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Fig. 14. The lithological section of the Zawiercie-Marciszow site (see Figs 11 and 16), as exposed in the municipal dump excavation in 2000 (reproduced from Budziszewska-Karwowska et al., 2010, fig. 2, based on Szulc et al., 2006, fig. 5; modified) and in the Kobylarz 1 well (Szulc et al., 2015) and at the Poreba site (based on Niedzwiedzki et al., 2014, fig. 1C and observations of the present authors). Ar- rows indicate alleged bone-rich horizons of the hypothetically-defined Lisowice level, suspected as a source for material exploited since 2009 in the adjacent mound of the Keuper deposits derived from the dig (see Figs 11, 15, 16). This approach to the correlation of the Silesian Keuper profiles was elaborated in detail by Srodon ef al. (2014), Considering the facies and microfacies characteristics of the main sediment types occurring in the both nearby-sit- uated both outcrops (Marciszow and Poreba), they are uni- form (Figs 13, 14). The dominant redbed facies abounds in evaporites (recently preserved as carbonate pseudomorphs),

Figure 14 The lithological section of the Zawiercie-Marciszow site (see Figs 11 and 16), as exposed in the municipal dump excavation in 2000 (reproduced from Budziszewska-Karwowska et al., 2010, fig. 2, based on Szulc et al., 2006, fig. 5; modified) and in the Kobylarz 1 well (Szulc et al., 2015) and at the Poreba site (based on Niedzwiedzki et al., 2014, fig. 1C and observations of the present authors). Ar- rows indicate alleged bone-rich horizons of the hypothetically-defined Lisowice level, suspected as a source for material exploited since 2009 in the adjacent mound of the Keuper deposits derived from the dig (see Figs 11, 15, 16). This approach to the correlation of the Silesian Keuper profiles was elaborated in detail by Srodon ef al. (2014), Considering the facies and microfacies characteristics of the main sediment types occurring in the both nearby-sit- uated both outcrops (Marciszow and Poreba), they are uni- form (Figs 13, 14). The dominant redbed facies abounds in evaporites (recently preserved as carbonate pseudomorphs),

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Fig. 1. A. Schematic geological map (after Bardzinski and Chybiorz, 2013), showing the locations of the localities studied in Upper Silesian region (outcrops and boreholes; for detail see Szulc et al., 2015), and B. location of the studied region and the key borehole in Poland.
Fig. 1. A. Schematic geological map (after Bardzinski and Chybiorz, 2013), showing the locations of the localities studied in Upper Silesian region (outcrops and boreholes; for detail see Szulc et al., 2015), and B. location of the studied region and the key borehole in Poland.
Fig. 2. Schematic section of the Upper Triassic of the Upper Silesia, and its partly formal (in higher part) lithostratigraphic subdivision after Szulc and Racki (2015; changed after Jewuta, 2010, fig. 4), with a focus on correlation with the Germanic Basin reference succession (“Stratigraphische Tabelle von Deutschland” 2002, Franz, 2008); note the occurrence of three bone-enriched levels in the Silesian Keuper, as shown here, but only two Upper Triassic bone beds are defined and discussed in this paper (cf. Szule and Racki, 2015; Szulc et al., 2015); the Ladinian bone-bed level corresponds to the Miedary Beds of Kotlicki (1974), and the “Miedary sandstone-mudstone member” of Kotlicki (1995; see also Szulc, 2007b; Sulej et al., 2011b).
Fig. 2. Schematic section of the Upper Triassic of the Upper Silesia, and its partly formal (in higher part) lithostratigraphic subdivision after Szulc and Racki (2015; changed after Jewuta, 2010, fig. 4), with a focus on correlation with the Germanic Basin reference succession (“Stratigraphische Tabelle von Deutschland” 2002, Franz, 2008); note the occurrence of three bone-enriched levels in the Silesian Keuper, as shown here, but only two Upper Triassic bone beds are defined and discussed in this paper (cf. Szule and Racki, 2015; Szulc et al., 2015); the Ladinian bone-bed level corresponds to the Miedary Beds of Kotlicki (1974), and the “Miedary sandstone-mudstone member” of Kotlicki (1995; see also Szulc, 2007b; Sulej et al., 2011b).
Fig. 3. | Simplified lithological column of the Krasiejéw succession (after Szulc 2005, fig. 2, modified; see also Bilan, 1975), as the stratotype of the boundary between the Ozimek Mudstone-Evaporite Member with the Patoka Marly Mudstone-Sandstone Member (Szulc and Racki, 2015), and photographs of selected sedimentary features of the Keuper succession in Krasiejow. A. Gypsum-bearing (arrowed) red mudstones from Ozimek Mbr. B. Celestite crystals from Krasiejow clay pit. Photograph courtesy of Eligiusz Szeteg. C. Typical varie- gated mudstones and claystones of the Patoka Member, composed of alluvial sediments interlayered with regolith horizons (r). D. Two layers of reworked palaeosoil grains (c) included in alluvial deposits. E. Conglomerates composed of sieved pedogenic nodules. Note the erosive, rounded scour casts at the base (arrowed). F. Complex palaeosoil section composed of lower spotty interval, followed by vertisol with slickensides and covered by bluish alluvial sediments. G. Carbonate nodular palaeosoil. H. Gray fluvial-dominated sediments featur- ing the upper part of the section in Krasiejow pit. I. Metaposaurid skulls from the main bone-bearing horizon. Photographs C and E by Michat Matysik.
Fig. 3. | Simplified lithological column of the Krasiejéw succession (after Szulc 2005, fig. 2, modified; see also Bilan, 1975), as the stratotype of the boundary between the Ozimek Mudstone-Evaporite Member with the Patoka Marly Mudstone-Sandstone Member (Szulc and Racki, 2015), and photographs of selected sedimentary features of the Keuper succession in Krasiejow. A. Gypsum-bearing (arrowed) red mudstones from Ozimek Mbr. B. Celestite crystals from Krasiejow clay pit. Photograph courtesy of Eligiusz Szeteg. C. Typical varie- gated mudstones and claystones of the Patoka Member, composed of alluvial sediments interlayered with regolith horizons (r). D. Two layers of reworked palaeosoil grains (c) included in alluvial deposits. E. Conglomerates composed of sieved pedogenic nodules. Note the erosive, rounded scour casts at the base (arrowed). F. Complex palaeosoil section composed of lower spotty interval, followed by vertisol with slickensides and covered by bluish alluvial sediments. G. Carbonate nodular palaeosoil. H. Gray fluvial-dominated sediments featur- ing the upper part of the section in Krasiejow pit. I. Metaposaurid skulls from the main bone-bearing horizon. Photographs C and E by Michat Matysik.
Fig. 4. | Three main correlation variants of the Krasiejow clay pit section with the updated reference German Keuper profile (in basin margin facies) of Baden-Wiirttemberg (Nitsch, 2011) and Polish stratigraphic schemes (Dadlez and Kopik, 1963; Becker et al., 2008: Szulc and Racki, 2015): (A) with the Lehrberg Beds (Steigerwald Fm), based on the original vertebrate evidence of Dzik et al. (2000), fa- voured, among others, by the inference from conchostracan dating (Kozur and Weems, 2010); (B) with the Blasensandstein or Coburg Sandstein of the Hassberge Fm, supported by revised vertebrate data (Milner and Schoch, 2004; Butler et al., 2014, fig. 1B) and macrofloral evidence (Pacyna, 2014), respectively; (C) with the Arnstadt Fm, deduced initially from facies development and palyno- stratigraphic dating (Szulc, 2005, 2007a; cf. also Gruszka and Zielinski, 2008), confirmed by the present, integrative, stratigraphic study (see Fig. 17); the Weser Fm is a lateral equivalent in central basin facies. Note more continuous deposition in Silesia region than assumed in DST 2002 (Szulc et al., 2015), recorded in the transition from the Upper Gipskeuper to Steinmergel facies at Krasiejow (= Ozimek and Patoka mbrs of Grabowa Fm, respectively, Fig. 3; Szulc and Racki, 2015).
Fig. 4. | Three main correlation variants of the Krasiejow clay pit section with the updated reference German Keuper profile (in basin margin facies) of Baden-Wiirttemberg (Nitsch, 2011) and Polish stratigraphic schemes (Dadlez and Kopik, 1963; Becker et al., 2008: Szulc and Racki, 2015): (A) with the Lehrberg Beds (Steigerwald Fm), based on the original vertebrate evidence of Dzik et al. (2000), fa- voured, among others, by the inference from conchostracan dating (Kozur and Weems, 2010); (B) with the Blasensandstein or Coburg Sandstein of the Hassberge Fm, supported by revised vertebrate data (Milner and Schoch, 2004; Butler et al., 2014, fig. 1B) and macrofloral evidence (Pacyna, 2014), respectively; (C) with the Arnstadt Fm, deduced initially from facies development and palyno- stratigraphic dating (Szulc, 2005, 2007a; cf. also Gruszka and Zielinski, 2008), confirmed by the present, integrative, stratigraphic study (see Fig. 17); the Weser Fm is a lateral equivalent in central basin facies. Note more continuous deposition in Silesia region than assumed in DST 2002 (Szulc et al., 2015), recorded in the transition from the Upper Gipskeuper to Steinmergel facies at Krasiejow (= Ozimek and Patoka mbrs of Grabowa Fm, respectively, Fig. 3; Szulc and Racki, 2015).
Fig. 5. — Lithological succession of the clay pit at Lipie Slaskie and nearby boreholes (cf. Szule et al., 2006, fig. 5), with marked revised lithostratigraphy (formal units after Szule and Racki, 2015 and Szule et al., 2015), bone- and macroflora-bearing intervals (partly after Pienkowski et al., 2014, fig. 4) and palynologically dated level (PZ IVb; Fijatkowska-Mader et al., 2015; LS3 — sample studied by Anna Fijatkowska-Mader, see Fig. 6). Stratigraphic correlations of Pienkowski et al. (2014, fig. 4) are presented for comparison; note an errone- ously estimated thickness of the Lipie Slaskie section (12 m instead 8 m; marked by arrow) by the authors of the Warsaw group since pa- per of Dzik et al. (2008a), as well as misinterpreted red beds as primary depositional units (see Fig. 9); true red beds occur in the Lipie 2 well below an erosional surface.
Fig. 5. — Lithological succession of the clay pit at Lipie Slaskie and nearby boreholes (cf. Szule et al., 2006, fig. 5), with marked revised lithostratigraphy (formal units after Szule and Racki, 2015 and Szule et al., 2015), bone- and macroflora-bearing intervals (partly after Pienkowski et al., 2014, fig. 4) and palynologically dated level (PZ IVb; Fijatkowska-Mader et al., 2015; LS3 — sample studied by Anna Fijatkowska-Mader, see Fig. 6). Stratigraphic correlations of Pienkowski et al. (2014, fig. 4) are presented for comparison; note an errone- ously estimated thickness of the Lipie Slaskie section (12 m instead 8 m; marked by arrow) by the authors of the Warsaw group since pa- per of Dzik et al. (2008a), as well as misinterpreted red beds as primary depositional units (see Fig. 9); true red beds occur in the Lipie 2 well below an erosional surface.
Fig. 6. | Miospores from the Lipie Slaskie clay-pit (courtesy of Anna Fijatkowska-Mader). For the location of sample LS3 see Fig. 5 Scale 30 um. A. Anapiculatisporites telephorus (Pautsch) Klaus. B. Enzonalasporites vigens Leschik. C. Ovalipollis cf. rarus Klaus. D O. ovalis Krutzsch. E. Brachysaccus neomundanus (Leschik) Madler. F. Duplicisporites granulatus Leschik. G. Praecirculina granife (Leschik) Klaus. H. Granuloperculatipollis rudis Venktachala et Goczan. I, J. Classopollis meyeriana (Klaus) Venktachala et Goczan. K Geopollis zwolinskae (Lund) Brenner. L. Monosulcites sp.
Fig. 6. | Miospores from the Lipie Slaskie clay-pit (courtesy of Anna Fijatkowska-Mader). For the location of sample LS3 see Fig. 5 Scale 30 um. A. Anapiculatisporites telephorus (Pautsch) Klaus. B. Enzonalasporites vigens Leschik. C. Ovalipollis cf. rarus Klaus. D O. ovalis Krutzsch. E. Brachysaccus neomundanus (Leschik) Madler. F. Duplicisporites granulatus Leschik. G. Praecirculina granife (Leschik) Klaus. H. Granuloperculatipollis rudis Venktachala et Goczan. I, J. Classopollis meyeriana (Klaus) Venktachala et Goczan. K Geopollis zwolinskae (Lund) Brenner. L. Monosulcites sp.
Fig. 7. Schematic geological section across outcrops in the Lisowice - Lipie Slaskie area (A; from Bardziski and Chybiorz, 2013), and the Wozniki Limestone Mbr above the brown mudstones, mostly covered by a rubbish dump, as recently visible (November 2014) in an inactive quarry on the Lisowice Hill, situated some 400 m N of the pit (B; see Figs 5 and 8, compare Szulc et al., 2006, fig. 8B; see also Gasiorowski ef al., 1986; courtesy of Waldemar Bardzinski).
Fig. 7. Schematic geological section across outcrops in the Lisowice - Lipie Slaskie area (A; from Bardziski and Chybiorz, 2013), and the Wozniki Limestone Mbr above the brown mudstones, mostly covered by a rubbish dump, as recently visible (November 2014) in an inactive quarry on the Lisowice Hill, situated some 400 m N of the pit (B; see Figs 5 and 8, compare Szulc et al., 2006, fig. 8B; see also Gasiorowski ef al., 1986; courtesy of Waldemar Bardzinski).
Fig. 8. | Wozniki limestones at Lipie Slaskie, with post-evapo- ritic cherts (A; arrowed), photo taken in 1996 (compare Fig. 7B); and gypsum pseudomorphs preserved in these cherts (B; thin sec- tion).
Fig. 8. | Wozniki limestones at Lipie Slaskie, with post-evapo- ritic cherts (A; arrowed), photo taken in 1996 (compare Fig. 7B); and gypsum pseudomorphs preserved in these cherts (B; thin sec- tion).
Fig. 9. | Apparent “redbeds” from the Lipie Slaskie section. A. Lateral pinching of red colour (left side of the section; arrowed) in the “Lower red bed” of Piehkowski et al. (2014). B. Complex strike-slip fault surfaces covered with a red Fe oxide patina. C, D. Details from Fig. 9B. E. Topmost part of the section cropping out in the clay pit. F. Secondary reddening (arrowed) of the primary grey sediments from the “Upper red beds” of Pienkowski et al. (2014).
Fig. 9. | Apparent “redbeds” from the Lipie Slaskie section. A. Lateral pinching of red colour (left side of the section; arrowed) in the “Lower red bed” of Piehkowski et al. (2014). B. Complex strike-slip fault surfaces covered with a red Fe oxide patina. C, D. Details from Fig. 9B. E. Topmost part of the section cropping out in the clay pit. F. Secondary reddening (arrowed) of the primary grey sediments from the “Upper red beds” of Pienkowski et al. (2014).
Fig. 10. Composite section (A) and field photographs (B, C) of the Wozniki clay pit succession. Stratigraphic position of bone-bearing horizons of the Lisowice level are approximated from Sulej et a/. (201 1a, fig. 1A).
Fig. 10. Composite section (A) and field photographs (B, C) of the Wozniki clay pit succession. Stratigraphic position of bone-bearing horizons of the Lisowice level are approximated from Sulej et a/. (201 1a, fig. 1A).
Fig. 12. Photographs of the Poreba locality, taken in April 2008. A. View of the western part of fresh excavation, adjacent to the inactive municipal dump (see Fig. 11). B. Newly exposed horizontally laminated conglomeratic to sandstone layer in a mudstone series in the southern wall, in the upper part of the section. Courtesy of Krystyn Rubin. The stratigraphic position of the bone-bearing interval was clearly determined by two observations: (1) the bone- bearing strata occur just below the Wozniki Limestone cover, sparsely outcropping in the Kobylarz hill top (Fig. 11), and are associated with microbial, coquinoid and lime conglomeratic layers (Racki, 2010, figs 1, 2; Szulc et al., 2015, fig. 1SC—E), and (2) palynostratigraphic dating of the strata as the IVb Subzone (Heunisch in Szulc et al., 2006; see also Sadlok and Wawrzyniak, 2013). As in the nearby Poreba site, located 1.7 km NW, differently preserved, partly reworked bone material is found in rare conglomer- atic layers (Fig. 15B, C), whilst isolated and well-preserved remains occur in grey marly mudstones and claystones with carbonate concretions (see Racki, 2010, fig. 1; Fig. 15D). Large dicynodonts and predatory archosaurs of the genus Smok are especially distinct elements identified in the col- lected, not very rich bone material (Budziszewska-Karwow- A quite different stratigraphic concept, presented lastly by Niedzwiedzki et al. (2014, p. 1122), is therefore aston- ishing, especially in that the previous data are not discussed by these authors. The Warsaw group suggests that the Mar- ciszow site lies about 20-30 m above the Norian Poreba
Fig. 12. Photographs of the Poreba locality, taken in April 2008. A. View of the western part of fresh excavation, adjacent to the inactive municipal dump (see Fig. 11). B. Newly exposed horizontally laminated conglomeratic to sandstone layer in a mudstone series in the southern wall, in the upper part of the section. Courtesy of Krystyn Rubin. The stratigraphic position of the bone-bearing interval was clearly determined by two observations: (1) the bone- bearing strata occur just below the Wozniki Limestone cover, sparsely outcropping in the Kobylarz hill top (Fig. 11), and are associated with microbial, coquinoid and lime conglomeratic layers (Racki, 2010, figs 1, 2; Szulc et al., 2015, fig. 1SC—E), and (2) palynostratigraphic dating of the strata as the IVb Subzone (Heunisch in Szulc et al., 2006; see also Sadlok and Wawrzyniak, 2013). As in the nearby Poreba site, located 1.7 km NW, differently preserved, partly reworked bone material is found in rare conglomer- atic layers (Fig. 15B, C), whilst isolated and well-preserved remains occur in grey marly mudstones and claystones with carbonate concretions (see Racki, 2010, fig. 1; Fig. 15D). Large dicynodonts and predatory archosaurs of the genus Smok are especially distinct elements identified in the col- lected, not very rich bone material (Budziszewska-Karwow- A quite different stratigraphic concept, presented lastly by Niedzwiedzki et al. (2014, p. 1122), is therefore aston- ishing, especially in that the previous data are not discussed by these authors. The Warsaw group suggests that the Mar- ciszow site lies about 20-30 m above the Norian Poreba
Fig. 11. Localization of the tetrapod localities near municipal waste dumps and the borehole Kobylarz | in the Zawiercie-Poreba boundary area on a Google Earth satellite photograph.
Fig. 11. Localization of the tetrapod localities near municipal waste dumps and the borehole Kobylarz | in the Zawiercie-Poreba boundary area on a Google Earth satellite photograph.
Fig. 15. Field (A, B), palaeontological (C, D) and microfacies (E, F) aspects of the Keuper deposits stored in the mound near municipa dump dig at Zawiercie-Marciszow (see Figs 11, 14; for further detail see in Szulc et al., 2015, figs 16, 17). A .View southward from th muddy top of the waste pile, with visible abandoned, overgrown, and modern waste municipal dumps (see Fig. 11). B, C. Block of grade polymictic lime conglomerate (with dolomite clasts) in the heap, with visible bone cross section (arrowed in B, see also Racki, 2010, fig 2B), and the recovered fragment of cracked, probably dicynodont long bone in two views (C). D. An articulated tetrapod tail in limeston concretion (coll. Waldemar Bardzinski). E. Micritic-sandy microfacies of the coquina-oncoidal lime comglomerate, to show co-occut rence of coalified wood debris (W) and disarticulated ostracodes (Os, arrowed). F. Finely-laminated calcareous microbial envelope o: large unionid shell, to show the zone with vertically oriented, fine tubular structures, corresponding to cyanobacterial colonies, in th stromatolite-like deposit. Photographs taken by Maria Racka in May 2009 (A, B) and courtesy of Ewa Budziszewska-Karwowska (C, D and Jozef Kazmierczak (F).
Fig. 15. Field (A, B), palaeontological (C, D) and microfacies (E, F) aspects of the Keuper deposits stored in the mound near municipa dump dig at Zawiercie-Marciszow (see Figs 11, 14; for further detail see in Szulc et al., 2015, figs 16, 17). A .View southward from th muddy top of the waste pile, with visible abandoned, overgrown, and modern waste municipal dumps (see Fig. 11). B, C. Block of grade polymictic lime conglomerate (with dolomite clasts) in the heap, with visible bone cross section (arrowed in B, see also Racki, 2010, fig 2B), and the recovered fragment of cracked, probably dicynodont long bone in two views (C). D. An articulated tetrapod tail in limeston concretion (coll. Waldemar Bardzinski). E. Micritic-sandy microfacies of the coquina-oncoidal lime comglomerate, to show co-occut rence of coalified wood debris (W) and disarticulated ostracodes (Os, arrowed). F. Finely-laminated calcareous microbial envelope o: large unionid shell, to show the zone with vertically oriented, fine tubular structures, corresponding to cyanobacterial colonies, in th stromatolite-like deposit. Photographs taken by Maria Racka in May 2009 (A, B) and courtesy of Ewa Budziszewska-Karwowska (C, D and Jozef Kazmierczak (F).
Zonation of the Silesian Keuper based on two geochemical indices. The average values are given in the table
Zonation of the Silesian Keuper based on two geochemical indices. The average values are given in the table
Fig. 18. Diagram showing the range of uncertainty in timing of the Upper Triassic stages (after Ogg, 2012, figs 25.6 and 25.7; compare Lucas et al., 2012) and the range of the possible correlation error for these boundaries with global palynozones (according to Kiirschner and Herngreen, 2010; adopted by Ogg, 2012, fig. 25.7, in “Geological Time Scale 2012”; GTS 2012) and the original and updated Polish palynozones (see also Fijatkowska-Mader et al., 2015); arrows show the strikingly different positions of the palynozone boundaries on the basis of index species ranges in Cirilli (2010, fig. 2), against the first appearance datum (FAD) of these species in Ktirschner and Herngreen (2010, fig. 3; see also Barth and Kozur, 2011).
Fig. 18. Diagram showing the range of uncertainty in timing of the Upper Triassic stages (after Ogg, 2012, figs 25.6 and 25.7; compare Lucas et al., 2012) and the range of the possible correlation error for these boundaries with global palynozones (according to Kiirschner and Herngreen, 2010; adopted by Ogg, 2012, fig. 25.7, in “Geological Time Scale 2012”; GTS 2012) and the original and updated Polish palynozones (see also Fijatkowska-Mader et al., 2015); arrows show the strikingly different positions of the palynozone boundaries on the basis of index species ranges in Cirilli (2010, fig. 2), against the first appearance datum (FAD) of these species in Ktirschner and Herngreen (2010, fig. 3; see also Barth and Kozur, 2011).
Fig. 19. Diagram showing the important differences in strati- graphic distribution of bone-bearing deposits in the Silesian Upper Triassic proposed by the authors of the Warsaw group (230 Ma for Krasiejow; Dzik and Sulej, 2007; 205 Ma for Lipie Slaskie: Skawina and Dzik, 2011) and in the present paper. Uncertainty in ages of the Upper Triassic stages (taken from, Ogg 2012; see Fig. 18) is marked as dotted boundary lines, as well as an extent of dat- ing ambiguity for particular bone-bearing units (light grey ar- rows), shown by the both research groups.
Fig. 19. Diagram showing the important differences in strati- graphic distribution of bone-bearing deposits in the Silesian Upper Triassic proposed by the authors of the Warsaw group (230 Ma for Krasiejow; Dzik and Sulej, 2007; 205 Ma for Lipie Slaskie: Skawina and Dzik, 2011) and in the present paper. Uncertainty in ages of the Upper Triassic stages (taken from, Ogg 2012; see Fig. 18) is marked as dotted boundary lines, as well as an extent of dat- ing ambiguity for particular bone-bearing units (light grey ar- rows), shown by the both research groups.
Fig. 20. Stratigraphic correlation of Upper Silesian vertebrate-bearing levels with an appropriate German middle Keuper reference suc- cession in Lower Saxony (after Arp et al., 2005, fig. 2). Note that only major KrasiejOw bone-rich horizons are shown (see Fig. 3).
Fig. 20. Stratigraphic correlation of Upper Silesian vertebrate-bearing levels with an appropriate German middle Keuper reference suc- cession in Lower Saxony (after Arp et al., 2005, fig. 2). Note that only major KrasiejOw bone-rich horizons are shown (see Fig. 3).
Fig. 22. Stratigraphy-facies and climatostratigraphy schema of the middle and upper Keuper of Upper Silesia, to show overall strati- graphic position and relationships of bone- and flora-rich horizons (with reference to four generalized succession types, see Fig. 17 and Szulc et al., 2015; modified after Szulc and Racki, 2015, fig. 9); palyzonation scheme after Orlowska-Zwolinska (1983; see Fijatkowska- Mader et al., 2015).
Fig. 22. Stratigraphy-facies and climatostratigraphy schema of the middle and upper Keuper of Upper Silesia, to show overall strati- graphic position and relationships of bone- and flora-rich horizons (with reference to four generalized succession types, see Fig. 17 and Szulc et al., 2015; modified after Szulc and Racki, 2015, fig. 9); palyzonation scheme after Orlowska-Zwolinska (1983; see Fijatkowska- Mader et al., 2015).
Fig. 23. Sketch diagram of environmental evolution and main facies distribution of the southern German Keuper (from Kelber a Nitsch, 2005, fig. 2), with reference to the Silesian lithostratigraphy scheme and stratigraphic context of bone-rich levels. Tetrapod reco structions are after Dmitry Bogdanov (https://pl.wikipedia.org/wiki/Dicynodonty#/media/File:Dicynodont_from_PolandDB. jpg; https://upload.wikimedia.org/wikipedia/commons/6/6b/Metoposaurus_diagnosticus_kraselovi_1DB.jpg).
Fig. 23. Sketch diagram of environmental evolution and main facies distribution of the southern German Keuper (from Kelber a Nitsch, 2005, fig. 2), with reference to the Silesian lithostratigraphy scheme and stratigraphic context of bone-rich levels. Tetrapod reco structions are after Dmitry Bogdanov (https://pl.wikipedia.org/wiki/Dicynodonty#/media/File:Dicynodont_from_PolandDB. jpg; https://upload.wikimedia.org/wikipedia/commons/6/6b/Metoposaurus_diagnosticus_kraselovi_1DB.jpg).
Fig. 24. Environmental model for the Lipie Slaskie tetrapod locality (after Jewula, 2010, fig. 22); forest fires are shown after Marynowski and Simoneit (2009).
Fig. 24. Environmental model for the Lipie Slaskie tetrapod locality (after Jewula, 2010, fig. 22); forest fires are shown after Marynowski and Simoneit (2009).
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