Acta Geologica Polonica, Vol. 66 (2016), No. 1, pp. 59–84 DOI: 10.1515/agp-2015-0025

Inoceramid stratigraphy and depositional architecture of the Campanian and Maastrichtian of the Miechów Synclinorium (southern Poland)

AGATA JURKOWSKA

AGH University of Science and Technology, Faculty of Geology, Geophysics and Environmental Protection Mickiewicza 30, 30-059 Krakow, Poland. E-mail: [email protected]

ABSTRACT:

Jurkowska, A. 2016. Inoceramid stratigraphy and depositional architecture of the Campanian and Maastrichtian of the Miechów Synclinorium (southern Poland). Acta Geologica Polonica, 66 (1), 59–84. Warszawa.

Dynamic evolution of the Campanian and Maastrichtian (Upper Cretaceous) of the Miechów Synclinorium is presented. Through chronostratigraphic analysis, the geometry of the Campanian and Maastrichtian of the area is interpreted, while microfacies analysis allowed determination of some of the paleoenvironmental parameters (rate of sedimentation, bottom condition and terrigenous input). The chronostratigraphy is based on inoceramid biostratigraphy. Nine inoceramid zones are recognized: Sphenoceramus patootensiformis, Sphaeroceramus sarumensis-Cataceramus dariensis and ‘Inoceramus’ azerbaydjanensis-‘Inoceramus’ vorhelmensis, ‘Inocera- mus’ tenuilineatus, Sphaeroceramus pertenuiformis, ‘Inoceramus’ inkermanensis and ‘Inoceramus’ costaecus- ‘Inoceramus’ redbirdensis (Campanian); Endocostea typica and Trochoceramus radiosus (Maastrichtian). Five unconformities (isochronous in the study area) represented by horizons of slower sedimentation rate, were rec- ognized. They correlate with eustatic sea-level changes, well recorded in European successions (Jarvis et al. 2002, 2006; Niebuhr et al. 2011). Unconformity horizons allow six alloformations to be distinguished. The thickness of particular chronostratigraphic units within the Campanian and Lower Maastrichtian increases progressively toward the axis of the Danish-Polish Trough, which indicates that the inversion of the trough could not have started before the Late Maastrichtian.

Key words: Upper Cretaceous; Miechów Synclinorium; Inoceramid bivalves; Biostratigraphy; Inversion of the Danish-Polish Trough.

INTRODUCTION of the Danish-Polish Trough (Marcinowski 1974; Walaszczyk 1992; Kutek 1996; Krzywiec 2006). This is During the Late Cretaceous, the area of the present because of its marginal position, which made the area Miechów Synclinorium was a marginal part of the Pol- sensitive to both regional (Subhercynian tectonics ish-Danish Trough (Text-fig. 1). The area is critical for movements) and global events (eustatic changes). These the interpretation of the evolution of extra-Carpathian events affected the sedimentary history of the area and Poland and first of all for deciphering the final stages are well recorded in available geological successions. (Campanian and Maastrichtian) of the inversion history Progress in the field was hindered so far by relatively 60 AGATA JURKOWSKA

Institute of Geological Sciences, Jagiellonian University in Kraków, and at the AGH University of Science and Technology in Kraków. The palaeontological material is housed at the In- stitute of Geological Sciences of the Jagiellonian Uni- versity in Kraków (collection No. UJ/220P/I). The ben- tonites were analysed by Jackson’ s procedure (1969) at the Clay Minerals Laboratory of the Institute of Geo- logical Sciences, Jagiellonian University in Kraków, and at the AGH University of Science and Technology in Kraków. Due to the lack of complete borehole cores, only the borehole cards hosted at the PIG-PIB were used.

PREVIOUS STUDIES

Stolley (1897), using belemnites, subdivided the Text-fig. 1. Tectonic-sketch map of Poland (without the Cenozoic cover) (after Upper Santonian, Campanian and Maastrichtian (his Pożaryski 1974; modified after Żelaźniewicz 2008 and Żelaźniewicz et al. 2011) Senonian) into the lower part, with Actinocamax west- falicus and Actinocamax granulatus, and the upper, with Actinocamax quadratus and Belemnitella mu- rough chronostratigraphic recognition of the Campan- cronata. Already in 1906 Smoleński recognised the ian and Maastrichtian of the synclinorium, which is lower unit with Actinocamax quadratus and the upper critical in the proper interpretation of the basin evolu- unit with Belemnitella mucronata from the Upper Cre- tion. The existing studies are either too general (older taceous of Bonarka. In the NW part of the Miechów publications, e.g., Sujkowski 1926, 1934; Paszewski Synclinorium, Mazurek (1924, 1926, 1948) described 1927; Kowalski 1948), or are limited geographically beds with A. granulatus, A. quadratus and B. mu- (e.g. Rutkowski 1965; Łyczewska 1965). However, as cronata. Sujkowski (1926) distinguished zones with demonstrated in some recent publications (Jagt et al. Actinocamax verus and A. granulatus and with A. quad- 2004; Machalski et al. 2004; Walaszczyk et al. 2008) the ratus and B. mucronata in the Wolbrom area. Kowalski Campanian and Maastrichtian of the Miechów Syncli- (1948), Bukowy (1956), Senkowicz (1959), Rutkowski norium contain most of the stratigraphically important (1965), Pożaryski (1966) used a stratigraphical inter- fossil groups that can serve for constructing a refined pretation based on cephalopods and echinoids, pro- chronostratigraphy of the upper Upper Cretaceous of the posed by Pożaryski (1938, 1948) and Kongiel (1962) area. (Text-fig. 2). The Santonian/Campanian boundary was This paper presents the Campanian and Maastricht- defined with the last occurrence (LO) of the crinoid ian inoceramid-based chronostratigraphic framework Marsupites testudinarius and the first occurrence (FO) of the Miechów Synclinorium, based on which the de- of Actinocamax quadratus, and in the lower part, positional architecture and sedimentary history of the Actinocamax quadratogranulatus was documented area is discussed. (Pożaryski 1938). The Lower/Upper Campanian bound- ary was defined at the FO of Belemnitella mucronata (Kongiel 1962). The group of B. langei, composed of MATERIALS AND METHODS three species, Belemnitella minor and Belemenitella najdini and Belemnitella langei (Kongiel 1962), was sig- Forty-one sections, mostly from the southern and nificant in the Upper Campanian (Kongiel 1962). The central parts of the Miechów Synclinorium, were stud- B. mucronata Zone was divided using ammonites into ied. Every section is documented with lithological and the lower part, with Acanthoscaphites spiniger, middle palaeontological samples. 220 specimens of inoceramid part with Hamites phaleratus, and an upper part with bivalves were collected and brought from the field. Bostrochyceras polyplocum. The LO of the latter taxon Three hundred and fifty thin sections were prepared in defined the Campanian/Maastrichtian boundary the AGH University of Science and Technology in (Pożaryski 1938). The Lower Maastrichtian was char- Kraków and studied under the optical microscope at the acterised by Belemnitella lanceolata lanceolata and 61 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND

Goniotethis quadrata

Sphenoceramus

Uintacrinus

Text-fig. 2. Correlation of inoceramid zonation applied herein (after Walaszczyk 1997, 2004; Walaszczyk et al. 2008), with zonations based on ammonites, echi- noids and belemnites for the Campanian and Lower Maastrichtian of Poland (Middle Vistula section; Błaszkiewicz 1980; Machalski 2012; Remin 2012, 2015) and Northern Germany (Schulz et al. 1984); and with faunal assemblages of Rutkowski (1965) 62 AGATA JURKOWSKA

Belemnitella lanceolata occidentalis (Kongiel 1962). Kowalski 1948; Marcinowski 1974; Walaszczyk 1992). Acantoscaphites tridens, Hoploscaphites constrictus At least the Upper Coniacian, Santonian and basal Cam- vulgaris, Bostrychoceras schloenbachi and Pachydiscus panian seems to be complete in the northern part of the aff. neubergicus were considered the characteristic Miechów Synclinorium (Walaszczyk 1992; Remin forms of the Lower Maastrichtian (Pożaryski 1948). A 2004, 2010). The upper part, the Campanian and Lower foraminiferal scheme for the Campanian and Maas- Maastrichtian, is composed of a monotonous succession trichtian was proposed by Gawor-Biedowa and of siliceous limestones (opokas) with marly horizons. Wytwicka (1960) and was used by Rutkowski (1965). The total thickness of the Campanian–Maastrichtian Senkowicz (1959) proposed a more detailed local strati- succession is about 300 m in the south-western part of graphic scheme within the zones of Campanian and the Miechów Synclinorium, and 500 m in its north-east- Maastrichtian of the NW part of the Miechów Syncli- ern part. norium (earlier described by Mazurek 1924, 1926, The so-called mid-Cretaceous transgression in extra- 1948), based on lithology and echinoids. Senkowicz Carpathian Poland started in the Middle Albian, cover- (1959) and Rutkowski (1976) reported the occurrence ing rapidly most of its territory (Pożaryski 1960, Mar- of sandy organodetrital limestones which were regarded cinowski 1974). The initial facies variability of the to be either of Maastrichtian or Late Campanian age and Albian and Cenomanian was quickly followed by facies were discussed by Machalski et al. (2004) who dated unification during the Early Turonian. With the excep- them as Miocene. An ammonite-belemnite zonation tion of the Sudetes Mountains area, where siliciclastic proposed by Błaszkiewicz (1980), described from the sedimentation prevailed until the Santonian, the rest of Campanian and Maastrichtian of the Middle Vistula the area is characterized by carbonate facies; limestones River, has never been used for the studied sequence. Re- are restricted to the Kraków Swell area, while in other cently, the inoceramid zonation of the Santonian and regions, opoka-marly facies dominate (Marcinowski Campanian of the Miechów Synclinorium was pub- 1974; Walaszczyk 1992). lished by Walaszczyk (1992), Jagt et al. (2004), Ju- rkowska et al. (2015), ammonite zonation by Machal- ski et al. (2004), and foraminiferal biostratigraphy by STAGE AND SUBSTAGE SUBDIVISION Dubicka (2015). The authors correlate the biostrati- graphical zonations with the belemnites/echinoids zona- With the exception of the base of the Maastrichtian tion described from North Germany (Schulz et al. 1984) Stage, all other stage and substage definitions of the (Text-fig. 2). The inoceramid biostratigraphy of the Campanian and Maastrichtian are still provisionary. Campanian and Lower Maastrichtian of the Miechów The current, widely followed recommendations (see Synclinorium was presented by Jurkowska (2014; see Ogg and Hinnov 2012) were agreed mostly during the also Jurkowska and Uchman 2013; Jurkowska et al. 1995 Brussels’ Symposium on Cretaceous Stage Bound- 2015). aries (Rawson et al. 1996). As no formal requirements exist, however, definitions accepted in this paper, are shortly commented below. GEOLOGICAL SETTING The base of the Campanian was provisionally de- fined with the last occurrence of the stemless, pan- The Miechów Synclinorium is the SE part of the demic crinoid species Marsupites testudinarius Szczecin-Łódź-Miechów Synclinorium. To the SW the (Schlotheim, 1820) (Hancock and Gale 1996; see also synclinorium passes gradually into the Silesian-Cra- Gale et al. 2008). As, however, this crinoid maybe lim- cow Homocline, and to the NE into the Holy Cross seg- ited to some environments, the base of the reversed po- ment of the Mid-Polish Anticlinorium (Text-fig. 1). The larity Chron C33r, which approximates the crinoid level, Cretaceous of the Miechów Synclinorium, represented is evenly considered as the primary boundary marker by the Albian through the Lower Maastrichtian, overlies (see comments in Ogg and Hinnov 2012). the Jurassic substrate unconfomably and, in its central According to the Brussels Symposium (e.g., Raw- and southern parts, it is covered by the Miocene of the son et al. 1996), the tripartite subdivision of the Cam- Carpathian Foredeep (Pożaryski 1977). The Cretaceous panian stage is recommended. There are no formal def- succession of the Miechów Synclinorium is distinctly initions of particular substages, and the US Western two-fold (Text-fig. 3). Its lower, Albian through San- Interior subdivision scheme (e.g., Cobban et al. 2006) tonian part, is composed of siliciclastic and carbonate is recommended (see Ogg and Hinnov 2012), and fol- units, relatively thin and stratigraphically largely in- lowed herein. The bases of the middle and upper Cam- complete (Sujkowski 1926, 1934; Różycki 1937, 1938; panian substages in the US Western Interior ammonite 63 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND

Text-fig. 3. Geological map of the Miechów Synclinorium (Dadlez et al. 2000; modified) with studied localities scheme are defined with the first appearances of am- the International Commission on Stratigraphy (Ogg monites, Baculites obtusus and Didymoceras nebras- and Hinnov 2012), is defined as a statistical average cense, respectively (e.g., Cobban 1994; Cobban et al. of twelve bioevents recognized in the Campanian- 2006; see also Ogg and Hinnov, 2012). Due to the en- Maastrichtian boundary interval in the Tercis les Bains demic character of these ammonites, the biostratigraphic (SW France) stratotypic section (Odin 1996, 2001; position of these boundaries in the European Campan- Odin and Lamaurelle 2001). In inoceramid terms this ian is interpreted with inoceramids (Walaszczyk et al. boundary correlates to the upper part of the ‘Inocer- 2001, 2002a, b; Odin and Walaszczyk 2003; Walaszczyk amus’ redbirdensis Zone, and approximates the FO of 2004). Accordingly, the base of the middle Campanian inoceramid species Endocostea typica (Walaszczyk et lies within the ‘I’. azerbaydjanensis – ‘I’. vorhelmensis al. 2002; Odin and Walaszczyk 2003; see also Ogg Zone, and the base of the upper Campanian within the and Hinnov 2012). This new definition places the ‘I’. tenuilineatus Zone (see also Ogg and Hinnov 2012). base of the Maastrichtian in the lower part of the The Campanian/Maastrichtian boundary, one of Belemnella obusta Zone (e.g., Niebuhr et al. 2011; the Cretaceous stage boundaries already approved by Keutgen et al. 2012), which is distinctly higher than 64 AGATA JURKOWSKA the FAD of Belemnella lanceolata (Schlotheim, Microfacially the Lower Campanian opokas repre- 1813), the traditional marker of the Campanian–Maas- sent wackestone/packstone with foraminifera and trichtian boundary in the Boreal Realm (e.g., spicules of siliceous sponges (Text-fig. 4a, b). There are Birkelund 1957; Schulz et al. 1984). also sponge fragments, echinoids and bivalves. An ad- The Maastrichtian Stage is commonly subdivided mixture of detrital quartz and glauconite is insignificant. into two substages (Odin 1996; Ogg and Hinnov 2012). The marls, which occur as interbeds in opokas, represent In the Boreal Europe, the base of the upper Maastricht- wackestone with foraminifera and spicules, and have a ian is traditionally placed at the base of the belemnite slightly higher content of detrital quartz and glauconite zone of Belemnitella junior (see e.g., Schulz et al. 1984), in comparison to opoka. which is correlated to the base of the potential am- All Campanian–Lower Maastrichtian localities are monite marker of this boundary, i.e., Menuites fresvil- briefly characterized below in alphabetical order. Their lensis (Suenes) (see e.g., Odin 1996; see also stratigraphic position is shown in Text-fig. 5 and their Walaszczyk et al. 2010). In inoceramid terms, this geographical location in Text-fig. 3. boundary corresponds to the top, or lies within the up- per part of the Trochoceramus radiosus Zone (see Biała Wielka [N 50° 41ʹ 17.19ʺ; E 19° 39ʹ 42.52ʺ]; Walaszczyk et al. 2009, 2010; Walaszczyk and Kennedy working quarry in the S. sarumensis-C. dariensis Zone 2011). opokas with marly intercalations (Jurkowska et al. 2015). Fossils are common, especially sponges and bi- valves; inoceramid bivalves are rare. LOCALITIES AND CAMPANIAN-MAAS- TRICHTIAN SUCCESSION Bibice; historical outcrop of Małecki (1989), Zapałow- icz-Bilan et al. (2009), c. 10 km N of Kraków. Based on The Campanian-Lower Maastrichtian succession in archival collection of rock samples and inoceramids, the the Miechów Synclinorium is accessible in a series of outcrop represents opokas with cherts of the S. saru- natural and artificial (abandoned quarries) exposures. mensis-C. dariensis Zone. The exposures are concentrated in the southern part of the area (Text-fig. 3). The tectonics of the Campanian Bonarka [N 50°2ʹ17.39ʺ; E 19°57ʹ15.44ʺ]; historical, and Maastrichtian of the study area is not well recog- abandoned quarry (currently nature reserve), now nized. Previous authors (Sujkowski 1926, 1934; within the town of Kraków, in the uppermost Santon- Rutkowski 1965; Jurkiewicz 1970; Łyczewska 1971, ian–Lower Campanian S. patootensiformis Zone (Ju- 1972; Kwapisz 1978; Szajn 1980; Walczowski 1984; rkowska et al. 2015), represented by grey marls and Baran 1985; Bukowy 1968; Woiński 1991; Boratyn opokas with marly interlayers (see e.g., Smoleński and Brud 1993; Rutkowski and Mądry 1994) reported 1906; Panow 1934; Alexandrowicz 1954; Barczyk many uncertain faults; some of them were recognized 1956; Gradziński 1972; Kudrewicz and Olszewska- during the fieldwork. Nejbert 1997). The grey marls yielded abundant echi- noids, belemnites and crinoids (Marsupites testudi- narius in the lower part); the opokas contain common Lower Campanian sponges and bivalves.

The Lower Campanian succession starts with grey Iwanowice [N 50° 11ʹ4. 74ʺ; E 19°59ʹ3.43ʺ]; natural ex- marls, and overlies the Santonian glauconitic marls posure in the eastern part of the village (Słomniki area) (Bonarka, Zabierzów) or, unconformably, the Upper in the S. sarumensis-C. dariensis (Jurkowska et al. Jurassic limestones (Rutkowski 1965). In the upper 2015) Zone opokas with marly interlayers. Rare fossils part, opokas with marly horizons and cherts dominate. are dominated by sponges and bivalves with sporadic Chert nodules are either chaotic (Bonarka, Biała Wielka, Cataceramus balticus. Iwanowice, Zabierzów) or occur in horizons (Wierz- chowisko, Jeżówka 1 and Jeżówka 2). Two bentonite Jeżówka 1 [N 50°24ʹ41.37ʺ; E 19°50ʹ12.42ʺ]; aban- horizons are noticed (Wierzchowisko and Jeżówka 2) in doned quarry. The lower part of the section, capped by the lower part of the Lower Campanian. The Sphaero- glauconitic limestone, represents the S. sarumensis -C. ceramus sarumensis–Cataceramus dariensis inoce- dariensis Zone. The glauconitic limestone contains ramid Zone was recognized by its index taxa; the level common sponges, echinoids (Galeola sp.), ammonites, of the Sphenoceramus patootensiformis Zone was doc- crinoids and bivalves. The overlying opoka series be- umented by foraminifera (Jurkowska et al. 2015). longs to the upper part of the Cataceramus beckumen- 65 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND sis Zone (see Jagt et al. 2004; Dubicka 2015). It contains Zbyczyce [N 50° 41ʹ 28. 13ʺ; E 19° 37ʹ 28. 66ʺ]; his- rare sponges, echinoids and inoceramids (C. dariensis), torical outcrop in the S. patootensiformis Zone (Ju- as well as ammonites and belemnites. rkowska et al. 2015) opoka of Hurcewicz (1966). Fos- sils are relatively rare, dominated by sponges and Jeżówka 2 [N 50°24ʹ50.98ʺ; E 19°49ʹ4.43ʺ]; natural ex- inoceramid imprints. posure of opokas with cherts and marly horizons. The lower part, assigned to the S. patootensiformis Zone and Middle Campanian basal S. sarumensis-C. dariensis Zone (Jurkowska et al. 2015), contains a bentonite horizon. The fossils are The Middle Campanian succession starts with quite abundant, mainly sponges echinoids, bivalves (in- opokas with marly interlayers (Rzeżuśnia, Falniów, oceramids are rare, mainly imprints). The marly hori- Parkoszowice 1, 2 and Poradów). Cherts occur chaoti- zons yielded additionally echinoids, belemnites and cally only in the lower part of the Rzeżuśnia succession. solitary corals. Two inoceramid zones were documented in the Middle Campanian: ‘I’. azerbaydjanensis- ‘I’. vorhelmensis Pniaki [N 50° 41ʹ 17.19ʺ; E 19° 39ʹ 42.52ʺ]; aban- Zone (also documented near Busko Zdrój, in the NE part doned quarry of the S. patootensiformis Zone opoka of the Miechów Synclinorium by Walaszczyk et al. with thin marly intercalations (Jurkowska et al. 2015). 2008) and ‘I’. tenuilineatus Zone. The Cataceramus It provided relatively common sponges, bivalves and subcompressus Zone has not been documented by in- rare echinoids. oceramids, however an ammonite equivalent, Bostrychoceras polyplocum Zone, was reported by Poskwitów [N 50° 13ʹ 24. 57ʺ; E 20° 0ʹ 41. 77ʺ]; tem- Rutkowski (1965). porary road-cutting along the main street in the village Microfacially, opokas are represented by packstone (described by Mączyńska 1968, and Kudrewicz and with foraminifera and spicules (Text-fig. 4c, d). The Olszewska-Nejbert 1997). It is composed of marly other organic components comprise fragments of bi- opokas with cherts of the S. sarumensis-C. dariensis valves and echinoids. An admixture of detrital quartz Zone. Opokas contain common echinoids and sponges; (<0.1 mm) and glauconite (0.2 mm) grains is significant. single specimens of C. dariensis were found. Falniów [N 50° 22ʹ 32. 54ʹ E 19° 57ʹ 56. 35ʹ]; natural Wierzchowisko [N 50°22ʹ 9.35ʺ; E 19°49’5.21ʺ]; exposure at the NW end of the village on the fields be- abandoned quarry in the S. patootensiformis and S. hind the houses. The ‘I’. azerbaydjanensis- ‘I’. vorhel- sarumensis-C. dariensis Zone (see Jagt et al. 2004; Ju- mensis Zone opokas with marly horizons and rich rkowska et al. 2015; Dubicka 2015). The exposed sponges and echinoids, are exposed. The middle part of succession is represented by opokas with marly inter- the succession contains horizons with abundant baculi- calations; a single chert horizon occurs in the middle tid ammonites and inoceramids (‘I’. azerbaydjanensis of the succession. Rare sponges and echinoids were and ‘I’. vorhelmensis) with glauconitic coatings. noticed. Parkoszowice 1 [N 50° 18ʹ 59. 39ʹ; E 20° 3ʹ 36. 86ʺ]; Wola Więcławska [N 50°10ʹ 51.67ʺ; E 20° 0ʹ 58.61ʺ]; abandoned quarry in the eastern bank of the Piotrówka natural exposure in the S. sarumensis -C. dariensis stream in the village. The quarry exposes the I’. tenuilin- Zone opoka with marly intercalations. In the middle of eatus Zone opokas with marly interlayers. In the lower the succession, marly horizons with numerous inoce- part of the section, horizons with baculitids occur. In the ramids (C. balticus) occur. Sponges, echinoids and large topmost part of the quarry, glauconitic marly opoka S. sarumensis inoceramids were noted in the opokas. horizons with oysters, massive sponges, ichnofossils and gastropods were noticed. Fossils of sponges, ammonites, Zabierzów [N 50° 6ʹ 50. 08ʺ; E 19° 47ʹ 15. 76ʺ]; inac- bivalves and gastropods are common throughout the tive reclaimed quarry. Glauconitic horizons documented section. ‘I’. tenuilineatus specimens are common, es- in the lower part of the succession represent the Upper pecially in the lower part of the succession. Catacera- Santonian (Alexandrowicz 1956; Rutkowski 1965; mus goldfussianus (d’Orbigny, 1847) and ‘Inoceramus’ Świerczewska-Gładysz 2010). The Santonian/Lower nebrascensis Owen, 1852 were also found. Campanian boundary runs in grey marls (Rutkowski 1965) overlying the glauconitic horizon. The next series Parkoszowice 2 [N 50° 18ʹ 53. 96ʹ; E 20° 3ʹ 19. 12ʺ]; of opokas with cherts represents probably the S. pa- natural exposure on the eastern bank of the Piotrówka tootensiformis Zone. stream in the village of Parkoszowice in the I’. tenuilin- 66 AGATA JURKOWSKA eatus opokas with marly horizons. Fossils are abundant, fossiliferous with abundant sponges, inoceramids (‘I.’ including mainly the inoceramids C. goldfussianus and inkermanensis, ‘Inoceramus’ cobbani Walaszczyk et ‘Inoceramus’ borilensis Jolkicev, 1962. al. 2002a, and ‘Inoceramus’ magniumbonatus Dou- glas, 1942), echinoids, belemnites, large gastropods and Rzeżuśnia [ N 50° 20ʹ 9.98ʺ; E 19° 58ʹ 15.53ʺ]; aban- plants (Debeya haldemiana, Debey ex Saporta and Mar- doned quarry in the eastern end of the village represents ion, 1873, and Debeya cf. paulinae sp. nov., Halamski I’. azerbaydjanensis- ‘I’. vorhelmensis opokas with 2013). In the upper part (‘I.’ costaceus-‘I.’ redbirdensis marly interlayers (Jagt et al. 2004). In the lower part of Zone) of the section, fossils become rare and there are the succession, opokas with cherts occur. Fossils are only single representatives of inoceramids (‘I.’ quite common: sponges, inoceramids [‘I’. vorhelmensis costaceus, E. aff. typica). (Walaszczyk, 1997), ‘I’. azerbaydjanensis Aliev, 1939 and C. balticus (Böhm, 1907)], echinoids, ammonites Komorów; historical locality of Hurcewicz (1960; and and belemnites. Two horizons with mass-occurrence probably of Rutkowski 1965), near Miechów. Based on inoceramids and baculitids with glauconitic coatings inoceramids (archival specimens), the section repre- were observed. sents the Sphaeroceramus pertenuiformis Zone (Ju- rkowska et al. 2015). Poradów [N 50°20’5.12’’; E 20°3’5.95’’]; natural ex- posure in the ‘I’. tenuilineatus, (Jurkowska et al. 2015) Muniakowice [N 50° 17ʹ 7.99ʺ; E 20° 7ʹ 10.85ʺ]; seven Zone marly opoka with marly horizons. Fossils are abandoned quarries in the southern end of the village. common: sponges, echinoids, bivalves and belemnites. Rocks are exposed in two of them only. Sandy opokas In the lower part of the succession there is a horizon with (‘I.’ inkermanensis) with a marly horizon were de- fragments of huge platyceramid inoceramids. scribed (from the topmost part of the succession). Fos- sils are abundant: mainly sponges, bivalves and am- Upper Campanian monites. ‘The inoceramid fauna is characterized by ‘I.’ inkermanensis and ‘I’. magniumbonatus (Douglas, The Upper Campanian is represented by sandy 1942). opokas with grey marl horizons. Three inoceramid Zones are documented: Sphaeroceramus pertenui- Nasiechowice [N 50° 18ʹ 30.09ʺ; E 20° 8ʹ 2.28ʺ]; aban- formis, ‘Inoceramus’ inkermanensis and ‘Inoceramus’ doned quarry in the southern slope of the village of costaceus –‘Inoceramus’ redbirdensis. The ‘Inoceramus’ Nasiechowice. Only a 2-m-thick opoka bed with marl altus Zone has not been documented. horizons in the lower part, and glauconitic marly opokas, Upper Campanian opokas represent bioclastic highly bioturbated in the upper part, are available for ob- wackestone (in the lower part of the succession) and servation. Specimens of ‘I.’ redbirdensis were found in packstone with spicules and foraminifera (in the upper opokas below the glauconitic horizon. part) (Text-fig. 4 e, f). They also contain sponges, bi- valves, echinoids and high admixture of detrital quartz Rakoszyn [N 50° 38ʹ 40.64ʺ; E 20° 5ʹ 50.78ʺ]; tempo- (0.1–0.3 mm) and glauconite grains (0.3 mm). rary road-cutting along the main road from Rakoszyn to Trzciniec, in Upper Campanian sandy opokas. A single Głogowiany-Stara Wieś [N 50° 27ʹ 58.23ʺ; E 20° specimen of ‘I.’ nebrascensis and rare sponges and 6ʹ 48.11ʺ]; abandoned quarry in the eastern end of the echinoids were only found. village. A section of 4.5-m-thick highly bioturbated marly opokas with sandy opoka horizons was described. Strzeżów 1 [N 50° 22ʹ 28. 3ʺ; E 20 24ʹ 7.38ʺ]; inactive Fossils are common, but preserved fragmentarily quarry in the ‘I.’ inkermanensis-‘I.’ costaecus sandy (sponges, bivalves and ammonites). ‘Inoceramus’ alae- opokas with marl horizons. Fossils are frequent: formis Zekeli, 1852, and huge representatives of Platyc- sponges, bivalves (pectenids), belemnites, gastropods eramus sp. were found. and echinoids. The rich inoceramid fauna includes: ‘I.’ inkermanensis, ‘I’. costaecus, C. balticus, Inoceramus Jędrzejów [N 50° 31ʹ 5.05ʺ; E 20° 17ʹ 4.76ʺ]; tempo- pierrensis (Walaszczyk, Cobban and Harris 2001). rary road-cutting in the northern part of the town of Ję- drzejów. The succession is composed of sandy opokas Uniejów-Parcela [N 50° 25ʹ 41.9ʺ; E 19° 56ʹ 51.13ʺ]; and marls of the ‘I.’ inkermanensis and ‘I.’ costaceus-‘I.’ outcrop of marly opokas in the lower part, and sandy redbirdensis zones (Świerczewska-Gładysz and Ju- opokas in the upper part. In the middle of the succession, rkowska 2013). The ‘I.’ inkermanensis Zone is very there is a horizon with phosphorite concretions in the 67 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND lower part, and with glauconitic grains, quartz and phos- Brynica Mokra [N 50° 39ʹ 30.20ʺ; E 20° 10 48.63ʺ]; phorite concretions in the upper part. All sponges, bi- temporary road-cutting along the main road in the vil- valves and belemnites detected in the horizon are pre- lage. A 2-m-thick section of sandy and marly opokas served incomplete. The topmost part of the horizon is with numerous inocerams, sponges, echinoids and represented by highly bioturbated opokas with abundant belemnites was described. Inoceramids are very frequent inoceramids (C. goldfussianus) and pectenids. The ich- and dominated by C. subcircularis, indicating the upper nofossils are filled with green, carbonate clasts. Above part of the E. typica Zone. the horizon, 6-m-thick sandy opokas can be observed. Inoceramids are represented by C. goldfussianus, which Dziewięcioły [N 50°18ʹ 22.21ʺ; E 20°10ʹ 28.71ʺ]; aban- are very common and probably indicate the S. doned quarry along the main road in the village. It ex- pertenuiformis Zone (similar situations were described poses sandy opokas with frequent inoceramids and sin- in the Middle Vistula Valley by Walaszczyk 2004). gle ammonites. Horizons with mass-occurrence of inoceramids dominated by C. subcircularis, Catacera- Wężerów [N 50° 16ʹ 14.51ʺ; E 20° 3ʹ 5.49ʺ]; exposure mus barabini (Morton, 1834), Cataceramus glendivensis behind the buildings in the eastern part of the village. It Walaszczyk, Cobban and Harries, 2001 were described exposes a 3-m-thick succession of opokas with marly from the middle and the top parts of the succession. The horizons, of the S. pertenuiformis Zone. Fossils are rich, opokas represent the upper part of the E. typica Zone. including mainly bivalves, sponges, gastropods and echi- noids. Inoceramids are represented by S. pertenuiformis Jelcza Wielka [N 50° 30ʹ 47ʺ; E 20° 24ʹ 52.24ʺ]; aban- and Cataceramus ellipticus (Giers, 1964). doned quarry in the village of Jelcza Wielka (in previ- ous publications referred to as Wrocieryż). Foraminiferal Lower Maastrichtian stratigraphy of the exposed highly sandy opokas was provided by Dubicka and Peryt (2012), and it correlates The Lower Maastrichtian is represented by sandy with the T. radiosus Zone. Specimens of the scaphitid opokas (with a variable content of detrital quartz, gen- ammonite Hoploscaphites constrictus were also de- erally increasing towards the top) with marly interlay- scribed from the section (Machalski, personal commu- ers (sandy marly opokas were found only in the SE part nication 2014). of the study area). Two inoceramid zones were docu- mented: Endocostea typica and Trochoceramus radio- Kowala [N 50° 28ʹ 46.03ʺ E 20° 32ʹ 50.53ʺ]; natural ex- sus. The stratigraphic position of the sections of Antolka, posure on the left bank of the Nida River in the village Widnica, Tunel, Słaboszowice and Michałów is based of Kowala. It exposes sandy opokas of the E. typica on lithological correlation to the sections of Strzeżów 2 Zone, with frequent C. subcircularis and single echi- and Wola Chroberska, from which Trochoceramus ra- noids. diosus (archival collections) was described (Walaszczyk et al.1996). Kozubów [N 50° 26ʹ 15.3ʺ; E 20° 29 ʹ43. 38ʺ]; natural Microfacially, opokas from the lower part of the exposure in the NW slope in the village of Kozubów. It Lower Maastrichtian represent packstone with reveals the upper part of E. typica Zone sandy opokas foraminifera and spicules (Text-fig. 4g, h), and high ad- with highly bioturbated limestones and marl horizons. mixture of detrital quartz (0.1–0.2 mm). Opokas from Abundant inoceramid fauna occurs in opokas, domi- the upper part of the succession represent wackestone nated by C. subcircularis, C. barabini and Cataceramus with spicules and foraminifera. Detrital quartz in this balticus (Böhm, 1907). part of the succession is abundant and the size of quartz grains increases upwards (Antolka and Tunel: <0.3 Michałów [N 50° 29ʹ 51.72ʺ; E 20° 27ʹ 51.23ʺ]; aban- mm, and Strzeżów 2 and Widnica: 0.3–0.6 mm). doned quarry in Lower Maastrichtian highly sandy opokas with marly horizons. Based on geological map- Antolka [N 50° 24ʹ 26.28ʺ; E 20° 5ʹ 28.66ʺ]; abandoned ping data and a lithological comparison with Jelcza quarry near the road to Cisie. It exposes a 5-m-thick suc- Wielka, the rocks probably represent the T. radiosus cession of highly sandy, yellow opokas with marly in- Zone. terlayers. Only traces of deep-burrowing bivalves (Lu- cina sp.) and ichnofossils were found. Behind the Pełczyska [N 50° 21ʹ 34.58ʺ; E 20° 33ʹ 40.14ʺ]; natu- quarry, along the road to Cisie, there is a small exposure ral outcrop in the E. typica Zone marly opokas. Rich of white sandy opokas with frequent small Cataceramus fauna includes sponges, bivalves, belemnites and ich- subcircularis (Meek, 1876). nofossils. Mass occurrence of small inoceramids of En- 68 AGATA JURKOWSKA 69 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND docostea typica Withfiled, 1877 and Cataceramus sub- posure near the railway station in Tunel. It exposes T. ra- circularis is observed. diosus Zone sandy and highly sandy opokas with marly horizons. Only single fossils of bivalves (Lucina sp.) and Pińczów [N 50° 32ʹ 13.41ʺ E 20° 32ʹ 16.69ʺ]; natural ex- ichnofossils can be found. posure along the road from Pińczów to Kije. It exposes sandy opokas of the E. typica Zone. The opokas contain Widnica [N 50° 23ʹ 56.31ʺ; E 20° 1ʹ 39.95ʺ]; abandoned a rich inoceramid fauna dominated by C. subcircularis. quarry. Highly sandy opokas with marly horizons were described from the T. radiosus Zone. Fossils are un- Rzędowice [N 50° 26ʹ 21.11ʺ; 20° 5ʹ 22.64ʺ]; natural common: only single bivalves and prisms of inoce- outcrop in the southern bank of the village. Thick suc- ramid shells were found. cession of highly sandy; yellow opokas of the T. radio- sus Zone was described. Only rare specimens of T. ra- Wola Chroberska [N 50° 23ʹ5 8.49ʺ; E 20° 31ʹ 16. diosus were noticed. 72ʺ]; natural exposure along the road from Wola Chroberska to Odrzywół, mentioned by Łyczewska Słaboszowice [N 50° 34ʹ 50.51ʺ; E 20° 11ʹ 22.29ʺ]; in- (1965) and Mazurek (1924). It exposes the T. radiosus active quarry in the southern bank of the village. Yellow, Zone highly sandy opokas. Fossils are relatively rare, highly sandy opokas were described. Only fragments of only some fragments of inocerams were found. Archival prismatic shells of inoceramds were found. Based on specimens of T. radiosus from this section are stored at lithological similarities, the opoka probably represent Warsaw University (Walaszczyk et al. 1996). the T. radiosus Zone.

Strzeżów Pierwszy 1 [ N 50° 22ʹ 47.56ʺ; E 20° 9ʹ 30. INOCERAMID BIOZONATION 16ʺ]; temporary road-cutting along the main road in the Strzeżów Pierwszy. The succession starts with glau- Inoceramid biostratigraphy enables application of conitic marls and marly opokas with phosphorite con- unified zonation recognized recently in the Western In- cretions and common fossils (Spondylus bivalves, belem- terior (US) (Walaszczyk et al. 2001), Tercis (France) nites, echinoids), but preserved incomplete. Marls are (Walaszczyk et al. 2002a), northern Germany highly bioturbated. The marls are overlain by white (Walaszczyk 1997) and in the Middle Vistula River sandy opokas with abundant inoceramids dominated by section (Walaszczyk 2004). C. subcircularis and C. barabini, sponges, Spondylus bi- In inoceramid terms, the studied succession com- valves and small echinoids. The overlying opoka con- prises an interval from the S. patootensiformis Zone up to tains only one specimen of Spyridoceramus tegulatus the T. radiosus Zone. The Lower Campanian inoceramid (Von Hagenov, 1842) form A and T. radiosus (archival succession can be compared with sections in northern collection of Warsaw University see Walaszczyk et al. Germany (Walaszczyk 1997). Inoceramids in this part of 1996). White sandy opokas are separated from yellow the succession are rare and the state of their recognition highly sandy opokas by horizons with phosphorite con- is poor. The inoceramid record of the Upper Campanian cretions, detrital quartz and glauconitic grains. The col- and Lower Maastrichtian of the study area can be directly lected and archival specimens indicate that the section compared to the succession known from the Middle Vis- represents the upper part of the E. typica Zone-T. radio- tula River section (Walaszczyk 2004) and from Tercis sus Zone (yellow highly sandy opokas). (Walaszczyk et al. 2002a). Although it requires further studies, it seems that inoceramid diversity (actually rich- Strzeżów 2 [N 50° 22ʹ 56.6ʺ; E 20° 25ʹ 7.34ʺ]; three ness) is lower than in the Middle Vistula area. inactive quarries on the opposite side of the main road in Strzeżów Pierwszy yellow highly sandy opokas Sphenoceramus patootensiformis interval Zone. The with marly horizons represent the T. radiosus Zone. base of the zone is defined by the FO of the index Fossils are rare, only adapted for deep burrowing bi- taxon, and the top by the FO of S. sarumensis and/or C. valves Lucina sp. and ichnofossils were noticed. dariensis (see Walaszczyk 1997). This zone corresponds to the upper part of the Marsupites/granulata, granu- Tunel [N 50° 26ʹ 3.79ʺ; E 19° 59ʹ 33.34ʺ]; natural ex- lataquadrata, lingua-granulata and the lower part of the

Text-fig. 4. a, b – Packstone with numerous foraminifera and spicules from Wierzchowisko, S. sarumensis-C. dariensis Zone (Lower Campanian) (a) crossed nicols (b). c, d – Bioclastic packstone with quartz grains from Parkoszowice 1, ‘I.’ tenuilineatus Zone (Middle Campanian) (c) crossed nicols (d). e, f – Bioclastic pack- stone with abundant quartz grains from Strzeżów 1, ‘I.’ inkermanensis Zone (Upper Campanian) (e) crossed nicols (f). g, h – Bioclastic packstone with numerous quartz and glauconitic grains from Strzeżów Pierwszy 1, T. radiosus Zone (Lower Maastrichtian) (g) crossed nicols (h) 70 AGATA JURKOWSKA

Text-fig. 5. Lithology and inoceramid biostratigraphy of the studied sections 71 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND pilula Zone (Walaszczyk 1997; Jagt et al. 2004). In the Spaheroceramus sarumensis–Cataceramus dariensis study area, this zone was recognized by micropalaeon- interval Zone. The base of the zone is defined by the FO tological equivalents (Jurkowska et al. 2015) of the index taxa, and the top by the FO of C. becku-

Text-fig. 6. a – Cataceramus dariensis (Dobrov and Pavlova, 1959), Bibice, S. sarumensis–C. dariensis Zone; ING UJ/220P/I/1, × 0.97. b – ‘Inoceramus’ vorhel- mensis (Walaszczyk, 1997), Rzeżuśnia, ‘I.’ azerbaydjanensis– ‘I.’ vorhelmensis; ING UJ/220P/I/4, × 0.97. c – ‘Inoceramus’ tenuilineatus Hall and Meek, 1856, Parkoszowice 1, ‘I.’ tenuilineatus Zone; ING UJ/220P/I/8, × 0.97. d – ‘Inoceramus’ azerbaydjanensis Aliev, 1939, Rzeżuśnia, ‘I.’ azerbaydjanensis– ‘I.’ vorhelmen- sis Zone; ING UJ/220P/I/15, × 0.97. e – ‘Inoceramus’ borilensis Jolkicev, 1962, Parkoszowice 1, ‘I.’ tenuilineatus Zone; ING UJ/220P/I/20, x 0.97. f – Cataceramus copetdagensis (Arzumanova, 1965), Bibice, S. sarumensis–C. dariensis Zone; ING UJ/220P/I/21, × 0.97 72 AGATA JURKOWSKA mensis (Walaszczyk 1997). This zone corresponds to the and the FO of ‘I.’ costaecus (Walaszczyk 2004). This upper part of the pilula, senonensis, papillosa, conica- zone is documented by numerous inoceramids: ‘I’. gracilis and gracilis/senior zones (Walaszczyk 1997). In inkermanensis (Text-fig. 7c), I. balticus, ‘I’. smirnovi the study area, the zone was documented by C. darien- (Text-fig. 8a) and ‘I’. magniumbonatus (Text-fig. 8b). sis (Text-fig. 6a) and micropalaeontological equiva- The ‘I.’ inkermanensis Zone corresponds to the middle lents (Jurkowska et al. 2015). Horizons with mass oc- and upper parts of the Nostoceras hyatti ammonite Zone currence of C. balticus and C. copetdagensis (Text-fig. (Walaszczyk 2004). 6f) were found in this zone. ‘Inoceramus’ costaecus and ‘Inoceramus’ redbird- Catacearmus beckumensis interval Zone. The base of ensis Zones. This interval is between the FO of ‘I.’ the zone is defined by the FO of the index taxon, and the costaecus (Text-fig. 9b) and the FO of E. typica top by the FO of the ‘I.’ azerbaydjanensis-‘I.’ vorhel- (Walaszczyk 2004). The two index taxa occur in the mensis assemblage (Walaszczyk 1997). The presence of succession; ‘I.’ costaecus appears first and is followed this zone was suggested by Jagt et al. (2004) above the by ‘I.’ redbirdensis (Text-fig. 9f) appears after the FO glauconitic horizon in the Jeżówka 1 section. This zone of ‘I.’ costaecus. This zone corresponds to the interval corresponds to the conica/mucronata Zone. from the Belemnella lanceolata up to middle part of the Belemnella vistulensis Zone (Remin 2012; com- ‘Inoceramus’ azerbaydjanensis-vorhelmensis interval pare also Keutgen et al. 2012 for zonation based on dif- Zone. The base of the zone is defined by the FO of the ferent methodology) and presumably to the basal part index taxon, and the top by the FO of C. subcompres- of the B. occidentalis Zone of Błaszkiewicz (1980) (see sus (Walaszczyk 2004). This zone corresponds to the also: Walaszczyk 2004). The FO of E. typica was ac- stobaei/bisiplana and vulgaris/bisiplana zones (Jagt et cepted as the beginning of the Lower Maastrichtian al. 2004). In the study area the zone was identified by (Ogg and Hinnov 2012). the index taxon (Text-fig. 6b, d), which coincides with C. balticus and C. ellipticus. Endocostea typica interval Zone. The zone ranges be- tween the FO of the index taxon (Text-fig. 7d) and the ‘Inoceramus’ tenuilineatus interval Zone. The base of FO of T. radiosus (Walaszczyk 2004). Horizons with the zone is defined by the FO of the index taxon (Text- mass occurrence of small (< 4 cm) inoceramids are fig. 6 c), and the top by the FO of S. pertenuiformis characteristic of this zone (Walaszczyk 2004). The (Walaszczyk 2004) (Text-fig. 7e). This zone was iden- lower part of the zone with E. typica (Text-fig. 7d) and tified by the index taxon and correlated with the lower C. subcircularis (Text-fig. 9d, e) was recognized in part of the Didymoceras donezianum ammonite Zone Pełczyska. In the remaining part of the study area only (Błaszkiewicz 1980; Walaszczyk 2004). I. borilensis the upper part of the zone was identified. E. typica dis- (Text-fig. 6e), C. goldfussianus (Text-fig. 7a), ‘I.’ ne- appears in the upper part of the zone, but C. barabini, brascensis (Text-fig. 7 b) and fragments of huge platyc- C. glendivensis (Text-fig. 9c) and C. balticus appear in- eramids were also found. Inoceramid fauna occurs in stead. The E. typica Zone corresponds to the Belem- horizons. The lower part of the ‘I’. tenuilineatus Zone nella obtusa Zone of Remin (2012) without its basal has not been found in the study area and the uppermost part which is equal to the upper part of the Belemnella part is absent due to a sedimentary gap (glauconitic vistulensis B. sp. G and B. sp. F zones (compare, horizon), thus the lowermost Upper Campanian was de- Remin 2012). termined by the FO of S. pertenuiformis. Trochoceramus radiosus interval Zone. This interval is Sphaeroceramus pertenuiformis interval Zone. The between the FO of T. radiosus and the FO of ‘Inocera- base of the zone is defined by the FO of the index taxon mus’ ianjonaensis Sornay, 1973 (Walaszczyk et al. (Text-fig. 7e), and the top by the FO of ‘I.’ altus 2002a, b, 2010). (Walaszczyk 2004). This zone was identified by finds of Two specimens from the archival collection of Alo- the index taxon and correlated with the upper part of the jzy Mazurek come from the Wola Chroberska and D. donezianum Zone (Błaszkiewicz 1980; Walaszczyk Strzeżów sections (Walaszczyk et al. 1996). One spec- 2004). C. ellipticus (Text-fig. 7f) and abundant C. gold- imen was collected by the author in the Rzędowice sec- fussianus were also found. tion. S. tegulatus forma A (Text-fig. 9a) were also noted in the T. radiosus Zone. This zone corresponds to at least ‘Inoceramus’ inkermanensis interval Zone. The zone to the upper part of the Belemnella obtusa Zone (Remin ranges between the FO of the index taxon (Text-fig. 7c) 2012). 73 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND

Text-fig. 7. a – Cataceramus goldfussianus (dʹ Orbigny, 1847), Parkoszowice 2, ‘I.’ tenuilineatus Zone; ING UJ/220P/I/25, × 1. b – ‘Inoceramus’ nebrascensis Owen, 1852, Parkoszowice 2, ‘I.’ tenuilineatus Zone; ING UJ/220P/I/35, × 1. c – ‘Inoceramus’ inkermanensis Dobrov and Pavlova, 1959, Jędrzejów, ‘I.’ inkermanensis Zone; ING UJ/220P/I/36, × 1. d – Endocostea typica Withfield, 1877, Pełczyska, E. typica Zone; ING UJ/220P/I/44, × 1. e – Sphaeroceramus pertenuiformis Walaszczyk, Cobban and Harries, 2001, Wężerów, S. pertenuiformis Zone; ING UJ/220P/I/46, x 1. f – Cataceramus ellipticus (Giers, 1964), Wężerów, S. pertenuiformis Zone; ING UJ/220P/I/47, × 1 74 AGATA JURKOWSKA

Text-fig. 8. a – ‘Inoceramus’ smirnovi Walaszczyk, 2004, Jędrzejów, ‘I.’ inkermanensis Zone; ING UJ/220P/I/48, × 1. b – ‘Inoceramus’ magniumbonatus Walaszczyk, 2004, Jędrzejów, ‘I.’ inkermanensis Zone; ING UJ/220P/I/49, × 1

EVOLUTION OF THE STUDY AREA DURING THE conitic grains and/or phosphorite concretions were rec- CAMPANIAN AND MAASTRICHTIAN ognized in the studied succession (Text-fig. 5). The contents of glauconitic grains, quartz and phosphorite Global sea-level changes concretions are different for each horizon. Four of them were recognized earlier, and used to subdivide the Cam- Five unconformities represented by horizons of panian–Maastrichtian succession into three units slower sedimentation rate, enriched with quartz, glau- (Rutkowski 1965, Table. 1). Biostratigraphic analysis al- 75 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND

Text-fig. 9. a – Spyridoceramus tegulatus (von Hagenow, 1842) form A, Strzeżów Pierwszy 2, ? T. radiosus Zone; ING UJ/220P/I/51, × 1. b – ‘Inoceramus’ costa- ecus Khalafova, 1966, Jędrzejów, ‘I.’ costaecus– ‘I.’ redbirdensis Zone; ING UJ/220P/I/52, × 1. c – Cataceramus? glendivensis Walaszczyk, Cobban and Harries, 2001, Dziewięcioły, E. typica Zone; ING UJ/220P/I/72, × 1. d, e – Cataceramus subcircularis (Meek, 1876), Dziewięcioły, E. typica Zone; ING UJ/220P/I/126, × 1. f – ‘Inoceramus’ redbirdensis Walaszczyk, Cobban and Harries, 2001, Nasiechowice, ‘I.’ costaecus– ‘I.’ redbirdensis Zone; ING UJ/220P/I/127, × 1 76 AGATA JURKOWSKA lows determining the stratigraphic position of the hori- Late Campanian Event (Voigt et al. 2012) (= Late zons, to correlate them with eustatic sea-level trends. Campanian Grobkreide Event; Niebuhr et al. 2011) (Text-fig. 5). The horizon from Parkoszowice 1 consists Marsupites transgression (Text-fig. 5). The oldest glau- of 3-m-thick marly opokas with glauconitic grains. conitic horizon was described from the western part of the Common oysters (Pycnodonte sp.), gastropods and Miechów Synclinorium: Zabierzów, Bonarka (Gradz- large sponges were reported. This horizon, which is an iński 1972), Korzkiew (Kurdrewicz and Olszewska-Ne- effect of slower or absence of sedimentation, could be jbert 1997), Wielkanoc (Świerczewska-Gładysz and Ol- connected with the Late Campanian Event (LCE) de- szewska-Nejbert 2009), Słomniki core (Rutkowski 1961), scribed by Voigt et al. (2012) from France, England, Potok Mały IG1 (Jurkiewicz 1980), Jędrzejów IG1 (Ju- Italy and Germany (Niebuhr et al. 2011), which is rkiewicz 1999), Włoszczowa IG1 (Pożaryski 1966; Ju- manifested by a negative δ13C excursion. In Tercis rkiewicz 1990). The horizon is 0.5–1.0 m thick and is en- (France), the LCE was recognized between the interval riched with glauconitic grains and inoceramid prisms. without any ammonite and inoceramid documentation Świerczewska-Gładysz and Olszewska-Nejbert (2009) and the ‘I.’ altus Zone (Odin and Lamurelle 2001; described redeposited (Middle Coniacian and Middle Walaszczyk et al. 2002a). The horizon from Parkos- Santonian) sponges in the glauconitic marls from the zowice 1 represents the ‘I.’ tenuilineatus Zone and is quarry of Wielkanoc. Bukowy (1956), Alexandrowicz older than the LCE, although it could be producd by an (1960) and Rutkowski (1965) included the glauconitic event connected with LCE. Such is the case with the marls into the Santonian (see Walaszczyk 1992 who in- horizon identified in Uniejów-Parcela. This horizon cluded the glauconitic marls into the upper Santonian, S. starts with a boundary enriched with quartz grains, patootensiformis Zone) based on finds of the crinoid phosphorite concretions and glauconitic grains. The Marsupites testudinarius in grey marls above the horizon. upper part is highly bioturbated and the bioturbation is In the central and NE part of the synclinorium, the equiv- infilled with glauconitic clasts and phosphorite con- alent of the glauconitic marls is a sandy horizon, known cretions. from the Jaronowice IG1 (Jurkiewicz 1976) and Książ Wielki IG1 (Jurkiewicz 1991) borehole cores and from Campanian–Maastrichtian Boundary Events the Kije section (Walaszczyk 1992; Remin 2004). (=CMBE) (Text-fig. 5). It was described by Jung et al. This horizon could be interpreted as a record of the (2012) from the Pacific, France, England and Egypt Marsupites transgression recognized in Europe (Niebuhr (Jarvis et al. 2002), and is manifested by a strong neg- 1995; Ernst and Wood 2000). Based on carbon stable- ative δ13C excursion, which is an effect of supposed isotope variation through the Campanian–Maastrichtian, cooling. The horizon recognized in Nasiechowice and Jarvis et al. (2002, 2006) recognized the Marsupites Strzeżów Pierwszy 1 from the upper part of the ‘I.’ red- transgression in Tunisia, France and England. The trans- birdensis Zone and the lower part of the E. typica Zone gression was also reported from Madagascar could be associated with the CMBE. The correlation of (Walaszczyk et al. 2014). these events on a global scale is controversial due to lack of precise stratigraphic data. Jarvis et al. (2002) deter- Mucronata transgression (Niebuhr 1995) (= Middle mine the start of the negative δ13C excursion in the Campanian Event, Jarvis et al. 2002; 2006) (Text-fig. 5). Gansserina gansseri foraminiferal Zone, which corre- The glauconitic horizon from Jeżówka 1 was also rec- lates with the Belemnella lanceolata belemnite Zone and ognized from Grzegorzowice Wielkie, Lipna Wola the‘I.’ redbirdensis to E. typica Zones (Ogg and Hinnov (Rutkowski 1965), and Bibice (Panow 1934). It is also 2012). Jung et al. (2012) show many small δ13C peaks known from boreholes drilled in the SE part of the syn- during the CMBE and extended the CMBE to the T. ra- clinorium (Heller and Moryc 1984). The horizon con- diosus Zone (see also Voigt et al. 2012). Voigt et al. sists of limestone clasts with glauconitic coatings con- (2012) connect the CMBE with global tectonic move- tained in marly deposits; the thickness of the horizon is ments rather than climate cooling. In these terms, the up- about 40 cm. It is underlain by limestone with Tha- per horizon from Strzeżów Pierwszy 1 could be a result lassinoides burrows. The horizon could have been pro- of a short-term sea-level pulse. duced by the Mucronata transgression, described from The older horizon from Nasiechowice and Strzeżów Germany (Niebuhr 1995), Tunisia, France, England Pierwszy 1 comprises a 1.5-m-thick marly opoka en- (Jarvis et al. 2002; 2006), and Spain (Küchler 2000). riched with glauconitic grains, quartz and fragmentar- The transgression started at the beginning of the B. mu- ily preserved fossils (only Spondylus sp. are preserved cronata Zone (the Early–Late Campanian boundary in whole). The horizon is strongly bioturbated and the traditional European subdivision). sediment infilling ichnofossil burrows does not contain 77 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND glauconite grains. The younger horizon from Strzeżów Alloformation II Pierwszy 1 is characterized by opokas with quartz, phosphorite concretions and rare glauconitic grains. The limestone in glauconitic coatings recognized in the Jeżówka 1 section indicates the lower bound- Alloformations ary of alloformation II, and the upper boundary is marked by the glauconitic horizon known from Inoceramid biostratigraphy is the most useful Parkoszowice I. method for chronostratigraphic analysis of the Cam- The horizon from the Jeżówka 1 section was also panian and Maastrichtian of the Miechów Synclino- found in Lipna Wola, Grzegorzowice Wielkie rium. Its usefulness is limited to the exposed succes- (Rutkowski 1965) and Bibice (Panow 1934) and from sions; inoceramids are rarely found in cores. For the cores in the SE part of the Miechów Synclinorium reconstruction of the depositional architecture of the (Heller and Moryc 1984). study area, a more precise chronostratigrapic analysis is The thickness of alloformation II is about 100 m. needed. Alloformation II is represented by marly opokas with The described horizons are useful for distinguishing cherts (in its lower part) and opokas with marly horizons alloformations in the Campanian and Maastrichtian of (in its upper part). The fossils are abundant: sponges, in- the Miechów Synclinorium. All of them are correlated oceramids, baculitids. In the lower part of alloformation with global eustatic sea-level changes, which makes II, there are two horizons of abundant baculitids and in- them isochronous in the area studied. oceramids in glauconitic coatings (Rzeżuśnia section). Six alloformations have been distinguished in ac- Microfacially, the opokas represent packstone with cordance with the Polish Rules of Stratigraphy (Racki foraminifers and spicules, the quartz content is in- and Narkiewicz 2006). Most of them represent third-or- significant. der eustatic sea-level changes (Haq et al. 1987). Alloformation II is correlated with the C. becku- mensis − ‘I.’ tenuilineatus zones. Alloformation I Alloformation III The lower boundary is defined by Santonian glau- conitic marls (or sandy marl horizon), and the upper one The lower boundary of alloformation III is indi- by the Lower Campanian horizon with limestone in cated by the glauconitic horizon from the Parkoszowice glauconitic coatings. The lower horizon is well exam- 1 section, and the upper boundary by the glauconitic- ined in the western part of the Miechów Synclinorium phosphorite horizon from the Uniejów-Parcela section. and in cores (see section: ‘Marsupites transgression’). The glauconitic horizon from the Parkoszowice 1 sec- In the NW part of the study area it correlates with the tion was also noticed in the Włoszczowa Trough by sandy marl horizon (Remin 2004). The glauconitic Pożaryski (1966). marls are overlain by grey marls and opokas with cherts. The thickness of alloformation III is estimated in the Locally, the grey marls lie on Jurassic limestones southern part of the Miechów Synclinorium at 10 m, and (Rutkowski 1965). in the northern part at 30−60 m. The thickness of alloformation I is variable: 2−10 m Alloformation III consists of fossiliferous opokas in the western part (Gradziński 1972, Świerczewska- with marly horizons. Microfacially, it is represented by Gładysz 2010, Jurkiewicz 1974), 40−45 m in the cen- bioclastic wackestone/packstone with quartz (0.1−0.2 tral (Rutkowski 1961, Jurkiewicz 1976, Jurkiewicz mm) and glauconitic grains (0.1 mm). 1990) and eastern parts of the Miechów Synclinorium Alloformation III spans the interval of the upper part (Heller and Moryc 1984). of the ‘I.’ tenuilineatus Zone to the S. pertenuiformis The opokas contain abundant fossils represented by Zone. epibenthos (sponges, bivalves) and endobenthos (echi- noids); nektonic organisms (ammonites and belemnites) Alloformation IV are rare. Microfacially, the opokas represent wackestone/ Alloformation IV has been distinguished between packstone with spicules and foraminifers. Fragments of the glauconitic-phosphorite horizon from the Uniejów- sponges, echinoids and bivalves also occur. Quartz and Parcela section and the glauconitic horizon from glauconite are rare. Strzeżów Pierwszy 1. The former was also described by Alloformation I represents the upper part of the S. Pożaryski (1966) from the northern part of the Miechów pinniformis Zone to the S. sarumensis-C. dariensis Zone. Synclinorium. 78 AGATA JURKOWSKA

Alloformation IV is represented by fossiliferous, Danish-Polish Trough could not have started before the sandy opokas with marly horizons. Microfacially, the Late Maastrichtian, which is in agreement with sugges- opokas represent bioclastic wackestone/packstone with tions presented earlier by Kutek and Głazek (1972), and abundant quartz grains (0.1−0.3 mm). Świdrowska and Hakenberg (1999). It is significantly Alloformation IV spans between the S. perte- later than in the NE border of the Holy Cross Mountains, nuiformis and E. typica zones (including a gap com- where the geophysical data show that the uplift move- prising the‘I’.altus Zone). ment started in the Late Turonian?–Early Coniacian (Krzywiec 2002, 2006; Krzywiec et al. 2009; see also Alloformation V Dadlez et al. 1997; Leszczyński 2010). Signs of synsed- imentary uplit tectonics during this time were not noted The lower boundary is indicated by the glau- in the Miechów Synclinorium. conitic horizon examined in the Strzeżów Pierwszy 1 Five unconformity horizons, representing third-or- section, and the upper boundary by the phosphorite der eustatic sea-level changes (Haq et al. 1987), well horizon known from the Strzeżów Pierwszy 1 section. recorded in European successions (Jarvis et al. 2006, Alloformation V consists of white sandy opokas Niebuhr et al. 2011), have been identified. with marly horizons. The lower part of the succession The lowest quartz content is found in opokas and was recognized only in the Pełczyska section and is rep- marls of alloformations I and II, and it increases in allo- resented by fossiliferous marly opokas. Microfacially, formations III and IV; in opokas and marls of allofor- the opokas are packstone with spicules and foraminifers; mation V and VI it is abundant. It is difficult to indicate the admixture of quartz and glauconite grains is high. the sediment provenance area; further investigations The thickness of alloformation V is variable: about are necessary. Up-section, but not lateral, changes in the 60 m in the SW part of the Miechów Synclinorium, and size of quartz grains in the Lower Maastrichtian sandy about 130 m in the NE. opokas described by Rutkowski (1960) were observed Alloformation V spans between the E. typica Zone also by the present author. These could not be interpreted to the lower part of the T. radiosus Zone. as an indicator of a sediment supply area. An area lying S/SW from the studied sections was indicated as a good Alloformation VI provenance area for the S part of the Miechów Syncli- norium (Kutek and Głazek 1972; Hakenberg and The youngest alloformation was defined between Świdrowska 1998; Świdrowska and Hakenberg 1999). the phosphorite horizon described from Strzeżów Pier- Also the area lying N/NE from the Miechów Synclino- wszy 1 and the youngest Maastrichtian deposits avail- rium, in the Holy Cross Mountains, was pointed out as able in the Miechów Synclinorium. a supplementary area (Małopolska Land; Jaskowiak- Alloformation VI consists of sandy, yellow opokas Schoeneichowa and Krassowska 1988). The data from with marly interlayers. Fossils are rare, represented by leaf floras from the Miechów Synclinorium also suggest single inoceramids and other bivalves (Lucina sp.). Mi- that, during the Campanian, there must have existed up- crofacially, the opokas represent packstone with lifted areas in the Holy Cross part of the Danish-Polish spicules, foraminifers. The admixture of quartz grains Trough (Halamski 2013). The leaf flora and a greater in- (0.2−0.5 mm) is significant. put of quartz were interpreted as a sign of the beginning The thickness of alloformation VI is about 20−30 m of inversion of the Danish-Polish Trough. New data pre- in the SW part of the Miechów Synclinorium, and reach sented in this paper show that tectonic evolution of the up about to 50 m in the NE part. study area could be more complicated. It is difficult to The alloformation is represented by the T. radiosus estimate whether the quartz content was an effect of eu- Zone. static sea-level changes or tectonic movements in the Danish-Polish Trough (Walaszczyk and Remin 2015). Evolution of the study area

The chronostratigraphic and microfacies analyses CONCLUSIONS provide a basis to analyze the thickness and facies changes in the Campanian and Maastrichtian in the study 1. In the Campanian–Lower Maastrichtian deposits of area. The thickness of particular chronostratigraphic the Miechów Synclinorium, nine inoceramid zones, units within the Campanian and Lower Maastrichtian in- excluding C. beckumensis, C. subcompressus and ‘I.’ creases progressively towards the axis of the Mid-Polish altus, were identified by finds of the index taxa. Anticlinorium, which suggests that the inversion of the 2. Five glauconitic horizons enriched with quartz and 79 CAMPANIAN AND MAASTRICHTIAN (CRETACEOUS) OF SOUTHERN POLAND

phosphorite nodules correlate with eustatic sea-level Arzumanova, E.M. 1965. New representatives of the family peaks well recognized in Europe. Inoceramidae from the lower Campanian deposits of east- 3. Unconformity horizons allow the determination of six ern Kopet-Dag. Izvestia Akademii Nauk Turkmenskoy alloformations which are isochronous within the SSR, Seria Fizyko-technicheskich, Khimicheskich i Geo- Miechów Synclinorium. logicheskich Nauk, 1 (1965), 100−110. [In Russian] 4. The thickness of particular alloformation units in- Baran, E. 1985. Przekrój poprzeczny przez synklinę Słomnik. creases progressively toward the axis of the Danish- Unpublished report, National Geological Archive; War- Polish Trough, which indicates that the inversion of saw. the trough in the Miechów Synclinorium could not Barczyk, W. 1956. On the Upper Chalk Deposits on Bonarka have started before the Late Maastrichtian. near Cracow. Studia Societatis Scientiarium Torunensis, 5. The increasing quartz input in the Campanian–Lower 3, 1–23. [In Polish] Maastrichtian could be an effect of eustatic or tec- Birkelund, T. 1957. Upper Cretaceous belemnites from Den- tonic movements in the Danish-Polish Trough. mark. Biologiske Skrifter. Det Kongelige Danske Viden- skabernes Selskab, 9, 1–69. Böhm, J. 1907. Inoceramus Cripsi auct. Abhandlungen der Koniglich-Preussischen Geologischen Landesanstalt, Acknowledgements Neue Folge, 56, 41–58. Błaszkiewicz, A. 1980. Campanian and Maastrichtian am- I am particularly grateful to Prof. Ireneusz Walaszczyk for monites of the Middle Vistula River Valley, Poland: a his help and care during the development of the project and stratigraphic-paleontological study. Prace Instytutu Geo- for a careful review of the manuscript. I am very grateful to logicznego, 92, 1–63. Dr Zbigniew Remin, Dr Krzysztof Leszczyński and Christo- Boratyn, J. and Brud, S. 1993. Objaśnienia do szczegółowej pher J. Wood for constructive comments on an earlier version mapy geologicznej Polski 1:50000. Arkusz Słomniki (M- of the manuscript. Many thanks also go to Dr hab. Ewa 34-65-A), pp. 1–55. Wydawnictwa Geologiczne; Świerczewska-Gładysz, Prof. Jacek Rutkowski and Dr Zofia Warszawa. [In Polish] Dubicka, for their help during the last years of the PhD study. Bukowy, S. 1956. Contributions to the geology of the Silesian I am greatly indebted to Anna and Tadeusz Jurkowscy, Kamil and Cracovian regions. Biuletyn Instytutu Geologicznego, and Karolina Kowalscy, and Paula Dobosz, for their help in 108, 17– 82. the fieldwork, and to Krzysztof Paulo for allowing the field- Bukowy, S. 1968. Objaśnienia do szczegółowej mapy geo- work in Jędrzejów. This paper presents some of the results of logicznej Polski 1:50000. Arkusz Wolbrom (M34-52D), a PhD National Science Centre Project No. PRO- pp. 1–48. Wydawnictwa Geologiczne; Warszawa. 2011/01/N/ST/10/07717, undertaken at the Institute of Geo- Cobban, W.A. 1993. Diversity and distribution of Late Cre- logical Sciences Jagiellonian University in Kraków entitled taceous ammonites, Western Interior, United States. In: ‘Inoceramid stratigraphy and depositional architecture of the Caldwell, W.G.E. and Kauffman, E.G. (Eds), Evolution of upper Upper Cretaceous in the Miechów Trough’ and of ad- the Western Interior Basin. Geological Association of ditional post-doctoral further research at the AGH University Canada, Special Paper, 39, 435–451. of Science and Technology in Kraków (DS 11.11.140.626). Cobban, W.A., Walaszczyk, I., Obradovich, J.D. and McKin- ney, K.C. 2006. A USGS Zonal table for the Upper Cre- taceous, Middle Cenomanian-Maastrichtian of the West- REFERENCES ern Interior of the United States based on ammonites, inoceramids and radiometric ages. U.S Geological Survey Aliev, M.M. 1939. Inoceramidae of the Cretaceous deposits in Open File-Report, 45 pp. the northern part of Minor Caucas. Trudy Geolo- Dadlez, R., Jóźwiak, W. and Młynarski, S. 1997. Subsidence gitscheskovo Institura Akademii Nauk SSSR, Azerbayd- and inversion in the western part of Polish basin – data janskij Filial, 12 (63), 213–259. [In Russian] from seismic velocities. Geological Quaterly, 41, 197–208. Alexandrowicz, S. 1954. Turonian of the southern part of the Dadlez, R., Marek, S. and Pokorski, J. 2000. Geological map Cracow Upland. Acta Geologica Polonica, 4, 361–391. of Poland; scale: 1:1000000. Państwowy Instytut Geo- [In Polish] logiczny; Warszawa. Alexandrowicz, S.W. 1956. Globotruncana assemblages in the De Saporta, G. and Marion, A.F. 1873. Essai sur l’etat de la Touronian in the Cracow region. Acta Geologica vegetation l’epoque des marnes heersiennes de Gelinden. Polonica, 4, 41–63. [In Polish with English summary] Mémoires couronnés et mémoires des savants étrangers Alexandrowicz, S. 1960. Budowa geologiczna okolic Tyńca. publiés par l’Académie royale des sciences, des lettres et Biuletyn Instytutu Geologicznego, 152, 5−93. des beaux−arts de Belgique 37, 3–94. 80 AGATA JURKOWSKA

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Manuscript submitted: 22nd July 2015 Revised version accepted: 5th December 2015