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The uppermost Emsian and lower Eifelian in the Kielce Region of the Holy Cross Mts. Part I: Lithostratigraphy

The uppermost Emsian and lower Eifelian in the Kielce Region of the Holy Cross Mts. Part I:... Wójcik, K. 2015. The uppermost Emsian and lower in the Kielce Region of the Holy Cross Mts. Part I: Lithostratigraphy. Acta Geologica Polonica, 65 (2), 141­179. Warszawa. The paper provis a scription of primary geological logs, characteristics and formal lithostratigraphy of the uppermost Emsian and lower of the Kielce Region of the Holy Cross Mts., central Poland. Nine sections of this interval, representing the whole area of the Kielce Region, and ranging between the Lower vonian clastics of the Winna Formation and the Middle vonian carbonates of the Kowala Formation were studied. The succession is divid into the Barania Góra Dolomite and Limestone Formation and the Wojciechowice Dolomite Formation. Six are distinguished within the former. In the western part of the region these are (in stratigraphical orr): Porzecze Claystone Meer, Dbska Wola Dolomite Meer, Dbrowa Limestone Meer, and Brzeziny Dolomite Meer. In the eastern part, the formation is divid into the Janczyce Dolomite Meer and the Jurkowice Dolomite Meer. Additionally, the Wszachów Dolomite Meer and Nowy Staw Dolomite Meer are distinguished within the overlying . The of the uppermost Emsian­ succession ranges from ca. 200 m in the eastern part to ca. 130 m in the western part of the Kielce Region. Key words: Lithostratigraphy; vonian; ; Holy Cross Mountains; Dolomites. INTRODUCTION At the turn of the Early and Middle vonian, a first-orr transgression-regression cycle began, with a generally transgressive regime prevailing during the Middle and early Late vonian (Johnson et al. 1985; Sandberg et al. 2002). Great changes occurred in facies arrangement and palaeogeography on the southern edge of Laurussia. Post-Caledonian palaeotopography, regional extension due to Rhenohercynian Ocean spreading, local tectonic activity and pulsatory sealevel rise were the main factors that controlled the sedimentary processes during the early stage of the transgression (Belka and Narkiewicz 2008). As a result, a broad Laurussian shelf appeared, and a huge system of shallow-marine carbonate ramps and platformtarted to velop (Text-fig. 1). In the latest Emsian, the transgression reached the area of the present Holy Cross Mts. (HCM). The palaeogeographical and facies velopment of the area was related to first-orr global sea-level fluctuations with minor contribution of local tectonic events (Racki and Narkiewicz 2000; Szulczewski 1978, 1995a, 2006; Textfig. 2). This consecutively resulted in: (i) late Emsian termination of continental sedimentation and velopment of marginal and marine clastic position (Lobanowski 142 KRYSTIAN WÓJCIK 1971, 1981, 1991; Szulczewski and Porbski 2008); (ii) latest Emsian­early retrogradation of clastic lithotypes beyond the Holy Cross area and velopment of carbonate lagoonal environments (Wójcik 2013); (iii) early short-term constitution of open-marine environments (Malec 2005; Wójcik 2013); (iv) late unification of shallow carbonate shelf environments (Skompski and Szulczewski 1994; Narkiewicz and Narkiewicz 2010; Niedwiedzki et al. 2010; Narkiewicz and Ratellack 2014; Wójcik 2013; Narkiewicz et al. 2015); (v) Givetian to Frasnian transformation of a carbonate shelf into an isolated reef-rimmed shallow-marine "Dyminy" carbonate platform surround by eper Lysogóry and Chciny-Zbrza intrashelf basins (Szulczewski 1971; Racki 1993; Racki et al. 2002; Wójcik 2012); (vi) late Frasnian to early Famennian drowning of a carbonate platform and its transformation into a pelagic platform (Szulczewski 1978; Szulczewski et al. 1996; Wójcik 2009, 2012); and (vii) late Famennian­Early Carboniferous unification of ep marine marly sedimentation (Szulczewski 1971, 1973, 1995, 2006). The upper Emsian and the , being the olst parts of the transgressive succession, are a subject of intensive investigations in the Kielce (southern) Region of the HCM, including stratigraphical analyses and re- construction of facies velopment. The part of the succession unr study spans between the Winna and the Kowala and inclus a nuer of informal and poorly recognized lithostratigraphical (see Narkiewicz and Olkowicz-Paprocka 1983; Narkiewicz et al. 2006; Fijalkowska-Mar and Malec 2011). The poor finition of these , as well as poor unrstanding of facies patterns, geographical and stratigraphical distribution, and mutual relations between the , has led to markedly different interpretations of the area's history at the turn of the Early vonian transgression (compare: Racki and Turnau 2000; Narkiewicz et al. 2006; Belka and Narkiewicz 2008; Fijalkowska-Mar and Malec 2011; see also Text-fig. 4). Therefore, before crucial issues referring to the studied interval can be addressed (such as the time, directions and causes of the transgression, architecture of facies tracks, or eustatic vs tectonic control of the changes observed in the sedimentary environment), a reliable timespace facies architecture must be worked out. As the available data do not allow the introduction of a refined sequence stratigraphical framework, the pattern presented herein is a formal lithostratigraphical scheme, which is the subject of the present paper. All other issues will be addressed elsewhere. nudation areas land sedimentation shallow-marine clastic sdimentation shallow-marine carbonate sedimentation ep marine sedimentation transport direction Sa xo e Zon gian ne ryn ubian Zo ldan th Mo Zo ne Rhenohercyni e Zon e ngia n Zo n ury th ian Saxo ldanub Mo Text-fig. 1. Main sedimentary zones along the southern Laurussian shelf during the early stage of the vonian transgression: A ­ in the Late Emsian, B ­ in the (modified after Milaczewski 1980 and Mabille and Boulvain 2007). Small rectangles ­ Holy Cross Mts an 143 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Local sea level changes Lithostratigraphy Global sea level changes LYSOGÓRY R. KIELCE REGION Upper Sitkówka connsed sequence Beds IIf FAMENNIAN IIf UPPER VONIAN marly complex IIe IIe FRASNIAN IId cignia Beds tritic limestones IId IIc IIc Kostomloty Beds Wietrznia Beds MIDDLE VONIAN Nieczulice Beds Kadzielnia Lower Sitkówka Beds Jawica IIb IIa GIVETIAN IIa If Id Pokrzywianka B. witomarz Beds Laskowa Beds IIb Szydlowiec Beds Ie investigated interval If Id Ic Skaly Beds WOJCIECHOWICE Fm Eiflian Dolomites Dbrowa Horizon GR. Fm ZAGÓRZE Fm LOWER VONIAN EMSIAN Ic Ib Ib LOCHKOV. PRAG. Ia BARCZA Fm Ia pre-Ia Text-fig. 2. vonian lithostratigraphy of the Holy Cross Mts. compared with local and global sea level changes (after Sandberg et al. 2002; Narkiewicz et al. 2006, Belka and Narkiewicz 2008). White square ­ investigated interval GEOLOGICAL BACKGROUND The Palaeozoic of the Holy Cross Mountains (HCM) iubdivid by the Holy Cross Dislocation into the northern (Lysogóry) and southern (Kielce) . These are parts of the Lysogóry and Malopolska terranes respectively, and both belong to the Trans-European Suture Zone (TESZ) ­ an amalgamation of terranes consolidated at the turn of the Silurian and vonian (Nawrocki 2000, 2003; Nawrocki and Poprawa 2006; Nawrocki et al. 2007; Narkiewicz 2007; Belka and Narkiewicz 2008). Although small re- locations of particular structural of the TESZ took place during the Variscan orogeny (Konon 2006, 2007), large-scale post-Silurian displacements are questionable. Palaeomagnetic data from the Nawodzice Sandstones (Nawrocki et al. 2007), Mójcza Limestone (Schätz et al. 2006), as well as from the Bardo Diabase (Nawrocki 2000; Nawrocki et al. 2013) indicate a similar position of the Malopolska Block in relation to Baltica since the Carian. Thieems to be confirmed also by the presence of similar enmic faunas (e.g. Chimaerothyris dorowiensis, Stuncka 1983), as well as of unique facies (Spirifer sandstones: 144 KRYSTIAN WÓJCIK Stuncki and Stuncka 1986) in the vonian in both HCM regions. However, the HCM cannot be treated as a united and facially homogeneous area during the vonian. In spite of a common transgressive regime prevailing throughout the area, significant differences occur in facies velopment between the northern and southern HCM regions, which are expressed in succession , lithological variety and by diachroneity of lithostratigraphical boundaries of corresponding (Szulczewski 1995, 2006; Textfig. 2). The facies autonomy and tectonic separateness of the Lysogóry and Malopolska are especially well expressed in the Lower vonian: regressive facies and a more or less continuouuccession in the northern region correspond to a great stratigraphical gap and the Silurian/vonian unconformity in the southern unit (Szulczewski 1995, 2006; Kozlowski 2008; compare with Kowalczewski et al. 1998 and Malec 1993, 2001). (2011). The original subdivision of Malec (2005) is preserved herein (Text-figs 2 and 3). The upper part of the is referred to the fined by Klossowski (1985), who subdivid it into the Chmielowiec Meer in the lower part, and the Crystalline Dolomites Meer in the upper part (see tailed scription in Skompski and Szulczewski 1994). Narkiewicz and Narkiewicz (2010; see also Narkiewicz and Ratellack 2014; Narkiewicz and Narkiewicz 2014; Grabowski et al. 2015; Narkiewicz et al. 2015) revised the and referred the upper meer to the Kowala Formation. Kielce Region In the Kielce Region, the Emsian/ boundary succession was the subject of only a few investigations, limited to general lithological scriptions (see Textfigs 2, 4). Czarnocki (1957) distinguished the Placorm Sandstone, which he referred to the Lower vonian (Emsian). More recently, Tarnowska (1976, 1981 and 1987) subdivid thiuccession into the following : Lower Mudstone, Middle Sandstone, Upper Mudstone and Upper Sandstone. The lowermost unit was later refined as the Haliszka Formation (Fijalkowska-Mar and Malec 2011; after Tarnowska 1995). The remaining three , in the rank of , have been includ to the Winna Formation (see Tarnowska 1988; Belka and Narkiewicz 2008, p. 395; Fijalkowska-Mar and Malec 2011). In the western part of the region, Czarnocki (1957) distinguished the Dbrowa Horizon and the Dolomites, which overlie the Placorm Sandstone. Stuncka (1983) interpreted the Dbrowa Horizon as a biostratigraphical unit ­ the taxon range zone of Chimaerothyris (Spirifer) dorowiensis. Two additional lithological : the Pyrite-bearing and Siritic Claystone Meer and the Dolomite Meer, still below the Dbrowa Horizon, have been revealed in a series of boreholes: Dbrowa-D5 (Tarnowska and Malec 1987), (Kowalczewski 1979; Malec 1979, 1980, 1984a; Fijalkowska-Mar and Malec 2011), Zarby 2 (Malec 1984b), and Dyminy-2 (Tarnowska 1987; Filipiak 2011). These have also been documented in the north-western part of the region: in the Szydlówek trench (Malec and Stuncki 1988) and in the Skrzetle trench (Malec 1993, 2001a, see also the discussions in Kowalczewski et al. 1998; Narkiewicz 2002; Szulczewski 2006; Kozlowski 2008). In the eastern part of the Kielce Region, Narkiewicz et al. (1981) and Narkiewicz and Olkowicz-Paprocka (1983) reported the existence of two lithological EXISITING LITHOSTRATIGRAPHY IN THE HOLY CROSS MOUNTAINS Lysogóry Region In the Lysogóry region, the upper Emsian to succession is well recognized (Czarnocki 1919, 1950, 1957; Pajchlowa 1957; Lobanowski 1971, 1981, 1990; Kowalczewski 1971; Adamczak 1976; Klossowski 1985; Malec 2001, 2002, 2005; Szulczewski and Porbski 2008; Narkiewicz and Narkiewicz 2010, 2014; Niedwiedzki et al. 2010; Fijalkowska-Mar and Malec 2011; Filipiak 2011; Narkiewicz and Ratellack 2014; Grabowski et al. 2015; Narkiewicz et al. 2015). The Lower vonian is ca. 550 m thick and is divid into the Bostów, Klonów, Barcza, and Zagórze (see Narkiewicz et al. 2006; Text-fig. 2). The 110 m thick Zagórze Formation is the olst vonian transgressive unit (Szulczewski and Porbski 2008), clearly Emsian in age (Malec 2001, 2005; Filipiak 2011). The uppermost Emsian and lower beds, 95 to 160 m thick, are distinguished as the Grzegorzowice Formation (Text-fig. 2), and are subdivid into eight : (1) Bukowa Góra Claystone; (2) Warszówek Dolomite; (3) Godów Marl; (4) Wydryszów Limestone; (5) Kapkazy Sandstone; (6) Rzepin Dolomite; (7) Zachelmie Siltstone and Sandstone; and (8) Dbrowa Limestone (Malec 2005; Textfig. 3). Such a broad finition of the Grzegorzowice Formation was rejected by Szulczewski (2006) and by Szulczewski and Porbski (2008), albeit followed by Fijalkowska-Mar and Malec (2011) and by Filipiak 145 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Text-fig. 3. Lithostratigraphical schemes around the upper Emsian and in the Lysogóry Region of the Holy Cross Mts. according to Malec (2005), supplemented by palynostratigraphical data of Filipiak (2011). 1-8 ­ Grzegorzowice Formation: 1 ­ Bukowa Góra Meer, 2 ­ Warszówek Meer, 3 ­ Godów Meer, 4 ­ Wydryszów Meer, 5 ­ Rzepin Meer, 6 ­ Kapkazy Meer, 7 ­ Dbrowa Meer, 8 ­ Zachelmie Meer of postulated age (Janczyce-1 borehole core and Jurkowice quarry). In stratigraphical orr these are the Fossiliferous and Bioturbated Dolomicrites and Dolosparites Unit, and the Unfossiliferous Crypto- and Fine-crystalline Dolomites Unit. The authors treated the as facies-equivalents of the Dbrowa Horizon and the Dolomites respectively. Romanek and Rup (1990) recognized similar in in the Kowala 1 borehole core. Summarizing, the Emsian/ boundary succession of the Kielce Region is composed of a nuer of lithologically variable, poorly recognized and inaquately fined , spanning an interval between the Lower vonian siliciclastics of the Winna Formation and the Middle vonian­Frasnian carbonates of the Kowala Formation (Text-figs 2, 4). However, a simple and straightforward formalization of these is difficult. This is because of the equivocal finition of the Dbrowa Horizon ­ the crucial lithostratigraphical unit of the analyzed succession. So far, the unit was variously fined as: (1) lithological unit of limestones and marls with abundant fossils (= Dbrowa Horizon according to Gürich 1896; = complex VIII in Pajchlowa 1957; = Grzegorzowice Limestone Meer in Malec 2001b, 2002; = Kielce Limestone in Tarnowska 1987; = Dbrowa Limestone Meer in Malec 2005); (2) limestones, dolomites and shales with fossils and/or bioturbations that overlie the Lower vonian siliciclastics and unrlie the Unfossiliferous Crypto- and Fine-crystalline Dolomites (= Couvinian in Czarnocki 1950, 1957; = complexes III-VIII in Pajchlowa 1957; = Dbrowa Horizon in Filonowicz 1973, = complexes D and E in Glazek et al. 1981, = Fossiliferous and Bioturbated Dolomicrites and Dolosparites unit in Narkiewicz et al. 1981 and Narkiewicz and Olkowicz-Paprocka 1983); and finally, (3) taxon range zone of Chimaerothyris (Spirifer) dorowiensis (Stuncka 1983). Also the and stratigraphical/geographical ranges of the , which unrlie the Dbrowa Horizon ­ the Pyrite-bearing and Siritic Claystone Meer and the Dolomite Meer, are poorly recognized. Finally, distinguishing between the Dolomites in the western part of the region and the Unfossiliferous Crypto- and Fine-crystalline Dolomites in the eastern part of the region is unreliable. 146 KRYSTIAN WÓJCIK Narkiewicz and OlkoCzarnocki (1938, 1950, 1957) wicz-Paprocka (1983) N Western part Eastern part Narkiewicz et al. 2006 Dolomites Crypto- to Finely Crystalline Unfossilliferous Dolostones Dolomites Belka and Narkiewicz and Fijalkowska-Mar this work Narkiewicz 2008 Narkiewicz 2010 and Malec 2011 S N S N S W E W E WOJCIECHOWICE Crypto- to Finely Fm Crystalline Unfossilliferous WOJCIECHOWICE Fm Dolostones Bioturbated (= Dolostones) Brzeziny Dolomite Jurkowice Dbrowa Horizon EMSIAN Fossilliferous and Bioturbated Dolomicrites and Dolosparites DH BG Dbrowa Horizon Dbrowa Horizon Dbrowa Horizon GRZEGORZOWICE Fm (Dbrowa ) Dbrowa Limestone omi Dolb M CM Dbrowa Jan czy ce M DW Placorm Sandstone Placorm Sandstone PS Placorm Sandstone gap te Text-fig. 4. Lithostratigraphical schemes around the upper Emsian and in the Kielce Region of the Holy Cross Mts. according to various authors. BG ­ Bukowa Góra shales, DH ­ Dbrowa Horizon, PSCM ­ Pyrite-bearing and Siritic Claystone Meer, DW ­ , P ­ Porzecze Meer METHODS The Upper Emsian and posits have been recognized in nine sections in the Kielce Region (Textfig. 5). In the eastern part, five sections have been investigated: Jurkowice, Winna and Wszachów quarries, Wszachówka River valley and the Janczyce-1 borehole core. In addition, comments are ma on the published data from the Zarby 2 borehole core (Malec 1984b). In the western part, four sections have been recognized: the Zbrza, Brzeziny and trenches, and the borehole core. These investigations are supplemented by published data from the Dyminy-2 (Tarnowska 1987) and Kowala 1 (Romanek and Rup 1990) borehole cores. Some of the investi- gated sections (trenches) were only temporary exposures excavated during work on public water conduits, and thus any renewed research would need new excavations. The studied sections represent from 33 to 203 m long continuouuccessions of the uppermost Emsian and . About 2000 lithological samples, including 420 polished slabs, 250 thin sections, 108 conodont samples and 4970 measurements have been analyzed. Biostratigraphical analyses and measurements have been performed in the laboratories of the Faculty of Geology, University of Warsaw and in the Palaeomagnetic Laboratory in the Polish Geological Institute ­ National Research Institute. Dbrowa D-5 Skrzetle Szydlówek LYSOGÓRY REGION Dua Skala IG-5 Wola Zamkowa IG-1 Zarby 2 Warszawa HCM Kowala 1 Chciny Dyminy-2 Brzeziny Zbrza Winna Janczyce-1 Haliszka IG-1 Wszachówka River Wszachów Upper vonian and Carboniferous Middle vonian Lower vonian Lower Paleozoic Holy Cross Fault KIELCE REGION Jurkowice 10km previous investigationection investigated Text-fig. 5. Location of the investigated sections. Geological map of the Palaeozoic core of the Holy Cross Mts. after Konon (2006 and citations therein), simplified 147 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Zbrza 32.1 m . . ~29.37 ZB2 I. corniger corniger I. c. retropressus I. werneri I. struvei ZB1 CZ6 ~28.32 ZA6 ~27.67 S ~28.80 26 CZ5 ZA5 CZ4 ZA4 ~29.39 S SSSS CZ3 CZ2 CZ1 ~39.08 ZA3 ZA2 ~40.7 Dbrowa Meer ~61.09 ZA1 S 15.8 m . . . . . .. .... .... .... .... .... .. .... .... .. . . .. .... .... .... .... .... .... .... .... . . . . .......... . . . . . . ..... .. .. . . .. . .. . .. . .. . .. . .. . .. . .. . .. . .. . . . . . . . . . .. . .. . .. . .. . .. . I. introlevatus . . . . .. .. .. . . .. .. .. .. . . .. .. .. .. .. .. .. .. .. . . . . . .. .. .. .. .. .. .. .. .. . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. .. ... .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . . ... . . . . . . . . .. . . ... ... . .... .. . . . . . . . . . . . . . . . ... .. .... .. .. ... . .. .. .. .. . . . . . . .. .. .. .. .. .. .. . . . . . . ..... .... . . . . . . . . . . . . . . . .. . . .. .. .. .. . . . . . . .. .. .. .. .. .. . .... .... ... .. .. .... .... .. ..... .... .... .. . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . ZB6 ~6.89 .... .... .... .... .... .... .. .... .... .... .... .... . .... .... .... .. ... .... .... . .... .... .... .... .... .... .. .... .... .... .... .... . . . . . . . .... .... .... .... .... .... .... .... ... . .. . . .. .. .. .. .. .. .. . . . . . . . . . . .. . . . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ... .. .. .. .. .. .. .. .. .. .. .. . .. .. ... . . . . . . . . .. .. .. .. .. .. .. .. .. .. . . . . . . . . . . . . . . . . . .. . . . . . .. .. . . .. .. .. .. .. .. ...... .. ...... .. ...... .. ........ . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. .. . .. .. .. .. . . .. . . .. .. . . .. .. . . .. .. . . .. .. . . .. .. . .. .. .. .. .. .. .. . . . .. WINNA Formation Icriodus corniger leptus ZB5 . . . . . . . . . . . .. . . . . ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ MS major trends MS minor trends cyclothems MS average CZ1 cyclothemes conodont samples bioturbation structures brachiopods Ch. dorowiensis lumachelles tentaculoids . crinoids rugose corals Thamnopora sp. asselages tabulate coraltromatoporoids placorms ZB5 CZ3 SS . . ZB4 ~28.67 . ... . .. . . . .. .. . . . . ZB3 ~34.33 2 ~ ~ . .~ . . ~ . . . . ~ ~ ~ ~ . . .. . . . . ~ ~ ~ ~ . . .. . . . . ~ ~ ~ ~ . . .. . . . . ~ ~ ~ ~ ~ ~ ~ ~ . . .. . . . . ~ . . ~. . .~. . . ~ ~ ~ ~ ~ . . .. . . . . ~ ~ ~ . .~ .. .. . . . ~ ~ ~. . . ~. . . . .. .. . . . . .. .. . . . . ~ ~ ~ ~ . . . .. . . . . . . . .. . . . . limestones intercalated with marly shales marly shales with limestone lenses marltromatoporoid-coral dolomitic biostrome dolomicrites intercalated with dolomitic claystones dolomitic thamnopora-shaleandy dolomicrites with wavy lamination claystones ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~~ . . ... . . . . . . . . .. . . . . . . . . .. . . . . . . . .. .. . .. . . . . . . . . . . . . .. . . . . .. . . .. . . .. . . . . . . . . . . .. . .. .. . .. . . .. . . . ZB2 . . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . .. . . . . . .. . . . . . . . . . . . . . . . . . . . . .. . . . . . . .. .. .. .. .. . .. .. .. . .. .. .. .. .. .. .. .. . . . . . . .. .. . .. .. .. .. . .. . .. .. .. .. .. . .. . . . . .. . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . siltstoneandstones Text-fig. 6. Lithological succession, and in the Zbrza section 148 KRYSTIAN WÓJCIK SCRIPTION OF SECTIONS Zbrza The section is located in the vicinity of the village of Zbrza, in the south-western part of the Kielce Region: 50°4327.0N, 20°3349.0E (Pl. 6). The Palaeozoic rocks in this locality are exposed in the Zbrza Antycline as a part of the Wolica-Zbrza Fold, the largest tectonic structure of the southern Mesozoic surrounding of the HCM. The Carian to Upper vonian strata of the area were the subject of tailed investigations (czkowski and Tomczyk 1969; Filonowicz 1968, 1973; Kucia 1987; Wójcik 2009, 2012; see also Czarnocki 1919; Stuncka 1983; Hajlasz 1967; Racki 1993, p. 95). The Zbrza Anticline is also one of the most important outcrops of the Dbrowa Horizon (Gürich 1896; Zbroja et al. 2007). So far, however, the Emsian to succession of the area has been scribed only in general (Filonowicz 1973; Malec and Romanek 1994; Filipiak 2011). The Lower­Middle vonian boundary succession in the village of Zbrza was exposed during the construction of public water conduits in spring 2011. The exposure ran from the southern end of the village (house no. 1) and continued 175 m to the north. At present, it can be traced along the drains. The exposed succession was 61 m thick and has been divid into 16 lithological (Text-fig. 6 and Pl. 1). 345 lithological samples, 125 polished slabs, 50 thin sections and 911 measurements were analyzed. Unit 1 (2 m thick) is composed of 25­35 cm thick beds of light grey, medium-grained flat-bedd quartz sandstones with intercalations of green siltstone laminae. Unit 2 (5.4 m thick) is composed of red and red-violet siltstones alternating with thin layers of violet finegrained quartz-muscovite sandstones predominating in the lowermost (1.6 m thick) and uppermost (1.1 m thick) parts of the unit. A 2.7 m thick package of green claystones occurs in the middle part. Unit 3 (3.2 m thick) is composed of 5­40 cm thick beds of light grey quartz sandstones with flat or lowangle cross-bedding, intercalated by thin packages of green claystones. Thin lenses of placorm breccias occur on the upper surfaces of two sandstone beds. Unit 4 (0.5 m thick) is composed of green claystones, reduced tectonically at the top. Unit 5 (3.2 m thick) is composed of two thick beds of light grey medium-grained cross-bedd quartz sandstones (55 and 100 cm thick) and few thinner sandstone beds intercalated by thin and discontinuous laminae of green claystones. Unit 6 (1.7 m thick) is composed of brown to yellow dolomitic claystones, which constitute the base of the vonian carbonate succession. A few lenses of yellow-weathering dolomitic sandy marls occur in the upper part. Unit 7 (1.15 m thick) is composed of several 10­30 cm thick beds of reddish marly/sandy dolomicriteeparated by thin packages of brown dolomitic claystones. Unit 8 (3.7 m thick) is composed of a cyclic succession of the following packages: Package A: greenish dolomitic claystones (20­40 cm thick) with abundant Thamnopora sp.; Package B: yellowish marly dolomicrites with abundant Thamnopora sp. (15­40 cm thick); Package C: yellowish sandy dolomicrites with wavy lamination and single thamnoporoid remains; Package D: yellowish sandy dolomicrites in single massive beds (30 cm thick). The packages are arranged into 3 cyclothems (ABCD, ABCD, ABCACAD), the of which ranges between 1.2 and 1.3 m. Unit 9 (12.4 m thick) is characterized by a subtle cyclicity of the following packages: Package E: grey-violet dolomicrites and dolomitic limestones (20­40 cm thick) with flat surfaces, intercalated by brown dolomitic claystones; single rugose corals and tabulates occur within the dolomites; Package F: reddish marly dolomicrites with wavy surfaces, intercalated by brown dolomitic claystones; Package G: thin beds of yellow sandy dolomitic claystones. The packages are arranged into 3 cyclothems (EFG, EFG, EFG), the of which ranges between 2.0 and 2.7 m. The cyclicity vanishes in the upper part represented by reddish dolomicrites with single corals. Unit 10 (30­95 cm thick) is composed of three beds of reddish stromatoporoid-coral dolomites with predominant Thamnopora sp. and rugose corals overgrown by tabular stromatoporoids. There are also lenses of crinoid tritus. In the Zbrza Anticline, the posits of this unit build several bioherms, up to a dozen or so metres high. 149 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Unit 11 (65 cm thick) is composed of greenish marly shales with lenses of monospecific (Chimaerothyris dorowiensis) brachiopod lumachelles and crinoidal limestones. The brachiopods are well preserved, complete and oriented vertically. Adult forms predominate, with no signs of reposition. The lenses cut the unrlying shale laminae, but are smoothly covered by the overlying beds. Unit 12 (2.2­3 m thick) is composed of yellow- to greenish marls. Single brachiopods, crinoids and tentaculoids occur within the marls. Unit 13 (4.6 m thick) is composed of greenish marly shales with lenses of monospecific (Chimaerothyris dorowiensis) brachiopod lumachelles and crinoidal limestones, similar to those in unit 11. The abundance of organotritic limestone horizons increases towards the top of the unit. The coarse-grained beds are dominated by tritus of brachiopods (Chonetes angustestriata, Athyris concentrica and rare Chimaerothyris dorowiensis). Less common are tentaculoids (Tentaculitechlotheimi, T. subconicus), gastropods (Murchisonia sp.), crinoids, bryozoans, tabulate corals (Thamnopora sp.), rugose corals, molluscs, microconchids, trilobites (chenella dorowiensis) and rare cephalopods. Unit 14 (8.8 m thick) is composed of several tens of grey thin-bedd limestones intercalated by green marly shales. Three main lithological types of limestones can be distinguished: · grained limestones with fossil tritus throughout: brachiopods and tentaculoids with minor contribution of gastropods, bryozoans, tabulate and rugose corals, molluscs, trilobites and cephalopods occur. The lower surfaces have a clearly erosional character, while the upper surfaces are indistinct and show a gradual transition into micrite. Some grained limestonehow grad bedding, with brachiopod coquinas at the top. Skolithos isp. filled up with green marls appears at the tops of some of the surfaces; · flaser limestones: tritus of fossils build 1­2 cm thick laminae/strips within a micritic matrix; · micritic limestones: grey, grey-greenish and greyreddish thin-bedd marly limestones with bioturbation structures and occasional flat lamination. Chonetes angustestriata in monospecific lumachelles appear rarely on top surfaces. This is a second type of autochthonous brachiopod lumachelles in the section. The three types of limestones within the unit show approximately equal proportions. Unit 15 (2.5 m thick) is composed of light grey and reddish sandy dolomicrites and dolomitic marls intercalated by brown dolomitic claystones. 11 thin beds of dolomitic sandy marls (ca. 12­15 cm thick), with a nodular texture to wavy lamination, occur in the lower part of the unit, Very thin layers of reddish marls occur above. Unit 16 (9.5 m thick) is composed of grey, thin-bedd grained limestones, flaser limestones (micritic limestones, in which smudges and/or irregular laminae of grains occur) and micritic limestones intercalated by green marly shales, similar as in unit 14. The micritic limestones predominate in the upper part of the unit. Biostratigraphy A collection of 75 conodont specimens from 34 dissolved samples (21 positive) has been obtained, and the following taxa were intified: Icriodus corniger corniger, I. corniger leptus, I. curvirostratus, I. introlevatus, I. corniger retropressus, I. werneri, and I. struvei. The asselage documents the Polygnathus costatus and P. c. costatus zones, with the boundary between them recognized in unit 14 (see Text-fig. 6). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). A collection of 718 samples rived from 7-cm intervals in the carbonate part of the succession (Dbska Wola and Zbrza ) has been measured. Average MS is 27.2×10-8m3/kg. The MS curve is divid into 4 major asymmetrical fluctuations/trends (Textfig. 6): Trend A is 13.3 m thick and ranges from unit 6 to the upper part of unit 9. The trend is divid into 6 minor fluctuations: ZA1: 2.6 m thick with average MS 61.09×10-8m3/kg; ZA2: 1.4 m thick with average MS 40.7×10-8m3/kg, ZA3: 1.2 m thick with average MS 39.08×10-8m3/kg, ZA4: 3.4 m thick with average MS 29.39×10-8m3/kg, ZA5: 2.6 m thick with average MS 28.8×10-8m3/kg, ZA6: 2.1 m thick with average MS 27.67×10-8m3/kg; Trend B is 16.3 m thick and ranges from the upper part of unit 9 to the upper part of unit 14. The trend is divid into 6 minor fluctuations: ZB1: 1.6 m thick with average MS 28.32×10-8m3/kg, ZB2: 2.8 m thick with average MS 29.37×10-8m3/kg, ZB3: 1.6 m thick with average MS 34.33×10-8m3/kg, 150 KRYSTIAN WÓJCIK ZB4: 2.8 m thick with average MS 28.67×10-8m3/kg, ZB5: 3.5 m thick with average MS 15.74×10-8m3/kg, ZB6: 4 m thick with average MS 6.89×10-8m3/kg; Trend C is 6.5 m thick and ranges from unit 15 to the lower part of unit 16. The average MS in trend C is 6.89×10-8m3/kg; Trend D inclus the uppermost part of the succession, with the of at least 6 m, and the average MS of 4,86×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Brzeziny The section is located in the south-western part of the Kielce Region, in the eastern part of the Chciny Anticline: 50°4614.6N, 20°3448.2E (Pl. 6). The Emsian­ transition was recognized in the western part of the antycline by Glazek et al. (1981) in the vicinity of the town of Chciny. The Lower vonian siliciclastics cropping out in that area are very thin (only a few metres thick), a typical Dbrowa Horizon is lacking (dolomites with bioturbation structures and grained intercalations occur in the lower part of the succession), and only the dolomites are commonly present in small outcrops along the Castle Hill. The topmost part of the succession ­ the Dolomites, is partly exposed in the nearby Radkowice and Jawica quarries. In the vicinity of the village of Brzeziny, the of the clastic succession increases and the Dbrowa Horizon appears. So far, the succession has not been scribed. Only very general remarks can be found in Filonowicz (1973) and Stuncka (1983). A 56 m thick succession of Emsian and posits in the village of Brzeziny was recognized by the author in 2010. A 65 m long trench was ma, longitudinally cutting the southern slope of the Siedliskowa Hill, running along the northern si of road no. 763, ca. 100 m east of the cemetery and 150 m north of house no. 271 on Chciska Street. The exposed succession was 56 m thick and has been divid into 8 lithological (Text-fig. 7 and Pl. 2). 220 lithological samples, 80 polished slabs, 27 thin sections, 21 conodont samples and 380 measurements were analyzed. Unit 1 (1.6 m thick) is composed of 7­12 cm thick beds of yellow medium-grained quartz sandstones with placorm remains. A 25 cm thick breccia occurs at the top. Unit 2 (5.6 m thick) is composed of grey siltstones, which predominate in the lower and upper parts of the unit. Thin layers of red-violet fine-grained quartzmuscovite sandstones occur in the middle part. Unit 3 (90 cm thick) is composed of brown dolomitic claystones overlain by four beds of yellow and violet dolomitic sandy marls with intercalations of claystones Unit 4 (13.5 m thick) is composed of 5­35 cm thick beds of marly dolomites intercalated by very thin laminae of brown claystones. Unit 5 (8.2 m thick) is composed of 1­10 cm thick beds of grey-violet marly dolomicrites with intercalations of brown claystones. Chondrites isp. horizons and dolosparite laminae/strips occur in the thickest dolomite beds, albeit not forming indivi dual beds. Unit 6 (6.9 m thick) is composed of two, 95 and 35 cm thick packages of green marly shales with monospecific (Chimaerothyris dorowiensis) brachiopod lumachelle lenses (compare with 11 and 13 in the Zbrza section). Packages of 10­25 cm thick beds of grey limestones occur in the middle and upper parts of the unit. Similarly as in the Zbrza section, three types of limestones can be distinguished: micritic, flaser and grained limestones. Chimaerothyris dorowiensis and Chonetes angustestriata are the most frequent brachiopods. In some beds, crinoids are also present. Gastropods (Murchisonia sp.), tentaculoids, microconchids, as well aingle trilobites (chenella sp.), corals and cephalopods are less common. Bioturbation structures (Chondrites isp.) occur in almost all beds, and are especially abundant around the grained laminae/strips. Unit 7 (3.05 m thick) is composed of 5­25 cm thick beds of green micritic dolomitic limestones. Intercalations of brown dolomitic claystones occur in the lower part. Single brachiopods (Chonetep.) and crinoids are also present. Unit 8 (15.9 m thick) is composed of 5­40 cm thick beds of red to violet marly dolomicrites with intercalations of brown dolomitic claystones. Several thicker, greenish beds occur in the middle part of the unit and aingle tabular beds in its upper part. Fossils are very rare and limited to thin sparry laminae/strips. Bioturbation horizons, dominated by Chondrites isp., occur more frequently. 151 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Brzeziny I. struvei Brzeziny Meer ~43.12 BB1 ~43.00 BA3 SS S Icriodus corniger corniger I. corniger retropressus group I. werneri I. amabilis BA2 ~47.03 39.6 m ~52.16 BA1 S S I. curvirostratus I. introlevatus 6.9 m Dbrowa Meer WINNA Formation . . . . . BB3 ~16.49 . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 0 30 29.4 m MS major trends MS minor trends ~52.16 MS average conodont samples bioturbation structures brachiopods lumachelles tentaculoids . crinoids rugose corals placorms BB5 limestones intercalated with marly shales marly shales with limestone lenses BB2 dolomitic limestones dolomicrites intercalated with dolomitic claystones claystones ~40.45 . .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. sandstones Text-fig. 7. Lithological succession, and in the Brzeziny section 152 KRYSTIAN WÓJCIK Biostratigraphy A collection of 87 from 21 dissolved (14 positive) samples has been obtained, and the following taxa were distinguished: Icriodus corniger corniger, Icriodus corniger retropressus group (including. I. c. retropressus Bultynck 1970 and I. n. sp. Narkiewicz 2013), Icriodus curvirostratus, Icriodus introlevatus, Icriodus werneri, Icriodutruvei, Icriodus amabilis. The asselage documents two ­ Polygnathus costatus and P. c. costatus, with the boundary between them established in the lower part of unit 6 (Text-fig. 7). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). A collection of 380 samples from 15-cm intervals has been measured. Average MS is 26,9×10-8m3/kg. The MS curve is divid into 4 major asymmetric fluctuations/trends (Text-fig. 7): Trend A is 11 m thick and ranges from the base of unit 3 to the upper part of unit 4. The trend is divid into 3 minor fluctuations: BA1: 2.9 m thick with average MS 52.16×10-8m3/kg, BA2: 4.3 m thick with average MS 47.03×10-8m3/kg, BA3: 3.8 m thick with average MS 43.87×10-8m3/kg, 25 polished slabs, 16 thin sections, 15 conodont samples and 429 measurements were analyzed in the section (Text-fig. 8). Unit 1 (9 m thick) is composed of grey to green claystone and siltstone packages interbedd with thinbedd yellow sandstones. Single placorm impressions occur. Unit 2 (2.3 m thick) is composed of thin-bedd yellow fine-grained quartz sandstones with placorm impressions and charred remains, and with thin intercalations of siltstone packages. Unit 3 (3.7 m thick) is composed of a 65 cm thick package of red-brown dolomitic claystones in the lower part and a 1.5 m thick package of brown dolomitic marls in the middle part. 20 ­ 30 cm thick browngreen and grey-green marly limestones with fenestral structures occur in the uppermost part of the unit. Two beds of nodular limestones with single cystoids and gastropods, topped by intraformational breccias, are present in the uppermost part of the unit. The unit can be clearly distinguished from the overlying posits due to the presence of limestone beds and fossils. An important feature is the absence of Chimaerothyris dorowiensis and other fossils typical of the Dbrowa Horizon. Unit 4 (27 m thick) is composed of a cyclic succession of the following packages: Package A (5­17 cm thick): brown dolomitic claystones; Package B (0.6­4.2 m thick): thin-bedd greenish to violet dolomitic marls with rare horizons of bioturbation structures; Package C (1.2­2.8 m thick): thin- to medium-bedd reddish to violet laminated marly dolomicrites with rare stromatolites. The unit is divid into 5 ABC cyclothems, the of which ranges between 2.25 and 6.45 m. Biostratigraphy Of the 15 dissolved samples only one was positive, yielding two specimens of the conodont Icriodutruvei. This taxon indicates an age not olr than the upper part of the Polygnathus costatus costatus Zone of the stage (Text-fig. 8). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). Trend B is 15.8 m thick and ranges from the upper part of unit 4 to the middle part of unit 6. The trend is divid into 3 minor fluctuations: BB1: 5.4 m thick with average MS 43.12×10-8m3/kg, BB2: 3.6 m thick with average MS 40.45×10-8m3/kg, BB3: 6.8 m thick with average MS 16.49×10-8m3/kg, Trend C is 6.6 m thick and it ranges from the upper part of the unit 6 to the lower part of the unit 8. The average MS is 26.9×10-8m3/kg. Trend D is 10 m thick and inclus the upper part of the succession (unit 8). The average MS is 22.27×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). The section is located in the central-western part of the Kielce Region: 50°5027.1N, 20°2857.8E (Pl. 6). A 33 m thick succession of Emsian and posits of the Dyminy Anticline was temporarily exposed in the village of in 2011. A 75 m long trench, excavated during public water conduit construction, was located along the eastern si of road S8, starting from the overpass to the north. The succession has been divid into 4 lithological (Text-fig. 8). 76 lithological samples, 153 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. gastropods cystoids calcisphaerids ostracods laminations MS major trends MS average conodont samples bioturbation structures intraformational breccias A collection of 429 samples rived from 7-cm intervals has been measured. Average MS is 13× 10-8m3/kg. The MS curve is divid into 4 major asymmetric fluctuations/trends (Text-fig. 8): Trend B is 3.5 m thick and eraces unit 3. Average MS is 13.59×10-8m3/kg, Trend C is 5.7 m thick and eraces the lower part of unit 4. Average MS is 18.32×10-8m3/kg, Trend D is 3.1 m thick and it ranges through the middle part of the unit 4. Average MS is 13.32×10-8m3/kg, Trend E is 13.5 m thick and eraces the upper part of unit 4. Average MS is 8.02×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Kowala 1 borehole (Romanek and Rup 1990, Narkiewicz 1991) susceptibility magnetic ~13.32 ~18.32 6 ~13.59 4 2.8 m 2 .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. . .. . .. . .. . .. . .. . . . . . dolomitic claystones claystones . .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. The location of the Kowala 1 borehole is 50°4804.52N, 20°3335.96E (central-western part of the Kielce Region; central part of the GalziceBolechowice Syncline). The core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. The core went through a complete, 993.6 m thick vonian succession, reaching the Carian below (Racki 1985, Romanek and Rup 1990, Narkiewicz et al. 1990, akowa and Radlicz 1990, Nehring-Lefeld 1990, Turnau 1990, Narkiewicz 1991). The siliciclastics at the base of the vonian succession are only 2 m thick and are followed by ca. 140 m thick carbonates. Romanek and Rup 1990 (see also Narkiewicz 1991) subdivid the latter into a 97 m thick Bioturbated Dolomites with Macrofossils Unit (882.7­989.7 m pth), and a circa 30 m thick tritic and Laminated Dolomite Unit (846.8­882.7 m pth). The first unit is composed mostly of bioturbated dolomicrites and dolomicrosparites with Chondrites isp. asselages. Single brachiopods, corals, stromatoporoids and crinoids are present and are especially abundant in the upper part of the unit (884.0­889.9 m pth). The second unit is composed of flat-laminated dolomicrites and tritic dolomites with horizons of intraformational breccias and oolites. Dyminy-2 borehole (Tarnowska 1987, Filipiak 2011) The location of the Dyminy-2 borehole is 50°4850.88N, 20°3833.61E (central-western part Brzeziny Meer S costatus - eifilius .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . I. struvei .. . .. . .. . .. . . . . . . . .. .. .. .. . .. . .. . .. . .. . .. . . . . .. .. .. .. .. .. .. .. .. .. .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. limestones cuboid fissility marls dolomicrites with claystone intercal. sandstones Text-fig. 8. Lithological succession, and in the section 154 KRYSTIAN WÓJCIK of the Kielce Region; southern li of the Dyminy Antycline). The core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. The 222 m ep Dyminy-2 borehole went through the Lower vonian to succession. Tarnowska (1987) divid the succession into 4 : Lower vonian siliciclastics, Lower Dolomite Unit, Dbrowa Horizon (Kielce Limestone), and Upper Dolomite Unit. The Lower Dolomite Unit (137.7­ 109.0 m pth) is composed of sandy dolomites and dolosparites with crinoids, corals, stromatoporoids, brachiopods, ostracods and fishes. Above, unfossiliferous laminated dolomicrites with fenestral structures occur. The Dbrowa Horizon (109.0­96.0 m pth) is composed of bioclastic limestones with ostracods, crinoids, brachiopods, gastropods, , tentaculoids, trilobites, foraminifers and fish remains. The Upper Dolomite Unit is built of dolomicrosparites and bioturbated dolomites in the lower part (96.0­45.0 m pth) and unfossiliferous dolomicrites with microbial lamination in the upper part (45.0­15.0 m pth). Filipiak (2011) intified the velatalangii palynostratigraphic Zone within the Dbrowa Horizon. He also indicates the position of the Emsian/ boundary interval at pths between 143.0 and 110.0 m. Szydlówek, Skrzetle, Dbrowa D5 (Malec and Stuncki 1988, Malec 1993, 2001, Tarnowska and Malec 1987) The Emsian and posits in the northwestern part of the Kielce Region were recognized in the Szydlówek road-cutting (Malec and Stuncki 1988) and Skrzetle trench sections (Malec 1993, 2001), as well as in the Dbrowa D5 (Tarnowska and Malec 1987) and (Kowalczewski 1979; Fijalkowska-Mar and Malec 2011) borehole cores. The sections exposed the Pyrite-bearing and Siritic Claystone Meer, which overlies the Winna Formation. The posits are black to yellow in colour in the lower part, and red and brown-red at the top of the unit. Sirite nodules, limonite breccias, and siltstone and sandstones intercalations occur frequently, but the carbonate content is also significant. Rare brachiopods, including Chimaerothyris dorowiensis, as well as crinoids and tentaculoids occur. Foraminifers (Amphitremoida, Lagenammina, Saccammina, Hyperammina and different morphotypes of Webbinelloia), ostracods, and (Icriodus corniger retropressus group, I. corniger corniger and I. corniger cf. leptus) are also present. In the Dbrowa D5 borehole core, the Pyrite-bearing and Siritic Claystone Meer is overlain by the Dbrowa Horizon, composed of few metres of predominantly micritic and grained limestones. It yield abundant Chimaerothyris dorowiensis, algae, ostracods, foraminifers, and rare (Icriodus werneri). The Dbrowa Horizon is not present in the Szydlówek and Skrzetle sections, in which the pyrite-bearing and siritic claystones are overlain by dolomites. Single brachiopods, tentaculoids, corals and , as well as horizons of bioturbation structures occur within the lower part of the dolomitic succession. borehole The location of the borehole is 50°5656.96N, 20°3034.64E (north-western part of the Kielce Region; northern li of the Miedziana Góra Anticline). The core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. The borehole cored the most complete Emsian­ succession in the north-western part of the Kielce Region. A tailed lithological scription can be found in Kowalczewski (1979; see also Fijalkowska-Mar and Malec 2011). In the present paper thicription iupplemented by measurements (Text-fig. 9). The succession of the borehole is 66 m thick (Text-fig. 9). Fijalkowska-Mar and Malec (2011) divid it into 4 lithological : Upper Sandstone Meer of the Winna Formation (7.0­12.9 m, 5.1 m thick); Pyrite-bearing and Siritic Claystone Meer (12.9­19.2 m, 5.4 m thick); Dolomite Meer (19.2­39.5 m, 15.6 m thick); and Dbrowa Limestone Meer (39.5­116.5 m, 33.8 m thick). Biostratigraphy The stratigraphy of the section was presented by Malec (1979, 1980, 1984, 1990, 1992 and 1993) and summarized in Fijalkowska-Mar and Malec (2011). Accordingly, the boundary between the Lower and Middle vonian was located within the Dbrowa Meer, at 62.7 m pth, based on the first appearance of the conodont Icriodus corniger retropressus. However, it should be noted that no were record below this pth. This long barren interval may therefore easily represent age as well. 155 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. pth . . . . . PB4 ~25.80 39.5 m . . . . . . ~33.83 PA3 PB3 ~36.41 PA2 ~39.20 . . ~44.39 PA1 .. . .......................................................... .. .... ...... ... . .............. ...... ............. ... . . . ..... . Icriodus werneri I. corniger retropressus I. corniger corniger . . . . . . . . .. . .. . . . .. . .. . .. .. .. ... .. . . .. .. . ... .. .... ... . . . . .. .... .... .. ~37.27 PB2 . . . ... . .. . . ............................................................................................................... . . ........................................................... . .. .. ... . .. . . .... .. Dbrowa Meer 19.2 m ~~ ~~ ~~ ~~ ~~ ~~ ~~ ~~ ~~ PB5 . . . Porzecze Meer . . MS major trends MS minor trends MS average conodont samples bioturbation structures brachiopods tentaculoids crinoids rugose corals tabulate coraltromatoporoids laminations grained intercalations coralline intercalations . .............. . ... .................................................................................................................................................. . ... .. .... .. .. . .... . .. . .. . . ~~ ~~ ~~ ~~ . .. ... .. . .. .. . ... .. crinoidal limestones limestones intercalated with marly shales limestones dolomicrites intercalated with dolomitic shaleiritehales 12.9 m ~ ~~ ~~ ~ ~~ ~ ~ ~~ ~~ ~ ~~ ~ ~ ~~ ~~ ~ ~~ ~ . .. . ~~ . .. ~~~~ ~~. . . .. ~ ~~ ~~ ~ ~~ ~ ~. .~~.~~ ~ ~ ~~ . .~~ ~~ .. . . .. ~~ ~~ . . . .. ...... ~~. .. . . ... ~ ~ .... . ~~~ ~~ ~ ~~ ~~ ~ ~~~ ~ ~ ...................... . .. . ~ ... ...~..~..~. .. .~.~..~..~..~ . . . . ~ . ... ... .. . ~...~..~. ...~.~.. .~. ... .. .. .. .. .. .. .. .. .. . . . . . PA4 ~33.8 80 100 Text-fig. 9. Lithological succession (after Kowalczewski 1979), (after Fijalkowska-Mar and Malec 2011) and (this work) in the borehole core . . ~38.12 PB1 ~ ~ ~ ~ ~ ~~~ ~~~~~~~~~~~~~ ~~~ ~ ~ ~ ~ ~ ~~~ ~ ~ ~ ~ ~ ~~~ ~ ~ ~ ~ ~ ~~~ . . ....... . . . .................................................... .................. .................................... siltstoneandstones ~ ~~ ~~ ..... . ~ . . . . ~ ~ ~~~. .~.~. .~.~. 156 KRYSTIAN WÓJCIK A collection of 553 samples rived from 20-cm intervals has been measured. Average MS is 36.08× 10-8m3/kg. Two major MS fluctuations/trends (A­B), divid into minor fluctuations, are intified (Text-fig. 9): Trend A ranges from 21.3 m to 45.1 m pth and is divid into 4 minor fluctuations: PA1: 21.3­26.6 m pth, average MS 44.39 ×10-8m3/kg, PA2: 26.6­32.8 m pth, average MS 39.20×10-8m3/kg, PA3: 32.8­40.5 m pth, average MS 33.83×10-8m3/kg, PA4: 40.5­45.1 m pth, average MS 33.80×10-8m3/kg; thin sections, as well as 766 measurements were analyzed in the section. Unit 1 (5.6 m thick) is exposed in the olst part of the quarry. Thin- and medium-bedd grey laminated dolomicrites occur in the lowermost part of the succession, just several metres above the sandstones of the Winna Formation. They are intercalated by thin packages of dolomitic shales. Horizons of bioturbation structures (Chondrites isp.) appear on the surfaces, as well as within the beds. Numerous conulariids, plants remains and molluscs occur within the grained laminae/strips. Brachiopods (Gypidula sp.) are locally abundant, building monospecific lumachelles. Unit 2 (12 m thick) is composed of 20­50 cm thick beds of brown-grey dolomicrites and fine-crystalline dolomites with wavy interbedding. Thin laminae of black dolomitic shales occur on some surfaces. Thin tentaculoid lumachelles with tritus of bryozoans, crinoids and gastropods appear at the top of some beds, while numerous brachiopods (Gypidula) occur at the tops of others. Chondrites isp. concentrations with single Planolites isp. are common and constitute characteristic, blueweathering 15 cm thick bioturbation horizons in the upper part of the unit. tritus of shelly fossils occurs throughout. Unit 3 (18.8 m thick) is composed of up to 2.5 m thick beds of grey-blue weathering nodular dolomicrites intercalated by strongly bioturbated horizons. The nodules are more or less isolated, up to 5 cm in diameter, and surround by residual laminae/strips of clay minerals. In some parts, the nodular texture changes into wavy/irregular bedding. Single Gypidula sp. appear on the upper surfaces. The bioturbation horizons reach a of up to 40 cm and contain a nse and compact network of Chondrites isp. burrows and rare Planolites isp. Rare laminae of tritic material with crushed crinoids and brachiopods also appear. The burrows penetrate the rock completely, resulting in the bed being subdivid into minor irregular more or less isolated sub-beds. The nodular structure disappears in the upper part of the unit and the dolomite beds become more regular and homogeneous. A 30 cm thick regolith horizon covered by a distinctive (clearly visible in the quarry) 20 cm thick package of orange clays occurs in the topmost part of the unit. Unit 4 (18.5 m thick) is composed of up to 2 m thick beds of yellow-weathering nodular dolomites with bioturbation horizons. There are irregular lenses of homo- Trend B ranges from 45.1 m to 116.5 m pth and is divid into 4 minor fluctuations: PB1: 45.1­64.0 m pth, average MS 38.12×10-8m3/kg, PB2: 64.0­79.5 m pth, average MS 37.27×10-8m3/kg, PB3: (79.5­97.1 m pth, average MS 36.41×10-8m3/kg, PB4: 97.1­116.5 m pth, average MS 25.80×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Jurkowice Quarry The section is located in the south-eastern part of the Kielce Region: 50°3739N, 21°2126E (Pl. 6). and Givetian carbonates are exposed in the Jurkowice and Budy quarries. The vonian of the area was intensively studied (Czermiski and Ryka 1962; Pajchlowa and Stasiska 1965; Kamierczak 1971; Baliski 1973; Olempska 1979; Narkiewicz et al. 1981; Narkiewicz 1991; Racki 1993; Racki and Sobo-Podgórska 1993; Preat and Racki 1993; Hajlasz 1993; Zdanowski 1997), however, most of the studies were dicated to the Givetian. The was reported by Narkiewicz et al. (1981) and Zdanowski (1997). According to them, a ca. 100 m thick succession, exposed in the Jurkowice quarry, may be subdivid into a Fossiliferous and Bioturbated Dolomicrites and Dolosparites Unit at the base (43 m thick) and a Unfossiliferous Crypto- and Finecrystalline Dolomites Unit at the top (>58 m thick). Zdanowski (1997) documented the early age of the lower unit (Polygnathus costatus costatus conodont Zone). The carbonates currently exposed in the Jurkowice quarry represent approximately the same stratigraphical interval as documented in the papers referred to above. The section available at present is located ca. 150 m north of the quarrying front as it was in 1997. A new lithological log, measurements and sedimentological investigations were provid in 2011 and 2012. The succession has been divid into six lithological (Text-fig. 10). 120 lithological samples, including 45 polished slabs and 27 157 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Jurkowice quarry dolomitic shales/ claystones grained (intraclast-ooid) dolomites dolomicrites crinoid dolomites nodular dolomites bioturbation horizonts laminations, stromatolites breccias MS major trends MS average bioturbation structures gypidulids, lingulids tentaculoids, crinoids tabulates, conulariids plants 2 ~17.10 Nowy Staw Meer Wszachów Meer S ~~~~ SS EE2 ~14.01 SS 66.2 m 66 S 1 ~15.09 56.0 m EE1 ~12.01 I. corniger retropressus group I. werneri I. struvei 46 ~17.44 3 6 ~13.92 Icriodus corniger corniger CE Text-fig. 10. Lithological succession, (after Zdanowski 1997, revised) and in the Jurkowice quarry section 158 KRYSTIAN WÓJCIK geneous crinoid dolomites with Thamnopora sp. tritus. Three (up to 2 m) thick homogeneous beds of crinoid dolomites occur at the top of the unit. Unit 5 (10.3 m thick) is composed of dark, micritic and bituminous dolomicrites. The absence of bioturbation structures and shelly fossils, and the presence of a distinct horizon of stromatolitic domes, are characteristic features. Medium-bedd dark micritic dolomites with flat to wavy surfaces coated with iron crusts, intercalated by black dolomitic shales predominate in the lower part of the unit. Flat laminations are common in this part. A continuous bed of stromatolites, with 40 cm domes, and with irregular internal laminations, occur in the upper part. A package of dolomitic shales compensates the dome-relief, and a 2.5 m thick package of dark dolomicrites with flat laminations occur at the top. Unit 6 is composed of a cyclic succession of the following lithological packages: Package A: thick-bedd yellowish grained dolomites with flaser laminations and erosional lower surfaces. The flaser lamination is expressed aeveral cm long micritic, more or less continuous laminae/strips within a grained, intraclast-ooid matrix. The micritic laminae/strips build small stromatolitic domes at the tops of the grained beds; Package B: green micritic dolomites with flat laminations and intraformational breccia horizons (10­30 cm thick); Package C: green to yellowish dolomitic shales (up to 10 cm thick); Package D: variegated siltstones (up to 5 cm thick). The packages are arranged into 8 ABCD cyclothems, the of which ranges between 1.0 and 1.8 m. The uppermost part of the Jurkowice succession is composed of similar posits, with a domination of variegated (greenish) dolomitic shales with breccia horizons. The posits are strongly fold and thrust into particular blocks, interpreted as collapse breccias (see Narkiewicz 1991). Biostratigraphy Zdanowski (1997) collected 508 from 14 samples rived from the lower part of the succession (herein 1 to 4). The material has been revised by the author (Wójcik 2013 and in preparation), who intified the following taxa: Icriodus corniger corniger, I. c. retropressus group (including. I. c. retropressus Bultynck 1970 and I. n. sp. Narkiewicz 2013), I. werneri and I. struvei. The asselage indi- cates the lower part of the Polygnathus costatus costatus Zone (Text-fig. 10). No have been obtained from 5 and 6. A collection of 766 samples from 10-cm intervals has been measured. Average MS is 14.99×10-8m3/kg. Six mjor MS trends (CE ­ EE2), subdivid into minor fluctuations, are intified (Text-fig. 10): Trend CE is 7 m thick and ranges from unit 1 to the lower part of unit 2. Average MS is 13.92×10-8m3/kg; Trend 1 is 25 m thick and ranges from the upper part of unit 2 to the lower part of unit 3. Average MS is 15.09×10-8m3/kg; Trend 2 is 9 m thick and ranges from the upper part of unit 3 to the lower part of unit 4. Average MS is 17.1×10-8m3/kg; Trend 3 is 12 m thick and eraces the middle part of unit 4. Average MS is 17.44×10-8m3/kg; Trend EE1 is 9 m thick and ranges from the upper part of unit 4 to the lower part of unit 5. Average MS is 12.01×10-8m3/kg; Trend EE2 is 7 m thick and ranges from the upper part of unit 5 to the lower part of unit 6. Average MS is 14.01×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Wszachówka River valley The section is located in the eastern-central part of the Kielce Region: 50°469.1N, 21°729E (Pl. 6). The lowermost part of the vonian carbonate succession crops out south of the Winna quarry, along the Wszachówka River valley. An only partially exposed, ca. 50 m thick succession, watudied in 2012. The succession has been divid into 3 lithological (Textfig. 11). 60 lithological samples, 45 polished slabs and 22 thin sections were analyzed. Unit 1 (7.5 m thick) is composed of 10­30 cm thick beds of dark sandy dolomicrites with corals, algae, crinoid remains and bioturbation structures. Fossils are scattered within a marly matrix. Rare thin beds of dolomicrites with fenestral structures appear in the upper part of the unit. Unit 2 (30 m thick) is composed of thin- to mediuedd dark dolomicrites with abundant Chondrites-like bioturbation structures. 159 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Unit 3 (10 m thick) is composed of thin beds of dolomicrites. Chondrites isp. and single Planolites isp. appear on the upper surfaces together with single tentaculoids and gypidulids. Rare thin laminae of Gypidula lumachelles also occur. Biostratigraphy Two specimens from the Icriodus corniger retropressus group and 5 specimens of Icriodutruvei have been obtained from 8 studied conodont samples. They belong to two : Polygnathus costatus Zone and P. c. costatus Zone, with the boundary located probably within unit 2 (Text-fig. 11). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). Wszachów quarry The section is located in the eastern-central part of the Kielce Region: 50°4547.40N, 21°839.90E (Pl. 6). The Wszachów quarry iituated near the village of Krowianka, east of the town of Lagów and south of the Wszachówka River. The quarry exposes the lower part of vonian dolomites (below the Kowala Formation). A complete succession is exposed along the western wall of the quarry, on the 2nd and 3rd quarrying levels. A 78-m thick succession was recognized in 2012. The succession has been divid into four (Text-fig. 12 and Pl. 4). 120 lithological samples, 30 polished slabs, 16 thin sections, 25 conodont samples and 481 measurements were investigated. Unit 1 (18.5 m thick) is composed of thick beds of dolomicrites and fine-crystalline dolomites with a nodular texture. Nodules, up to a dozen or so cm in diameter, are more or less isolated and surround by thin black clay smudges. The 1.0­2.2 m thick beds are separated by 20 cm thick horizons of Chondrites-dominated bioturbation structures. A distinctive, 15 cm thick package of black shales occurs at the top. Unit 2 (9.3 m thick) is composed of thick beds of finecrystalline homogeneous dolomites with single crinoids. Unit 3 (22.5 m thick) is composed of posits characterized by a black colour and the absence of fossils and bioturbation structures. Four lithological packages in a cyclic succession can be distinguished: Wszachówka River valley costatus - eifilius Janczyce Meer . . . . .. . .. ... .. .. dolomicrites with intercalations of dolomitic shales dolomicrites with bioturbation structures horizons grained dolomicrites fenestral structures laminations bioturbation structures gypidulids tentaculoids crinoids algae Thamnopora sp. asselages Text-fig. 11. Lithological succession and in the Wszachówka River valley near Lagów Icriodus corniger retropressus Icriodutruvei SSSS SSS S S 160 KRYSTIAN WÓJCIK Wszachów quarry dolomitic shales/ claystones grained (intraclast-ooid) dolomites dolomicrites crinoid dolomites nodular dolomites bioturbation horizonts susceptibility magnetic MS major trends MS average bioturbation structures crinoids intraclasts, ooids laminations, stromatolites breccias ~15.31 EE1 Nowy Staw Meer ~6.87 28.05 m ~18.09 3 ~11.25 54.4 m Icriodutruvei S S 2 ~24.03 S Wszachów Meer S EE2 46 ~16.34 S 1 ~22.35 Text-fig. 12. Lithological succession, and in the Wszachów quarry section 161 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Package A: medium-bedd dolomicrites with flat lamination intercalated by black dolomitic shales (up to 3 m thick). Laminations are regular, flat and continuous; Package B: thick-bedd grained (intraclast) dolomites with erosional lower surfaces. They are characterized by a flaser texture expressed by alternating micritic matrix and 2­5 cm thick grained (intraclast) laminae/strips; Package C: medium-bedd laminated dolomicrites with stromatolitic domes at the tops of the beds. Irregular, wavy lamination and thin intraformational breccia horizons occur within; Package D: yellowish to greenish variegated sandy siltstones and claystones a dozen or so cm thick. The scribed packages are arranged into 8 ABCD cyclothems, the of which ranges between 2 and 4.5 m. Unit 4 (22 m thick) is composed of a cyclic succession of the following lithological packages: Package A: black dolomicrites with (occasional) flat lamination (dozen or so cm thick); Package B: light-grey grained (ooid-intraclast) dolomites with flaser lamination and erosional lower surfaces. 2­5 cm thick laminae/strips of ooid and intraclast dolosparites cut the dolomicritic matrix; Package C: grey-green dolomicrites with wavy laminations, stromatolites and intraformational breccias; Package D: greenish to yellowish dolomitic siltstones and claystones with sparry laminae/ lenses. The scribed posits are arranged into 5 ABCD cyclothems, the of which ranges between 2.4 and 3.4 m. This cyclicity disappears in the middle part of the unit, in which a thick package of laminated dolomicrites appear. Grained dolomites reappear in the upper part. Distinctive beds of white dolomitic oosparites occur at the top of the section. Biostratigraphy Only 3 specimens of Icriodutruvei have been obtained from 3 samples (25 dissolved). They indicate the Polygnathus costatus costatus Zone or younger (Textfig. 17). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). A collection of 481 samples rived from 15-cm intervals has been measured. Average MS is 14.77× 10-8m3/kg. Seven major MS fluctuations (1 ­ ) are intified (Text-fig. 14): Trend 1 is 5.2 m thick and eraces the lower part of unit 1. Average MS is 22.35×10-8m3/kg; Trend 2 is 9.6 m thick and eraces the middle part of unit 1. Average MS is 24.03×10-8m3/kg; Trend 3 is 12.1 m thick and ranges from the upper part of unit 1 to the upper part of unit 2. Average MS is 18.09×10-8m3/kg; Trend EE1 is 10 m thick and ranges from the uppermost part of unit 2 to the lower part of unit 3. Average MS is 15.31×10-8m3/kg; Trend EE2 is 10.2 m thick and eraces the middle part of unit 3. Average MS is 16.34×10-8m3/kg; Trend FE1 is 10 m thick and ranges from the upper part of unit 3 to the lower part of unit 4. Average MS is 11.25×10-8m3/kg; Trend is 9.15 m thick and eraces the middle part of unit 4. Average MS is 6.87×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Winna quarry The location of the Winna section is 50°4622.55N, 21°740.75E (Pl. 6). The Winna quarry is located between the villages of Nowy Staw, Winna and Wszachów, on the northern si of the Wszachówka River. vonian dolomites belonging to the upper part of the Unfossiliferous Crypto and Fine-crystalline Dolomites Unit of Narkiewicz and Olkowicz-Paprocka (1981) and to the lower part of the Kowala Formation (Narkiewicz 1991) are exposed in the quarry. A complete succession crops out along the western wall on the 2nd quarrying level. A 42 m thick lower part of the succession watudied in 2011. The succession has been subdivid into 5 lithological (Text-fig. 13 and Pl. 5). 70 lithological samples, 30 polished slabs, 21 thin sections, 12 conodont samples and 335 measurements were investigated. Unit 1 (15 m thick) is composed of a cyclic succession of the following lithological packages: Package A: thick-bedd light grey grained (oolite and intraclast) dolomites with flaser textures. All lower surfaces have an erosional character. In the lower part of the unit grained dolomites constitute separate beds; in the upper part, they occur as lenses within the dolomicrites. Flaser textures are expressed as grained (ooid-intraclast) intercalations within the dolomicritic matrix. Package B: green-grey dolomicrites with wavy lamination and stromatolites. The wavy lamination occurs 162 KRYSTIAN WÓJCIK within internal structures of the stromatolitic domes, and only in the external part are their shapes parallel to the domes. Numerous horizons and lenses of intraformational breccias occur within the laminites. Package C: grey and grey-green dolomicrites with flat lamination; Package D: yellow to green-yellow sandy-muscovite dolomitic siltstones and sparry laminae/strips (evaporation pseudomorphs). The scribed posits are arranged into 11 ABCD cyclothems with an average of ca. 1 m. Unit 2 (7.8 m thick) is composed of 50­100 cm thick beds of green-grey dolomicrites with subtle flat lamination. A 50 cm thick bed of rhythmically laminated dolomite, a 40 cm thick nodular dolomicrite (bioturba- tion structures) and a 30 cm thick intraformational breccia/regolith with an iron coat occur at the top of the unit. Unit 3 (11.3 m thick) is composed of 70 to 250 cm thick beds of fine- to medium-crystalline dolosparites. Numerous remnants of stromatoporoids and corals occur, concentrating in flat horizons within the beds. Unit 4 (9.6 m thick) is composed of blue-green weathering, 10­60 cm thick packages of sandy dolomitic siltstones with sparry laminae/strips intercalated by thick beds of dolosparites. Unit 5 is composed of a thick succession of thick-bedd dolosparites with stromatoporoid and coral remnants. .. . . .. . . . . . . .. . . .. . .. . Winna quarry motely sandy siltstones with evaporatic pseudomorphoses dolomitic shales/ claystones laminated dolomicrites/ stromatolites grained (intraclast-ooid) dolomites dolosparitetromatoporoid-coral dolosparites dolomicrites zebra dolomites with intraformational breccia stromatolites laminations regolithes ooids intraclasttromatoporoid rugose corals . .. . . . .. . .. . . . . . . . . . .. . .. . . .. .. . . . . . . .. . . . . . .. . . .. . .. . . .. . . . .. . . .. . . .. . . .. . . . .. . . .. . .. . . . . .. . . .. . . .. . . . . .. . . . .. . . . .. . . . . ... .. .. .. . . . .. .. . . .. . . . . . . .. . . .. . .. . . .. . . .. .. . . .. .. . . .. .. .. .. .. . . . . .. .. . . .. .. . . .. .. .. .. .. . . . . .. .. . . .. .. . . .. .. .. .. .. . Nowy Staw Meer KOWALA Formation 4 24.7 m Text-fig. 13. Lithological succession and in the Winna quarry section 163 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Biostratigraphy No were found in the 12 dissolved samples. A collection of 355 samples rived from 12.5 cm intervals has been used for MS measurements. No evint MS fluctuations are found (Text-fig. 13). The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Janczyce-1 borehole The location of the Janczyce-1 borehole is 50°4538.27N, 21°1328.96E (central-eastern part of the Kielce Region). The core is posited in the National Geological Archive in Halinów. The 1251.6 m ep Janczyce-1 borehole waituated in the Piotrów Syncline, east of the town of Lagów. A report on the complete vonian succession was published by Narkiewicz and Olkowicz-Paprocka (1983) and Narkiewicz (1991). The lithologies of the interval between 1033.0 and 1251.6 m have been scribed and measurements have been ma (Text-fig. 14). Unit 1 (pth: 1246.0­1251.6 m) is composed of light grey fine-grained quartz sandstones with flat bedding intercalated by bioturbated horizons of wavy-laminated dolomitic siltstones/heterolits. The upper boundary has been fined arbitrarily at the level where the grain-supported framework disappears, and quartz grains become suspend within the dolomitic matrix. Unit 2 (pth: 1246.0­1203.0 m; 37 m thick) is composed of a cyclic succession of the following packages: Package A: 20 to 150-cm thick beds of thamnoporoid dolomites with 30­60 cm thick intercalations of intraclast dolomites with minor contributions of coral and crinoid tritus; Package B: up to a few metres thick dolomicrites. Wavy laminations and/or nodular structures occur in the two lowermost cyclothems. Very thin intercalations of intraclast grained dolomites appear. Package C: 2 to 4 m thick grey-green dolomicrites with fenestral fabrics. The fabric is probably connected with a primary laminated texture. Small stromatolitic domes appear in the topmost part of some of the packages. The packages are arranged into 5 ABC cyclothems with es of 6 m, 9 m, 13.5 m, 3.5 m and 5 m respectively. Unit 3 (pth: 1203.0­1182.2 m; ca. 20 m thick). It is represented by interbedd packages of nodular dolomicrites and bioturbated horizons with grained laminae. The proportions of these posits varies along the succession. In the lower part (pth: 1203.0­1194.8 m), structureless or subtly laminated dolomicrites predominate. Wavy-laminated dolomicrites occur above. Single laminae of intraclast grained dolomites with single brachiopod and crinoid remains also occur. The gree of bioturbation increases in the upper part of the unit (pth: 1194.8­1182.2 m), in which a fine nodular texture is common. Chondrites-dominated structures concentrate in individual horizons. Single grained laminae, dominated by crinoid and brachiopod tritus occur in this part of the unit. Unit 4 (pth: 1182.2­1097.7 m; ca. 70 m thick). The lower part of the unit (pth: 1182.2­1155.0 m) is dominated by up to a few metres thick packages of dolomicrites with wavy lamination interbedd with up to 1 m thick bioturbation horizons (Chondrites-dominated). Rare laminae of brachiopod-crinoid remains occur, as well as monospecific brachiopod lumachelles (pth 1167.8 m). Blue-weathering nodular dolomicrites occur in the upper part of the unit (pth: 1155.0­1107.2 m). The more or less isolated nodules are emphasized by black clay laminae/strips. In some places, especially in the upper part, the nodular structure disappears or becomes more regular to form a flat lamination. The last fossils, including shelly fossils and ichnofossils, occur there. Unit 5 (pth 1107.2­1097.7 m; 10.5 m thick) is composed of dark grey dolomicrites void of fossils and bioturbation structures. Subtle flat lamination appears in the upper part of the unit. It is more evint at the top, where a 15 cm thick stromatolitic dome occurs. Unit 6 (pth: 1097.7­1023.0 m; 74 m thick) is composed of dolomicrites with subtle lamination and thick beds of intraformational breccias and grained dolomites. The grained dolomites occur in up to 1.5 m thick beds. Flaser wavy lamination, expressed as alternating micritic and intraclast-ooid grained laminae, occur within the unit. In the middle part of the succession (pth: 1097.7­1079.7 m), several packages of 1­1.5 m thick oolitic dolomites are clearly visible. A collection of 937 samples rived from 25-cm intervals has been measured. Average MS is 33.34× 10-8m3/kg. Nine major MS fluctuations/trends (BE ­ ) are intified (Text-fig. 14): 164 KRYSTIAN WÓJCIK Janczyce-1 dolomicrites dolomicrites with fenestral structures dolomicrites with wavy laminations thamnoporid dolomicriteandstones oolite/intraclats intercalations laminated dolomicrites nodular dolomicrites dolomicrites with bioturbation horizons highly bioturbated dolomicrites tectonic breccias intraformational brecciatromatolites laminations bioturbation structures ooids 1 Th pth .. .. .. .. .. .. -. .- -. .- -. .- MS major trends MS average gastropods crinoids brachiopods rugose corals Thamnopora sp. Janczyce-1 simplified SS SSSS ... . .. Nowy Staw Meer 1107.2 m S Nowy Staw Meer FE1 EE2 EE1 3 1203.0 m Wsz. . S 2 1 Janczyce Meer S S CE S BE BE4 Janczyce Meer BE3 Wszachów . 1097.7 m 1246.0 m ....................... . -. . -. . -. . -. .- - .- - .- - .- ...................... ....................... BE2 .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . -. . -. . -. . -. . -. . -. .- - .- - .- - .- - .- - .- - - . -. . - ..-.. .-..-. .-.. --..-.. . . -. . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..... BE1 Text-fig. 14. Lithological succession and in the Janczyce-1 borehole core 165 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Trend BE ranges from 1246.0 to 1180.0 m pth, average MS is 42.48×10-8m3/kg. The trend iubdivid into 4 minor MS fluctuations: BE1 ­ BE4; Trend CE ranges from 1180.0 to 1155.25 m pth, average MS is 36.37×10-8m3/kg; Trend 1 ranges from 1155.25 to 1132.5 m pth, average MS is 48.6×10-8m3/kg; Trend 2 ranges from 1132.5 to 1123.0 m pth, average MS is 24.03×10-8m3/kg; Trend 3 ranges from 1123.0 to 1109.5 m pth, average MS is 38.3×10-8m3/kg; Trend EE1 ranges from 1109.5 to 1099.5 m pth, average MS is 33.68×10-8m3/kg; Trend EE2 ranges from 1099.5 to 1091.0 m pth, average MS is 33.39×10-8m3/kg; Trend FE1 ranges from 1091.0 to 1080.0 m pth, average MS is 27.06×10-8m3/kg; Trend ranges from 1080.0 to 1069.5 m pth, average MS is 15.69×10-8m3/kg; The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Zarby 2 borehole (Tarnowska 1976, Malec 1984b, Fijalkowska-Mar and Malec 2011) The location of the Zarby 2 borehole is 50°4702.79N, 21°0247.23E (central part of the Kielce Region; Lagów Syncline). The core is posited in the National Geological Archive in Leszcze. The 1375 m ep Zarby 2 borehole cored the Lower vonian ­ succession. Tarnowska (1976) divid the clastic part of the succession into 4 lithological : Lower Siltstone Meer with Volcanites (1146.4­1218.2 m pth); Middle Sandstone Meer (1131.4­1146.4 m pth), Upper Siltstone Meer with Volcanites (1089.7­1131.4 m pth), and Upper Sandstone Meer (1080.1­1089.7 m pth). The first unit is fined as the Haliszka Formation, the remaining three belong to the Winna Formation (FijalkowskaMar and Malec 2011). The siliciclastics are overlain by sandy dolomites with remnants of corals and stromatoporoids (1075.6­1080.1 m pth), followed by the Dolomites. Malec (1984b) and Fijalkowska-Mar and Malec (2011) noticed the presence of carbonate beds with within the upper part of the Upper Siltstone Meer. proposed herein. The lithostratigraphical are fined (Text-figs 15 and 16) according to "Polskie Zasady Stratygrafii" (Polish Stratigraphical Co) fined by Racki and Narkiewicz (2006). BARANIA GÓRA DOLOMITE AND LIMESTONE FORMATION (Polish name: formacja dolomitów i wapieni z Baraniej Góry) rivation of name. From Barania Hill in the Zbrza Anticline, from where the most complete succession has been scribed. finition. The Barania Góra Formation is composed of various types of fossiliferous or bioturbated dolomites and limestones (belonging to separate ), which overlie the clastic posits of the Winna Formation and unrlie the unfossiliferous dolomites of the . Stratotype and hypostratotypes. The type area of the Barania Góra Formation is located in the south-western part of the Kielce Region ­ in the Zbrza Anticline, on the western slope of Barania Hill, along the road scarp at the southern end of the village of Zbrza (Text-figs 5 and 6 and Pl. 6). The section in Zbrza is the stratotype section of the lower part of the formation. The Dyminy-2 borehole core (at 45.0 ­ 96.0 m pth) is the stratotype of the upper part of the formation (the core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce). The hypostratotypes for the eastern part of the Kielce Region are fined in the Jurkowice section and in the Janczyce-1 borehole core. Boundaries. The Barania Góra Formation is unrlain by the Winna Formation and overlain by the . The lower boundary is fined at the base of a carbonate succession. In the western part of the Kielce Region this is the base of the Porzecze, Dbska Wola or Dyminy . It can be traced in the Zbrza (base of unit 6, Text-fig. 6), Brzeziny (base of unit 3, Text-fig. 7), (base of unit 3, Text-fig. 8) and Skrzetle (see scription in Malec 1993) sections, and in the Dyminy-2 (137.7 m pth, see Tarnowska 1987), Dbrowa D5 (71.5 m pth, see Tarnowska and Malec 1987) and (19.2 m pth, see Kowalczewski 1979 and Fijalkowska-Mar and Malec 2011) borehole cores. In the eastern part, it can be traced in the Jurkowice section (base of unit 1, Text-fig. 10) and LITHOSTRATIGRAPHY Based on the geological documentation presented, a formal lithostratigraphical scheme for the upper Emsian and lower of the Kielce Region of the HCM is 166 KRYSTIAN WÓJCIK ? ? Brzeziny E MIDDLE VONIAN costatus ? ? Jurkowice ~ ~ .. ..~ ~ . .. .~ . .. .~ . .. .~ . . e ~ ~ ~ ~ b la M Porzecz Dbska Wo ~ . .. ~ . .. ~ . .. ~ .. ..~ .. ..~ . .. ~ . .. ~ . . ~ ~ . . ~ . . ~ . . ~ . ~ .. ~ . . ~ .~ . .~ . ..~ . ~ . . ~ . .. ~ . .. ~ . .. ~ . .. ~ . .. ~ . .. ~ . .. ~ .WINNA. Formation ~ . .. ~ . .. . . . ~ . . ~ . ~ . ~ . ~ . ~ . ~ . ~ . ~ . ~ .. ~~ .1. ~ . ~~ . . ~ . ~ . . ~ . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . . . ~ . . ~ . . ~ . . ~ . . ~. . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~. . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~ ~ ~ ~ ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. 6 Dbrowa inated dolomites and sandy dolomites arranged (occasionally) into cyclic successions (); fossiliferous limestones, marls, marly shales with brachiopod lumachelle intercalations (Dbrowa Meer); thin-bedd dolomites with horizons of bioturbation structures (Brzeziny Meer); coral-bearing dolomicrites, laminated dolomicrites and fenestral dolomicrites arranged into cyclic successions (Janczyce Meer); and thick-bedd nodular dolomites and crinoidal dolomites with horizons of bioturbation structures (). Origin. The formation represents a shallow-marine carbonate-clastic sedimentation during the earliest stage of the vonian transgression, before constitution of a carbonate platform. The posits belonging to particular originated in different sedimentary environments; from lagoonal, through stromatoporoid-coral shallows to open-marine areas (occasionally below storm wave base) on a distally-steepening ramp (Wójcik 2013 and in preparation). Age. The formation is early in age. The conodont material collected indicates the interval between the Polygnathus costatus Zone and the lower part of the P. c. costatus Zone (Wójcik 2013 and in preparation), albeit a latest Emsian age is postulated by FijalkowskaMar and Malec (2011) for the lowermost part of the formation (Porzecze Meer). The age is confirmed by the Janczyce M in the Janczyce-1 borehole core (1246.0 m pth, Textfig. 14). The upper boundary is fined as the last occurrence of bioturbated or fossiliferous dolomite. In the western part of the region it can be traced in the Dyminy-2 borehole core (45.0 m pth, see Tarnowska 1987). In the eastern part, it is exposed in the Jurkowice (base of the unit 5, Text-fig. 10) and Wszachów (base of the unit 3, Text-fig. 3) sections, and in the Janczyce1 borehole core (1107.2 m pth). Occurrence and . The Barania Góra Formation is limited to the Kielce Region of the Holy Cross Mountains. The formation is divid into six , but a consirable lithological variety occurs between the eastern and western parts of the region. Two ­ the Janczyce and Jurkowice , with a coined of ca. 130 m, are limited to the eastern part. Four ­ the Porzecze, Dbska Wola, Dbrowa and Brzeziny , with a coined of up to ca. 70 m, are limited to the western part. Additionally, in the western part of the Kielce Region, a lateral lithological variability occurs: the Dbrowa Meer is limited to the north-western and south-western part of the region and is absent in the central-western part. . The Barania Góra Formation inclus pyritebearing and siritic claystones (Porzecze Meer); coral-bearing dolomites, micritic dolomites, wavy-lam- L. VONIAN EMSIAN patulus Text-fig. 15. Lithostratigraphical scheme around the upper Emsian and in the Kielce Region of the Holy Cross Mts. (longitudinal organization) 167 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. LOWER VONIAN MIDDLE VONIAN EMSIAN patulus costatus ? Acinosporites apiculatus­Grandispora protea [AP] ? Grandispora Grandispora protea [Pro] ? velata [Vel] Kowala 1 Dbrowa D-5 Szydlówek Skrzetle Dyminy-2 Brzeziny D . .. . ~ . . . ~ ~ .~ . P . ~~ ~ .. ~ . . DW . .. .~ .. . .. . ~ .. . ~ ~. ~ .. . . ~ . ~.. . .~ . . . .. ~.. .~.. .~. .~. . . ~.. . ~. ~ ~ ~ ~ .. ~ . . ~ . . ~ .~. .~ ~. ~ . . ~ . ~ . ~ . .~ . ~ . . ~ . . ~ . . ~ . ~ .. ~ . ~ .. ~ .. ~ . ~ .. ~ ~ ....~ ....~ .... ~ . . ~ . . ~. ~. ~. ~. . . .~. . . .~. . . .~. . . .~. ..~. . . .~. . .~. . .~. ~ .~. . . ~ ~ ~ ~ WINNA Formation . ~. ~. ~ ~ . ~ . . ~ . . ~ . . ~ .~~ . ~~ .. ~~ 1 .~~ .. . ~ .. ~ ~ . . ~ .. . ~ .. . ~ .. . . ~ . . . . ~. ~. . ~. ~. . ~. ~. . ~ . ~ ~ ~ ~ ~ . . ~. . ~. . . . ~ . . ~ . . ~ . . ~ . .~ . . ~ . . ~ . . ~ . . ~ . . Chciny Zbrza Brzeziny ? ? Winna Nowy Staw 1 MIDDLE VONIAN Wszachów Wszachów costatus Jurkowice Wszachówka River Janczyce-1 Janczyce 1 . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~. . ~. . ~. . ~ . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~ ~ ~ ~ ~ ~ ~ ~ .. . ~. .. . ~. .. . ~ .. . ~. .. . ~ .. . ~ . . ~ . . ~ . . ~ . . .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ . ~ ~ ~ . ~ ~. ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . WINNA Formation .. .. .. . . ~ ~ ~ ~ ~ ~ ~1 ~ ~ . . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~~. .. .~~ . .. .~~. .. .~~. .. .~~ .. .~~. .. .~~ . .. .~~. .. .~~. .. ~ . .. .~~. .. .~~ . .. .~~. .. .~~. .. .~~ .. .~~ .. . ~ .. .~~ . . . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . . . ~ . . ~ . . ~ . . ~ . . ~. . ~. . . Zarby 2 L. V. EMSIAN patulus Jurkowice Text-fig. 16. Lithostratigraphical schemes around the upper Emsian and in the Kielce Region of the Holy Cross Mts. (latitudinal organization) supplemented by palynostratigraphical data of Filipiak (2011). A ­ western part of the region, B ­ eastern part of the region. P ­ Porzecze Meer, DW ­ , D ­ Dbrowa Meer 168 KRYSTIAN WÓJCIK palynostratigraphical data of Fijalkowska-Mar and Malec (2011) and Filipiak (2011). Porzecze Claystone Meer (Polish name: ogniwo ilowców z Porzecza) rivation of name. From the borehole core, in which a complete succession was available. Earlier names. The meer was earlier distinguished as: the Ore-bearing Claystones and Siltstones Meer (Tarnowska and Malec 1987, Fijalkowska-Mar and Malec 2011), the Ore-bearing Claystones (Malec 1986, 1993), the Pyrite-bearing Claystones from Szydlówek (Malec and Stuncki 1988) and the Pyrite-bearing and Siritic Claystone Meer (Fijalkowska-Mar and Malec 2011). finition. The Porzecze Meer overlies the clastics of the Winna Formation and unrlies the succession of dolomites or limestones in the northern and north-western parts of the Kielce Region. The meer is fined as a package of brown, black and yellowish pyrite-bearing claystones and siltstones with sirite concretions. Stratotype and hypostratotypes. The town of Kielce is the type area of the Porzecze Meer. The stratotypes of the lower and upper parts of the meer are located in the Skrzetle and Szydlówek sections respectively. Boundaries. The Porzecze Meer is unrlain by the Winna Formation and overlain by the or the Brzeziny Meer (if the Dbrowa Meer is absent). The lower boundary is fined as the base of the pyrite-bearing or limonite-bearing claystone package that unrlies the carbonate succession. It can be traced in the Skrzetle section and in the Porzecze IG5A borehole core at 12.9 m pth. The upper boundary is fined as the base of the first continuous bed of dolomite or limestone. It is exposed in the Szydlówek section and in the (19.2 m pth) and Dbrowa D5 (at 71.5 m pth) borehole cores. Occurrence and . The Porzecze Meer occurs in several sections in the northern and north-western part of the Kielce Region (Text-fig. 5). The meer occurs in the Szydlówek (30 m thick; see scription in Malec and Stuncki 1988) and Skrzetle (5.7 m thick; see scription in Malec 1993 and 2001) sections, as well as in the (5.4 m thick; see scription in Kowalczewski 1979, Fijalkowska-Mar and Malec 2011; Text-fig. 9) and Dbrowa D5 (71.5 ­ 103.5 m pth; see scription in Tarnowska and Malec 1987) borehole cores. The presence of similar posits was also noticed in the Stara Góra IG-1 and Wola Zamkowa 2 borehole cores (Stuncka 1983), as well as in old shafts near the villages of Daleszyce, Górno, Bakowice and Piotrów. The meer disappears in the central and southern parts of the Kielce Region. . The Porzecze Meer is composed of brown to black structureless or wavy-laminated claystones with frooidal pyrite, yellowish structureless claystones with sirite concretions, and dolomitic claystones and siltstones (Tarnowska and Malec 1987, Malec and Stuncki 1988, Malec 1993). Fossils. The numerous benthic agglutinated foraminifers represent an autochthonous asselage. Rare crinoids, remnants of bryozoans, brachiopods (including Chimaerothyris dorowiensis), tentaculoids and occur in the upper part of the unit, probably of allochthonous origin (Tarnowska and Malec 1987, Malec 1987, Malec and Stuncki 1988, Malec 1993). . Not measured. Origin. The Porzecze Meer representhallow-marine lagoonal sedimentation, with open marine influences in the upper part of the unit (Wójcik 2013 and in preparation). Age. The asselage of collected by Malec (1993) and discussed in Fijalkowska-Mar and Malec (2011) indicates the interval between the uppermost Emsian (Polygnathus costatus patulus conodont Zone) and lower (Polygnathus costatus conodont Zone). Wójcik (2013 and in preparation) suggested an early age only. Dbska Wola Dolomite Meer (Polish name: ogniwo dolomitów z Dbskiej Woli) rivation of name. From the village of Dbska Wola, where the posits were intified for the first time (Filonowicz 1973). Earlier names. The meer was earlier distinguished as: the Dolomite Meer in Fijalkowska-Mar and Malec (2011) and the Dolomitic Unit below the Dbrowa Horizon in the Dyminy-2 borehole core in Tarnowska (1987). finition. The is composed of dolomites (dolomicrites and fine-crystalline dolosparites with occasional abundant corals), which unrlie the Dbrowa Meer. 169 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Stratotype and hypostratotypes. The type area is located in the Zbrza Anticline, on the western slope of the Barania Hill, along the road scarp at the southern end of the village of Zbrza. The Zbrza section is the stratotype section of the meer (Text-figs 5, 6 and Pls 1, 6). The hypostratotype is established in the Dyminy-2 borehole core between 137.7 and 110.0 m pth. Boundaries. The is unrlain by the Winna Formation or the Porzecze Meer and overlain by the Dbrowa Meer. The lower boundary is fined as the base of a dolomitic succession ­ the base of brown dolomitic claystones or dolomicrites. It was established in the core at the base of the first dolomite bed (19.2 m pth), in the Brzeziny section at the base of unit 3 and in the Zbrza section at the base of unit 6. The upper boundary is fined as the base of limestones, marls or marly shales of the Dbrowa Meer. It was established at the top of unit 10 in the Zbrza section, at the top of unit 5 in the Brzeziny section and at the top of the last dolomite bed in the core (39.5 m pth). Occurrence and . The occurs in the south-western part of the Kielce Region (Text-fig. 5, Pl. 6). It can be traced along the Chciny and Dyminy Anticlines. The meer occurs in the Zbrza ( from 6 to 10, 16 m thick; Text-fig. 6 and Pls 1, 6) and Brzeziny ( from 3 to 5, 22.5 m thick; Textfig. 7 and Pls 2, 6) sections, as well as in the Dyminy2 (between 137.7 and 110.0 m pth, 28 m thick; see scription in Tarnowska 1987) and (between 19.2 and 39.5 m pth, 15.6 m thick; see scription in Kowalczewski 1979 and FijalkowskaMar and Malec 2011; Text-fig. 9) borehole cores. The presence of dolomites unrlying the Dbrowa Meer has also been noted near the villages of Szczecno and Osiny. . The lowermost part of the unit is composed of brown dolomitic claystones and dolomicrites. In the middle part, the unit is composed of Thamnopora dolomicrites, fine-crystalline dolosparites with corals, marly dolomicrites with wavy lamination and dolomicrites, arranged in 5 to 6 cyclothems. The upper part of the meer is composed of stromatoporoid-coral biostromal dolomites. In the Brzeziny section, corals are absent and the cyclothems are not recognized, albeit cyclicity is visible on the MS curve. . The meer is generally characterized by high MS values, over 40×10-8 m3/kg in the lower part, creasing towards the top. The main asymmetric creasing trend A corresponds to the meer. Minor asymmetric (creasing) MS fluctuations correspond well to particular lithological cyclothems. The lower part of trend B begins in the upper part of the meer. Origin. The representhallowmarine, temporary cyclic carbonate sedimentation within lagoonal environments with isolated stromatoporoid-coral shallows and swells (Wójcik 2013 and in preparation). Age. Filipiak (2011) proved the latest Emsian­early age of the meer (protea palynostratigraphic Zone) in the Dyminy-2 borehole core and in the Zbrza section. Dbrowa Limestone Meer (Polish name: ogniwo wapieni z Dbrowy) rivation of name. From the village of Dbrowa (northern part of Kielce), in which the posits were recognized for the first time (Pusch 1833, Gürich 1896). Earlier names. The meer was earlier distinguished as: the Dbrowa Horizon in Gürich (1896) and Filonowicz (1973), the complex VIII in Pajchlowa (1957), the Kielce Limestone Unit in Tarnowska (1987), the Grzegorzowice Limestone Meer in Malec (2002) and the Dbrowa Limestone Meer in Tarnowska and Malec (1987), Malec (2005), Fijalkowska-Mar and Malec (2011), and Filipiak (2011). finition. The Dbrowa Meer was fined by Malec (2005) in the Grzegorzowice-Skaly section in the Lysogóry Region of the Holy Cross Mountains. A refined finition of the meer is proposed herein. The unit is composed of grey to greenish micritic limestones and fossiliferous grained and flaser limestones, marls and marly shales with a subordinate contribution of dolomites in separate internal packages. The presence of Chimaerothyris dorowiensis is an auxiliary criterion for distinguishing the meer. Stratotype and hypostratotypes. Malec (2005) established the Grzegorzowice-Skaly section in the Lysogóry Region as the stratotype section of the Dbrowa Meer. The Zbrza section is proposed herein as the hypostratotype section for the Kielce Region (Text-figs 5, 6 and Pls 1, 6). Boundaries. The Dbrowa Meer is unrlain by the Dbska Wola or the Porzecze and overlain by 170 KRYSTIAN WÓJCIK the Brzeziny Meer. The boundaries of the unit surround the lithosome of limestones, marls or marly shales within a dolomitic background. The lower boundary is fined as the base of the first limestone or marl bed or at the base of the first marly shales package. It can be traced in the borehole core at the base of the first limestone layer (39.5 m pth), in the Brzeziny section at the base of unit 6 and in the Zbrza section at the base of unit 11. The upper boundary is fined as the top of the last limestone bed. It can be traced at the top of unit 7 in the Brzeziny section. Occurrence and . The Dbrowa Meer occurs in both the Lysogóry and Kielce regions of the Holy Cross Mountains, albeit belonging to two different . In the Kielce Region, the meer is limited to the western part of the area (Text-fig. 5). The of the unit increases to the north-west and to the southwest. The unit is absent along the Dyminy Anticline in the western-central part of the area. The Dbrowa Meer occurs in the Zbrza ( 11 to 16, 28 m thick at least; Text-fig. 6 and Pls 1, 6) and Brzeziny ( 6 and , ca. 10 m thick; Text-fig. 7 and Pls 2, 6) sections, as well as in the (from 39.5 m pth to the end of the core, 30 m thick at least; Text-fig. 9), Dyminy-2 (96.0­109.0 m pth, 13 m thick; see scription in Tarnowska 1987) and Dbrowa D5 (66.0­71.5 m pth; see scription in Tarnowska and Malec 1987) borehole cores. The occurrence of limestones with Chimaerothyris dorowiensis was also noticed near the villages of Szczecno and Osiny. In the Lysogóry Region, the unit occurs in the Grzegorzowice-Skaly section (35 m thick; see scription in Malec 2005) and in the Kowalkowice 1 borehole core (111.2­92.5 m pth, ca. 10 m thick; see scription in Malec 2005). . The Dbrowa Meer is composed of micritic, grained and flaser limestones alternating with marls and marly shales. Marly intervals concentrate in the lower part of the unit in the Brzeziny and Zbrza sections. Numerous brachiopod lumachelles occur in these intervals. Grained and flaser limestones dominate in the lower and middle parts of the unit and rece in the upper part, in which micritic limestones predominate. Thin packages of dolomites occur within the unit in the Grzegorzowice-Skaly and Zbrza sections. Fossils. Shelly-fossils concentrate within grained beds and laminae/strips. Chimaerothyris dorowiensis, Athyris concentrica and Chonetes angustestriata are the most abundant brachiopods. Numerous tentaculoids, crinoids, gastropods, corals, and rare trilobites, holothurids, , microconchids, scolecodonts, bryozoans, hereloids, algae, ostracods and molluscs are present. Chondrites isp. and Skolithos isp. are the most numerous ichnofossils. . The Dbrowa Meer has generally high MS values in the lower part of the unit (from 35 to 40 ×10-8 m3/kg), creasing towards its top. Higher MS values at the base of the unit result from the greater content of marls and marly shales. The major asymmetric trend B generally corresponds to the meer and can be traced in all sections. Minor 3 to 6 MS fluctuations within trend B are also distinguishable. The major symmetric C and D trends are distinguished in the upper part of the unit in the Zbrza section. Origin. The Dbrowa Meer represents open-marine carbonate-clastic sediments posited on the middle and outer ramp, occasionally below the storm wave base (Wójcik 2013 and in preparation). Age. The stratigraphical range of the Dbrowa Meer spans from the upper part of the Polygnathus costatus conodont Zone to the lower part of the Polygnathus costatus costatus conodont Zone, within the lower . The age is proved by numerous , collected and scribed by Wójcik (2013 and in preparation). Brzeziny Dolomite Meer (Polish name: ogniwo dolomitów z Brzezin) rivation of name. From the Brzeziny section, in which a complete succession is available. finition. The Brzeziny Meer is a dolomitic unit unrlying the in the western part of the Kielce Region. As opposed to the , the meer contains horizons of bioturbation structures and thin grained intercalations. Dolomitic limestones occur subordinately at its base. Stratotype and hypostratotypes. The Brzeziny section is the stratotype section of the lower part of the unit (Text-figs 5, 7 and Pls 2, 6). The Dyminy-2 borehole core (45.0 and 96.0 m pth) is the stratotype section of the upper part of the unit (the core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. Boundaries. The Brzeziny Meer is unrlain by the Winna Formation or by the Porzecze and Dbrowa , and is overlain by the . 171 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. The lower boundary is fined as the base of the first dolomite bed above the Dbrowa Meer or above the Winna Formation or the Porzecze Meer, if the Dbrowa Meer is absent. The boundary can be traced in the Brzeziny section at the base of unit 8, in the section at the base of unit 3, in the Skrzetle and Szydlówek sections above the Porzecze Meer, as well as in the Dyminy-2 (at 96.0 m pth) and Dbrowa D5 (at 66.0 m pth) borehole cores. The upper boundary is fined at the top of the last bed with bioturbation structures. It can be traced in the Brzeziny and Zbrza sections, as well as in the Dyminy-2 borehole core (at 45.0 m pth). Occurrence and . The meer occurs in the western part of the Kielce Region in the Brzeziny (unit 8, 15 m thick at least; Text-fig. 7 and Pls 2, 6) and ( 3 and 4, 26 m thick at least; Text-fig. 8 and Pl. 6) sections, as well as in the Dyminy-2 (45.0­96.0 m pth, ca. 50 m thick; see scription in Tarnowska 1987) and Dbrowa D5 (5.2­66.0 m pth; see scription in Tarnowska and Malec 1987) borehole cores. posits includ in the meer were also scribed from the Skrzetle (Malec 1993, 2001), Szydlówek (Malec and Stuncki 1988) and Chciny (Glazek et al. 1981) sections. The Brzeziny Meer also occurs near the villages of Zbrza, Szczecno and Osiny. . The Brzeziny Meer is composed of thinbedd reddish structureless dolomicrites with horizons of bioturbation structures and grained laminae/ strips, intercalated with brown dolomitic claystones. Small stromatolites and fenestral fabrics appear sporadically. A package of dolomitic limestones occur at the base of the unit in the section. Fossils. Allochthonouhelly fossils occur within the grained intercalations. Single crinoids, tentaculoid remains, ostracods and are present. Paraautochthonous gypidulid asselages appear on some of the surfaces. Chondrites isp. predominate among the ichnofossils. . The meer has generally low MS values; ca. 22×10-8 m3/kg in Brzeziny section and 18×10-8 m3/kg in the lower part to 8 ×10-8 m3/kg in the upper part of the section. The major trends D correspond to the meer in the Brzeziny section, the major trends C, D and E occur in the section. Origin. The Brzeziny Meer representhallow-marine carbonates posited on the outer si of a distally steepened ramp (Wójcik 2013 and in preparation). Age. The meer is in age, not olr than the Polygnathus costatus conodont Zone in the Skrzetle and Szydlówek sections (Fijalkowska-Mar and Malec 2011) or than the Polygnathus costatus costatus conodont Zone in the Zbrza, Brzeziny and sections. The upper boundary is not dated, and probably runs within the Polygnathus costatus costatus conodont Zone. The age is postulated basing on collected and scribed by Wójcik (2013 and in preparation). Janczyce dolomite Meer (Polish name: ogniwo dolomitów z Janczyc) rivation of name. From the Janczyce-1 borehole core, in which a complete succession is available. finition. The Janczyce Meer occurs at the base of the vonian carbonate succession in the central-eastern part of the Kielce Region and is composed of a cyclic succession of as follows (from base to top): grained dolomicrites intercalated with thamnoporaboundstones, structureless dolomicrites, dolomicrites with wavy lamination and dark dolomicrites with fenestral structures. Stratotype. The interval of the Janczyce-1 borehole core between 1203 m and 1246 m pth is the stratotype section of the meer (Text-figs 5, 14). The core is posited in the National Geological Archive in Halinów. Boundaries. The Janczyce Meer is unrlain by the Winna Formation and overlain by the . The lower boundary is fined as the first layer of dolomites above the clastic succession and can be traced in the Janczyce-1 core at 1246.0 m pth. The upper boundary is fined as the top of the cyclic succession and can be traced in the same core at 1203.0 m pth. Occurrence and . The Janczyce Meer occurs in the eastern part of the Kielce Region, in the Janczyce-1 (unit 2, 37 m thick; Text-fig. 14) borehole core, as well as in the valley of the River Wszachówka (unit 1; Text-fig. 11 and Pl. 6). The presence of similar posits is also postulated in the Zarby 2 borehole core, at the base of the carbonate succession (see scription in Tarnowska 1976). . The meer is composed of grained (crinoid-intraclast) dolomicrites intercalated with Thamnopora-boundstones (a little sandy at the base of the unit), structureless dolomicrites, dolomicrites with wavy lamination and dark dolomicrites with fenestral 172 KRYSTIAN WÓJCIK structures. In the Janczyce-1 core, the strata are arranged into 5 cyclothems. Similar posits are partially exposed in the valley of the River Wszachówka, in which sandy dolomicrites, dolomites with wavy laminations and bioturbated dolomicrites with algae and coral remains occur. . The meer has medium MS values, with average around 42×10-8 m3/kg. The major BE trend has been distinguished within the unit. It is divid into BE1, BE2, BE3 and BE4 subtrends, which correlate well with the lithological cyclothems. Origin. The Janczyce Meer representhallow-marine cyclic carbonates posited in lagoonal environments (Wójcik 2013 and in preparation). Age. The meer is in age, and ranges from the Polygnathus costatus conodont Zone to the lower part of the Polygnathus costatus costatus conodont Zone according to conodont material collected and scribed by Wójcik (2013and in preparation). Jurkowice dolomite Meer (Polish name: ogniwo dolomitów z Jurkowic) rivation of name. After the village of Jurkowice, in which a quarry is located. Earlier names. The Fossiliferous and Bioturbated Dolomicrites and Dolosparites Unit in Narkiewicz et al. (1981), Narkiewicz and Olkowicz-Paprocka (1983) and Zdanowski (1997). finition. The is a dolomitic unit unrlying the in the eastern part of the Kielce Region. As opposed to the , nodular texture, thin-grained fossiliferous intercalations and horizons of intense Chondrites-like bioturbations occur in the . The unit can be easily distinguished from the Brzeziny Meer by the presence of nodular texture, greater of particular beds, and, occasionally also by blueish weathering. Stratotype and hypostratotypes. The Jurkowice quarry section is proposed as the stratotype section of the (Text-figs 5, 10 and Pls 3, 6). The Janczyce-1 borehole core between 1203.0 and 1104.0 m pth is proposed as the hypostratotype (Text-figs 5 and 14). Boundaries. The is unrlain by the Janczyce Meer of the Winna Formation and overlain by the . The lower boundary is fined in the Janczyce-1 borehole core at the pth of 1203.0 m, at the top of the last cyclothem, as well as in the Jurkowice quarry at the base of unit 1, above the sandstones belonging to the Winna Formation. The upper boundary is fined as the top of the last layer of crinoid dolomite or nodular dolomite in the succession. It is tected in the Janczyce-1 core at 1104.0 m pth, at the level where nodular texture and shelly fossils disappear, in the Jurkowice section at the top of unit 4 above the last crinoid dolomite layer, and in the Wszachów section at the top of unit 2 above the last nodular dolomite layer. Above the upper boundary, the horizons of bioturbation structures and shelly fossils disappear completely in the succession. Occurrence and . The occurs in the eastern part of the Kielce Region, in the Jurkowice ( 1 to 4, 55 m thick; Text-fig. 10 and Pls 3, 6) and Wszachów ( 1 and 2, 28 m thick at least; Text-fig. 12 and Pls 4, 6) sections, in the Wszachówka River valley ( 2 and 3; Text-fig. 11 and Pl. 6), as well as in the Janczyce-1 borehole core (1203.0­1104.0 m pth, ca. 90 thick; Text-fig. 14). . The meer is composed of medium-bedd dolomicrites with thin-grained fossiliferous intercalations, thick-bedd nodular dolomicrites and finecrystalline dolosparites, thick-bedd dolomicrites with crinoids, and thick-bedd crinoidal dolomites. The strata are intercalated by horizons of Chondrites-dominated bioturbation structures. Fossils. Numerous lingulids, molluscs, conulariids and plant remains occur within the grained intercalations/laminae in the lowermost part of the meer. Asselages of gypidulids, tentaculoids, crinoids, scolecodonts, and bryozoans remains occur in other separate laminae/strips. Gypidulids and tentaculoids build the single and very thin lumachelle horizons. Chondrites isp. with subordinate contribution of Planolites isp. predominate among the ichnofossils. . The meer has medium MS values, with an average from 15×10-8 m3/kg in Jurkowice section, through 20×10-8 m3/kg in the Wszachów section, up to 38×10-8 m3/kg in the Janczyce-1 borehole core. The major MS trends BE, CE, 1, 2 and 3 are distinguished within the unit. 173 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Origin. The representhallowing carbonate sedimentation on the middle part of the ramp and around crinoidal meadows (Wójcik 2013 and in preparation). Age. The Meer is in age and belongs to the lower part of the Polygnathus costatus costatus conodont Zone according to the conodont material collected by Zdanowski (1997) and revised and scribed by Wójcik (2013 and in preparation). WOJCIECHOWICE DOLOMITE FORMATION (Narkiewicz and Narkiewicz 2010) Wszachów Dolomite Meer (Polish name: ogniwo dolomitów z Wszachowa) rivation of name. From the village of Wszachów, in which a quarry is located. finition. The Wszachów Meer is a characteristic unit of dark unfossiliferous dolomites with a horizon of stromatolitic domes. Stratotype and hypostratotypes. The Wszachów section along the western wall of the quarry is the stratotype section of the Wszachów Meer (Text-figs 5, 12 and Pls 4, 6). The hypostratotype is established in the Jurkowice section along the eastern wall of the quarry (Text-figs. 5 and 10 and Pls 3, 6). Boundaries. The Wszachów Meer is unrlain by the Barania Góra Formation and overlain by the Nowy Staw Meer. The lower boundary is fined at the top of the last bed of nodular, bioturbated or crinoidal dolomites of the unrlying Barania Góra Formation. The boundary can be traced in the Jurkowice section at the base of unit 5, in the Wszachów section at the base of unit 3, and in the Janczyce-1 borehole core at 1104.0 m pth. The upper boundary is fined as the base of the first thick layer of intraclast-oolite dolomites, ca. 1 m above a characteristic horizon with stromatolitic domes. The boundary can be traced in the Jurkowice section at the base of unit 6, in the Wszachów section at the base of unit 4, and in the Janczyce-1 borehole core at 1097.0 m pth. Occurrence and . The meer is recognized in the eastern part of the Kielce Region, in the Wszachów (unit 3, 10 m thick; Text-fig. 12 and Pls 4, 5) and Jurkowice (unit 5, 10 m thick; Text-fig. 10 and Pls 3, 4) sections, as well as in the Janczyce-1 bore- hole core (1104­1097 m pth, ca. 7 m thick; Text-fig. 14). Similar posits were scribed also by Tarnowska in the Dyminy-2 borehole core (15.0­45.0 m pth). . The meer is composed of dark dolomicrites, dolomicrites with flat lamination, dolomicrites with wavy lamination, stromatolite horizons and variegated siltstones, organized in cyclothems. Fossils. Absence of any shelly fossils and ichnofossils. . The meer has generally low MS values, with an average from 13×10-8 m3/kg in the Jurkowice section, through 15.5×10-8 m3/kg in the Wszachów section, up to 33×10-8 m3/kg in the Janczyce1 borehole core. The major MS trends EE1 and EE2 are distinguished within the unit. Origin. The Wszachów Meer representhallowmarine carbonate sedimentation within lagoonal environments with a predominance of subtidal conditions (Wójcik 2013 and in preparation). Age. The meer is or younger in age, however, not olr than the lower part of the Polygnathus costatus costatus conodont Zone, as can be ducted from rived from the unrlying (Wójcik 2013 and in preparation). Nowy Staw Dolomite Meer (Polish name: ogniwo dolomitów z Nowego Stawu) rivation of name. From the village of Nowy Staw, in which the Winna quarry is located. finition. The Nowy Staw Meer is a distinctive unit comprising fine- to medium grained oolitic-intraclast dolomites intercalated by various kinds of dolomites and arranged into a cyclic succession. Stratotype and hypostratotypes. The vicinity of the town of Lagów is the type area of the meer. The Wszachów section is proposed as the stratotype of the lower part of the meer (Text-figs 5, 12 and Pls 4, 6). The Winna section is proposed as the stratotype of the upper part of the meer (Text-figs 5, 13 and Pls 5, 6). The Janczyce-1 borehole core interval between 1097.0 m and 1023.0 m pth is proposed as the hypostratotype section (Text-figs 5, 14). Boundaries. The Nowy Staw Meer is unrlain by the Wszachów Meer and overlain by the Kowala 174 KRYSTIAN WÓJCIK Formation. The lower boundary is fined as the base of the first thick bed of grained oolite-intraclast dolomites, ca. 1 m above a distinctive horizon of stromatolitic domes. The boundary can be traced in the Wszachów and Jurkowice sections at the base of 4 and 6 respectively, as well as in the Janczyce-1 borehole core at 1097.0 m pth. The upper boundary is fined as the base of the first stromatoporoid-coral dolomite bed. It is established in the Winna section, at the base of unit 3, where it is emphasized by a breccia/conglomerate layer, as well as in the Janczyce-1 borehole core at 1023.0 m pth. Occurrence and . The Meer is recognized in the eastern part of the Kielce Region, in the Janczyce-1 borehole core (pth interval between 1097 m and 1023 m, ca. 70 m thick; Text-fig. 14), as well as in the Jurkowice (unit 6; Text-fig. 10 and Pls 3, 6), Wszachów (unit 4; Text-fig. 12 and Pls 4, 6) and Winna ( 1 and 2; Text-fig. 13 and Pls 5, 6) sections. Similar posits have been scribed in the Kowala 1 borehole core by Romanek and Rup (1990, see also Narkiewicz 1991) between 882.7 and 846.8 m pth. . The Nowy Staw Meer comprises: dark grey dolomicrites with flat lamination, grained intraclast-oolitic dolomites, dolomicrites with wavy lamination, horizons of stromatolitic domes, greenish flat laminated dolomicrites, intraformational breccia horizons, and variegated siltstones and claystones with anhydrite pseudomorphs, arranged in several ca. 1.5m thick cyclothemes. The nuer of cyclothems differs between the sections. . The meer has generally low MS values, up to 10×10-8 m3/kg in the Winna and Wszachów sections, and somewhat higher, with an average of ca. 20×10-8 m3/kg, in the Janczyce-1 borehole core. The major MS trends EE2, FE1 and are distinguished in the lower part of the unit. There is a lack of any relation between the MS trends and the lithological cyclothems. Origin. The meer representhallow-marine carbonate cyclic sedimentation within lagoonal environments with a predominance of inter- and supratidal conditions (Wójcik 2013 and in preparation). Age. The Nowy Staw Meer is or younger in age, and not olr than the lower part of the Polygnathus costatus costatus Zone (Wójcik 2013 and in preparation). DISCUSSION A tailed lithological scription of the succession and recognition of actual geographical and stratigraphical organization and the extent of particular lithological constitute basic requirements in reconstructing the three-dimensional architecture of any stratigraphical interval, and form the basis of subsequent regional palaeogeographical reconstructions. Such studies were missing for the uppermost Emsian and in the Kielce Region, an interval critical for unrstanding the onset and early of the vonian transgression over the area of the present day Holy Cross Mountains. This paper fulfils the gap. The investigations reported herein, carried out in nine sections and supplemented by published data, representing both the eastern and western parts of the Kielce Region, have revealed great lateral and vertical lithological variability around the Emsian­ boundary interval in the area. One new formation ­ the Barania Góra Formation ­ has been fined and divid into six . Additionally, two new have been distinguished within the overlying (Text-figs 15, 16). Although a strong lithological variability of the studied interval was reflected in the reports of former researches (Text-fig. 4), the geographical/stratigraphical distribution and characteristics of particular lithostratigraphical unit was not, so far, fully unrstood. Moreover, their position within a transgressive vonian succession was uncertain. One of the main issues, which need serious consiration before constructing a complete lithostratigraphical scheme, concerned the geographical continuity of particular distinguished in the Kielce Region; to what extent the apparently similar lithosomes are really the same in the eastern and western parts of the region (Text-figs 15, 16). The Porzecze Formation predominates in the north-western part of the Kielce Region; however, similar posits occur also in its north-central and even north-eastern parts (Tarnowska 1976; Malec 1986; Fijalkowska-Mar and Malec 2011). Three : the Dbska Wola, Dbrowa and Brzeziny are limited to the western part of the Kielce Region. Their occurrence does not cross the Daleszyce tectonic lineament (see Konon 2006), and they are absent in the Bardo Syncline, Jurkowice-Budy section, and in the vicinity of Lagów. The correspond to the Janczyce and Jurkowice distinguished in the eastern part of the region. The is the first unit that occurs broadly in the whole area of the Kielce Region (compare Narkiewicz 1991 and Narkiewicz and Narkiewicz 2010; sea also Text-figs 15, 16). 175 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Among the many differences in the uppermost Emsian and succession between the eastern and western parts of the Kielce Region, one more has to be emphasized ­ the of the succession. Although the difference is most accentuated within the Winna Formation, in which the varies from 2 m in the western part to 200 m in the eastern part (compare Glazek et al. 1981; Romanek and Rup 1990 with Tarnowska 1976), it is also pronounced within the overlying carbonate . Below the , a ca. 70 m thick succession in the western part (Porzecze, Dbska Wola, Dbrowa, Brzeziny ) corresponds to ca. 130 m thick carbonates in the eastern part of the region (Janczyce and Jurkowice ). This disproportion gradually creases in younger strata. The differences in and of particular are also visible in their lateral organization (Text-fig. 16). It is well exemplified in the western part of the Kielce Region, in which the of the Dbrowa Meer is highest in the north-western and south-western parts (up to 40 m) and gradually creases in the central part, where the meer disappears completely: in the vicinity of the towns of Chciny and Dyminy, the Brzeziny Meer directly overlies the Winna Formation (Glazek et al. 1981). If the lithostratigraphical divisions of the uppermost Emsian and between the Lysogóry and Kielce regions are compared, there are only two lithostratigraphical having clear analogies (compare Text-fig. 3 with Text-fig. 15). The first is the Dbrowa Meer, which in the Lysogóry Region belongs to the Grzegorzowice Formation, and which in the Kielce Region is incorporated into the Barania Góra Formation. The second unit is the . The carbonates between the Winna and Kowala , with ranging from ca. 130 m in the western part, to ca. 200 m in the eastern part of the Kielce Region, correspond to ca. 450 m thick posits of the Grzegorzowice and s in the Lysogóry Region. The last issue, which needs to be addressed, is the stratigraphical position of the studied succession. This is broadly discussed in Wójcik (2013) and will be presented in separate papers (Wójcik in preparation), and is only briefly discussed in the present paper. All the distinguished lithostratigraphical have diachronous boundaries. The most important boundary is the base of the carbonate succession. Generally, carbonate appear earlier in the western part of the region, especially in the north-western and south-western areas, in the Polygnathus costatus conodont Zone in the early or even earlier. In the eastern part of the region, the carbonatetart close to the Polygnathus costatus /Polygnathus costatus costatus boundary. A younger position of the top of the Winna Formation in the eastern part of the Kielce Region is also confirmed by found by Malec (1984b, see also Fijalkowska-Mar and Malec 2011) within the upper part of the unit in the Zarby 2 borehole core. CONCLUSIONS The Emsian/ transition in the Kielce Region of the Holy Cross Mts. inclus various lithological , which overlie the Lower vonian clastics of the Winna Formation and unrlie the Middle vonian stromatoporoid-coral dolomites and limestones of the Kowala Formation. The were posited during an early stage of the vonian transgression. A lithological scription of nine sections and a proposed formal lithostratigraphical division are presented. Six are distinguished within a newly fined Barania Góra Formation. In the western part of the Kielce Region these are: the Porzecze, Dbska Wola, Dbrowa, and Brzeziny , with a total reaching ca. 70 m. The Janczyce and Jurkowice , ca. 130 m thick, are distinguished in the eastern part. These strata correspond to the Grzegorzowice Formation in the Lysogóry Unit. Above that, the Wszachów and Nowy Staw , with a total ranging from ca. 60 to 90 m, are distinguished within the . Acknowledgments. I am particularly grateful to Prof. Stanislaw Skompski, Prof. Jerzy Nawrocki, Prof. Michal Szulczewski and Dr. Jacek Grabowski for their help and care during realization of the project. Dr. Piotr Luczyski and Prof. Ireneusz Walaszczyk are thanked for their helpful and careful review of the manuscript. Many thanks also to Dr. Piotr Luczyski, Dr. Zbigniew Remin, Dr. Anna yliska, Dr. Wojciech Kozlowski, Dr. Mikolaj Zapalski, Prof. Ireneusz Walaszczyk, Mrs Irena Sarnacka and, especially, Mr. Boguslaw Waksmundzki for their kind help during the last years of the PhD study. This work is dicated to J., M., and K. This paper presents the results of a PhD National Science Centre Project no. 2011/01/N/ST10/00604, entitled: "Facies velopment of the Kielce Region of the Holy Cross Mountains during the early stage of the vonian transgression (Emsian­ boundary interval)". 176 KRYSTIAN WÓJCIK http://www.deepdyve.com/assets/images/DeepDyve-Logo-lg.png Acta Geologica Polonica de Gruyter

The uppermost Emsian and lower Eifelian in the Kielce Region of the Holy Cross Mts. Part I: Lithostratigraphy

Wójcik, Krystian
Acta Geologica Polonica , Volume 65 (2) – Jun 1, 2015
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de Gruyter
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2300-1887
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2300-1887
DOI
10.1515/agp-2015-0006
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Abstract

Wójcik, K. 2015. The uppermost Emsian and lower in the Kielce Region of the Holy Cross Mts. Part I: Lithostratigraphy. Acta Geologica Polonica, 65 (2), 141­179. Warszawa. The paper provis a scription of primary geological logs, characteristics and formal lithostratigraphy of the uppermost Emsian and lower of the Kielce Region of the Holy Cross Mts., central Poland. Nine sections of this interval, representing the whole area of the Kielce Region, and ranging between the Lower vonian clastics of the Winna Formation and the Middle vonian carbonates of the Kowala Formation were studied. The succession is divid into the Barania Góra Dolomite and Limestone Formation and the Wojciechowice Dolomite Formation. Six are distinguished within the former. In the western part of the region these are (in stratigraphical orr): Porzecze Claystone Meer, Dbska Wola Dolomite Meer, Dbrowa Limestone Meer, and Brzeziny Dolomite Meer. In the eastern part, the formation is divid into the Janczyce Dolomite Meer and the Jurkowice Dolomite Meer. Additionally, the Wszachów Dolomite Meer and Nowy Staw Dolomite Meer are distinguished within the overlying . The of the uppermost Emsian­ succession ranges from ca. 200 m in the eastern part to ca. 130 m in the western part of the Kielce Region. Key words: Lithostratigraphy; vonian; ; Holy Cross Mountains; Dolomites. INTRODUCTION At the turn of the Early and Middle vonian, a first-orr transgression-regression cycle began, with a generally transgressive regime prevailing during the Middle and early Late vonian (Johnson et al. 1985; Sandberg et al. 2002). Great changes occurred in facies arrangement and palaeogeography on the southern edge of Laurussia. Post-Caledonian palaeotopography, regional extension due to Rhenohercynian Ocean spreading, local tectonic activity and pulsatory sealevel rise were the main factors that controlled the sedimentary processes during the early stage of the transgression (Belka and Narkiewicz 2008). As a result, a broad Laurussian shelf appeared, and a huge system of shallow-marine carbonate ramps and platformtarted to velop (Text-fig. 1). In the latest Emsian, the transgression reached the area of the present Holy Cross Mts. (HCM). The palaeogeographical and facies velopment of the area was related to first-orr global sea-level fluctuations with minor contribution of local tectonic events (Racki and Narkiewicz 2000; Szulczewski 1978, 1995a, 2006; Textfig. 2). This consecutively resulted in: (i) late Emsian termination of continental sedimentation and velopment of marginal and marine clastic position (Lobanowski 142 KRYSTIAN WÓJCIK 1971, 1981, 1991; Szulczewski and Porbski 2008); (ii) latest Emsian­early retrogradation of clastic lithotypes beyond the Holy Cross area and velopment of carbonate lagoonal environments (Wójcik 2013); (iii) early short-term constitution of open-marine environments (Malec 2005; Wójcik 2013); (iv) late unification of shallow carbonate shelf environments (Skompski and Szulczewski 1994; Narkiewicz and Narkiewicz 2010; Niedwiedzki et al. 2010; Narkiewicz and Ratellack 2014; Wójcik 2013; Narkiewicz et al. 2015); (v) Givetian to Frasnian transformation of a carbonate shelf into an isolated reef-rimmed shallow-marine "Dyminy" carbonate platform surround by eper Lysogóry and Chciny-Zbrza intrashelf basins (Szulczewski 1971; Racki 1993; Racki et al. 2002; Wójcik 2012); (vi) late Frasnian to early Famennian drowning of a carbonate platform and its transformation into a pelagic platform (Szulczewski 1978; Szulczewski et al. 1996; Wójcik 2009, 2012); and (vii) late Famennian­Early Carboniferous unification of ep marine marly sedimentation (Szulczewski 1971, 1973, 1995, 2006). The upper Emsian and the , being the olst parts of the transgressive succession, are a subject of intensive investigations in the Kielce (southern) Region of the HCM, including stratigraphical analyses and re- construction of facies velopment. The part of the succession unr study spans between the Winna and the Kowala and inclus a nuer of informal and poorly recognized lithostratigraphical (see Narkiewicz and Olkowicz-Paprocka 1983; Narkiewicz et al. 2006; Fijalkowska-Mar and Malec 2011). The poor finition of these , as well as poor unrstanding of facies patterns, geographical and stratigraphical distribution, and mutual relations between the , has led to markedly different interpretations of the area's history at the turn of the Early vonian transgression (compare: Racki and Turnau 2000; Narkiewicz et al. 2006; Belka and Narkiewicz 2008; Fijalkowska-Mar and Malec 2011; see also Text-fig. 4). Therefore, before crucial issues referring to the studied interval can be addressed (such as the time, directions and causes of the transgression, architecture of facies tracks, or eustatic vs tectonic control of the changes observed in the sedimentary environment), a reliable timespace facies architecture must be worked out. As the available data do not allow the introduction of a refined sequence stratigraphical framework, the pattern presented herein is a formal lithostratigraphical scheme, which is the subject of the present paper. All other issues will be addressed elsewhere. nudation areas land sedimentation shallow-marine clastic sdimentation shallow-marine carbonate sedimentation ep marine sedimentation transport direction Sa xo e Zon gian ne ryn ubian Zo ldan th Mo Zo ne Rhenohercyni e Zon e ngia n Zo n ury th ian Saxo ldanub Mo Text-fig. 1. Main sedimentary zones along the southern Laurussian shelf during the early stage of the vonian transgression: A ­ in the Late Emsian, B ­ in the (modified after Milaczewski 1980 and Mabille and Boulvain 2007). Small rectangles ­ Holy Cross Mts an 143 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Local sea level changes Lithostratigraphy Global sea level changes LYSOGÓRY R. KIELCE REGION Upper Sitkówka connsed sequence Beds IIf FAMENNIAN IIf UPPER VONIAN marly complex IIe IIe FRASNIAN IId cignia Beds tritic limestones IId IIc IIc Kostomloty Beds Wietrznia Beds MIDDLE VONIAN Nieczulice Beds Kadzielnia Lower Sitkówka Beds Jawica IIb IIa GIVETIAN IIa If Id Pokrzywianka B. witomarz Beds Laskowa Beds IIb Szydlowiec Beds Ie investigated interval If Id Ic Skaly Beds WOJCIECHOWICE Fm Eiflian Dolomites Dbrowa Horizon GR. Fm ZAGÓRZE Fm LOWER VONIAN EMSIAN Ic Ib Ib LOCHKOV. PRAG. Ia BARCZA Fm Ia pre-Ia Text-fig. 2. vonian lithostratigraphy of the Holy Cross Mts. compared with local and global sea level changes (after Sandberg et al. 2002; Narkiewicz et al. 2006, Belka and Narkiewicz 2008). White square ­ investigated interval GEOLOGICAL BACKGROUND The Palaeozoic of the Holy Cross Mountains (HCM) iubdivid by the Holy Cross Dislocation into the northern (Lysogóry) and southern (Kielce) . These are parts of the Lysogóry and Malopolska terranes respectively, and both belong to the Trans-European Suture Zone (TESZ) ­ an amalgamation of terranes consolidated at the turn of the Silurian and vonian (Nawrocki 2000, 2003; Nawrocki and Poprawa 2006; Nawrocki et al. 2007; Narkiewicz 2007; Belka and Narkiewicz 2008). Although small re- locations of particular structural of the TESZ took place during the Variscan orogeny (Konon 2006, 2007), large-scale post-Silurian displacements are questionable. Palaeomagnetic data from the Nawodzice Sandstones (Nawrocki et al. 2007), Mójcza Limestone (Schätz et al. 2006), as well as from the Bardo Diabase (Nawrocki 2000; Nawrocki et al. 2013) indicate a similar position of the Malopolska Block in relation to Baltica since the Carian. Thieems to be confirmed also by the presence of similar enmic faunas (e.g. Chimaerothyris dorowiensis, Stuncka 1983), as well as of unique facies (Spirifer sandstones: 144 KRYSTIAN WÓJCIK Stuncki and Stuncka 1986) in the vonian in both HCM regions. However, the HCM cannot be treated as a united and facially homogeneous area during the vonian. In spite of a common transgressive regime prevailing throughout the area, significant differences occur in facies velopment between the northern and southern HCM regions, which are expressed in succession , lithological variety and by diachroneity of lithostratigraphical boundaries of corresponding (Szulczewski 1995, 2006; Textfig. 2). The facies autonomy and tectonic separateness of the Lysogóry and Malopolska are especially well expressed in the Lower vonian: regressive facies and a more or less continuouuccession in the northern region correspond to a great stratigraphical gap and the Silurian/vonian unconformity in the southern unit (Szulczewski 1995, 2006; Kozlowski 2008; compare with Kowalczewski et al. 1998 and Malec 1993, 2001). (2011). The original subdivision of Malec (2005) is preserved herein (Text-figs 2 and 3). The upper part of the is referred to the fined by Klossowski (1985), who subdivid it into the Chmielowiec Meer in the lower part, and the Crystalline Dolomites Meer in the upper part (see tailed scription in Skompski and Szulczewski 1994). Narkiewicz and Narkiewicz (2010; see also Narkiewicz and Ratellack 2014; Narkiewicz and Narkiewicz 2014; Grabowski et al. 2015; Narkiewicz et al. 2015) revised the and referred the upper meer to the Kowala Formation. Kielce Region In the Kielce Region, the Emsian/ boundary succession was the subject of only a few investigations, limited to general lithological scriptions (see Textfigs 2, 4). Czarnocki (1957) distinguished the Placorm Sandstone, which he referred to the Lower vonian (Emsian). More recently, Tarnowska (1976, 1981 and 1987) subdivid thiuccession into the following : Lower Mudstone, Middle Sandstone, Upper Mudstone and Upper Sandstone. The lowermost unit was later refined as the Haliszka Formation (Fijalkowska-Mar and Malec 2011; after Tarnowska 1995). The remaining three , in the rank of , have been includ to the Winna Formation (see Tarnowska 1988; Belka and Narkiewicz 2008, p. 395; Fijalkowska-Mar and Malec 2011). In the western part of the region, Czarnocki (1957) distinguished the Dbrowa Horizon and the Dolomites, which overlie the Placorm Sandstone. Stuncka (1983) interpreted the Dbrowa Horizon as a biostratigraphical unit ­ the taxon range zone of Chimaerothyris (Spirifer) dorowiensis. Two additional lithological : the Pyrite-bearing and Siritic Claystone Meer and the Dolomite Meer, still below the Dbrowa Horizon, have been revealed in a series of boreholes: Dbrowa-D5 (Tarnowska and Malec 1987), (Kowalczewski 1979; Malec 1979, 1980, 1984a; Fijalkowska-Mar and Malec 2011), Zarby 2 (Malec 1984b), and Dyminy-2 (Tarnowska 1987; Filipiak 2011). These have also been documented in the north-western part of the region: in the Szydlówek trench (Malec and Stuncki 1988) and in the Skrzetle trench (Malec 1993, 2001a, see also the discussions in Kowalczewski et al. 1998; Narkiewicz 2002; Szulczewski 2006; Kozlowski 2008). In the eastern part of the Kielce Region, Narkiewicz et al. (1981) and Narkiewicz and Olkowicz-Paprocka (1983) reported the existence of two lithological EXISITING LITHOSTRATIGRAPHY IN THE HOLY CROSS MOUNTAINS Lysogóry Region In the Lysogóry region, the upper Emsian to succession is well recognized (Czarnocki 1919, 1950, 1957; Pajchlowa 1957; Lobanowski 1971, 1981, 1990; Kowalczewski 1971; Adamczak 1976; Klossowski 1985; Malec 2001, 2002, 2005; Szulczewski and Porbski 2008; Narkiewicz and Narkiewicz 2010, 2014; Niedwiedzki et al. 2010; Fijalkowska-Mar and Malec 2011; Filipiak 2011; Narkiewicz and Ratellack 2014; Grabowski et al. 2015; Narkiewicz et al. 2015). The Lower vonian is ca. 550 m thick and is divid into the Bostów, Klonów, Barcza, and Zagórze (see Narkiewicz et al. 2006; Text-fig. 2). The 110 m thick Zagórze Formation is the olst vonian transgressive unit (Szulczewski and Porbski 2008), clearly Emsian in age (Malec 2001, 2005; Filipiak 2011). The uppermost Emsian and lower beds, 95 to 160 m thick, are distinguished as the Grzegorzowice Formation (Text-fig. 2), and are subdivid into eight : (1) Bukowa Góra Claystone; (2) Warszówek Dolomite; (3) Godów Marl; (4) Wydryszów Limestone; (5) Kapkazy Sandstone; (6) Rzepin Dolomite; (7) Zachelmie Siltstone and Sandstone; and (8) Dbrowa Limestone (Malec 2005; Textfig. 3). Such a broad finition of the Grzegorzowice Formation was rejected by Szulczewski (2006) and by Szulczewski and Porbski (2008), albeit followed by Fijalkowska-Mar and Malec (2011) and by Filipiak 145 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Text-fig. 3. Lithostratigraphical schemes around the upper Emsian and in the Lysogóry Region of the Holy Cross Mts. according to Malec (2005), supplemented by palynostratigraphical data of Filipiak (2011). 1-8 ­ Grzegorzowice Formation: 1 ­ Bukowa Góra Meer, 2 ­ Warszówek Meer, 3 ­ Godów Meer, 4 ­ Wydryszów Meer, 5 ­ Rzepin Meer, 6 ­ Kapkazy Meer, 7 ­ Dbrowa Meer, 8 ­ Zachelmie Meer of postulated age (Janczyce-1 borehole core and Jurkowice quarry). In stratigraphical orr these are the Fossiliferous and Bioturbated Dolomicrites and Dolosparites Unit, and the Unfossiliferous Crypto- and Fine-crystalline Dolomites Unit. The authors treated the as facies-equivalents of the Dbrowa Horizon and the Dolomites respectively. Romanek and Rup (1990) recognized similar in in the Kowala 1 borehole core. Summarizing, the Emsian/ boundary succession of the Kielce Region is composed of a nuer of lithologically variable, poorly recognized and inaquately fined , spanning an interval between the Lower vonian siliciclastics of the Winna Formation and the Middle vonian­Frasnian carbonates of the Kowala Formation (Text-figs 2, 4). However, a simple and straightforward formalization of these is difficult. This is because of the equivocal finition of the Dbrowa Horizon ­ the crucial lithostratigraphical unit of the analyzed succession. So far, the unit was variously fined as: (1) lithological unit of limestones and marls with abundant fossils (= Dbrowa Horizon according to Gürich 1896; = complex VIII in Pajchlowa 1957; = Grzegorzowice Limestone Meer in Malec 2001b, 2002; = Kielce Limestone in Tarnowska 1987; = Dbrowa Limestone Meer in Malec 2005); (2) limestones, dolomites and shales with fossils and/or bioturbations that overlie the Lower vonian siliciclastics and unrlie the Unfossiliferous Crypto- and Fine-crystalline Dolomites (= Couvinian in Czarnocki 1950, 1957; = complexes III-VIII in Pajchlowa 1957; = Dbrowa Horizon in Filonowicz 1973, = complexes D and E in Glazek et al. 1981, = Fossiliferous and Bioturbated Dolomicrites and Dolosparites unit in Narkiewicz et al. 1981 and Narkiewicz and Olkowicz-Paprocka 1983); and finally, (3) taxon range zone of Chimaerothyris (Spirifer) dorowiensis (Stuncka 1983). Also the and stratigraphical/geographical ranges of the , which unrlie the Dbrowa Horizon ­ the Pyrite-bearing and Siritic Claystone Meer and the Dolomite Meer, are poorly recognized. Finally, distinguishing between the Dolomites in the western part of the region and the Unfossiliferous Crypto- and Fine-crystalline Dolomites in the eastern part of the region is unreliable. 146 KRYSTIAN WÓJCIK Narkiewicz and OlkoCzarnocki (1938, 1950, 1957) wicz-Paprocka (1983) N Western part Eastern part Narkiewicz et al. 2006 Dolomites Crypto- to Finely Crystalline Unfossilliferous Dolostones Dolomites Belka and Narkiewicz and Fijalkowska-Mar this work Narkiewicz 2008 Narkiewicz 2010 and Malec 2011 S N S N S W E W E WOJCIECHOWICE Crypto- to Finely Fm Crystalline Unfossilliferous WOJCIECHOWICE Fm Dolostones Bioturbated (= Dolostones) Brzeziny Dolomite Jurkowice Dbrowa Horizon EMSIAN Fossilliferous and Bioturbated Dolomicrites and Dolosparites DH BG Dbrowa Horizon Dbrowa Horizon Dbrowa Horizon GRZEGORZOWICE Fm (Dbrowa ) Dbrowa Limestone omi Dolb M CM Dbrowa Jan czy ce M DW Placorm Sandstone Placorm Sandstone PS Placorm Sandstone gap te Text-fig. 4. Lithostratigraphical schemes around the upper Emsian and in the Kielce Region of the Holy Cross Mts. according to various authors. BG ­ Bukowa Góra shales, DH ­ Dbrowa Horizon, PSCM ­ Pyrite-bearing and Siritic Claystone Meer, DW ­ , P ­ Porzecze Meer METHODS The Upper Emsian and posits have been recognized in nine sections in the Kielce Region (Textfig. 5). In the eastern part, five sections have been investigated: Jurkowice, Winna and Wszachów quarries, Wszachówka River valley and the Janczyce-1 borehole core. In addition, comments are ma on the published data from the Zarby 2 borehole core (Malec 1984b). In the western part, four sections have been recognized: the Zbrza, Brzeziny and trenches, and the borehole core. These investigations are supplemented by published data from the Dyminy-2 (Tarnowska 1987) and Kowala 1 (Romanek and Rup 1990) borehole cores. Some of the investi- gated sections (trenches) were only temporary exposures excavated during work on public water conduits, and thus any renewed research would need new excavations. The studied sections represent from 33 to 203 m long continuouuccessions of the uppermost Emsian and . About 2000 lithological samples, including 420 polished slabs, 250 thin sections, 108 conodont samples and 4970 measurements have been analyzed. Biostratigraphical analyses and measurements have been performed in the laboratories of the Faculty of Geology, University of Warsaw and in the Palaeomagnetic Laboratory in the Polish Geological Institute ­ National Research Institute. Dbrowa D-5 Skrzetle Szydlówek LYSOGÓRY REGION Dua Skala IG-5 Wola Zamkowa IG-1 Zarby 2 Warszawa HCM Kowala 1 Chciny Dyminy-2 Brzeziny Zbrza Winna Janczyce-1 Haliszka IG-1 Wszachówka River Wszachów Upper vonian and Carboniferous Middle vonian Lower vonian Lower Paleozoic Holy Cross Fault KIELCE REGION Jurkowice 10km previous investigationection investigated Text-fig. 5. Location of the investigated sections. Geological map of the Palaeozoic core of the Holy Cross Mts. after Konon (2006 and citations therein), simplified 147 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Zbrza 32.1 m . . ~29.37 ZB2 I. corniger corniger I. c. retropressus I. werneri I. struvei ZB1 CZ6 ~28.32 ZA6 ~27.67 S ~28.80 26 CZ5 ZA5 CZ4 ZA4 ~29.39 S SSSS CZ3 CZ2 CZ1 ~39.08 ZA3 ZA2 ~40.7 Dbrowa Meer ~61.09 ZA1 S 15.8 m . . . . . .. .... .... .... .... .... .. .... .... .. . . .. .... .... .... .... .... .... .... .... . . . . .......... . . . . . . ..... .. .. . . .. . .. . .. . .. . .. . .. . .. . .. . .. . .. . . . . . . . . . .. . .. . .. . .. . .. . I. introlevatus . . . . .. .. .. . . .. .. .. .. . . .. .. .. .. .. .. .. .. .. . . . . . .. .. .. .. .. .. .. .. .. . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. .. ... .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . . ... . . . . . . . . .. . . ... ... . .... .. . . . . . . . . . . . . . . . ... .. .... .. .. ... . .. .. .. .. . . . . . . .. .. .. .. .. .. .. . . . . . . ..... .... . . . . . . . . . . . . . . . .. . . .. .. .. .. . . . . . . .. .. .. .. .. .. . .... .... ... .. .. .... .... .. ..... .... .... .. . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . ZB6 ~6.89 .... .... .... .... .... .... .. .... .... .... .... .... . .... .... .... .. ... .... .... . .... .... .... .... .... .... .. .... .... .... .... .... . . . . . . . .... .... .... .... .... .... .... .... ... . .. . . .. .. .. .. .. .. .. . . . . . . . . . . .. . . . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ... .. .. .. .. .. .. .. .. .. .. .. . .. .. ... . . . . . . . . .. .. .. .. .. .. .. .. .. .. . . . . . . . . . . . . . . . . . .. . . . . . .. .. . . .. .. .. .. .. .. ...... .. ...... .. ...... .. ........ . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. .. . .. .. .. .. . . .. . . .. .. . . .. .. . . .. .. . . .. .. . . .. .. . .. .. .. .. .. .. .. . . . .. WINNA Formation Icriodus corniger leptus ZB5 . . . . . . . . . . . .. . . . . ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ MS major trends MS minor trends cyclothems MS average CZ1 cyclothemes conodont samples bioturbation structures brachiopods Ch. dorowiensis lumachelles tentaculoids . crinoids rugose corals Thamnopora sp. asselages tabulate coraltromatoporoids placorms ZB5 CZ3 SS . . ZB4 ~28.67 . ... . .. . . . .. .. . . . . ZB3 ~34.33 2 ~ ~ . .~ . . ~ . . . . ~ ~ ~ ~ . . .. . . . . ~ ~ ~ ~ . . .. . . . . ~ ~ ~ ~ . . .. . . . . ~ ~ ~ ~ ~ ~ ~ ~ . . .. . . . . ~ . . ~. . .~. . . ~ ~ ~ ~ ~ . . .. . . . . ~ ~ ~ . .~ .. .. . . . ~ ~ ~. . . ~. . . . .. .. . . . . .. .. . . . . ~ ~ ~ ~ . . . .. . . . . . . . .. . . . . limestones intercalated with marly shales marly shales with limestone lenses marltromatoporoid-coral dolomitic biostrome dolomicrites intercalated with dolomitic claystones dolomitic thamnopora-shaleandy dolomicrites with wavy lamination claystones ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~~ . . ... . . . . . . . . .. . . . . . . . . .. . . . . . . . .. .. . .. . . . . . . . . . . . . .. . . . . .. . . .. . . .. . . . . . . . . . . .. . .. .. . .. . . .. . . . ZB2 . . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . .. . . . . . .. . . . . . . . . . . . . . . . . . . . . .. . . . . . . .. .. .. .. .. . .. .. .. . .. .. .. .. .. .. .. .. . . . . . . .. .. . .. .. .. .. . .. . .. .. .. .. .. . .. . . . . .. . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . siltstoneandstones Text-fig. 6. Lithological succession, and in the Zbrza section 148 KRYSTIAN WÓJCIK SCRIPTION OF SECTIONS Zbrza The section is located in the vicinity of the village of Zbrza, in the south-western part of the Kielce Region: 50°4327.0N, 20°3349.0E (Pl. 6). The Palaeozoic rocks in this locality are exposed in the Zbrza Antycline as a part of the Wolica-Zbrza Fold, the largest tectonic structure of the southern Mesozoic surrounding of the HCM. The Carian to Upper vonian strata of the area were the subject of tailed investigations (czkowski and Tomczyk 1969; Filonowicz 1968, 1973; Kucia 1987; Wójcik 2009, 2012; see also Czarnocki 1919; Stuncka 1983; Hajlasz 1967; Racki 1993, p. 95). The Zbrza Anticline is also one of the most important outcrops of the Dbrowa Horizon (Gürich 1896; Zbroja et al. 2007). So far, however, the Emsian to succession of the area has been scribed only in general (Filonowicz 1973; Malec and Romanek 1994; Filipiak 2011). The Lower­Middle vonian boundary succession in the village of Zbrza was exposed during the construction of public water conduits in spring 2011. The exposure ran from the southern end of the village (house no. 1) and continued 175 m to the north. At present, it can be traced along the drains. The exposed succession was 61 m thick and has been divid into 16 lithological (Text-fig. 6 and Pl. 1). 345 lithological samples, 125 polished slabs, 50 thin sections and 911 measurements were analyzed. Unit 1 (2 m thick) is composed of 25­35 cm thick beds of light grey, medium-grained flat-bedd quartz sandstones with intercalations of green siltstone laminae. Unit 2 (5.4 m thick) is composed of red and red-violet siltstones alternating with thin layers of violet finegrained quartz-muscovite sandstones predominating in the lowermost (1.6 m thick) and uppermost (1.1 m thick) parts of the unit. A 2.7 m thick package of green claystones occurs in the middle part. Unit 3 (3.2 m thick) is composed of 5­40 cm thick beds of light grey quartz sandstones with flat or lowangle cross-bedding, intercalated by thin packages of green claystones. Thin lenses of placorm breccias occur on the upper surfaces of two sandstone beds. Unit 4 (0.5 m thick) is composed of green claystones, reduced tectonically at the top. Unit 5 (3.2 m thick) is composed of two thick beds of light grey medium-grained cross-bedd quartz sandstones (55 and 100 cm thick) and few thinner sandstone beds intercalated by thin and discontinuous laminae of green claystones. Unit 6 (1.7 m thick) is composed of brown to yellow dolomitic claystones, which constitute the base of the vonian carbonate succession. A few lenses of yellow-weathering dolomitic sandy marls occur in the upper part. Unit 7 (1.15 m thick) is composed of several 10­30 cm thick beds of reddish marly/sandy dolomicriteeparated by thin packages of brown dolomitic claystones. Unit 8 (3.7 m thick) is composed of a cyclic succession of the following packages: Package A: greenish dolomitic claystones (20­40 cm thick) with abundant Thamnopora sp.; Package B: yellowish marly dolomicrites with abundant Thamnopora sp. (15­40 cm thick); Package C: yellowish sandy dolomicrites with wavy lamination and single thamnoporoid remains; Package D: yellowish sandy dolomicrites in single massive beds (30 cm thick). The packages are arranged into 3 cyclothems (ABCD, ABCD, ABCACAD), the of which ranges between 1.2 and 1.3 m. Unit 9 (12.4 m thick) is characterized by a subtle cyclicity of the following packages: Package E: grey-violet dolomicrites and dolomitic limestones (20­40 cm thick) with flat surfaces, intercalated by brown dolomitic claystones; single rugose corals and tabulates occur within the dolomites; Package F: reddish marly dolomicrites with wavy surfaces, intercalated by brown dolomitic claystones; Package G: thin beds of yellow sandy dolomitic claystones. The packages are arranged into 3 cyclothems (EFG, EFG, EFG), the of which ranges between 2.0 and 2.7 m. The cyclicity vanishes in the upper part represented by reddish dolomicrites with single corals. Unit 10 (30­95 cm thick) is composed of three beds of reddish stromatoporoid-coral dolomites with predominant Thamnopora sp. and rugose corals overgrown by tabular stromatoporoids. There are also lenses of crinoid tritus. In the Zbrza Anticline, the posits of this unit build several bioherms, up to a dozen or so metres high. 149 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Unit 11 (65 cm thick) is composed of greenish marly shales with lenses of monospecific (Chimaerothyris dorowiensis) brachiopod lumachelles and crinoidal limestones. The brachiopods are well preserved, complete and oriented vertically. Adult forms predominate, with no signs of reposition. The lenses cut the unrlying shale laminae, but are smoothly covered by the overlying beds. Unit 12 (2.2­3 m thick) is composed of yellow- to greenish marls. Single brachiopods, crinoids and tentaculoids occur within the marls. Unit 13 (4.6 m thick) is composed of greenish marly shales with lenses of monospecific (Chimaerothyris dorowiensis) brachiopod lumachelles and crinoidal limestones, similar to those in unit 11. The abundance of organotritic limestone horizons increases towards the top of the unit. The coarse-grained beds are dominated by tritus of brachiopods (Chonetes angustestriata, Athyris concentrica and rare Chimaerothyris dorowiensis). Less common are tentaculoids (Tentaculitechlotheimi, T. subconicus), gastropods (Murchisonia sp.), crinoids, bryozoans, tabulate corals (Thamnopora sp.), rugose corals, molluscs, microconchids, trilobites (chenella dorowiensis) and rare cephalopods. Unit 14 (8.8 m thick) is composed of several tens of grey thin-bedd limestones intercalated by green marly shales. Three main lithological types of limestones can be distinguished: · grained limestones with fossil tritus throughout: brachiopods and tentaculoids with minor contribution of gastropods, bryozoans, tabulate and rugose corals, molluscs, trilobites and cephalopods occur. The lower surfaces have a clearly erosional character, while the upper surfaces are indistinct and show a gradual transition into micrite. Some grained limestonehow grad bedding, with brachiopod coquinas at the top. Skolithos isp. filled up with green marls appears at the tops of some of the surfaces; · flaser limestones: tritus of fossils build 1­2 cm thick laminae/strips within a micritic matrix; · micritic limestones: grey, grey-greenish and greyreddish thin-bedd marly limestones with bioturbation structures and occasional flat lamination. Chonetes angustestriata in monospecific lumachelles appear rarely on top surfaces. This is a second type of autochthonous brachiopod lumachelles in the section. The three types of limestones within the unit show approximately equal proportions. Unit 15 (2.5 m thick) is composed of light grey and reddish sandy dolomicrites and dolomitic marls intercalated by brown dolomitic claystones. 11 thin beds of dolomitic sandy marls (ca. 12­15 cm thick), with a nodular texture to wavy lamination, occur in the lower part of the unit, Very thin layers of reddish marls occur above. Unit 16 (9.5 m thick) is composed of grey, thin-bedd grained limestones, flaser limestones (micritic limestones, in which smudges and/or irregular laminae of grains occur) and micritic limestones intercalated by green marly shales, similar as in unit 14. The micritic limestones predominate in the upper part of the unit. Biostratigraphy A collection of 75 conodont specimens from 34 dissolved samples (21 positive) has been obtained, and the following taxa were intified: Icriodus corniger corniger, I. corniger leptus, I. curvirostratus, I. introlevatus, I. corniger retropressus, I. werneri, and I. struvei. The asselage documents the Polygnathus costatus and P. c. costatus zones, with the boundary between them recognized in unit 14 (see Text-fig. 6). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). A collection of 718 samples rived from 7-cm intervals in the carbonate part of the succession (Dbska Wola and Zbrza ) has been measured. Average MS is 27.2×10-8m3/kg. The MS curve is divid into 4 major asymmetrical fluctuations/trends (Textfig. 6): Trend A is 13.3 m thick and ranges from unit 6 to the upper part of unit 9. The trend is divid into 6 minor fluctuations: ZA1: 2.6 m thick with average MS 61.09×10-8m3/kg; ZA2: 1.4 m thick with average MS 40.7×10-8m3/kg, ZA3: 1.2 m thick with average MS 39.08×10-8m3/kg, ZA4: 3.4 m thick with average MS 29.39×10-8m3/kg, ZA5: 2.6 m thick with average MS 28.8×10-8m3/kg, ZA6: 2.1 m thick with average MS 27.67×10-8m3/kg; Trend B is 16.3 m thick and ranges from the upper part of unit 9 to the upper part of unit 14. The trend is divid into 6 minor fluctuations: ZB1: 1.6 m thick with average MS 28.32×10-8m3/kg, ZB2: 2.8 m thick with average MS 29.37×10-8m3/kg, ZB3: 1.6 m thick with average MS 34.33×10-8m3/kg, 150 KRYSTIAN WÓJCIK ZB4: 2.8 m thick with average MS 28.67×10-8m3/kg, ZB5: 3.5 m thick with average MS 15.74×10-8m3/kg, ZB6: 4 m thick with average MS 6.89×10-8m3/kg; Trend C is 6.5 m thick and ranges from unit 15 to the lower part of unit 16. The average MS in trend C is 6.89×10-8m3/kg; Trend D inclus the uppermost part of the succession, with the of at least 6 m, and the average MS of 4,86×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Brzeziny The section is located in the south-western part of the Kielce Region, in the eastern part of the Chciny Anticline: 50°4614.6N, 20°3448.2E (Pl. 6). The Emsian­ transition was recognized in the western part of the antycline by Glazek et al. (1981) in the vicinity of the town of Chciny. The Lower vonian siliciclastics cropping out in that area are very thin (only a few metres thick), a typical Dbrowa Horizon is lacking (dolomites with bioturbation structures and grained intercalations occur in the lower part of the succession), and only the dolomites are commonly present in small outcrops along the Castle Hill. The topmost part of the succession ­ the Dolomites, is partly exposed in the nearby Radkowice and Jawica quarries. In the vicinity of the village of Brzeziny, the of the clastic succession increases and the Dbrowa Horizon appears. So far, the succession has not been scribed. Only very general remarks can be found in Filonowicz (1973) and Stuncka (1983). A 56 m thick succession of Emsian and posits in the village of Brzeziny was recognized by the author in 2010. A 65 m long trench was ma, longitudinally cutting the southern slope of the Siedliskowa Hill, running along the northern si of road no. 763, ca. 100 m east of the cemetery and 150 m north of house no. 271 on Chciska Street. The exposed succession was 56 m thick and has been divid into 8 lithological (Text-fig. 7 and Pl. 2). 220 lithological samples, 80 polished slabs, 27 thin sections, 21 conodont samples and 380 measurements were analyzed. Unit 1 (1.6 m thick) is composed of 7­12 cm thick beds of yellow medium-grained quartz sandstones with placorm remains. A 25 cm thick breccia occurs at the top. Unit 2 (5.6 m thick) is composed of grey siltstones, which predominate in the lower and upper parts of the unit. Thin layers of red-violet fine-grained quartzmuscovite sandstones occur in the middle part. Unit 3 (90 cm thick) is composed of brown dolomitic claystones overlain by four beds of yellow and violet dolomitic sandy marls with intercalations of claystones Unit 4 (13.5 m thick) is composed of 5­35 cm thick beds of marly dolomites intercalated by very thin laminae of brown claystones. Unit 5 (8.2 m thick) is composed of 1­10 cm thick beds of grey-violet marly dolomicrites with intercalations of brown claystones. Chondrites isp. horizons and dolosparite laminae/strips occur in the thickest dolomite beds, albeit not forming indivi dual beds. Unit 6 (6.9 m thick) is composed of two, 95 and 35 cm thick packages of green marly shales with monospecific (Chimaerothyris dorowiensis) brachiopod lumachelle lenses (compare with 11 and 13 in the Zbrza section). Packages of 10­25 cm thick beds of grey limestones occur in the middle and upper parts of the unit. Similarly as in the Zbrza section, three types of limestones can be distinguished: micritic, flaser and grained limestones. Chimaerothyris dorowiensis and Chonetes angustestriata are the most frequent brachiopods. In some beds, crinoids are also present. Gastropods (Murchisonia sp.), tentaculoids, microconchids, as well aingle trilobites (chenella sp.), corals and cephalopods are less common. Bioturbation structures (Chondrites isp.) occur in almost all beds, and are especially abundant around the grained laminae/strips. Unit 7 (3.05 m thick) is composed of 5­25 cm thick beds of green micritic dolomitic limestones. Intercalations of brown dolomitic claystones occur in the lower part. Single brachiopods (Chonetep.) and crinoids are also present. Unit 8 (15.9 m thick) is composed of 5­40 cm thick beds of red to violet marly dolomicrites with intercalations of brown dolomitic claystones. Several thicker, greenish beds occur in the middle part of the unit and aingle tabular beds in its upper part. Fossils are very rare and limited to thin sparry laminae/strips. Bioturbation horizons, dominated by Chondrites isp., occur more frequently. 151 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Brzeziny I. struvei Brzeziny Meer ~43.12 BB1 ~43.00 BA3 SS S Icriodus corniger corniger I. corniger retropressus group I. werneri I. amabilis BA2 ~47.03 39.6 m ~52.16 BA1 S S I. curvirostratus I. introlevatus 6.9 m Dbrowa Meer WINNA Formation . . . . . BB3 ~16.49 . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 0 30 29.4 m MS major trends MS minor trends ~52.16 MS average conodont samples bioturbation structures brachiopods lumachelles tentaculoids . crinoids rugose corals placorms BB5 limestones intercalated with marly shales marly shales with limestone lenses BB2 dolomitic limestones dolomicrites intercalated with dolomitic claystones claystones ~40.45 . .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. sandstones Text-fig. 7. Lithological succession, and in the Brzeziny section 152 KRYSTIAN WÓJCIK Biostratigraphy A collection of 87 from 21 dissolved (14 positive) samples has been obtained, and the following taxa were distinguished: Icriodus corniger corniger, Icriodus corniger retropressus group (including. I. c. retropressus Bultynck 1970 and I. n. sp. Narkiewicz 2013), Icriodus curvirostratus, Icriodus introlevatus, Icriodus werneri, Icriodutruvei, Icriodus amabilis. The asselage documents two ­ Polygnathus costatus and P. c. costatus, with the boundary between them established in the lower part of unit 6 (Text-fig. 7). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). A collection of 380 samples from 15-cm intervals has been measured. Average MS is 26,9×10-8m3/kg. The MS curve is divid into 4 major asymmetric fluctuations/trends (Text-fig. 7): Trend A is 11 m thick and ranges from the base of unit 3 to the upper part of unit 4. The trend is divid into 3 minor fluctuations: BA1: 2.9 m thick with average MS 52.16×10-8m3/kg, BA2: 4.3 m thick with average MS 47.03×10-8m3/kg, BA3: 3.8 m thick with average MS 43.87×10-8m3/kg, 25 polished slabs, 16 thin sections, 15 conodont samples and 429 measurements were analyzed in the section (Text-fig. 8). Unit 1 (9 m thick) is composed of grey to green claystone and siltstone packages interbedd with thinbedd yellow sandstones. Single placorm impressions occur. Unit 2 (2.3 m thick) is composed of thin-bedd yellow fine-grained quartz sandstones with placorm impressions and charred remains, and with thin intercalations of siltstone packages. Unit 3 (3.7 m thick) is composed of a 65 cm thick package of red-brown dolomitic claystones in the lower part and a 1.5 m thick package of brown dolomitic marls in the middle part. 20 ­ 30 cm thick browngreen and grey-green marly limestones with fenestral structures occur in the uppermost part of the unit. Two beds of nodular limestones with single cystoids and gastropods, topped by intraformational breccias, are present in the uppermost part of the unit. The unit can be clearly distinguished from the overlying posits due to the presence of limestone beds and fossils. An important feature is the absence of Chimaerothyris dorowiensis and other fossils typical of the Dbrowa Horizon. Unit 4 (27 m thick) is composed of a cyclic succession of the following packages: Package A (5­17 cm thick): brown dolomitic claystones; Package B (0.6­4.2 m thick): thin-bedd greenish to violet dolomitic marls with rare horizons of bioturbation structures; Package C (1.2­2.8 m thick): thin- to medium-bedd reddish to violet laminated marly dolomicrites with rare stromatolites. The unit is divid into 5 ABC cyclothems, the of which ranges between 2.25 and 6.45 m. Biostratigraphy Of the 15 dissolved samples only one was positive, yielding two specimens of the conodont Icriodutruvei. This taxon indicates an age not olr than the upper part of the Polygnathus costatus costatus Zone of the stage (Text-fig. 8). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). Trend B is 15.8 m thick and ranges from the upper part of unit 4 to the middle part of unit 6. The trend is divid into 3 minor fluctuations: BB1: 5.4 m thick with average MS 43.12×10-8m3/kg, BB2: 3.6 m thick with average MS 40.45×10-8m3/kg, BB3: 6.8 m thick with average MS 16.49×10-8m3/kg, Trend C is 6.6 m thick and it ranges from the upper part of the unit 6 to the lower part of the unit 8. The average MS is 26.9×10-8m3/kg. Trend D is 10 m thick and inclus the upper part of the succession (unit 8). The average MS is 22.27×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). The section is located in the central-western part of the Kielce Region: 50°5027.1N, 20°2857.8E (Pl. 6). A 33 m thick succession of Emsian and posits of the Dyminy Anticline was temporarily exposed in the village of in 2011. A 75 m long trench, excavated during public water conduit construction, was located along the eastern si of road S8, starting from the overpass to the north. The succession has been divid into 4 lithological (Text-fig. 8). 76 lithological samples, 153 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. gastropods cystoids calcisphaerids ostracods laminations MS major trends MS average conodont samples bioturbation structures intraformational breccias A collection of 429 samples rived from 7-cm intervals has been measured. Average MS is 13× 10-8m3/kg. The MS curve is divid into 4 major asymmetric fluctuations/trends (Text-fig. 8): Trend B is 3.5 m thick and eraces unit 3. Average MS is 13.59×10-8m3/kg, Trend C is 5.7 m thick and eraces the lower part of unit 4. Average MS is 18.32×10-8m3/kg, Trend D is 3.1 m thick and it ranges through the middle part of the unit 4. Average MS is 13.32×10-8m3/kg, Trend E is 13.5 m thick and eraces the upper part of unit 4. Average MS is 8.02×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Kowala 1 borehole (Romanek and Rup 1990, Narkiewicz 1991) susceptibility magnetic ~13.32 ~18.32 6 ~13.59 4 2.8 m 2 .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. . .. . .. . .. . .. . .. . . . . . dolomitic claystones claystones . .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. The location of the Kowala 1 borehole is 50°4804.52N, 20°3335.96E (central-western part of the Kielce Region; central part of the GalziceBolechowice Syncline). The core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. The core went through a complete, 993.6 m thick vonian succession, reaching the Carian below (Racki 1985, Romanek and Rup 1990, Narkiewicz et al. 1990, akowa and Radlicz 1990, Nehring-Lefeld 1990, Turnau 1990, Narkiewicz 1991). The siliciclastics at the base of the vonian succession are only 2 m thick and are followed by ca. 140 m thick carbonates. Romanek and Rup 1990 (see also Narkiewicz 1991) subdivid the latter into a 97 m thick Bioturbated Dolomites with Macrofossils Unit (882.7­989.7 m pth), and a circa 30 m thick tritic and Laminated Dolomite Unit (846.8­882.7 m pth). The first unit is composed mostly of bioturbated dolomicrites and dolomicrosparites with Chondrites isp. asselages. Single brachiopods, corals, stromatoporoids and crinoids are present and are especially abundant in the upper part of the unit (884.0­889.9 m pth). The second unit is composed of flat-laminated dolomicrites and tritic dolomites with horizons of intraformational breccias and oolites. Dyminy-2 borehole (Tarnowska 1987, Filipiak 2011) The location of the Dyminy-2 borehole is 50°4850.88N, 20°3833.61E (central-western part Brzeziny Meer S costatus - eifilius .. . .. . .. . .. . .. . .. . .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . I. struvei .. . .. . .. . .. . . . . . . . .. .. .. .. . .. . .. . .. . .. . .. . . . . .. .. .. .. .. .. .. .. .. .. .. . . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. limestones cuboid fissility marls dolomicrites with claystone intercal. sandstones Text-fig. 8. Lithological succession, and in the section 154 KRYSTIAN WÓJCIK of the Kielce Region; southern li of the Dyminy Antycline). The core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. The 222 m ep Dyminy-2 borehole went through the Lower vonian to succession. Tarnowska (1987) divid the succession into 4 : Lower vonian siliciclastics, Lower Dolomite Unit, Dbrowa Horizon (Kielce Limestone), and Upper Dolomite Unit. The Lower Dolomite Unit (137.7­ 109.0 m pth) is composed of sandy dolomites and dolosparites with crinoids, corals, stromatoporoids, brachiopods, ostracods and fishes. Above, unfossiliferous laminated dolomicrites with fenestral structures occur. The Dbrowa Horizon (109.0­96.0 m pth) is composed of bioclastic limestones with ostracods, crinoids, brachiopods, gastropods, , tentaculoids, trilobites, foraminifers and fish remains. The Upper Dolomite Unit is built of dolomicrosparites and bioturbated dolomites in the lower part (96.0­45.0 m pth) and unfossiliferous dolomicrites with microbial lamination in the upper part (45.0­15.0 m pth). Filipiak (2011) intified the velatalangii palynostratigraphic Zone within the Dbrowa Horizon. He also indicates the position of the Emsian/ boundary interval at pths between 143.0 and 110.0 m. Szydlówek, Skrzetle, Dbrowa D5 (Malec and Stuncki 1988, Malec 1993, 2001, Tarnowska and Malec 1987) The Emsian and posits in the northwestern part of the Kielce Region were recognized in the Szydlówek road-cutting (Malec and Stuncki 1988) and Skrzetle trench sections (Malec 1993, 2001), as well as in the Dbrowa D5 (Tarnowska and Malec 1987) and (Kowalczewski 1979; Fijalkowska-Mar and Malec 2011) borehole cores. The sections exposed the Pyrite-bearing and Siritic Claystone Meer, which overlies the Winna Formation. The posits are black to yellow in colour in the lower part, and red and brown-red at the top of the unit. Sirite nodules, limonite breccias, and siltstone and sandstones intercalations occur frequently, but the carbonate content is also significant. Rare brachiopods, including Chimaerothyris dorowiensis, as well as crinoids and tentaculoids occur. Foraminifers (Amphitremoida, Lagenammina, Saccammina, Hyperammina and different morphotypes of Webbinelloia), ostracods, and (Icriodus corniger retropressus group, I. corniger corniger and I. corniger cf. leptus) are also present. In the Dbrowa D5 borehole core, the Pyrite-bearing and Siritic Claystone Meer is overlain by the Dbrowa Horizon, composed of few metres of predominantly micritic and grained limestones. It yield abundant Chimaerothyris dorowiensis, algae, ostracods, foraminifers, and rare (Icriodus werneri). The Dbrowa Horizon is not present in the Szydlówek and Skrzetle sections, in which the pyrite-bearing and siritic claystones are overlain by dolomites. Single brachiopods, tentaculoids, corals and , as well as horizons of bioturbation structures occur within the lower part of the dolomitic succession. borehole The location of the borehole is 50°5656.96N, 20°3034.64E (north-western part of the Kielce Region; northern li of the Miedziana Góra Anticline). The core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. The borehole cored the most complete Emsian­ succession in the north-western part of the Kielce Region. A tailed lithological scription can be found in Kowalczewski (1979; see also Fijalkowska-Mar and Malec 2011). In the present paper thicription iupplemented by measurements (Text-fig. 9). The succession of the borehole is 66 m thick (Text-fig. 9). Fijalkowska-Mar and Malec (2011) divid it into 4 lithological : Upper Sandstone Meer of the Winna Formation (7.0­12.9 m, 5.1 m thick); Pyrite-bearing and Siritic Claystone Meer (12.9­19.2 m, 5.4 m thick); Dolomite Meer (19.2­39.5 m, 15.6 m thick); and Dbrowa Limestone Meer (39.5­116.5 m, 33.8 m thick). Biostratigraphy The stratigraphy of the section was presented by Malec (1979, 1980, 1984, 1990, 1992 and 1993) and summarized in Fijalkowska-Mar and Malec (2011). Accordingly, the boundary between the Lower and Middle vonian was located within the Dbrowa Meer, at 62.7 m pth, based on the first appearance of the conodont Icriodus corniger retropressus. However, it should be noted that no were record below this pth. This long barren interval may therefore easily represent age as well. 155 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. pth . . . . . PB4 ~25.80 39.5 m . . . . . . ~33.83 PA3 PB3 ~36.41 PA2 ~39.20 . . ~44.39 PA1 .. . .......................................................... .. .... ...... ... . .............. ...... ............. ... . . . ..... . Icriodus werneri I. corniger retropressus I. corniger corniger . . . . . . . . .. . .. . . . .. . .. . .. .. .. ... .. . . .. .. . ... .. .... ... . . . . .. .... .... .. ~37.27 PB2 . . . ... . .. . . ............................................................................................................... . . ........................................................... . .. .. ... . .. . . .... .. Dbrowa Meer 19.2 m ~~ ~~ ~~ ~~ ~~ ~~ ~~ ~~ ~~ PB5 . . . Porzecze Meer . . MS major trends MS minor trends MS average conodont samples bioturbation structures brachiopods tentaculoids crinoids rugose corals tabulate coraltromatoporoids laminations grained intercalations coralline intercalations . .............. . ... .................................................................................................................................................. . ... .. .... .. .. . .... . .. . .. . . ~~ ~~ ~~ ~~ . .. ... .. . .. .. . ... .. crinoidal limestones limestones intercalated with marly shales limestones dolomicrites intercalated with dolomitic shaleiritehales 12.9 m ~ ~~ ~~ ~ ~~ ~ ~ ~~ ~~ ~ ~~ ~ ~ ~~ ~~ ~ ~~ ~ . .. . ~~ . .. ~~~~ ~~. . . .. ~ ~~ ~~ ~ ~~ ~ ~. .~~.~~ ~ ~ ~~ . .~~ ~~ .. . . .. ~~ ~~ . . . .. ...... ~~. .. . . ... ~ ~ .... . ~~~ ~~ ~ ~~ ~~ ~ ~~~ ~ ~ ...................... . .. . ~ ... ...~..~..~. .. .~.~..~..~..~ . . . . ~ . ... ... .. . ~...~..~. ...~.~.. .~. ... .. .. .. .. .. .. .. .. .. . . . . . PA4 ~33.8 80 100 Text-fig. 9. Lithological succession (after Kowalczewski 1979), (after Fijalkowska-Mar and Malec 2011) and (this work) in the borehole core . . ~38.12 PB1 ~ ~ ~ ~ ~ ~~~ ~~~~~~~~~~~~~ ~~~ ~ ~ ~ ~ ~ ~~~ ~ ~ ~ ~ ~ ~~~ ~ ~ ~ ~ ~ ~~~ . . ....... . . . .................................................... .................. .................................... siltstoneandstones ~ ~~ ~~ ..... . ~ . . . . ~ ~ ~~~. .~.~. .~.~. 156 KRYSTIAN WÓJCIK A collection of 553 samples rived from 20-cm intervals has been measured. Average MS is 36.08× 10-8m3/kg. Two major MS fluctuations/trends (A­B), divid into minor fluctuations, are intified (Text-fig. 9): Trend A ranges from 21.3 m to 45.1 m pth and is divid into 4 minor fluctuations: PA1: 21.3­26.6 m pth, average MS 44.39 ×10-8m3/kg, PA2: 26.6­32.8 m pth, average MS 39.20×10-8m3/kg, PA3: 32.8­40.5 m pth, average MS 33.83×10-8m3/kg, PA4: 40.5­45.1 m pth, average MS 33.80×10-8m3/kg; thin sections, as well as 766 measurements were analyzed in the section. Unit 1 (5.6 m thick) is exposed in the olst part of the quarry. Thin- and medium-bedd grey laminated dolomicrites occur in the lowermost part of the succession, just several metres above the sandstones of the Winna Formation. They are intercalated by thin packages of dolomitic shales. Horizons of bioturbation structures (Chondrites isp.) appear on the surfaces, as well as within the beds. Numerous conulariids, plants remains and molluscs occur within the grained laminae/strips. Brachiopods (Gypidula sp.) are locally abundant, building monospecific lumachelles. Unit 2 (12 m thick) is composed of 20­50 cm thick beds of brown-grey dolomicrites and fine-crystalline dolomites with wavy interbedding. Thin laminae of black dolomitic shales occur on some surfaces. Thin tentaculoid lumachelles with tritus of bryozoans, crinoids and gastropods appear at the top of some beds, while numerous brachiopods (Gypidula) occur at the tops of others. Chondrites isp. concentrations with single Planolites isp. are common and constitute characteristic, blueweathering 15 cm thick bioturbation horizons in the upper part of the unit. tritus of shelly fossils occurs throughout. Unit 3 (18.8 m thick) is composed of up to 2.5 m thick beds of grey-blue weathering nodular dolomicrites intercalated by strongly bioturbated horizons. The nodules are more or less isolated, up to 5 cm in diameter, and surround by residual laminae/strips of clay minerals. In some parts, the nodular texture changes into wavy/irregular bedding. Single Gypidula sp. appear on the upper surfaces. The bioturbation horizons reach a of up to 40 cm and contain a nse and compact network of Chondrites isp. burrows and rare Planolites isp. Rare laminae of tritic material with crushed crinoids and brachiopods also appear. The burrows penetrate the rock completely, resulting in the bed being subdivid into minor irregular more or less isolated sub-beds. The nodular structure disappears in the upper part of the unit and the dolomite beds become more regular and homogeneous. A 30 cm thick regolith horizon covered by a distinctive (clearly visible in the quarry) 20 cm thick package of orange clays occurs in the topmost part of the unit. Unit 4 (18.5 m thick) is composed of up to 2 m thick beds of yellow-weathering nodular dolomites with bioturbation horizons. There are irregular lenses of homo- Trend B ranges from 45.1 m to 116.5 m pth and is divid into 4 minor fluctuations: PB1: 45.1­64.0 m pth, average MS 38.12×10-8m3/kg, PB2: 64.0­79.5 m pth, average MS 37.27×10-8m3/kg, PB3: (79.5­97.1 m pth, average MS 36.41×10-8m3/kg, PB4: 97.1­116.5 m pth, average MS 25.80×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Jurkowice Quarry The section is located in the south-eastern part of the Kielce Region: 50°3739N, 21°2126E (Pl. 6). and Givetian carbonates are exposed in the Jurkowice and Budy quarries. The vonian of the area was intensively studied (Czermiski and Ryka 1962; Pajchlowa and Stasiska 1965; Kamierczak 1971; Baliski 1973; Olempska 1979; Narkiewicz et al. 1981; Narkiewicz 1991; Racki 1993; Racki and Sobo-Podgórska 1993; Preat and Racki 1993; Hajlasz 1993; Zdanowski 1997), however, most of the studies were dicated to the Givetian. The was reported by Narkiewicz et al. (1981) and Zdanowski (1997). According to them, a ca. 100 m thick succession, exposed in the Jurkowice quarry, may be subdivid into a Fossiliferous and Bioturbated Dolomicrites and Dolosparites Unit at the base (43 m thick) and a Unfossiliferous Crypto- and Finecrystalline Dolomites Unit at the top (>58 m thick). Zdanowski (1997) documented the early age of the lower unit (Polygnathus costatus costatus conodont Zone). The carbonates currently exposed in the Jurkowice quarry represent approximately the same stratigraphical interval as documented in the papers referred to above. The section available at present is located ca. 150 m north of the quarrying front as it was in 1997. A new lithological log, measurements and sedimentological investigations were provid in 2011 and 2012. The succession has been divid into six lithological (Text-fig. 10). 120 lithological samples, including 45 polished slabs and 27 157 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Jurkowice quarry dolomitic shales/ claystones grained (intraclast-ooid) dolomites dolomicrites crinoid dolomites nodular dolomites bioturbation horizonts laminations, stromatolites breccias MS major trends MS average bioturbation structures gypidulids, lingulids tentaculoids, crinoids tabulates, conulariids plants 2 ~17.10 Nowy Staw Meer Wszachów Meer S ~~~~ SS EE2 ~14.01 SS 66.2 m 66 S 1 ~15.09 56.0 m EE1 ~12.01 I. corniger retropressus group I. werneri I. struvei 46 ~17.44 3 6 ~13.92 Icriodus corniger corniger CE Text-fig. 10. Lithological succession, (after Zdanowski 1997, revised) and in the Jurkowice quarry section 158 KRYSTIAN WÓJCIK geneous crinoid dolomites with Thamnopora sp. tritus. Three (up to 2 m) thick homogeneous beds of crinoid dolomites occur at the top of the unit. Unit 5 (10.3 m thick) is composed of dark, micritic and bituminous dolomicrites. The absence of bioturbation structures and shelly fossils, and the presence of a distinct horizon of stromatolitic domes, are characteristic features. Medium-bedd dark micritic dolomites with flat to wavy surfaces coated with iron crusts, intercalated by black dolomitic shales predominate in the lower part of the unit. Flat laminations are common in this part. A continuous bed of stromatolites, with 40 cm domes, and with irregular internal laminations, occur in the upper part. A package of dolomitic shales compensates the dome-relief, and a 2.5 m thick package of dark dolomicrites with flat laminations occur at the top. Unit 6 is composed of a cyclic succession of the following lithological packages: Package A: thick-bedd yellowish grained dolomites with flaser laminations and erosional lower surfaces. The flaser lamination is expressed aeveral cm long micritic, more or less continuous laminae/strips within a grained, intraclast-ooid matrix. The micritic laminae/strips build small stromatolitic domes at the tops of the grained beds; Package B: green micritic dolomites with flat laminations and intraformational breccia horizons (10­30 cm thick); Package C: green to yellowish dolomitic shales (up to 10 cm thick); Package D: variegated siltstones (up to 5 cm thick). The packages are arranged into 8 ABCD cyclothems, the of which ranges between 1.0 and 1.8 m. The uppermost part of the Jurkowice succession is composed of similar posits, with a domination of variegated (greenish) dolomitic shales with breccia horizons. The posits are strongly fold and thrust into particular blocks, interpreted as collapse breccias (see Narkiewicz 1991). Biostratigraphy Zdanowski (1997) collected 508 from 14 samples rived from the lower part of the succession (herein 1 to 4). The material has been revised by the author (Wójcik 2013 and in preparation), who intified the following taxa: Icriodus corniger corniger, I. c. retropressus group (including. I. c. retropressus Bultynck 1970 and I. n. sp. Narkiewicz 2013), I. werneri and I. struvei. The asselage indi- cates the lower part of the Polygnathus costatus costatus Zone (Text-fig. 10). No have been obtained from 5 and 6. A collection of 766 samples from 10-cm intervals has been measured. Average MS is 14.99×10-8m3/kg. Six mjor MS trends (CE ­ EE2), subdivid into minor fluctuations, are intified (Text-fig. 10): Trend CE is 7 m thick and ranges from unit 1 to the lower part of unit 2. Average MS is 13.92×10-8m3/kg; Trend 1 is 25 m thick and ranges from the upper part of unit 2 to the lower part of unit 3. Average MS is 15.09×10-8m3/kg; Trend 2 is 9 m thick and ranges from the upper part of unit 3 to the lower part of unit 4. Average MS is 17.1×10-8m3/kg; Trend 3 is 12 m thick and eraces the middle part of unit 4. Average MS is 17.44×10-8m3/kg; Trend EE1 is 9 m thick and ranges from the upper part of unit 4 to the lower part of unit 5. Average MS is 12.01×10-8m3/kg; Trend EE2 is 7 m thick and ranges from the upper part of unit 5 to the lower part of unit 6. Average MS is 14.01×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Wszachówka River valley The section is located in the eastern-central part of the Kielce Region: 50°469.1N, 21°729E (Pl. 6). The lowermost part of the vonian carbonate succession crops out south of the Winna quarry, along the Wszachówka River valley. An only partially exposed, ca. 50 m thick succession, watudied in 2012. The succession has been divid into 3 lithological (Textfig. 11). 60 lithological samples, 45 polished slabs and 22 thin sections were analyzed. Unit 1 (7.5 m thick) is composed of 10­30 cm thick beds of dark sandy dolomicrites with corals, algae, crinoid remains and bioturbation structures. Fossils are scattered within a marly matrix. Rare thin beds of dolomicrites with fenestral structures appear in the upper part of the unit. Unit 2 (30 m thick) is composed of thin- to mediuedd dark dolomicrites with abundant Chondrites-like bioturbation structures. 159 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Unit 3 (10 m thick) is composed of thin beds of dolomicrites. Chondrites isp. and single Planolites isp. appear on the upper surfaces together with single tentaculoids and gypidulids. Rare thin laminae of Gypidula lumachelles also occur. Biostratigraphy Two specimens from the Icriodus corniger retropressus group and 5 specimens of Icriodutruvei have been obtained from 8 studied conodont samples. They belong to two : Polygnathus costatus Zone and P. c. costatus Zone, with the boundary located probably within unit 2 (Text-fig. 11). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). Wszachów quarry The section is located in the eastern-central part of the Kielce Region: 50°4547.40N, 21°839.90E (Pl. 6). The Wszachów quarry iituated near the village of Krowianka, east of the town of Lagów and south of the Wszachówka River. The quarry exposes the lower part of vonian dolomites (below the Kowala Formation). A complete succession is exposed along the western wall of the quarry, on the 2nd and 3rd quarrying levels. A 78-m thick succession was recognized in 2012. The succession has been divid into four (Text-fig. 12 and Pl. 4). 120 lithological samples, 30 polished slabs, 16 thin sections, 25 conodont samples and 481 measurements were investigated. Unit 1 (18.5 m thick) is composed of thick beds of dolomicrites and fine-crystalline dolomites with a nodular texture. Nodules, up to a dozen or so cm in diameter, are more or less isolated and surround by thin black clay smudges. The 1.0­2.2 m thick beds are separated by 20 cm thick horizons of Chondrites-dominated bioturbation structures. A distinctive, 15 cm thick package of black shales occurs at the top. Unit 2 (9.3 m thick) is composed of thick beds of finecrystalline homogeneous dolomites with single crinoids. Unit 3 (22.5 m thick) is composed of posits characterized by a black colour and the absence of fossils and bioturbation structures. Four lithological packages in a cyclic succession can be distinguished: Wszachówka River valley costatus - eifilius Janczyce Meer . . . . .. . .. ... .. .. dolomicrites with intercalations of dolomitic shales dolomicrites with bioturbation structures horizons grained dolomicrites fenestral structures laminations bioturbation structures gypidulids tentaculoids crinoids algae Thamnopora sp. asselages Text-fig. 11. Lithological succession and in the Wszachówka River valley near Lagów Icriodus corniger retropressus Icriodutruvei SSSS SSS S S 160 KRYSTIAN WÓJCIK Wszachów quarry dolomitic shales/ claystones grained (intraclast-ooid) dolomites dolomicrites crinoid dolomites nodular dolomites bioturbation horizonts susceptibility magnetic MS major trends MS average bioturbation structures crinoids intraclasts, ooids laminations, stromatolites breccias ~15.31 EE1 Nowy Staw Meer ~6.87 28.05 m ~18.09 3 ~11.25 54.4 m Icriodutruvei S S 2 ~24.03 S Wszachów Meer S EE2 46 ~16.34 S 1 ~22.35 Text-fig. 12. Lithological succession, and in the Wszachów quarry section 161 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Package A: medium-bedd dolomicrites with flat lamination intercalated by black dolomitic shales (up to 3 m thick). Laminations are regular, flat and continuous; Package B: thick-bedd grained (intraclast) dolomites with erosional lower surfaces. They are characterized by a flaser texture expressed by alternating micritic matrix and 2­5 cm thick grained (intraclast) laminae/strips; Package C: medium-bedd laminated dolomicrites with stromatolitic domes at the tops of the beds. Irregular, wavy lamination and thin intraformational breccia horizons occur within; Package D: yellowish to greenish variegated sandy siltstones and claystones a dozen or so cm thick. The scribed packages are arranged into 8 ABCD cyclothems, the of which ranges between 2 and 4.5 m. Unit 4 (22 m thick) is composed of a cyclic succession of the following lithological packages: Package A: black dolomicrites with (occasional) flat lamination (dozen or so cm thick); Package B: light-grey grained (ooid-intraclast) dolomites with flaser lamination and erosional lower surfaces. 2­5 cm thick laminae/strips of ooid and intraclast dolosparites cut the dolomicritic matrix; Package C: grey-green dolomicrites with wavy laminations, stromatolites and intraformational breccias; Package D: greenish to yellowish dolomitic siltstones and claystones with sparry laminae/ lenses. The scribed posits are arranged into 5 ABCD cyclothems, the of which ranges between 2.4 and 3.4 m. This cyclicity disappears in the middle part of the unit, in which a thick package of laminated dolomicrites appear. Grained dolomites reappear in the upper part. Distinctive beds of white dolomitic oosparites occur at the top of the section. Biostratigraphy Only 3 specimens of Icriodutruvei have been obtained from 3 samples (25 dissolved). They indicate the Polygnathus costatus costatus Zone or younger (Textfig. 17). The conodont results and correlation are broadly discussed in Wójcik (2013 and in preparation). A collection of 481 samples rived from 15-cm intervals has been measured. Average MS is 14.77× 10-8m3/kg. Seven major MS fluctuations (1 ­ ) are intified (Text-fig. 14): Trend 1 is 5.2 m thick and eraces the lower part of unit 1. Average MS is 22.35×10-8m3/kg; Trend 2 is 9.6 m thick and eraces the middle part of unit 1. Average MS is 24.03×10-8m3/kg; Trend 3 is 12.1 m thick and ranges from the upper part of unit 1 to the upper part of unit 2. Average MS is 18.09×10-8m3/kg; Trend EE1 is 10 m thick and ranges from the uppermost part of unit 2 to the lower part of unit 3. Average MS is 15.31×10-8m3/kg; Trend EE2 is 10.2 m thick and eraces the middle part of unit 3. Average MS is 16.34×10-8m3/kg; Trend FE1 is 10 m thick and ranges from the upper part of unit 3 to the lower part of unit 4. Average MS is 11.25×10-8m3/kg; Trend is 9.15 m thick and eraces the middle part of unit 4. Average MS is 6.87×10-8m3/kg. The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Winna quarry The location of the Winna section is 50°4622.55N, 21°740.75E (Pl. 6). The Winna quarry is located between the villages of Nowy Staw, Winna and Wszachów, on the northern si of the Wszachówka River. vonian dolomites belonging to the upper part of the Unfossiliferous Crypto and Fine-crystalline Dolomites Unit of Narkiewicz and Olkowicz-Paprocka (1981) and to the lower part of the Kowala Formation (Narkiewicz 1991) are exposed in the quarry. A complete succession crops out along the western wall on the 2nd quarrying level. A 42 m thick lower part of the succession watudied in 2011. The succession has been subdivid into 5 lithological (Text-fig. 13 and Pl. 5). 70 lithological samples, 30 polished slabs, 21 thin sections, 12 conodont samples and 335 measurements were investigated. Unit 1 (15 m thick) is composed of a cyclic succession of the following lithological packages: Package A: thick-bedd light grey grained (oolite and intraclast) dolomites with flaser textures. All lower surfaces have an erosional character. In the lower part of the unit grained dolomites constitute separate beds; in the upper part, they occur as lenses within the dolomicrites. Flaser textures are expressed as grained (ooid-intraclast) intercalations within the dolomicritic matrix. Package B: green-grey dolomicrites with wavy lamination and stromatolites. The wavy lamination occurs 162 KRYSTIAN WÓJCIK within internal structures of the stromatolitic domes, and only in the external part are their shapes parallel to the domes. Numerous horizons and lenses of intraformational breccias occur within the laminites. Package C: grey and grey-green dolomicrites with flat lamination; Package D: yellow to green-yellow sandy-muscovite dolomitic siltstones and sparry laminae/strips (evaporation pseudomorphs). The scribed posits are arranged into 11 ABCD cyclothems with an average of ca. 1 m. Unit 2 (7.8 m thick) is composed of 50­100 cm thick beds of green-grey dolomicrites with subtle flat lamination. A 50 cm thick bed of rhythmically laminated dolomite, a 40 cm thick nodular dolomicrite (bioturba- tion structures) and a 30 cm thick intraformational breccia/regolith with an iron coat occur at the top of the unit. Unit 3 (11.3 m thick) is composed of 70 to 250 cm thick beds of fine- to medium-crystalline dolosparites. Numerous remnants of stromatoporoids and corals occur, concentrating in flat horizons within the beds. Unit 4 (9.6 m thick) is composed of blue-green weathering, 10­60 cm thick packages of sandy dolomitic siltstones with sparry laminae/strips intercalated by thick beds of dolosparites. Unit 5 is composed of a thick succession of thick-bedd dolosparites with stromatoporoid and coral remnants. .. . . .. . . . . . . .. . . .. . .. . Winna quarry motely sandy siltstones with evaporatic pseudomorphoses dolomitic shales/ claystones laminated dolomicrites/ stromatolites grained (intraclast-ooid) dolomites dolosparitetromatoporoid-coral dolosparites dolomicrites zebra dolomites with intraformational breccia stromatolites laminations regolithes ooids intraclasttromatoporoid rugose corals . .. . . . .. . .. . . . . . . . . . .. . .. . . .. .. . . . . . . .. . . . . . .. . . .. . .. . . .. . . . .. . . .. . . .. . . .. . . . .. . . .. . .. . . . . .. . . .. . . .. . . . . .. . . . .. . . . .. . . . . ... .. .. .. . . . .. .. . . .. . . . . . . .. . . .. . .. . . .. . . .. .. . . .. .. . . .. .. .. .. .. . . . . .. .. . . .. .. . . .. .. .. .. .. . . . . .. .. . . .. .. . . .. .. .. .. .. . Nowy Staw Meer KOWALA Formation 4 24.7 m Text-fig. 13. Lithological succession and in the Winna quarry section 163 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Biostratigraphy No were found in the 12 dissolved samples. A collection of 355 samples rived from 12.5 cm intervals has been used for MS measurements. No evint MS fluctuations are found (Text-fig. 13). The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Janczyce-1 borehole The location of the Janczyce-1 borehole is 50°4538.27N, 21°1328.96E (central-eastern part of the Kielce Region). The core is posited in the National Geological Archive in Halinów. The 1251.6 m ep Janczyce-1 borehole waituated in the Piotrów Syncline, east of the town of Lagów. A report on the complete vonian succession was published by Narkiewicz and Olkowicz-Paprocka (1983) and Narkiewicz (1991). The lithologies of the interval between 1033.0 and 1251.6 m have been scribed and measurements have been ma (Text-fig. 14). Unit 1 (pth: 1246.0­1251.6 m) is composed of light grey fine-grained quartz sandstones with flat bedding intercalated by bioturbated horizons of wavy-laminated dolomitic siltstones/heterolits. The upper boundary has been fined arbitrarily at the level where the grain-supported framework disappears, and quartz grains become suspend within the dolomitic matrix. Unit 2 (pth: 1246.0­1203.0 m; 37 m thick) is composed of a cyclic succession of the following packages: Package A: 20 to 150-cm thick beds of thamnoporoid dolomites with 30­60 cm thick intercalations of intraclast dolomites with minor contributions of coral and crinoid tritus; Package B: up to a few metres thick dolomicrites. Wavy laminations and/or nodular structures occur in the two lowermost cyclothems. Very thin intercalations of intraclast grained dolomites appear. Package C: 2 to 4 m thick grey-green dolomicrites with fenestral fabrics. The fabric is probably connected with a primary laminated texture. Small stromatolitic domes appear in the topmost part of some of the packages. The packages are arranged into 5 ABC cyclothems with es of 6 m, 9 m, 13.5 m, 3.5 m and 5 m respectively. Unit 3 (pth: 1203.0­1182.2 m; ca. 20 m thick). It is represented by interbedd packages of nodular dolomicrites and bioturbated horizons with grained laminae. The proportions of these posits varies along the succession. In the lower part (pth: 1203.0­1194.8 m), structureless or subtly laminated dolomicrites predominate. Wavy-laminated dolomicrites occur above. Single laminae of intraclast grained dolomites with single brachiopod and crinoid remains also occur. The gree of bioturbation increases in the upper part of the unit (pth: 1194.8­1182.2 m), in which a fine nodular texture is common. Chondrites-dominated structures concentrate in individual horizons. Single grained laminae, dominated by crinoid and brachiopod tritus occur in this part of the unit. Unit 4 (pth: 1182.2­1097.7 m; ca. 70 m thick). The lower part of the unit (pth: 1182.2­1155.0 m) is dominated by up to a few metres thick packages of dolomicrites with wavy lamination interbedd with up to 1 m thick bioturbation horizons (Chondrites-dominated). Rare laminae of brachiopod-crinoid remains occur, as well as monospecific brachiopod lumachelles (pth 1167.8 m). Blue-weathering nodular dolomicrites occur in the upper part of the unit (pth: 1155.0­1107.2 m). The more or less isolated nodules are emphasized by black clay laminae/strips. In some places, especially in the upper part, the nodular structure disappears or becomes more regular to form a flat lamination. The last fossils, including shelly fossils and ichnofossils, occur there. Unit 5 (pth 1107.2­1097.7 m; 10.5 m thick) is composed of dark grey dolomicrites void of fossils and bioturbation structures. Subtle flat lamination appears in the upper part of the unit. It is more evint at the top, where a 15 cm thick stromatolitic dome occurs. Unit 6 (pth: 1097.7­1023.0 m; 74 m thick) is composed of dolomicrites with subtle lamination and thick beds of intraformational breccias and grained dolomites. The grained dolomites occur in up to 1.5 m thick beds. Flaser wavy lamination, expressed as alternating micritic and intraclast-ooid grained laminae, occur within the unit. In the middle part of the succession (pth: 1097.7­1079.7 m), several packages of 1­1.5 m thick oolitic dolomites are clearly visible. A collection of 937 samples rived from 25-cm intervals has been measured. Average MS is 33.34× 10-8m3/kg. Nine major MS fluctuations/trends (BE ­ ) are intified (Text-fig. 14): 164 KRYSTIAN WÓJCIK Janczyce-1 dolomicrites dolomicrites with fenestral structures dolomicrites with wavy laminations thamnoporid dolomicriteandstones oolite/intraclats intercalations laminated dolomicrites nodular dolomicrites dolomicrites with bioturbation horizons highly bioturbated dolomicrites tectonic breccias intraformational brecciatromatolites laminations bioturbation structures ooids 1 Th pth .. .. .. .. .. .. -. .- -. .- -. .- MS major trends MS average gastropods crinoids brachiopods rugose corals Thamnopora sp. Janczyce-1 simplified SS SSSS ... . .. Nowy Staw Meer 1107.2 m S Nowy Staw Meer FE1 EE2 EE1 3 1203.0 m Wsz. . S 2 1 Janczyce Meer S S CE S BE BE4 Janczyce Meer BE3 Wszachów . 1097.7 m 1246.0 m ....................... . -. . -. . -. . -. .- - .- - .- - .- ...................... ....................... BE2 .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . -. . -. . -. . -. . -. . -. .- - .- - .- - .- - .- - .- - - . -. . - ..-.. .-..-. .-.. --..-.. . . -. . . . .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..... BE1 Text-fig. 14. Lithological succession and in the Janczyce-1 borehole core 165 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Trend BE ranges from 1246.0 to 1180.0 m pth, average MS is 42.48×10-8m3/kg. The trend iubdivid into 4 minor MS fluctuations: BE1 ­ BE4; Trend CE ranges from 1180.0 to 1155.25 m pth, average MS is 36.37×10-8m3/kg; Trend 1 ranges from 1155.25 to 1132.5 m pth, average MS is 48.6×10-8m3/kg; Trend 2 ranges from 1132.5 to 1123.0 m pth, average MS is 24.03×10-8m3/kg; Trend 3 ranges from 1123.0 to 1109.5 m pth, average MS is 38.3×10-8m3/kg; Trend EE1 ranges from 1109.5 to 1099.5 m pth, average MS is 33.68×10-8m3/kg; Trend EE2 ranges from 1099.5 to 1091.0 m pth, average MS is 33.39×10-8m3/kg; Trend FE1 ranges from 1091.0 to 1080.0 m pth, average MS is 27.06×10-8m3/kg; Trend ranges from 1080.0 to 1069.5 m pth, average MS is 15.69×10-8m3/kg; The MS results and correlation are broadly discussed in Wójcik (2013 and in preparation). Zarby 2 borehole (Tarnowska 1976, Malec 1984b, Fijalkowska-Mar and Malec 2011) The location of the Zarby 2 borehole is 50°4702.79N, 21°0247.23E (central part of the Kielce Region; Lagów Syncline). The core is posited in the National Geological Archive in Leszcze. The 1375 m ep Zarby 2 borehole cored the Lower vonian ­ succession. Tarnowska (1976) divid the clastic part of the succession into 4 lithological : Lower Siltstone Meer with Volcanites (1146.4­1218.2 m pth); Middle Sandstone Meer (1131.4­1146.4 m pth), Upper Siltstone Meer with Volcanites (1089.7­1131.4 m pth), and Upper Sandstone Meer (1080.1­1089.7 m pth). The first unit is fined as the Haliszka Formation, the remaining three belong to the Winna Formation (FijalkowskaMar and Malec 2011). The siliciclastics are overlain by sandy dolomites with remnants of corals and stromatoporoids (1075.6­1080.1 m pth), followed by the Dolomites. Malec (1984b) and Fijalkowska-Mar and Malec (2011) noticed the presence of carbonate beds with within the upper part of the Upper Siltstone Meer. proposed herein. The lithostratigraphical are fined (Text-figs 15 and 16) according to "Polskie Zasady Stratygrafii" (Polish Stratigraphical Co) fined by Racki and Narkiewicz (2006). BARANIA GÓRA DOLOMITE AND LIMESTONE FORMATION (Polish name: formacja dolomitów i wapieni z Baraniej Góry) rivation of name. From Barania Hill in the Zbrza Anticline, from where the most complete succession has been scribed. finition. The Barania Góra Formation is composed of various types of fossiliferous or bioturbated dolomites and limestones (belonging to separate ), which overlie the clastic posits of the Winna Formation and unrlie the unfossiliferous dolomites of the . Stratotype and hypostratotypes. The type area of the Barania Góra Formation is located in the south-western part of the Kielce Region ­ in the Zbrza Anticline, on the western slope of Barania Hill, along the road scarp at the southern end of the village of Zbrza (Text-figs 5 and 6 and Pl. 6). The section in Zbrza is the stratotype section of the lower part of the formation. The Dyminy-2 borehole core (at 45.0 ­ 96.0 m pth) is the stratotype of the upper part of the formation (the core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce). The hypostratotypes for the eastern part of the Kielce Region are fined in the Jurkowice section and in the Janczyce-1 borehole core. Boundaries. The Barania Góra Formation is unrlain by the Winna Formation and overlain by the . The lower boundary is fined at the base of a carbonate succession. In the western part of the Kielce Region this is the base of the Porzecze, Dbska Wola or Dyminy . It can be traced in the Zbrza (base of unit 6, Text-fig. 6), Brzeziny (base of unit 3, Text-fig. 7), (base of unit 3, Text-fig. 8) and Skrzetle (see scription in Malec 1993) sections, and in the Dyminy-2 (137.7 m pth, see Tarnowska 1987), Dbrowa D5 (71.5 m pth, see Tarnowska and Malec 1987) and (19.2 m pth, see Kowalczewski 1979 and Fijalkowska-Mar and Malec 2011) borehole cores. In the eastern part, it can be traced in the Jurkowice section (base of unit 1, Text-fig. 10) and LITHOSTRATIGRAPHY Based on the geological documentation presented, a formal lithostratigraphical scheme for the upper Emsian and lower of the Kielce Region of the HCM is 166 KRYSTIAN WÓJCIK ? ? Brzeziny E MIDDLE VONIAN costatus ? ? Jurkowice ~ ~ .. ..~ ~ . .. .~ . .. .~ . .. .~ . . e ~ ~ ~ ~ b la M Porzecz Dbska Wo ~ . .. ~ . .. ~ . .. ~ .. ..~ .. ..~ . .. ~ . .. ~ . . ~ ~ . . ~ . . ~ . . ~ . ~ .. ~ . . ~ .~ . .~ . ..~ . ~ . . ~ . .. ~ . .. ~ . .. ~ . .. ~ . .. ~ . .. ~ . .. ~ .WINNA. Formation ~ . .. ~ . .. . . . ~ . . ~ . ~ . ~ . ~ . ~ . ~ . ~ . ~ . ~ .. ~~ .1. ~ . ~~ . . ~ . ~ . . ~ . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . . . ~ . . ~ . . ~ . . ~ . . ~. . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~. . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~ ~ ~ ~ ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. 6 Dbrowa inated dolomites and sandy dolomites arranged (occasionally) into cyclic successions (); fossiliferous limestones, marls, marly shales with brachiopod lumachelle intercalations (Dbrowa Meer); thin-bedd dolomites with horizons of bioturbation structures (Brzeziny Meer); coral-bearing dolomicrites, laminated dolomicrites and fenestral dolomicrites arranged into cyclic successions (Janczyce Meer); and thick-bedd nodular dolomites and crinoidal dolomites with horizons of bioturbation structures (). Origin. The formation represents a shallow-marine carbonate-clastic sedimentation during the earliest stage of the vonian transgression, before constitution of a carbonate platform. The posits belonging to particular originated in different sedimentary environments; from lagoonal, through stromatoporoid-coral shallows to open-marine areas (occasionally below storm wave base) on a distally-steepening ramp (Wójcik 2013 and in preparation). Age. The formation is early in age. The conodont material collected indicates the interval between the Polygnathus costatus Zone and the lower part of the P. c. costatus Zone (Wójcik 2013 and in preparation), albeit a latest Emsian age is postulated by FijalkowskaMar and Malec (2011) for the lowermost part of the formation (Porzecze Meer). The age is confirmed by the Janczyce M in the Janczyce-1 borehole core (1246.0 m pth, Textfig. 14). The upper boundary is fined as the last occurrence of bioturbated or fossiliferous dolomite. In the western part of the region it can be traced in the Dyminy-2 borehole core (45.0 m pth, see Tarnowska 1987). In the eastern part, it is exposed in the Jurkowice (base of the unit 5, Text-fig. 10) and Wszachów (base of the unit 3, Text-fig. 3) sections, and in the Janczyce1 borehole core (1107.2 m pth). Occurrence and . The Barania Góra Formation is limited to the Kielce Region of the Holy Cross Mountains. The formation is divid into six , but a consirable lithological variety occurs between the eastern and western parts of the region. Two ­ the Janczyce and Jurkowice , with a coined of ca. 130 m, are limited to the eastern part. Four ­ the Porzecze, Dbska Wola, Dbrowa and Brzeziny , with a coined of up to ca. 70 m, are limited to the western part. Additionally, in the western part of the Kielce Region, a lateral lithological variability occurs: the Dbrowa Meer is limited to the north-western and south-western part of the region and is absent in the central-western part. . The Barania Góra Formation inclus pyritebearing and siritic claystones (Porzecze Meer); coral-bearing dolomites, micritic dolomites, wavy-lam- L. VONIAN EMSIAN patulus Text-fig. 15. Lithostratigraphical scheme around the upper Emsian and in the Kielce Region of the Holy Cross Mts. (longitudinal organization) 167 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. LOWER VONIAN MIDDLE VONIAN EMSIAN patulus costatus ? Acinosporites apiculatus­Grandispora protea [AP] ? Grandispora Grandispora protea [Pro] ? velata [Vel] Kowala 1 Dbrowa D-5 Szydlówek Skrzetle Dyminy-2 Brzeziny D . .. . ~ . . . ~ ~ .~ . P . ~~ ~ .. ~ . . DW . .. .~ .. . .. . ~ .. . ~ ~. ~ .. . . ~ . ~.. . .~ . . . .. ~.. .~.. .~. .~. . . ~.. . ~. ~ ~ ~ ~ .. ~ . . ~ . . ~ .~. .~ ~. ~ . . ~ . ~ . ~ . .~ . ~ . . ~ . . ~ . . ~ . ~ .. ~ . ~ .. ~ .. ~ . ~ .. ~ ~ ....~ ....~ .... ~ . . ~ . . ~. ~. ~. ~. . . .~. . . .~. . . .~. . . .~. ..~. . . .~. . .~. . .~. ~ .~. . . ~ ~ ~ ~ WINNA Formation . ~. ~. ~ ~ . ~ . . ~ . . ~ . . ~ .~~ . ~~ .. ~~ 1 .~~ .. . ~ .. ~ ~ . . ~ .. . ~ .. . ~ .. . . ~ . . . . ~. ~. . ~. ~. . ~. ~. . ~ . ~ ~ ~ ~ ~ . . ~. . ~. . . . ~ . . ~ . . ~ . . ~ . .~ . . ~ . . ~ . . ~ . . ~ . . Chciny Zbrza Brzeziny ? ? Winna Nowy Staw 1 MIDDLE VONIAN Wszachów Wszachów costatus Jurkowice Wszachówka River Janczyce-1 Janczyce 1 . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~. . ~. . ~. . ~ . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . ~ ~ ~ ~ ~ ~ ~ ~ .. . ~. .. . ~. .. . ~ .. . ~. .. . ~ .. . ~ . . ~ . . ~ . . ~ . . .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ .. .. ~ . ~ ~ ~ . ~ ~. ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . WINNA Formation .. .. .. . . ~ ~ ~ ~ ~ ~ ~1 ~ ~ . . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~ . . ~~. .. .~~ . .. .~~. .. .~~. .. .~~ .. .~~. .. .~~ . .. .~~. .. .~~. .. ~ . .. .~~. .. .~~ . .. .~~. .. .~~. .. .~~ .. .~~ .. . ~ .. .~~ . . . . . ~ . . ~ . . ~ . . ~ . . ~. . ~ . . ~ . . ~ . . ~ . . . . ~ . . ~ . . ~ . . ~ . . ~. . ~. . . Zarby 2 L. V. EMSIAN patulus Jurkowice Text-fig. 16. Lithostratigraphical schemes around the upper Emsian and in the Kielce Region of the Holy Cross Mts. (latitudinal organization) supplemented by palynostratigraphical data of Filipiak (2011). A ­ western part of the region, B ­ eastern part of the region. P ­ Porzecze Meer, DW ­ , D ­ Dbrowa Meer 168 KRYSTIAN WÓJCIK palynostratigraphical data of Fijalkowska-Mar and Malec (2011) and Filipiak (2011). Porzecze Claystone Meer (Polish name: ogniwo ilowców z Porzecza) rivation of name. From the borehole core, in which a complete succession was available. Earlier names. The meer was earlier distinguished as: the Ore-bearing Claystones and Siltstones Meer (Tarnowska and Malec 1987, Fijalkowska-Mar and Malec 2011), the Ore-bearing Claystones (Malec 1986, 1993), the Pyrite-bearing Claystones from Szydlówek (Malec and Stuncki 1988) and the Pyrite-bearing and Siritic Claystone Meer (Fijalkowska-Mar and Malec 2011). finition. The Porzecze Meer overlies the clastics of the Winna Formation and unrlies the succession of dolomites or limestones in the northern and north-western parts of the Kielce Region. The meer is fined as a package of brown, black and yellowish pyrite-bearing claystones and siltstones with sirite concretions. Stratotype and hypostratotypes. The town of Kielce is the type area of the Porzecze Meer. The stratotypes of the lower and upper parts of the meer are located in the Skrzetle and Szydlówek sections respectively. Boundaries. The Porzecze Meer is unrlain by the Winna Formation and overlain by the or the Brzeziny Meer (if the Dbrowa Meer is absent). The lower boundary is fined as the base of the pyrite-bearing or limonite-bearing claystone package that unrlies the carbonate succession. It can be traced in the Skrzetle section and in the Porzecze IG5A borehole core at 12.9 m pth. The upper boundary is fined as the base of the first continuous bed of dolomite or limestone. It is exposed in the Szydlówek section and in the (19.2 m pth) and Dbrowa D5 (at 71.5 m pth) borehole cores. Occurrence and . The Porzecze Meer occurs in several sections in the northern and north-western part of the Kielce Region (Text-fig. 5). The meer occurs in the Szydlówek (30 m thick; see scription in Malec and Stuncki 1988) and Skrzetle (5.7 m thick; see scription in Malec 1993 and 2001) sections, as well as in the (5.4 m thick; see scription in Kowalczewski 1979, Fijalkowska-Mar and Malec 2011; Text-fig. 9) and Dbrowa D5 (71.5 ­ 103.5 m pth; see scription in Tarnowska and Malec 1987) borehole cores. The presence of similar posits was also noticed in the Stara Góra IG-1 and Wola Zamkowa 2 borehole cores (Stuncka 1983), as well as in old shafts near the villages of Daleszyce, Górno, Bakowice and Piotrów. The meer disappears in the central and southern parts of the Kielce Region. . The Porzecze Meer is composed of brown to black structureless or wavy-laminated claystones with frooidal pyrite, yellowish structureless claystones with sirite concretions, and dolomitic claystones and siltstones (Tarnowska and Malec 1987, Malec and Stuncki 1988, Malec 1993). Fossils. The numerous benthic agglutinated foraminifers represent an autochthonous asselage. Rare crinoids, remnants of bryozoans, brachiopods (including Chimaerothyris dorowiensis), tentaculoids and occur in the upper part of the unit, probably of allochthonous origin (Tarnowska and Malec 1987, Malec 1987, Malec and Stuncki 1988, Malec 1993). . Not measured. Origin. The Porzecze Meer representhallow-marine lagoonal sedimentation, with open marine influences in the upper part of the unit (Wójcik 2013 and in preparation). Age. The asselage of collected by Malec (1993) and discussed in Fijalkowska-Mar and Malec (2011) indicates the interval between the uppermost Emsian (Polygnathus costatus patulus conodont Zone) and lower (Polygnathus costatus conodont Zone). Wójcik (2013 and in preparation) suggested an early age only. Dbska Wola Dolomite Meer (Polish name: ogniwo dolomitów z Dbskiej Woli) rivation of name. From the village of Dbska Wola, where the posits were intified for the first time (Filonowicz 1973). Earlier names. The meer was earlier distinguished as: the Dolomite Meer in Fijalkowska-Mar and Malec (2011) and the Dolomitic Unit below the Dbrowa Horizon in the Dyminy-2 borehole core in Tarnowska (1987). finition. The is composed of dolomites (dolomicrites and fine-crystalline dolosparites with occasional abundant corals), which unrlie the Dbrowa Meer. 169 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Stratotype and hypostratotypes. The type area is located in the Zbrza Anticline, on the western slope of the Barania Hill, along the road scarp at the southern end of the village of Zbrza. The Zbrza section is the stratotype section of the meer (Text-figs 5, 6 and Pls 1, 6). The hypostratotype is established in the Dyminy-2 borehole core between 137.7 and 110.0 m pth. Boundaries. The is unrlain by the Winna Formation or the Porzecze Meer and overlain by the Dbrowa Meer. The lower boundary is fined as the base of a dolomitic succession ­ the base of brown dolomitic claystones or dolomicrites. It was established in the core at the base of the first dolomite bed (19.2 m pth), in the Brzeziny section at the base of unit 3 and in the Zbrza section at the base of unit 6. The upper boundary is fined as the base of limestones, marls or marly shales of the Dbrowa Meer. It was established at the top of unit 10 in the Zbrza section, at the top of unit 5 in the Brzeziny section and at the top of the last dolomite bed in the core (39.5 m pth). Occurrence and . The occurs in the south-western part of the Kielce Region (Text-fig. 5, Pl. 6). It can be traced along the Chciny and Dyminy Anticlines. The meer occurs in the Zbrza ( from 6 to 10, 16 m thick; Text-fig. 6 and Pls 1, 6) and Brzeziny ( from 3 to 5, 22.5 m thick; Textfig. 7 and Pls 2, 6) sections, as well as in the Dyminy2 (between 137.7 and 110.0 m pth, 28 m thick; see scription in Tarnowska 1987) and (between 19.2 and 39.5 m pth, 15.6 m thick; see scription in Kowalczewski 1979 and FijalkowskaMar and Malec 2011; Text-fig. 9) borehole cores. The presence of dolomites unrlying the Dbrowa Meer has also been noted near the villages of Szczecno and Osiny. . The lowermost part of the unit is composed of brown dolomitic claystones and dolomicrites. In the middle part, the unit is composed of Thamnopora dolomicrites, fine-crystalline dolosparites with corals, marly dolomicrites with wavy lamination and dolomicrites, arranged in 5 to 6 cyclothems. The upper part of the meer is composed of stromatoporoid-coral biostromal dolomites. In the Brzeziny section, corals are absent and the cyclothems are not recognized, albeit cyclicity is visible on the MS curve. . The meer is generally characterized by high MS values, over 40×10-8 m3/kg in the lower part, creasing towards the top. The main asymmetric creasing trend A corresponds to the meer. Minor asymmetric (creasing) MS fluctuations correspond well to particular lithological cyclothems. The lower part of trend B begins in the upper part of the meer. Origin. The representhallowmarine, temporary cyclic carbonate sedimentation within lagoonal environments with isolated stromatoporoid-coral shallows and swells (Wójcik 2013 and in preparation). Age. Filipiak (2011) proved the latest Emsian­early age of the meer (protea palynostratigraphic Zone) in the Dyminy-2 borehole core and in the Zbrza section. Dbrowa Limestone Meer (Polish name: ogniwo wapieni z Dbrowy) rivation of name. From the village of Dbrowa (northern part of Kielce), in which the posits were recognized for the first time (Pusch 1833, Gürich 1896). Earlier names. The meer was earlier distinguished as: the Dbrowa Horizon in Gürich (1896) and Filonowicz (1973), the complex VIII in Pajchlowa (1957), the Kielce Limestone Unit in Tarnowska (1987), the Grzegorzowice Limestone Meer in Malec (2002) and the Dbrowa Limestone Meer in Tarnowska and Malec (1987), Malec (2005), Fijalkowska-Mar and Malec (2011), and Filipiak (2011). finition. The Dbrowa Meer was fined by Malec (2005) in the Grzegorzowice-Skaly section in the Lysogóry Region of the Holy Cross Mountains. A refined finition of the meer is proposed herein. The unit is composed of grey to greenish micritic limestones and fossiliferous grained and flaser limestones, marls and marly shales with a subordinate contribution of dolomites in separate internal packages. The presence of Chimaerothyris dorowiensis is an auxiliary criterion for distinguishing the meer. Stratotype and hypostratotypes. Malec (2005) established the Grzegorzowice-Skaly section in the Lysogóry Region as the stratotype section of the Dbrowa Meer. The Zbrza section is proposed herein as the hypostratotype section for the Kielce Region (Text-figs 5, 6 and Pls 1, 6). Boundaries. The Dbrowa Meer is unrlain by the Dbska Wola or the Porzecze and overlain by 170 KRYSTIAN WÓJCIK the Brzeziny Meer. The boundaries of the unit surround the lithosome of limestones, marls or marly shales within a dolomitic background. The lower boundary is fined as the base of the first limestone or marl bed or at the base of the first marly shales package. It can be traced in the borehole core at the base of the first limestone layer (39.5 m pth), in the Brzeziny section at the base of unit 6 and in the Zbrza section at the base of unit 11. The upper boundary is fined as the top of the last limestone bed. It can be traced at the top of unit 7 in the Brzeziny section. Occurrence and . The Dbrowa Meer occurs in both the Lysogóry and Kielce regions of the Holy Cross Mountains, albeit belonging to two different . In the Kielce Region, the meer is limited to the western part of the area (Text-fig. 5). The of the unit increases to the north-west and to the southwest. The unit is absent along the Dyminy Anticline in the western-central part of the area. The Dbrowa Meer occurs in the Zbrza ( 11 to 16, 28 m thick at least; Text-fig. 6 and Pls 1, 6) and Brzeziny ( 6 and , ca. 10 m thick; Text-fig. 7 and Pls 2, 6) sections, as well as in the (from 39.5 m pth to the end of the core, 30 m thick at least; Text-fig. 9), Dyminy-2 (96.0­109.0 m pth, 13 m thick; see scription in Tarnowska 1987) and Dbrowa D5 (66.0­71.5 m pth; see scription in Tarnowska and Malec 1987) borehole cores. The occurrence of limestones with Chimaerothyris dorowiensis was also noticed near the villages of Szczecno and Osiny. In the Lysogóry Region, the unit occurs in the Grzegorzowice-Skaly section (35 m thick; see scription in Malec 2005) and in the Kowalkowice 1 borehole core (111.2­92.5 m pth, ca. 10 m thick; see scription in Malec 2005). . The Dbrowa Meer is composed of micritic, grained and flaser limestones alternating with marls and marly shales. Marly intervals concentrate in the lower part of the unit in the Brzeziny and Zbrza sections. Numerous brachiopod lumachelles occur in these intervals. Grained and flaser limestones dominate in the lower and middle parts of the unit and rece in the upper part, in which micritic limestones predominate. Thin packages of dolomites occur within the unit in the Grzegorzowice-Skaly and Zbrza sections. Fossils. Shelly-fossils concentrate within grained beds and laminae/strips. Chimaerothyris dorowiensis, Athyris concentrica and Chonetes angustestriata are the most abundant brachiopods. Numerous tentaculoids, crinoids, gastropods, corals, and rare trilobites, holothurids, , microconchids, scolecodonts, bryozoans, hereloids, algae, ostracods and molluscs are present. Chondrites isp. and Skolithos isp. are the most numerous ichnofossils. . The Dbrowa Meer has generally high MS values in the lower part of the unit (from 35 to 40 ×10-8 m3/kg), creasing towards its top. Higher MS values at the base of the unit result from the greater content of marls and marly shales. The major asymmetric trend B generally corresponds to the meer and can be traced in all sections. Minor 3 to 6 MS fluctuations within trend B are also distinguishable. The major symmetric C and D trends are distinguished in the upper part of the unit in the Zbrza section. Origin. The Dbrowa Meer represents open-marine carbonate-clastic sediments posited on the middle and outer ramp, occasionally below the storm wave base (Wójcik 2013 and in preparation). Age. The stratigraphical range of the Dbrowa Meer spans from the upper part of the Polygnathus costatus conodont Zone to the lower part of the Polygnathus costatus costatus conodont Zone, within the lower . The age is proved by numerous , collected and scribed by Wójcik (2013 and in preparation). Brzeziny Dolomite Meer (Polish name: ogniwo dolomitów z Brzezin) rivation of name. From the Brzeziny section, in which a complete succession is available. finition. The Brzeziny Meer is a dolomitic unit unrlying the in the western part of the Kielce Region. As opposed to the , the meer contains horizons of bioturbation structures and thin grained intercalations. Dolomitic limestones occur subordinately at its base. Stratotype and hypostratotypes. The Brzeziny section is the stratotype section of the lower part of the unit (Text-figs 5, 7 and Pls 2, 6). The Dyminy-2 borehole core (45.0 and 96.0 m pth) is the stratotype section of the upper part of the unit (the core is posited in the National Geological Archive in the Holy Cross Branch of the Polish Geological Institute ­ National Research Institute in Kielce. Boundaries. The Brzeziny Meer is unrlain by the Winna Formation or by the Porzecze and Dbrowa , and is overlain by the . 171 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. The lower boundary is fined as the base of the first dolomite bed above the Dbrowa Meer or above the Winna Formation or the Porzecze Meer, if the Dbrowa Meer is absent. The boundary can be traced in the Brzeziny section at the base of unit 8, in the section at the base of unit 3, in the Skrzetle and Szydlówek sections above the Porzecze Meer, as well as in the Dyminy-2 (at 96.0 m pth) and Dbrowa D5 (at 66.0 m pth) borehole cores. The upper boundary is fined at the top of the last bed with bioturbation structures. It can be traced in the Brzeziny and Zbrza sections, as well as in the Dyminy-2 borehole core (at 45.0 m pth). Occurrence and . The meer occurs in the western part of the Kielce Region in the Brzeziny (unit 8, 15 m thick at least; Text-fig. 7 and Pls 2, 6) and ( 3 and 4, 26 m thick at least; Text-fig. 8 and Pl. 6) sections, as well as in the Dyminy-2 (45.0­96.0 m pth, ca. 50 m thick; see scription in Tarnowska 1987) and Dbrowa D5 (5.2­66.0 m pth; see scription in Tarnowska and Malec 1987) borehole cores. posits includ in the meer were also scribed from the Skrzetle (Malec 1993, 2001), Szydlówek (Malec and Stuncki 1988) and Chciny (Glazek et al. 1981) sections. The Brzeziny Meer also occurs near the villages of Zbrza, Szczecno and Osiny. . The Brzeziny Meer is composed of thinbedd reddish structureless dolomicrites with horizons of bioturbation structures and grained laminae/ strips, intercalated with brown dolomitic claystones. Small stromatolites and fenestral fabrics appear sporadically. A package of dolomitic limestones occur at the base of the unit in the section. Fossils. Allochthonouhelly fossils occur within the grained intercalations. Single crinoids, tentaculoid remains, ostracods and are present. Paraautochthonous gypidulid asselages appear on some of the surfaces. Chondrites isp. predominate among the ichnofossils. . The meer has generally low MS values; ca. 22×10-8 m3/kg in Brzeziny section and 18×10-8 m3/kg in the lower part to 8 ×10-8 m3/kg in the upper part of the section. The major trends D correspond to the meer in the Brzeziny section, the major trends C, D and E occur in the section. Origin. The Brzeziny Meer representhallow-marine carbonates posited on the outer si of a distally steepened ramp (Wójcik 2013 and in preparation). Age. The meer is in age, not olr than the Polygnathus costatus conodont Zone in the Skrzetle and Szydlówek sections (Fijalkowska-Mar and Malec 2011) or than the Polygnathus costatus costatus conodont Zone in the Zbrza, Brzeziny and sections. The upper boundary is not dated, and probably runs within the Polygnathus costatus costatus conodont Zone. The age is postulated basing on collected and scribed by Wójcik (2013 and in preparation). Janczyce dolomite Meer (Polish name: ogniwo dolomitów z Janczyc) rivation of name. From the Janczyce-1 borehole core, in which a complete succession is available. finition. The Janczyce Meer occurs at the base of the vonian carbonate succession in the central-eastern part of the Kielce Region and is composed of a cyclic succession of as follows (from base to top): grained dolomicrites intercalated with thamnoporaboundstones, structureless dolomicrites, dolomicrites with wavy lamination and dark dolomicrites with fenestral structures. Stratotype. The interval of the Janczyce-1 borehole core between 1203 m and 1246 m pth is the stratotype section of the meer (Text-figs 5, 14). The core is posited in the National Geological Archive in Halinów. Boundaries. The Janczyce Meer is unrlain by the Winna Formation and overlain by the . The lower boundary is fined as the first layer of dolomites above the clastic succession and can be traced in the Janczyce-1 core at 1246.0 m pth. The upper boundary is fined as the top of the cyclic succession and can be traced in the same core at 1203.0 m pth. Occurrence and . The Janczyce Meer occurs in the eastern part of the Kielce Region, in the Janczyce-1 (unit 2, 37 m thick; Text-fig. 14) borehole core, as well as in the valley of the River Wszachówka (unit 1; Text-fig. 11 and Pl. 6). The presence of similar posits is also postulated in the Zarby 2 borehole core, at the base of the carbonate succession (see scription in Tarnowska 1976). . The meer is composed of grained (crinoid-intraclast) dolomicrites intercalated with Thamnopora-boundstones (a little sandy at the base of the unit), structureless dolomicrites, dolomicrites with wavy lamination and dark dolomicrites with fenestral 172 KRYSTIAN WÓJCIK structures. In the Janczyce-1 core, the strata are arranged into 5 cyclothems. Similar posits are partially exposed in the valley of the River Wszachówka, in which sandy dolomicrites, dolomites with wavy laminations and bioturbated dolomicrites with algae and coral remains occur. . The meer has medium MS values, with average around 42×10-8 m3/kg. The major BE trend has been distinguished within the unit. It is divid into BE1, BE2, BE3 and BE4 subtrends, which correlate well with the lithological cyclothems. Origin. The Janczyce Meer representhallow-marine cyclic carbonates posited in lagoonal environments (Wójcik 2013 and in preparation). Age. The meer is in age, and ranges from the Polygnathus costatus conodont Zone to the lower part of the Polygnathus costatus costatus conodont Zone according to conodont material collected and scribed by Wójcik (2013and in preparation). Jurkowice dolomite Meer (Polish name: ogniwo dolomitów z Jurkowic) rivation of name. After the village of Jurkowice, in which a quarry is located. Earlier names. The Fossiliferous and Bioturbated Dolomicrites and Dolosparites Unit in Narkiewicz et al. (1981), Narkiewicz and Olkowicz-Paprocka (1983) and Zdanowski (1997). finition. The is a dolomitic unit unrlying the in the eastern part of the Kielce Region. As opposed to the , nodular texture, thin-grained fossiliferous intercalations and horizons of intense Chondrites-like bioturbations occur in the . The unit can be easily distinguished from the Brzeziny Meer by the presence of nodular texture, greater of particular beds, and, occasionally also by blueish weathering. Stratotype and hypostratotypes. The Jurkowice quarry section is proposed as the stratotype section of the (Text-figs 5, 10 and Pls 3, 6). The Janczyce-1 borehole core between 1203.0 and 1104.0 m pth is proposed as the hypostratotype (Text-figs 5 and 14). Boundaries. The is unrlain by the Janczyce Meer of the Winna Formation and overlain by the . The lower boundary is fined in the Janczyce-1 borehole core at the pth of 1203.0 m, at the top of the last cyclothem, as well as in the Jurkowice quarry at the base of unit 1, above the sandstones belonging to the Winna Formation. The upper boundary is fined as the top of the last layer of crinoid dolomite or nodular dolomite in the succession. It is tected in the Janczyce-1 core at 1104.0 m pth, at the level where nodular texture and shelly fossils disappear, in the Jurkowice section at the top of unit 4 above the last crinoid dolomite layer, and in the Wszachów section at the top of unit 2 above the last nodular dolomite layer. Above the upper boundary, the horizons of bioturbation structures and shelly fossils disappear completely in the succession. Occurrence and . The occurs in the eastern part of the Kielce Region, in the Jurkowice ( 1 to 4, 55 m thick; Text-fig. 10 and Pls 3, 6) and Wszachów ( 1 and 2, 28 m thick at least; Text-fig. 12 and Pls 4, 6) sections, in the Wszachówka River valley ( 2 and 3; Text-fig. 11 and Pl. 6), as well as in the Janczyce-1 borehole core (1203.0­1104.0 m pth, ca. 90 thick; Text-fig. 14). . The meer is composed of medium-bedd dolomicrites with thin-grained fossiliferous intercalations, thick-bedd nodular dolomicrites and finecrystalline dolosparites, thick-bedd dolomicrites with crinoids, and thick-bedd crinoidal dolomites. The strata are intercalated by horizons of Chondrites-dominated bioturbation structures. Fossils. Numerous lingulids, molluscs, conulariids and plant remains occur within the grained intercalations/laminae in the lowermost part of the meer. Asselages of gypidulids, tentaculoids, crinoids, scolecodonts, and bryozoans remains occur in other separate laminae/strips. Gypidulids and tentaculoids build the single and very thin lumachelle horizons. Chondrites isp. with subordinate contribution of Planolites isp. predominate among the ichnofossils. . The meer has medium MS values, with an average from 15×10-8 m3/kg in Jurkowice section, through 20×10-8 m3/kg in the Wszachów section, up to 38×10-8 m3/kg in the Janczyce-1 borehole core. The major MS trends BE, CE, 1, 2 and 3 are distinguished within the unit. 173 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Origin. The representhallowing carbonate sedimentation on the middle part of the ramp and around crinoidal meadows (Wójcik 2013 and in preparation). Age. The Meer is in age and belongs to the lower part of the Polygnathus costatus costatus conodont Zone according to the conodont material collected by Zdanowski (1997) and revised and scribed by Wójcik (2013 and in preparation). WOJCIECHOWICE DOLOMITE FORMATION (Narkiewicz and Narkiewicz 2010) Wszachów Dolomite Meer (Polish name: ogniwo dolomitów z Wszachowa) rivation of name. From the village of Wszachów, in which a quarry is located. finition. The Wszachów Meer is a characteristic unit of dark unfossiliferous dolomites with a horizon of stromatolitic domes. Stratotype and hypostratotypes. The Wszachów section along the western wall of the quarry is the stratotype section of the Wszachów Meer (Text-figs 5, 12 and Pls 4, 6). The hypostratotype is established in the Jurkowice section along the eastern wall of the quarry (Text-figs. 5 and 10 and Pls 3, 6). Boundaries. The Wszachów Meer is unrlain by the Barania Góra Formation and overlain by the Nowy Staw Meer. The lower boundary is fined at the top of the last bed of nodular, bioturbated or crinoidal dolomites of the unrlying Barania Góra Formation. The boundary can be traced in the Jurkowice section at the base of unit 5, in the Wszachów section at the base of unit 3, and in the Janczyce-1 borehole core at 1104.0 m pth. The upper boundary is fined as the base of the first thick layer of intraclast-oolite dolomites, ca. 1 m above a characteristic horizon with stromatolitic domes. The boundary can be traced in the Jurkowice section at the base of unit 6, in the Wszachów section at the base of unit 4, and in the Janczyce-1 borehole core at 1097.0 m pth. Occurrence and . The meer is recognized in the eastern part of the Kielce Region, in the Wszachów (unit 3, 10 m thick; Text-fig. 12 and Pls 4, 5) and Jurkowice (unit 5, 10 m thick; Text-fig. 10 and Pls 3, 4) sections, as well as in the Janczyce-1 bore- hole core (1104­1097 m pth, ca. 7 m thick; Text-fig. 14). Similar posits were scribed also by Tarnowska in the Dyminy-2 borehole core (15.0­45.0 m pth). . The meer is composed of dark dolomicrites, dolomicrites with flat lamination, dolomicrites with wavy lamination, stromatolite horizons and variegated siltstones, organized in cyclothems. Fossils. Absence of any shelly fossils and ichnofossils. . The meer has generally low MS values, with an average from 13×10-8 m3/kg in the Jurkowice section, through 15.5×10-8 m3/kg in the Wszachów section, up to 33×10-8 m3/kg in the Janczyce1 borehole core. The major MS trends EE1 and EE2 are distinguished within the unit. Origin. The Wszachów Meer representhallowmarine carbonate sedimentation within lagoonal environments with a predominance of subtidal conditions (Wójcik 2013 and in preparation). Age. The meer is or younger in age, however, not olr than the lower part of the Polygnathus costatus costatus conodont Zone, as can be ducted from rived from the unrlying (Wójcik 2013 and in preparation). Nowy Staw Dolomite Meer (Polish name: ogniwo dolomitów z Nowego Stawu) rivation of name. From the village of Nowy Staw, in which the Winna quarry is located. finition. The Nowy Staw Meer is a distinctive unit comprising fine- to medium grained oolitic-intraclast dolomites intercalated by various kinds of dolomites and arranged into a cyclic succession. Stratotype and hypostratotypes. The vicinity of the town of Lagów is the type area of the meer. The Wszachów section is proposed as the stratotype of the lower part of the meer (Text-figs 5, 12 and Pls 4, 6). The Winna section is proposed as the stratotype of the upper part of the meer (Text-figs 5, 13 and Pls 5, 6). The Janczyce-1 borehole core interval between 1097.0 m and 1023.0 m pth is proposed as the hypostratotype section (Text-figs 5, 14). Boundaries. The Nowy Staw Meer is unrlain by the Wszachów Meer and overlain by the Kowala 174 KRYSTIAN WÓJCIK Formation. The lower boundary is fined as the base of the first thick bed of grained oolite-intraclast dolomites, ca. 1 m above a distinctive horizon of stromatolitic domes. The boundary can be traced in the Wszachów and Jurkowice sections at the base of 4 and 6 respectively, as well as in the Janczyce-1 borehole core at 1097.0 m pth. The upper boundary is fined as the base of the first stromatoporoid-coral dolomite bed. It is established in the Winna section, at the base of unit 3, where it is emphasized by a breccia/conglomerate layer, as well as in the Janczyce-1 borehole core at 1023.0 m pth. Occurrence and . The Meer is recognized in the eastern part of the Kielce Region, in the Janczyce-1 borehole core (pth interval between 1097 m and 1023 m, ca. 70 m thick; Text-fig. 14), as well as in the Jurkowice (unit 6; Text-fig. 10 and Pls 3, 6), Wszachów (unit 4; Text-fig. 12 and Pls 4, 6) and Winna ( 1 and 2; Text-fig. 13 and Pls 5, 6) sections. Similar posits have been scribed in the Kowala 1 borehole core by Romanek and Rup (1990, see also Narkiewicz 1991) between 882.7 and 846.8 m pth. . The Nowy Staw Meer comprises: dark grey dolomicrites with flat lamination, grained intraclast-oolitic dolomites, dolomicrites with wavy lamination, horizons of stromatolitic domes, greenish flat laminated dolomicrites, intraformational breccia horizons, and variegated siltstones and claystones with anhydrite pseudomorphs, arranged in several ca. 1.5m thick cyclothemes. The nuer of cyclothems differs between the sections. . The meer has generally low MS values, up to 10×10-8 m3/kg in the Winna and Wszachów sections, and somewhat higher, with an average of ca. 20×10-8 m3/kg, in the Janczyce-1 borehole core. The major MS trends EE2, FE1 and are distinguished in the lower part of the unit. There is a lack of any relation between the MS trends and the lithological cyclothems. Origin. The meer representhallow-marine carbonate cyclic sedimentation within lagoonal environments with a predominance of inter- and supratidal conditions (Wójcik 2013 and in preparation). Age. The Nowy Staw Meer is or younger in age, and not olr than the lower part of the Polygnathus costatus costatus Zone (Wójcik 2013 and in preparation). DISCUSSION A tailed lithological scription of the succession and recognition of actual geographical and stratigraphical organization and the extent of particular lithological constitute basic requirements in reconstructing the three-dimensional architecture of any stratigraphical interval, and form the basis of subsequent regional palaeogeographical reconstructions. Such studies were missing for the uppermost Emsian and in the Kielce Region, an interval critical for unrstanding the onset and early of the vonian transgression over the area of the present day Holy Cross Mountains. This paper fulfils the gap. The investigations reported herein, carried out in nine sections and supplemented by published data, representing both the eastern and western parts of the Kielce Region, have revealed great lateral and vertical lithological variability around the Emsian­ boundary interval in the area. One new formation ­ the Barania Góra Formation ­ has been fined and divid into six . Additionally, two new have been distinguished within the overlying (Text-figs 15, 16). Although a strong lithological variability of the studied interval was reflected in the reports of former researches (Text-fig. 4), the geographical/stratigraphical distribution and characteristics of particular lithostratigraphical unit was not, so far, fully unrstood. Moreover, their position within a transgressive vonian succession was uncertain. One of the main issues, which need serious consiration before constructing a complete lithostratigraphical scheme, concerned the geographical continuity of particular distinguished in the Kielce Region; to what extent the apparently similar lithosomes are really the same in the eastern and western parts of the region (Text-figs 15, 16). The Porzecze Formation predominates in the north-western part of the Kielce Region; however, similar posits occur also in its north-central and even north-eastern parts (Tarnowska 1976; Malec 1986; Fijalkowska-Mar and Malec 2011). Three : the Dbska Wola, Dbrowa and Brzeziny are limited to the western part of the Kielce Region. Their occurrence does not cross the Daleszyce tectonic lineament (see Konon 2006), and they are absent in the Bardo Syncline, Jurkowice-Budy section, and in the vicinity of Lagów. The correspond to the Janczyce and Jurkowice distinguished in the eastern part of the region. The is the first unit that occurs broadly in the whole area of the Kielce Region (compare Narkiewicz 1991 and Narkiewicz and Narkiewicz 2010; sea also Text-figs 15, 16). 175 EMSIAN AND LITHOSTRATIGRAPHY IN THE HOLY CROSS MTS. Among the many differences in the uppermost Emsian and succession between the eastern and western parts of the Kielce Region, one more has to be emphasized ­ the of the succession. Although the difference is most accentuated within the Winna Formation, in which the varies from 2 m in the western part to 200 m in the eastern part (compare Glazek et al. 1981; Romanek and Rup 1990 with Tarnowska 1976), it is also pronounced within the overlying carbonate . Below the , a ca. 70 m thick succession in the western part (Porzecze, Dbska Wola, Dbrowa, Brzeziny ) corresponds to ca. 130 m thick carbonates in the eastern part of the region (Janczyce and Jurkowice ). This disproportion gradually creases in younger strata. The differences in and of particular are also visible in their lateral organization (Text-fig. 16). It is well exemplified in the western part of the Kielce Region, in which the of the Dbrowa Meer is highest in the north-western and south-western parts (up to 40 m) and gradually creases in the central part, where the meer disappears completely: in the vicinity of the towns of Chciny and Dyminy, the Brzeziny Meer directly overlies the Winna Formation (Glazek et al. 1981). If the lithostratigraphical divisions of the uppermost Emsian and between the Lysogóry and Kielce regions are compared, there are only two lithostratigraphical having clear analogies (compare Text-fig. 3 with Text-fig. 15). The first is the Dbrowa Meer, which in the Lysogóry Region belongs to the Grzegorzowice Formation, and which in the Kielce Region is incorporated into the Barania Góra Formation. The second unit is the . The carbonates between the Winna and Kowala , with ranging from ca. 130 m in the western part, to ca. 200 m in the eastern part of the Kielce Region, correspond to ca. 450 m thick posits of the Grzegorzowice and s in the Lysogóry Region. The last issue, which needs to be addressed, is the stratigraphical position of the studied succession. This is broadly discussed in Wójcik (2013) and will be presented in separate papers (Wójcik in preparation), and is only briefly discussed in the present paper. All the distinguished lithostratigraphical have diachronous boundaries. The most important boundary is the base of the carbonate succession. Generally, carbonate appear earlier in the western part of the region, especially in the north-western and south-western areas, in the Polygnathus costatus conodont Zone in the early or even earlier. In the eastern part of the region, the carbonatetart close to the Polygnathus costatus /Polygnathus costatus costatus boundary. A younger position of the top of the Winna Formation in the eastern part of the Kielce Region is also confirmed by found by Malec (1984b, see also Fijalkowska-Mar and Malec 2011) within the upper part of the unit in the Zarby 2 borehole core. CONCLUSIONS The Emsian/ transition in the Kielce Region of the Holy Cross Mts. inclus various lithological , which overlie the Lower vonian clastics of the Winna Formation and unrlie the Middle vonian stromatoporoid-coral dolomites and limestones of the Kowala Formation. The were posited during an early stage of the vonian transgression. A lithological scription of nine sections and a proposed formal lithostratigraphical division are presented. Six are distinguished within a newly fined Barania Góra Formation. In the western part of the Kielce Region these are: the Porzecze, Dbska Wola, Dbrowa, and Brzeziny , with a total reaching ca. 70 m. The Janczyce and Jurkowice , ca. 130 m thick, are distinguished in the eastern part. These strata correspond to the Grzegorzowice Formation in the Lysogóry Unit. Above that, the Wszachów and Nowy Staw , with a total ranging from ca. 60 to 90 m, are distinguished within the . Acknowledgments. I am particularly grateful to Prof. Stanislaw Skompski, Prof. Jerzy Nawrocki, Prof. Michal Szulczewski and Dr. Jacek Grabowski for their help and care during realization of the project. Dr. Piotr Luczyski and Prof. Ireneusz Walaszczyk are thanked for their helpful and careful review of the manuscript. Many thanks also to Dr. Piotr Luczyski, Dr. Zbigniew Remin, Dr. Anna yliska, Dr. Wojciech Kozlowski, Dr. Mikolaj Zapalski, Prof. Ireneusz Walaszczyk, Mrs Irena Sarnacka and, especially, Mr. Boguslaw Waksmundzki for their kind help during the last years of the PhD study. This work is dicated to J., M., and K. This paper presents the results of a PhD National Science Centre Project no. 2011/01/N/ST10/00604, entitled: "Facies velopment of the Kielce Region of the Holy Cross Mountains during the early stage of the vonian transgression (Emsian­ boundary interval)". 176 KRYSTIAN WÓJCIK

Journal

Acta Geologica Polonica – de Gruyter

Published: Jun 1, 2015

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