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Fig. 9. | Geological cross-section of the clay pit of the Patoka Brickyard, based mostly on the Patoka 1 well profile (Fig. 11) and reserve drill holes (B1—B5; after Bardzinski and Chybiorz, 2013)

Figure 9 | Geological cross-section of the clay pit of the Patoka Brickyard, based mostly on the Patoka 1 well profile (Fig. 11) and reserve drill holes (B1—B5; after Bardzinski and Chybiorz, 2013)

Related Figures (16)

ig. 1. | Geological map of the area studied (after Marks et al., 2006, modified; see Fig. 2 for the location details of the sections studied).
ig. 1. | Geological map of the area studied (after Marks et al., 2006, modified; see Fig. 2 for the location details of the sections studied).
Fig. 2. Simplified geological map (after Bardzinski and Chybiorz, 2013) showing the location of the localities studied (outcrops and boreholes) and Triassic to Lower Jurassic surface strata (see the regional geological setting in Fig. 1). Supplementary material is available online at: tegrated study of the bone-enriched Keuper interval in terms of stratigraphy, sedimentology, mineralogy and geochemis- try. This article complements an introductory proposal of a lithostratigraphic revision in Polish by Szule and Racki (2015), a stratigraphic setting to an accompanying polemi- cal review of the age, correlation and origin of the Upper Silesian bone beds by Szulc et al. (2015), and other papers in this ASGP thematic issue.
Fig. 2. Simplified geological map (after Bardzinski and Chybiorz, 2013) showing the location of the localities studied (outcrops and boreholes) and Triassic to Lower Jurassic surface strata (see the regional geological setting in Fig. 1). Supplementary material is available online at: tegrated study of the bone-enriched Keuper interval in terms of stratigraphy, sedimentology, mineralogy and geochemis- try. This article complements an introductory proposal of a lithostratigraphic revision in Polish by Szule and Racki (2015), a stratigraphic setting to an accompanying polemi- cal review of the age, correlation and origin of the Upper Silesian bone beds by Szulc et al. (2015), and other papers in this ASGP thematic issue.
Fig. 3. Schematic section of the Upper Triassic of Upper Silesia, with its partly formal (in upper part) lithostratigraphic subdivision af- ter Szulc and Racki (2015) and a distinct colour evolution from grey to a variegated-spotty succession of the Grabowa Fm (modified, after Jewuta, 2010, fig. 4), with a focus on correlation with the Germanic Basin reference units (““Stratigraphische Tabelle von Deutschland”, 2002; Franz, 2008). Informal formations (Chrzanéw, Bolestaw) based mostly on Becker et al. (2008), partly differing from units origi- nally defined by Bilan (1976) and Kotlicki (1995). Note the occurrence of three bone-enriched levels in the Silesian Keuper, but two in the Upper Triassic.
Fig. 3. Schematic section of the Upper Triassic of Upper Silesia, with its partly formal (in upper part) lithostratigraphic subdivision af- ter Szulc and Racki (2015) and a distinct colour evolution from grey to a variegated-spotty succession of the Grabowa Fm (modified, after Jewuta, 2010, fig. 4), with a focus on correlation with the Germanic Basin reference units (““Stratigraphische Tabelle von Deutschland”, 2002; Franz, 2008). Informal formations (Chrzanéw, Bolestaw) based mostly on Becker et al. (2008), partly differing from units origi- nally defined by Bilan (1976) and Kotlicki (1995). Note the occurrence of three bone-enriched levels in the Silesian Keuper, but two in the Upper Triassic.
Fig. 5. | Schematic representation of mid-Norian palaeogeogra- phy and sedimentary palaeoenvironments of the eastern part of Upper Silesia (note: not in scale). Two potential major sources for detritus distributed by fluvial sedimentation are shown by means of arrows: the Moesian terrane (inferred from compositional spec- trum of coarse-grained clastics; Mariusz Paszkowski, pers. comm., 2014; cf. Tari et al., 2012) and Upper Silesian Basin. Active fault- ing, related to the Krakow-Lubliniec sinistral(?) shear zone, pro- moted a carbonate spring depositional system (Wozniki Mbr; Szulc et al., 2006, 2015), and also primarily controlled the devel- opment of hiatuses and unconformities over the uplifted blocks. Fig. 4. Palaeogeographic location of Upper Silesia region and present-day distribution and facies map of the Norian (Steinmergel- keuper, modified from Feist-Burkhardt et a/., 2008, fig. 13.24B). Solid lines represent the reconstructed eastern Germanic Basin outline, the black arrow indicates the marine ingression from the Tethys Ocean and the grey ones illustrate possible clastic supply from the Moesian terrane (see Fig. 5).
Fig. 5. | Schematic representation of mid-Norian palaeogeogra- phy and sedimentary palaeoenvironments of the eastern part of Upper Silesia (note: not in scale). Two potential major sources for detritus distributed by fluvial sedimentation are shown by means of arrows: the Moesian terrane (inferred from compositional spec- trum of coarse-grained clastics; Mariusz Paszkowski, pers. comm., 2014; cf. Tari et al., 2012) and Upper Silesian Basin. Active fault- ing, related to the Krakow-Lubliniec sinistral(?) shear zone, pro- moted a carbonate spring depositional system (Wozniki Mbr; Szulc et al., 2006, 2015), and also primarily controlled the devel- opment of hiatuses and unconformities over the uplifted blocks. Fig. 4. Palaeogeographic location of Upper Silesia region and present-day distribution and facies map of the Norian (Steinmergel- keuper, modified from Feist-Burkhardt et a/., 2008, fig. 13.24B). Solid lines represent the reconstructed eastern Germanic Basin outline, the black arrow indicates the marine ingression from the Tethys Ocean and the grey ones illustrate possible clastic supply from the Moesian terrane (see Fig. 5).
Fig. 8. Transitional interval between the Stuttgart Fm and Grabowa Fm in the section of the Wozniki K1 borehole (Fig. 7), as a strati- graphic setting of the stratotype of the lower boundary of the Grabowa Fm (see Szulc and Racki, 2015, figs 3A—C, F and 5). A. Typical plant debris-bearing sandstones of the Schilfsandstein (depth 76.7—76.95 m). B, C, D. Overall (B) and close-up views (C, D) of the stratotype of the base of the Grabowa Fm at the top of a red, flaser-bedded silty layer (depth 68.8 m). E, F. Variegated mottled mudstones and sandstones of the Patoka Mbr (depth 36.4—36.55 and 23.9-24.0 m, respectively; compare Szulc and Racki, 2015, fig. 3F).
Fig. 8. Transitional interval between the Stuttgart Fm and Grabowa Fm in the section of the Wozniki K1 borehole (Fig. 7), as a strati- graphic setting of the stratotype of the lower boundary of the Grabowa Fm (see Szulc and Racki, 2015, figs 3A—C, F and 5). A. Typical plant debris-bearing sandstones of the Schilfsandstein (depth 76.7—76.95 m). B, C, D. Overall (B) and close-up views (C, D) of the stratotype of the base of the Grabowa Fm at the top of a red, flaser-bedded silty layer (depth 68.8 m). E, F. Variegated mottled mudstones and sandstones of the Patoka Mbr (depth 36.4—36.55 and 23.9-24.0 m, respectively; compare Szulc and Racki, 2015, fig. 3F).
Fig. 10. Distinguishing characteristics of the uppermost Patoka Mbr in the pit of the Patoka Brickyard (see Szulc and Racki, 2015, fig 4D, E). A. An overall view of the SE part of the excavation, with dominantly red-brownish Norian to ?Rhaetian transitional series. B. Up permost Norian -?Rhaetian red beds in the topmost part of the profile with remarkable light-coloured kaolinite intercalations. C. D. Uppe siderite concretionary level (C), and coalified and locally pyritized large stem fragment (D; Agathoxylon keuperianum in Philippe et al. 2015) in the middle, grey-greenish part of the section (see Fig. 9). Courtesy of W. Bardzin ski (A, B, D) and T. Krzykawski (C).
Fig. 10. Distinguishing characteristics of the uppermost Patoka Mbr in the pit of the Patoka Brickyard (see Szulc and Racki, 2015, fig 4D, E). A. An overall view of the SE part of the excavation, with dominantly red-brownish Norian to ?Rhaetian transitional series. B. Up permost Norian -?Rhaetian red beds in the topmost part of the profile with remarkable light-coloured kaolinite intercalations. C. D. Uppe siderite concretionary level (C), and coalified and locally pyritized large stem fragment (D; Agathoxylon keuperianum in Philippe et al. 2015) in the middle, grey-greenish part of the section (see Fig. 9). Courtesy of W. Bardzin ski (A, B, D) and T. Krzykawski (C).
Fig. 12. Selected characteristics of the Patoka Mbr, from the Kobylarz 1 (A, B) and Patoka 1 boreholes (C—E). A, B. Oncoidal-bivalve limestone (A), underlying grey mudstones with plant debris (B), typical of the Lisowice level (depth 7.05—7.25 m; see Fig. 16E). C. Sand- stones containing grey mudstone intraclasts and coarse-grained bone debris (arrow). Sandstones grade upward into dark laminated mudstones, assumed to be a possible equivalent of the Lisowice level (depth 118—120.5 m; see also the correlation variant C3 in Fig. 18). D. Multi-coloured mudstones with caliche horizon followed by debris-flow deposit, comprising reworked caliche nodules (depth 175.0-178.0 m). E. Sandstones with clasts of Carboniferous coal (depth 159.0—-159.2 m).
Fig. 12. Selected characteristics of the Patoka Mbr, from the Kobylarz 1 (A, B) and Patoka 1 boreholes (C—E). A, B. Oncoidal-bivalve limestone (A), underlying grey mudstones with plant debris (B), typical of the Lisowice level (depth 7.05—7.25 m; see Fig. 16E). C. Sand- stones containing grey mudstone intraclasts and coarse-grained bone debris (arrow). Sandstones grade upward into dark laminated mudstones, assumed to be a possible equivalent of the Lisowice level (depth 118—120.5 m; see also the correlation variant C3 in Fig. 18). D. Multi-coloured mudstones with caliche horizon followed by debris-flow deposit, comprising reworked caliche nodules (depth 175.0-178.0 m). E. Sandstones with clasts of Carboniferous coal (depth 159.0—-159.2 m).
Fig. 13. Lithological section of the middle Keuper succession in the Kobylarz | drill core (see Fig. 12A, B). A. Isolated bone (arrowed) in grey marly mudstone interval (depth 41.2—42.2 m). B. Reworked vadoids (LB) in brownish mudstone (depth 16.2—17.3 m).
Fig. 13. Lithological section of the middle Keuper succession in the Kobylarz | drill core (see Fig. 12A, B). A. Isolated bone (arrowed) in grey marly mudstone interval (depth 41.2—42.2 m). B. Reworked vadoids (LB) in brownish mudstone (depth 16.2—17.3 m).
Fig. 14. Lithological section of two typical middle Keuper successions from the Zawiercie-Olkusz region, as a starting point to an origi- nal proposition of the Grabowa Formation by Bilan (1976, copied figs 6 and 14, with arrowed bottom of the redefined formation; other original units italicized). Note that an explanation of the lithological logs was not given in Bilan’s (1976) publication and only the num- bered units were described.
Fig. 14. Lithological section of two typical middle Keuper successions from the Zawiercie-Olkusz region, as a starting point to an origi- nal proposition of the Grabowa Formation by Bilan (1976, copied figs 6 and 14, with arrowed bottom of the redefined formation; other original units italicized). Note that an explanation of the lithological logs was not given in Bilan’s (1976) publication and only the num- bered units were described.
Fig. 15. Lithofacies characteristics of the Patoka Mbr, with the Lisowice bone-bearing level, at the Poreba (A) and Zawiercie-Marci- szow (B-E) localities (see Szule et al., 2015). A. Large 14 m length conifer(?) tree trunk in dark grey mudstones (compare Sulej et al., 2012, fig. 2A—B) and calcareous conglomerates. B. Cross-section of smaller tree stem. C. Fine-grained limestone conglomerate of Lisow breccia type, with mussel valves of Tihkia(?) silesiaca Skawina and Dzik (see Skawina and Dzik, 2011, fig. 10C, D). D. Stromatolites (see Racki, 2010, fig. 3). E. Weathered bivalve-oncolite limestone, with pyritic encrustations (see Racki, 2010, fig. 2, and Fig. 16 for microfacies). Courtesy of W. Bardzinski (A), E. Budziszewska-Karwowska (B and M. Racka (C—E).
Fig. 15. Lithofacies characteristics of the Patoka Mbr, with the Lisowice bone-bearing level, at the Poreba (A) and Zawiercie-Marci- szow (B-E) localities (see Szule et al., 2015). A. Large 14 m length conifer(?) tree trunk in dark grey mudstones (compare Sulej et al., 2012, fig. 2A—B) and calcareous conglomerates. B. Cross-section of smaller tree stem. C. Fine-grained limestone conglomerate of Lisow breccia type, with mussel valves of Tihkia(?) silesiaca Skawina and Dzik (see Skawina and Dzik, 2011, fig. 10C, D). D. Stromatolites (see Racki, 2010, fig. 3). E. Weathered bivalve-oncolite limestone, with pyritic encrustations (see Racki, 2010, fig. 2, and Fig. 16 for microfacies). Courtesy of W. Bardzinski (A), E. Budziszewska-Karwowska (B and M. Racka (C—E).
Fig. 17. Typical association of charophyte algae (A—D, I) and ostracods (E-G) from the Norian Grabowa Fm (Olempska et al., 2012). A. Stellatochara. B, 1. Porochara. C. Stenochara. D. Stomochara. E, F, G. Suchonella sp. H. Darwinula oblonga (R6mer). Wozniki K1 well, depth 30.5 m (A-D), Patoka 1 well, depth 176.1 m (E—G); Wozniki K1 well, depth 18.5 m (1). Scale 200 um. Fig. 16. Oncolites developed on large unionid bivalve shells of the Lisowice bone-bearing level from Zawiercie-Marciszow (see Figs 12A and 15E; see Szulc et al., 2015). A. Two mussels with thick (ca. 2 cm thick), calcareous microbial envelope. B—E. Thin-section pho- tographs, showing the locally cracked microbial layers developed on dissolved aragonitic shell material (BS). Note cyanobacterial fabrics forming the oncoids (C, D), diagenetic pyrite crystals drown within the microbial coating (B), and an admixture of sandy fraction (upper part) and isolated ostracod valves (Os; E). Courtesy of Jozef Kazmierczak (A—D).
Fig. 17. Typical association of charophyte algae (A—D, I) and ostracods (E-G) from the Norian Grabowa Fm (Olempska et al., 2012). A. Stellatochara. B, 1. Porochara. C. Stenochara. D. Stomochara. E, F, G. Suchonella sp. H. Darwinula oblonga (R6mer). Wozniki K1 well, depth 30.5 m (A-D), Patoka 1 well, depth 176.1 m (E—G); Wozniki K1 well, depth 18.5 m (1). Scale 200 um. Fig. 16. Oncolites developed on large unionid bivalve shells of the Lisowice bone-bearing level from Zawiercie-Marciszow (see Figs 12A and 15E; see Szulc et al., 2015). A. Two mussels with thick (ca. 2 cm thick), calcareous microbial envelope. B—E. Thin-section pho- tographs, showing the locally cracked microbial layers developed on dissolved aragonitic shell material (BS). Note cyanobacterial fabrics forming the oncoids (C, D), diagenetic pyrite crystals drown within the microbial coating (B), and an admixture of sandy fraction (upper part) and isolated ostracod valves (Os; E). Courtesy of Jozef Kazmierczak (A—D).
Fig. 18. Integrated stratigraphic correlation of localities and boreholes studied with the reference composite Keuper section of Upper Silesia, comprising profiles at the Patoka 1 and Wozniki K- wells, with the combined use of lithostratigraphic (Szulc and Racki, 2015), palynostratigraphic (Fijatkowska-Mader et al., 2015; palynozone numbers after Orlowska-Zwolinska, 1983) and com prehensive mineralogical and chemostratigraphic (Srodon et al., 2014) premises. Note three alternative variants (C1-C3) of the correlation of the key Lipie Slaskie section with the Patoka borehol succession, discussed in Szulc et al. (2015).
Fig. 18. Integrated stratigraphic correlation of localities and boreholes studied with the reference composite Keuper section of Upper Silesia, comprising profiles at the Patoka 1 and Wozniki K- wells, with the combined use of lithostratigraphic (Szulc and Racki, 2015), palynostratigraphic (Fijatkowska-Mader et al., 2015; palynozone numbers after Orlowska-Zwolinska, 1983) and com prehensive mineralogical and chemostratigraphic (Srodon et al., 2014) premises. Note three alternative variants (C1-C3) of the correlation of the key Lipie Slaskie section with the Patoka borehol succession, discussed in Szulc et al. (2015).
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