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Location of the studied area marked with a red rectangle on simplified topographical map, showing roads, main rivers, forested and urbanized areas
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... part of the Istebna village in the vicinity of the Pietraszonka, Filipionka and Stoczek hamlets as well as in the western part of the Karolówka Range (Małopolska Province, Cieszyn County, Istebna Common). Geographically, this area is situated in the southern part of the Silesian Beskid mountain range, within the upper course of the river Olza (Fig. 1). The rocks were eroded in the source fork of the Olza River and in their tributaries flowing from the Karolówka ridge slopes. The springs of the Olza River take their origin from the area where the lower member of the Istebna Formation occurs. It is on the southwestern part of the Barania Góra (1220 m a.s.l.) massif, the second highest ...
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... series of four N-S striking outcrops represent the rocky landforms in the Stoczek area (Starzec et al., 2017). They extend out along the watershed range between the two uppermost branches of the Olza River and between the river's fork and the top of the range (Figs. 1 and 3). They belong to the table-like top or near table-like top outcrops. ...
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... although some other structures, e.g. parallel stratification, are emphasized by the weathering process. Most of the tors consist of a very coarse-grained sandy material, usually with dispersed gravel. Intervals with much coarser, gravel fraction can be also noticed. They are poorly sorted and consist of gravels and cobbles up to 15 cm in diameter (Fig. 10). Some of the beds are massive; others show parallel stratification (Fig. 5B & C). If a conglomerate interval is present, bed boundaries are easily noticeable. In case there are only sandstones the boundaries are hardly recognizable, which may be connected with original thickness of layers or amalgamation of two or more layers. Such a ...
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... or amalgamation of two or more layers. Such a characteristic feature results from collateral overlapping of subsequent currents carrying clastic material. A very distinctive feature of rocks in this area, rather not visible in other localities, is their fracturing. Joint fractures cut the rocks in perpendicular direction to the bedding surface ( Fig. 10B-D). Only a one-direction joint system is developed, striking approximately along N-S. Very often, fractures are widened at the base of the rock tor, forming a small, triangle-shaped cavern (Fig. 10B-D). The rock tor in the Filipionka area displays a very interesting example of facies succession, different than the other tors described. It ...
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... area, rather not visible in other localities, is their fracturing. Joint fractures cut the rocks in perpendicular direction to the bedding surface ( Fig. 10B-D). Only a one-direction joint system is developed, striking approximately along N-S. Very often, fractures are widened at the base of the rock tor, forming a small, triangle-shaped cavern (Fig. 10B-D). The rock tor in the Filipionka area displays a very interesting example of facies succession, different than the other tors described. It still consists of conglomerates and sandstones, with prevailing of the first lithology, however their relations are specific. These two lithologies are interbedded and their boundaries are usually ...
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... The rock tor in the Filipionka area displays a very interesting example of facies succession, different than the other tors described. It still consists of conglomerates and sandstones, with prevailing of the first lithology, however their relations are specific. These two lithologies are interbedded and their boundaries are usually very sharp (Fig. 11A). Besides thick layers of normal graded conglomerates, occurring also in other rock tors, this one is characterized by intervals with thin to medium alternating beds of sandstone and conglomerate (Fig. 11A-B). Some of the thin beds are discontinuous and pinch out. Sandstones show a flat base surface, whereas the top one can be either ...
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... the first lithology, however their relations are specific. These two lithologies are interbedded and their boundaries are usually very sharp (Fig. 11A). Besides thick layers of normal graded conglomerates, occurring also in other rock tors, this one is characterized by intervals with thin to medium alternating beds of sandstone and conglomerate (Fig. 11A-B). Some of the thin beds are discontinuous and pinch out. Sandstones show a flat base surface, whereas the top one can be either flat or uneven. This is a result of erosional (Fig. 11B) or deformation structures (Fig. 11C). The last ones are called load casts and have the form of drops or plumes of conglomerate descending into sandstone. ...
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... graded conglomerates, occurring also in other rock tors, this one is characterized by intervals with thin to medium alternating beds of sandstone and conglomerate (Fig. 11A-B). Some of the thin beds are discontinuous and pinch out. Sandstones show a flat base surface, whereas the top one can be either flat or uneven. This is a result of erosional (Fig. 11B) or deformation structures (Fig. 11C). The last ones are called load casts and have the form of drops or plumes of conglomerate descending into sandstone. These features develop when a denser layer of sediment is deposited on top of less-dense sediment. Such an arrangement is gravitationally unstable, causing penetration of the upper ...
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... in other rock tors, this one is characterized by intervals with thin to medium alternating beds of sandstone and conglomerate (Fig. 11A-B). Some of the thin beds are discontinuous and pinch out. Sandstones show a flat base surface, whereas the top one can be either flat or uneven. This is a result of erosional (Fig. 11B) or deformation structures (Fig. 11C). The last ones are called load casts and have the form of drops or plumes of conglomerate descending into sandstone. These features develop when a denser layer of sediment is deposited on top of less-dense sediment. Such an arrangement is gravitationally unstable, causing penetration of the upper layer into the lower one. This process ...
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... gravitationally unstable, causing penetration of the upper layer into the lower one. This process occurs shortly after sediment deposition and can be classified as a kind of soft-sediment deformation. Moreover, in some cases the uneven surface is a result of dipping of coarse and angular granules of the overlying conglomerate into sandy deposits (Fig. 11D) that can be interpreted rather as an effect of erosion of the bottom during deposition of coarser material than soft sediment deformations. The rock tors in the Karolówka ridge represent a similar character in terms of lithology and sedimentary structures, although they belong to the Czarna Wisełka Member (the lower part of the ...
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... to the Czarna Wisełka Member (the lower part of the Istebna Formation). They are composed of coarse-grained sandstones and conglomeratic sandstones. Bedding surfaces are rather indistinct and reveal the only form of a change in grain size. Coarser conglomeratic material of the overlaying bed is diffused into the sandy material of the lower bed (Fig. 12A). On weathered surfaces, sandstones display slightly undulating lines, more-or-less regularly spaced, often with upward-curving margins (Fig. 12B). They represent fluid escape structures, whose formation is related to soft-sediment deformation, as in the case of load casts. They are generated during the sediment consolidation process, ...
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... Bedding surfaces are rather indistinct and reveal the only form of a change in grain size. Coarser conglomeratic material of the overlaying bed is diffused into the sandy material of the lower bed (Fig. 12A). On weathered surfaces, sandstones display slightly undulating lines, more-or-less regularly spaced, often with upward-curving margins (Fig. 12B). They represent fluid escape structures, whose formation is related to soft-sediment deformation, as in the case of load casts. They are generated during the sediment consolidation process, that involves pore-fluid escape and sediment compaction resulting largely from gravitational loading (Lowe, 1975). ...
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Citations
... Sandstone-to-conglomeratic tors, as attractive natural geosites rich in various qualities, are perfectly in line with the development of geotourism and the promotion of geoeducation (e.g., Słomka & Kicińska-Świderska, 2004;Alexandrowicz, 2008;Strzeboński, 2009;Słomka, 2013;Starzec et al., 2017Starzec et al., , 2018Welc & Miśkiewicz, 2019Migoń & Pijet-Migoń, 2020;Alexandrowicz & Alexandrowicz, 2022). Such landscape components highlight the geological and morphological heterogeneity of abiotic nature and thus illustrate the exceptional value of the Carpathian geoheritage and the need for its conservation (e.g., Alexandrowicz et al., 2000). ...
... Such landscape components highlight the geological and morphological heterogeneity of abiotic nature and thus illustrate the exceptional value of the Carpathian geoheritage and the need for its conservation (e.g., Alexandrowicz et al., 2000). One such type of residual landforms is the tors in the Silesian Beskid Mts (Beskid Śląski) (e.g., Alexandrowicz, 1978;Słomka, 2013;Chybiorz & Kowalska, 2017;Starzec et al., 2017Starzec et al., , 2018Chybiorz et al., 2020;Sikora, 2022) that are built up of the lower part of the Istebna Formation deposits (sensu Strzeboński et al., 2017). Geologically, the denudational outliers developed on the Upper Cretaceous flysch bedrock within the Silesian Unit, which is part of the orogenic fold-thrust belt (continental accretionary prism) of the Outer Western Carpathians (Figs 1, 2) (cf. ...
... Burtanówna et al., 1937). These so-called exotics occur in the Istebna Formation predominantly in the form of megascopically recognisable fragments of crystalline rocks (e.g., Unrug, 1963; see also Strzeboński, 2005Strzeboński, , 2015Starzec et al., 2017Starzec et al., , 2018Gawęda et al., 2019;Strzeboński, 2022;Szczuka et al., 2022). In the region studied, the exotic clasts are mainly metamorphic rocks (mostly gneisses, granulites), to a lesser extent igneous rocks (primarily granitoids), and relatively rarely sedimentary rocks (e.g., hornstones or exceptionally limestones). ...
This study investigated residual landforms developed within of the flysch bedrock in the Outer Western Carpathians as sandstone-to-conglomeratic tors. The studied relic rocky forms are locally exposed on the valley slopes in the top and plateau parts of the Silesian Beskid Mts. The cognitive values of such relic landforms, especially in the context of their morphogenetic traits and shaping of their macro- and microrelief, are well known and described. In contrast to epigenetic processes, the sedimentological aspect of the origin of such siliciclastic rocky deposits is still subject to different approaches in terms of terminology and interpretation. Thus, the aim of this study is to describe the conditions of environmental settings and character of the sediment transport and deposition processes from gravity flows, and to present a depositional system model for such a variety of flysch deposits. This study also attempts to present geotourist and geoeducational attractiveness of the tors against the background of regional geodiversity, geoheritage, and geoprotection. The results yielded a synthetic morpho-litho-sedimentological and geotouristic specification of the rocky forms analysed. The residual rocky landforms are polygenic geomorphological elements developed as a consequence of multistage and different scale of morph-forming activity operating on the basis of litho-sedimentological and tectonic assumptions under the influence of denudation processes.
... Sandstone-to-conglomeratic tors, as attractive natural geosites rich in various qualities, are perfectly in line with the development of geotourism and the promotion of geoeducation (e.g., Słomka & Kicińska-Świderska, 2004;Alexandrowicz, 2008;Strzeboński, 2009;Słomka, 2013;Starzec et al., 2017Starzec et al., , 2018Welc & Miśkiewicz, 2019Migoń & Pijet-Migoń, 2020;Alexandrowicz & Alexandrowicz, 2022). Such landscape components highlight the geological and morphological heterogeneity of abiotic nature and thus illustrate the exceptional value of the Carpathian geoheritage and the need for its conservation (e.g., Alexandrowicz et al., 2000). ...
... Such landscape components highlight the geological and morphological heterogeneity of abiotic nature and thus illustrate the exceptional value of the Carpathian geoheritage and the need for its conservation (e.g., Alexandrowicz et al., 2000). One such type of residual landforms is the tors in the Silesian Beskid Mts (Beskid Śląski) (e.g., Alexandrowicz, 1978;Słomka, 2013;Chybiorz & Kowalska, 2017;Starzec et al., 2017Starzec et al., , 2018Chybiorz et al., 2020;Sikora, 2022) that are built up of the lower part of the Istebna Formation deposits (sensu Strzeboński et al., 2017). Geologically, the denudational outliers developed on the Upper Cretaceous flysch bedrock within the Silesian Unit, which is part of the orogenic fold-thrust belt (continental accretionary prism) of the Outer Western Carpathians (Figs 1, 2) (cf. ...
... Burtanówna et al., 1937). These so-called exotics occur in the Istebna Formation predominantly in the form of megascopically recognisable fragments of crystalline rocks (e.g., Unrug, 1963; see also Strzeboński, 2005Strzeboński, , 2015Starzec et al., 2017Starzec et al., , 2018Gawęda et al., 2019;Strzeboński, 2022;Szczuka et al., 2022). In the region studied, the exotic clasts are mainly metamorphic rocks (mostly gneisses, granulites), to a lesser extent igneous rocks (primarily granitoids), and relatively rarely sedimentary rocks (e.g., hornstones or exceptionally limestones). ...
This study investigated residual landforms developed within of the flysch bedrock in the Outer Western Carpathians as sandstone-to-conglomeratic tors. The studied relic rocky forms are locally exposed on the valley slopes in the top and plateau parts of the Silesian Beskid Mts. The cognitive values of such relic landforms, especially in the context of their morphogenetic traits and shaping of their macro- and microrelief, are well known and described. In contrast to epigenetic processes, the sedimentological aspect of the origin of such siliciclastic rocky deposits is still subject to different approaches in terms of terminology and interpretation. Thus, the aim of this study is to describe the conditions of environmental settings and character of the sediment transport and deposition processes from gravity flows, and to present a depositional system model for such a variety of flysch deposits. This study also attempts to present geotourist and geoeducational attractiveness of the tors against the background of regional geodiversity, geoheritage, and geoprotection. The results yielded a synthetic morpho-litho-sedimentological and geotouristic specification of the rocky forms analysed. The residual rocky landforms are polygenic geomorphological elements developed as a consequence of multistage and different scale of morph-forming activity operating on the basis of litho-sedimentological and tectonic assumptions under the influence of denudation processes.
... The Moravskoslezske Beskidy Mts, to Beskid Mały Mts in Poland, till the Silesian Beskid Mts in the western part of the Czech Republic is the extension of this formation and it is formed the Western Beskids mountains (Lexa et al. 2000;Strzeboński et al. 2017). The Istebna formation is formed by the superposition of two members of rock that are the Czarna Wisełka member (Lower Istebna Beds) with a thickness of 1500 m at the bottom and the Janoska, Jasnowice, and Kamesznica members (composed of Lower Istebna shales, upper Istebna sandstones, and upper Istebna shales part of Upper Istebna Beds) with a thickness of 400 m on the top (Burtanówna et al. 1937;Książkiewicz 1951;Starzec et al. 2018). The Istebna sandstone samples used in this research has been taken from the Sobolów open pit mine, which is part of the Janoska, Jasnowice, and Kamesznica members, with thickness from 1300 to 1600 m, (Strzeboński Fig. 1 AVS 1000 apparatus 2005). ...
The drilling-related geomechanics requires a better understanding of the encountered formation properties such as poroelastic parameters. This paper shows set of laboratory results of the dynamic Young’s modulus, Poisson’s ratio, and Biot’s coefficient for dry and water-saturated Istebna sandstone samples under a series of confining pressure conditions at two different temperatures. The predicted results from Wyllie’s equation were compared to the measured ones in order to show the effect of saturation on the rock weakening. A negative correlation has been identified between Poisson’s ratio, Biot’s coefficient and confining pressure, while a positive correlation between confining pressure and Young’s modulus. The predicted dynamic poroelastic rock properties using the P-wave value from Wyllie’s equation are different from measured ones. It shows the important influence of water saturation on rock strength, which is confirmed by unconfined compressive strength measurement. Linear equations have been fitted for the laboratory data and are useful for the analysis of coupled stress and pore pressure effects in geomechanical problems. Such results are useful for many drilling applications especially in evaluation of such cases as wellbore instability and many other drilling problems.
