes 2001;Oszczypko & Oszczypko-Clowes 2002, 2014Golonka et al. 2013;Kaczmarek et al. 2016;Oszczypko-Clowes et al. 2018). ...
The Western Outer Carpathians structure on Austria, Slovak, Czech and Polish territory is an effect of prolonged processes of the Cretaceous–Miocene folding, moving and uplifting. The Outer Carpathian nappes are thrust over other each other and over the North European Platform consisting of the crystalline basement covered by the Paleozoic–Miocene sedimentary rocks. The Jurassic–Lower Miocene deposits of these nappes correspond to more or less separate sedimentary basins that display a different lithostratigraphic development.
Several evolutionary stages could be distinguished in the Western Outer Carpathians. The synrift–postrift stage is expressed by the opening of the Alpine Tethys and the Protosilesian Basin and formation of two major domains – Magura and Silesian. The uplifted (Baška-Inwałd Ridge and Pavlov Carbonate Platform) and basinal zones (Bachowice and Mikulov basins) were formed within the North European Platform during this opening. The movement of the Central Carpathian plate led to the development of the accretionary wedge and reorganization of the Outer Carpathian basins during the synorogenic stage. The Magura Basin, Dukla Basin and Foremagura group of basins developed within the Magura Domain while the Silesian Basin, Skole Basin and Subsilesian Sedimentary Area developed within the Silesian Domain. The thick flysch sequences with olistostromes were deposited in these basins. The ridges divided basins were destroyed during the late orogenic stages and two basins remained: Krosno and Magura.
Several formations deposited within the Western Outer Carpathians basins contain organic-rich rocks, which can represent unconventional resources known as shale-gas and shale-oil. The Jurassic Mikulov Formation of Mikulov Basin, Lower Cretaceous Veřovice and Spas formations of the Protosilesian Basin and Rudawka Rymanowska Menilite Formation of the Krosno Basin contain organic-rich rocks, which can represent unconventional resources known as shale-gas and shale-oil. Parts of the anoxic shales have been hidden at the depth of few thousand meters during the folding and overthrusting movements.
The best structural conditions for unconventional hydrocarbon exploration occur at the depth of few thousand meters within the North European Platform below the Carpathian nappes and within the Silesian, Skole and Dukla nappes. The organic-rich rocks within the Alpine Tethys and Magura Basin require further investigations.
... In the opinion of the present author, a possible explanation for these differences in dating of the Szczawnica Formation is that the Early Miocene microfossils described by Oszczypko-Clowes et al. (2018) come from the youngest strata of the Magura Nappe, preserved as fragments along their contact with the Pieniny Klippen Belt but not from the Palaeogene formations. These Miocene strata represent the youngest parts of the Malcov Beds, which are widely known from the Polish and Slovak Magura Nappe (for details see Cieszkowski and Olszewska, 1986), as counterparts of the Oligocene-Miocene Menilite-Krosno series, known from more northerly nappes (the Malcov-Menilite series in Slovakia; Nemčok et al., 1968). ...
... Age interpretations presented by Oszczypko-Clowes et al. (2018) are, in the opinion of the present author, over-interpreted in a form not supported by data for the whole Jarmuta, Szczawnica and Magura formations. ...
... 1). Rich and uniform Early Eocene dinoflagellate cysts, found in both lithostratigraphic units, preclude the possibility of a Miocene age of them, as suggested by Oszczypko-Clowes et al. (2018). 3. The Szlachtowa Formation in the PD-9 borehole occurs at the depth 707.1-716.4 ...