Annales Societatis Geologorum Poloniae (2021), vol. 91: 203–251 doi: https://doi.org/10.14241/asgp.2021.15 A LOST CARBONATE PLATFORM DECIPHERED FROM CLASTS EMBEDDED IN FLYSCH: ŠTRAMBERK-TYPE LIMESTONES, POLISH OUTER CARPATHIANS Mariusz HOFFMANN 1, 2, Bogusław KOŁODZIEJ 2, * & Justyna KOWAL-KASPRZYK 3 1 Soletanche Polska, Warszawa, Poland, deceased 2016 2 Institute of Geological Sciences, Jagiellonian University, ul. Gronostajowa 3a, 30-387 Krak, Poland; e-mail: boguslaw.kolodziej@uj.edu.pl 3 Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology, Al. Mickiewicza 30, 30-059 Krak, Poland; e-mail: kowalj@agh.edu.pl * Corresponding author Hoffmann, M., Kołodziej, B. & Kowal-Kasprzyk, J., 2021. A lost carbonate platform deciphered from clasts embedded in flysch: Štramberk-type limestones, Polish Outer Carpathians. Annales Societatis Geologorum Poloniae, 91: 203–251. Abstract : Limestones designated the Štramberk-type are the most common carbonate exotic clasts (exotics) embedded in the uppermost Jurassic–Miocene flysch deposits of the Polish Outer Carpathians. About 80% of stratigraphically determinable carbonate exotics from the Silesian, Sub-Silesian and Skole units (nappes) are of Tithonian (mostly)–Berriasian (sporadically Valanginian) age. Astudy of these exotics revealed eight main facies types: coral-microbial boundstones (FT 1), microencruster-microbial-cement boundstones (FT 2), microbial and microbial-sponge boundstones (FT 3), detrital limestones (FT 4), foraminiferal-algal limestones (FT5), peloidal­bioclastic limestones (FT 6), ooid grainstones (FT 7), and mudstones-wackestones with calpionellids (FT 8). Štramberk-type limestones in Poland and the better known Štramberk Limestone in the Czech Republic are rem­nants of lost carbonate platforms, collectively designated the Štramberk Carbonate Platform. Narrow platforms were developed on intra-basinal, structural highs (some of them are generalized as the Silesian Ridge), with their morphology determined by Late Jurassic synsedimentary tectonics. An attempt was made to reconstruct the fa­cies distribution on the Tithonian–earliest Cretaceous carbonate platform. In the inner platform, coral-microbial patch-reefs (FT 1) grew, while the upper slope of the platform was the depositional setting for the microen­cruster-microbial-cement boundstones (FT 2). Microbial and microbial-sponge boundstones (FT 3), analogous to the Oxfordian–Kimmeridgian boundstones of the northern Tethyan shelf (also present among exotics), were developed in a deeper setting. In the inner, open part of the platform, foraminiferal-algal limestones (FT 5) and peloidal-bioclastic limestones (FT 6) were deposited. Poorly sorted, detrital limestones (FT 4), including clast­supported breccias, were formed mainly in a peri-reefal environment and on the margin of the platform, in a high-energy setting. Ooid grainstones (FT 7), rarely represented in the exotics, were formed on the platform margin. Mudstones-wackestones with calpionellids (FT 8) were deposited in a deeper part of the platform slope and/or in a basinal setting. In tectonic grabens, between ridges with attached carbonate platforms, sedimenta­tion of the pelagic (analogous to FT 8) and allodapic (“pre-flysch”) Cieszyn Limestone Formation took place. The most common facies are FT 4 and FT 1. Sedimentation on the Štramberk Carbonate Platform terminated in the earliest Cretaceous, when the platform was destroyed and drowned. It is recorded in a few exotics as thin, nep­tunian dykes (and large dykes in the Štramberk Limestone), filled with dark, deep-water limestones. Reefal facies of the Štramberk Carbonate Platform share similarities in several respects (e.g., the presence of the microencruster­microbial-cement boundstones) with reefs of other intra-Tethyan carbonate platforms, but clearly differ from pal­aeogeographically close reefs and coral-bearing facies of the epicontinental Tethyan shelf (e.g., coeval limestones from the subsurface of the Carpathian Foredeep and the Lublin Upland in Poland; the Ernstbrunn Limestone in Austria and Czech Republic). Corals in the Štramberk Limestone and Štramberk-type limestones are the world’s most diverse coral assemblages of the Jurassic–Cretaceous transition. The intra-basinal ridge (ridges), traditionally called the Silesian Cordillera, which evolved through time from an emerged part of the Upper Silesian Massif to an accretionary prism, formed the most important provenance area for carbonate exotic clasts in the flysch of the Silesian Series. They are especially common in the Lower Cretaceous Hradiště Formation and the Upper Cretaceous–Paleocene Istebna Formation. The Baška-Inwałd Ridge and the Sub-Silesian Ridge were the source areas for clasts from the Silesian and Sub-Silesian units (e.g., in the Hradiště Formation), while the Northern (Marginal) Ridge was the source for clasts from the Skole Unit (e.g., in the Maastrichtian–Paleocene Ropianka Formation). Key words: Reefs, facies, Štramberk Limestone, Silesian Ridge, Jurassic, Cretaceous, Carpathian Basin, Poland. Manuscript received 3 May 2020, accepted 7 August 2021 INTRODUCTION In the Polish Outer Carpathians, shallow-water car­bonate sedimentation is recorded only by carbonate clasts, redeposited bioclasts, and very rare, small, unrooted, poorly exposed klippen. Clasts of limestones are exotic to the dominant siliciclastic, uppermost Jurassic–Miocene flysch deposits. They were derived from extrabasinal and intra-basinal source areas of the Carpathian rocks, which periodically emerged and were destroyed. Such rocks were described as “exotic” since the 19th century (“exotischen Graniten”, “exotische Blöcke”; Morlot, 1847; Hohenegger, 1861). In the general geological literature, the term “exotic clasts” is usually used (Flügel, 2010, p. 172), whereas in the Polish geological literature, the term “exotics” (Polish “egzotyki” including also carbonate exotics), is also com­monly applied. On the basis of fossils, facies and microfaci­es, these clasts (pebbles, rarely blocks) are mostly described as Devonian–Carboniferous (Malik, 1978, 1979; Burtan et al., 1983; Tomaś et al., 2004) and Upper Jurassic–lower­most Cretaceous (the present paper and references therein), more rarely Middle Jurassic (Książkiewicz, 1935, 1956a; Barczyk, 1998; Olszewska and Wieczorek, 2001), Early Cretaceous (Oszczypko et al., 1992, 2006, 2020; Krobicki et al., 2005), Late Cretaceous (Książkiewicz, 1956a; Gasiński, 1998) and Palaeogene in age (Leszczyński, 1978; Rajchel and Myszkowska, 1998; Leszczyński et al., 2012; Minor-Wróblewska, 2017). At the beginning of these studies, the focus was on small, unrooted klippen, namely the Andrychów Klippen (called also Klippes) near Wadowice (Zeuschner, 1849; Hohenegger, 1861; Uhlig, 1904; Książkiewicz, 1935, 1971b; Nowak, 1976; Gasiński, 1998; Olszewska and Wieczorek, 2001), and in Kruhel Wielki, near Przemyśl (Niedźwiedzki, 1876; Wójcik, 1907, 1913, 1914; Bukowy and Geroch, 1956; Morycowa, 1988; Olszewska et al., 2009), now poorly exposed. Subsequently, exotic pebbles, much more common and providing data on more facies, were studied more frequently. The first attempt to describe exotics, in­cluding crystalline rocks, was presented by Nowak (1927). Jurassic–Cretaceous carbonate exotics at Bachowice, con­taining facies unknown at other localities in the Polish Outer Carpathians, were described by Książkiewicz (1956a). The preliminary results of studies, which encompassed the entire spectrum of carbonate exotics from the western part of the Polish Outer Carpathians, were presented by Burtan et al. (1984). Malik (1978, 1979) described both Palaeozoic and Mesozoic carbonate clasts in the Hradiště Sandstone of the Silesian Unit, but other studies were mostly concerned with the Štramberk-type limestones from selected outcrops. The studies of these limestones, if concerned with exot­ics at many localities, were focused on their fossil content (e.g., Kołodziej, 2003a; Bucur et al., 2005; Ivanova and Kołodziej, 2010; Kowal-Kasprzyk, 2014, 2018) or pre­sented only the preliminary results of facies studies (e.g., Hoffmann and Kołodziej, 2008; Hoffmann et al., 2008). Carbonate platforms, the existence of which was de­ciphered from detrital carbonate components, are called lost carbonate platforms (e.g., Belka et al., 1996; Flügel, 2010; Kukoč et al., 2012). Clasts and other shallow­water components are, metaphorically, witnesses to lost carbonate factories (the term is taken from Coletti et al., 2015). Analyses of the age and lithology of exotic clasts have been applied in the reconstruction of the provenance areas of the clasts and their palaeogeography and the de­velopment of the sedimentary sequences of the Polish Outer Carpathians (e.g., Książkiewicz, 1956b, 1962, 1965; Unrug, 1968; Oszczypko, 1975; Oszczypko et al., 1992, 2006; Hoffmann, 2001; Krobicki, 2004; Słomka et al., 2004; Malata et al., 2006; Poprawa and Malata, 2006; Poprawa et al., 2006a, b; Strzeboński et al., 2017; Kowal-Kasprzyk et al., 2020). Štramberk-typelimestones are most common among the exotics. It is a field term that refers to limestones, mostly beige in colour, that are supposed to be the age and facies equivalents of the Tithonian–lower Berriasian Štramberk Limestone in Moravia (Czech Republic; Eliáš and Eliášová, 1984; Picha et al., 2006). The Štramberk Limestone and the Štramberk-type limestones of both countries were deposited on platforms, attached to the intrabasinal ridges and margins of the basin of the Outer Carpathians. These platforms are collectively termed the Štramberk Carbonate Platform. The terms “Štramberk Limestone” and “Štramberk-type limestones” have been widely used in the area of the former Austro-Hungarian Empire for the field description of shal­low-water limestones of assumed Late Jurassic age, usually occurring within flysch deposits of the Outer Carpathians. Upper Jurassic–lowermost Cretaceous shallow-water lime­stones in Romania (commonly forming mountains or ridg­es, e.g., Pleş et al., 2013, 2016), in Bulgaria and Serbia (Tchoumatchenco et al., 2006), and Ukraine (Krajewski and Schlagintweit, 2018), and in Turkey (Masse et al., 2015) sometimes are referred to as the Štramberk-type lime­stones as well. In the Austrian-German literature similar limestones in the Alps are known as the Plassen Limestone (e.g., Steiger and Wurm, 1980; Schlagintweit et al., 2005). Biostratigraphic studies revealed that some carbonate clasts, accounting for several percent of the exotics and commonly called Štramberk-type limestones in the field, are in fact of Oxfordian–Kimmeridgian age. These limestones were gen­erally deposited in a deeper environment than were most fa­cies of the Štramberk-type limestones sensu stricto (Nowak, 1976; Olszewska and Wieczorek, 2001; Kowal-Kasprzyk, 2016; Kowal-Kasprzyk et al., 2020). The Štramberk Limestone occurs as olistoliths, blocks, and as smaller clasts in breccias and conglomerates in the Cretaceous flysch deposits of the Silesian Unit of the Outer Carpathians, Czech Republic (Moravia, mostly in the Kotouč Quarry, near Štramberk; Stramberg in the older literature). They are interpreted as the deposits of a carbonate platform, developed on the Baška Ridge, in the northern part of the Outer Carpathian basin (Eliáš and Eliášová, 1984; Picha et al., 2006). The Štramberk Limestone is rich in fossils, intensively studied already in the 19th century (for references: Blaschke, 1911; Vašíček and Skupien, 2004, 2005), including the world’s most diversified coral fauna of Tithonian–Berriasian age (e.g., Ogilvie, 1897; Eliášová, 1975, 1978, 1981a, 2008). The results of the detailed studies of Ogilvie (1897) on these coral assemblages, unique in many respects (128 species, in­cluding many endemic taxa) were communicated to a wider scientific community in Nature by Gregory (1898). Some of corals described by Ogilvie (1897) came from limestone blocks in the Silesian Nappe, Cieszyn, Silesia, in the west­ern part of the Polish Carpathians, for example at the lo­calities Iskrzyczyn (German name Iskritschin), Skoczów (Skotschau), Ustroń (Ustron), Wilamowice (Willamowitz), and Wiślica (Wischlitz); see also Geyer (1955). Maria Ogilvie Gordon started her career with studies of corals from the Štramberk Limestone. She was one of the prolific researchers of the later 19th century, a famous researcher on the Dolomites, in the Alps (Wachtler and Burek, 1997). The Štramberk-type limestones in Poland were the sub­ject of papers on microfossils and rarely on macrofossils, mostly corals (Table 1; short reviews in Kołodziej, 2015a, b; Salamon and Trzęsiok, 2015; Kowal-Kasprzyk, 2018), but there are rare sedimentological contributions, mostly concerned with the microfacies of the exotic clasts at se­lected sites. The Štramberk Limestone was rarely studied in terms of sedimentology (Eliáš and Eliášová, 1984, 1986; Hoffmann et al., 2017). The limestones in the Carpathians of the Czech Republic and Poland deserve attention, be­cause they are relatively rare examples of carbonate plat­forms, especially reefs, developed in the Tithonian and ear­liest Cretaceous. They are known mostly from the area of the earlier Tethyan domain (e.g., Steiger and Wurm, 1980; Eliáš and Eliášová, 1984; Morsilli and Bosellini, 1997; Shiraishi and Kano, 2004; Săsăran, 2006; Ivanova et al., Table 1 List of papers on micro- and macrofossils from the Štramberk-type limestones, Polish Outer Carpathians. Some palaeontological papers on the Štramberk Limestone published in the 19th century and at the beginning of 20th century (e.g., the paper on corals by Ogilvie, 1897) included descriptions of fossils from exotic clasts from the Cieszyn Silesia, western part of the Polish Outer Carpathians. These papers are not included in the list (see Blaschke, 1911). Group of fossils References Algae (benthic) Olszewska and Wieczorek (2001), Bucur et al. (2005) Ammonites Książkiewicz (1963, 1974) Bivalves Wójcik (1913, 1914), Książkiewicz (1963, 1974) Brachiopods Zeuschner (1857), Wójcik (1913, 1914), Książkiewicz (1974), Smirnova (1975) Bryozoa Hara and Kołodziej (2001) Calcareous dinoflagellate cysts Olszewska and Wieczorek (2001), Olszewska et al. (2011), Strzeboński et al. (2017) Calpionellids and chitinoidellids Morycowa (1964a, 1968, 1988), Geroch and Morycowa (1966), Olszewska and Wieczorek (2001), Ciborowski and Kołodziej (2001), Olszewska et al. (2011), Kowal-Kasprzyk (2014, 2018) Corals Morycowa (1964a, 1968, 1974, 2008), Kołodziej (1995, 1997b, 2003a, 2015b) Crinoids Salamon and Gorzelak (2010), Hess et al. (2011), Lach et al. (2015), Trzęsiok (2015) Crustaceans Patrulius (1966), Müller et al. (2000), Krobicki and Fraaije (2017) Echinoids Kroh (2015) Foraminifera Geroch and Morycowa (1966), Kołodziej (1997a), Kołodziej and Decrouez (1997), Król and Decrouez (2002), Decrouez and Morycowa (1997), Olszewska and Wieczorek (2001), Ivanova and Kołodziej (2004, 2010), Olszewska et al. (2011), Kowal-Kasprzyk (2016), Łapcik et al. (2016), Strzeboński et al. (2017) Gastropods Książkiewicz (1963) Microproblematica Kołodziej and Decrouez (1997), Kołodziej, (1997a), Bucur et al. (2005), Hoffmann et al. (2008), Kołodziej (2015b), Kołodziej et al. (2015), Kowal-Kasprzyk (2015, 2016) Sponges (calcified sponges/ sclerosponges) Podoba (2009) 2008, 2015; Krajewski, 2008; Schlagintweit and Gawlick, 2008; Rusciadelli et al., 2011; Ohga et al., 2013; Pleş et al., 2013, 2019; Chatalov et al., 2015; Kaya and Altiner, 2015; Hoffmann et al., 2017; Atasoy et al., 2018; Ricci et al., 2018a, b; Mircescu et al., 2019; Nembrini et al., 2021; and Leinfelder et al., 2002 for more references), in contrast to the Oxfordian–Kimmeridgian reefs of the Tethyan shelf (Leinfelder et al., 2002). The Oxfordian and Kimmeridgian were times of strong coral reef development (Insalaco et al., 1997; Leinfelder et al., 2002). Falling sea levels in the Tithonian and across the Jurassic–Cretaceous boundary (Haq et al., 1988) resulted in a marked decline in the ex-tent of the reefs (Leinfelder et al., 2002; Kiessling, 2008; Tennant et al., 2017). The aims of the present paper are to (1) describe the main facies represented in exotics of the Štramberk-type limestones, (2) attempt to interpret their depositional en­vironments, (3) propose the facies distribution on the car­bonate platform, and (4) discuss their palaeogeographical constraints. GEOLOGICAL SETTING Geological background The exotics were collected in the Polish Outer Carpathians, known also as the Flysch Carpathians (Fig. 1). These mountains constitute part of the Western Carpathians, which belong to the Alpine-Carpathian orogenic belt. Geographically, this area is situated in southern Poland, in the Beskidian Piedmont and in the Beskidy Mountains. Tectonically, the Outer Carpathians are composed of sever­al nappes (e.g., Książkiewicz, 1977). The Outer Carpathian nappes originated in the Miocene, as a result of continental plate collision (e.g., Ślączka, 1996; Oszczypko, 1997, 2004; Golonka et al., 2000, 2006b). The ridges separating the ba­sins were buried and subducted and the deposits of mainly the central parts of the basins are preserved (e.g., Sikora, 1976; Książkiewicz, 1977; Ślączka et al., 2006). Figure 2 shows the lithostratigraphy of the Silesian, Sub-Silesian and Skole series with the locations of the sites of the exotics studied (see also Table 2). The majority of the sample locations are situated in the Silesian Nappe – the second largest Outer Carpathian nappe, which continues Fig. 1. Tectonic map of the Polish and part of the Czech Outer Carpathians (after Lexa et al., 2000; Cieszkowski et al., 2009, modified and simplified), and the position of the Polish Carpathians in the Carpathian belt. Numbers of localities – see Table 3. The simplified location of geological and geographical units discussed in the paper located north of the Carpathians is shown. Subsurface geological units are in italics. Fig. 2. Lithostratigraphic profiles for sedimentary series of the Silesian, Sub-Silesian and Skole nappes with the sites of the exot­ics studied. Names of lithostratigraphic units according to Ślączka et al. (2006), Cieszkowski et al. (2012), and Łapcik et al. (2016). Lithostratigraphic units, from which studied exotic clasts were sampled, are labelled in bold letters. Units indicated with the mark * are particularly rich in exotics. in the areas of the Czech Republic and Ukraine. The sites with the exotics are also located in the lower nappes, i.e., the Sub-Silesian Nappe and the Skole Nappe. The Sub-Silesian Nappe occurs as narrow, discontinuous outcrops to the north of the Silesian Nappe. In the eastern part of the Polish Carpathians, these two nappes are thrust over the Skole Nappe. In the south, the Silesian Nappe borders with the Fore-Magura group of nappes and the Magura Nappe, the largest nappe of the Outer Carpathians. In the north, these nappes are thrust over the Miocene of the Carpathian Foredeep, and partly on the lower tectonic units, the Stebnik and Zgłobice units (the folded Miocene at the front of the Outer Carpathians). Exotics of the Štramberk-type lime­stones from the Fore-Magura group of nappes, the Magura Nappe and the Stebnik and Zgłobice units were not studied for this paper. The Silesian, Sub-Silesian and Skole nappes are com­posed mainly of thick flysch sequences, which are latest Jurassic–Miocene in age, but the oldest (latest Jurassic) deposits are preserved only locally in the Silesian Nappe. Initially, the flysch sequences were deposited in one sed­imentary basin, the Proto-Silesian Basin (e.g., Golonka et al., 2006b; Waśkowska et al., 2009), also termed the Severin–Moldavidic realm (Balintoni, 1998; Ślączka et al., 2006), in Romania commonly referred as to the Outer Dacides and the Moldavides (e.g., Săndulescu, 1988). At the end of the Early Cretaceous, the Proto-Silesian Basin was devel­oped again and deposition took place in several sub-basins separated by ridges (e.g., Książkiewicz, 1965; Golonka et al., 2000). The Sub-Silesian Series was deposited in shallow­er conditions than the Silesian and Skole series, possibly on the slope of the Sub-Silesian Ridge (e.g., Ślączka et al., 2006; Waśkowska et al., 2009), and variegated shales and marls are relatively frequent there. Provenance area of exotic carbonate clasts The source areas of the exotic clasts and other detrital ma­terial of the flysch deposits of the Polish Outer Carpathians are not preserved. The Outer Carpathian Basin was com­posed of some isolated subbasins, subdivided by intrabasi­nal ridges (the cordilleras of Książkiewicz, 1956b, 1965). Together with the margins of the basins, they were source areas that periodically emerged and were eroded (Figs 4, 5), and finally consumed, mostly during the Miocene subduc­tion (e.g., Sikora, 1976; Książkiewicz, 1977).The following Fig. 3. Palaeogeography and palaeoenvironment of the circum-Carpathian area during the latest Late Jurassic–earliest Early Cretaceous with the location of the carbonate platforms of the Štramberk-type limestones (after Golonka et al., 2006a, simplified and slightly modified). deposits were eroded on the ridges: (1) previously depos­ited flysch (so-called “cannibalism” sensu Matyszkiewicz and Słomka, 1994), (2) sediments contemporaneous with the flysch, but representing different environments (e.g., shallow-water carbonates), and (3) pre-flysch deposits. In the Carpathians, some ridges were distinguished, from which the Silesian Cordillera (Książkiewicz, 1965; Unrug, 1968), recently referred to as the Silesian Ridge, was the most important. Traditionally, this ridge is described as existing since the Late Jurassic and was the stable provenance area, located between the Silesian (initially: Proto-Silesian) and Magura basins (Fig. 5). According to Unrug (1968), there is no need to postulate a large land as the provenance area, but possibly relatively small ridges were eroded. Hoffmann (2001), on the basis of analysis of exotics from the western part of the Polish Outer Carpathians, found that structures of different ages and different compositions were described un­der the term “the Silesian Ridge”. In the Late Jurassic–Early Cretaceous, the Silesian Ridge possibly emerged as part of the Upper Silesian Massif (Brunovistulicum Terrane). Since the Albian–Turonian, the ridge was possibly a collision oro­gen, showing a thrust-nappe structure. It involved sediments of different environments, including Precambrian crystal­line rocks, limestones of the Štramberk Carbonate Platform and the Cretaceous flysch. The development of the accretion­ary prism of the Silesian Ridge also was assumed by other au­thors (Soták, 1990; Poprawa et al., 2002, 2006a; Oszczypko, 2004; Poprawa and Malata, 2006; Cieszkowski et al., 2009). The northern provenance area was active mostly in the early stage (till the end of the Early Cretaceous) of devel­opment the Proto-Silesian basin. It is thought that this area was the Baška-Inwałd Ridge, separating the Proto-Silesian Basin and the hypothetical Bachowice Basin (Figs 3–5; Książkiewicz, 1956a, 1965; Olszewska and Wieczorek, 2001; Golonka et al., 2008). The Bachowice Basin was supposed to be located north of the proto-Silesian Basin and the Baška-Inwałd Ridge (Książkiewicz, 1956a; Kowal-Kasprzyk et al., 2020). In the opinion of Hoffmann (2001), there was no broad Bachowice Basin. Hoffmann (2001) noticed the similarity in the lithologies of exotics from Bachowice with the southerly situated Cetechovice–Magura sedimentary unit (see Houša et al., 1963; Soták, 1990). He concluded that these sediments were included to the Sub-Silesian Unit during resedimentation and development of the accretionary prism of the orogen of the Silesian Ridge (see also Bucur et al., 2005, p. 108). The Baška Ridge (the Baška-Inwałd Ridge in the Polish literature) was the place where the Štramberk Limestone, known from Moravia, originated (Eliáš and Eliášová, 1984; Picha et al., 2006). The northern source area, especially since the Late Cretaceous, is commonly referred to as the Sub-Silesian (sometimes called Węglówka) Ridge. In the Sub-Silesian Unit, exotics, known mainly from the Lower Cretaceous deposits, are related to the later mentioned stage of intense activity of the Baška-Inwałd Ridge. Exotics in the younger Sub-Silesian flysch beds – deposited after the reorganisation of the Proto-Silesian Basin into several sedimentary areas – are not very common, because coarse-grained deposits oc­cur only locally in this unit. Fig. 5. Palaeotransport directions of detritalmaterial in the northern Carpathian basins in the latest Cretaceous; deposition of the Lower Istebna Formation (directions in conglomerates and thick-bedded sandstones), Ropianka Formation and local sandstones beds in the Sub-Silesian Series (after Książkiewicz, 1962; Unrug, 1963). Note that tectonic rotations in the Outer Carpathians are not included. Detrital material accumulating in the Skole Basin was derived from the Northern (Marginal) Ridge (Cordillera), meaning the southern part of the Upper Silesian and Małopolska massifs, and from the Sub-Silesian Ridge to the south (e.g., Książkiewicz, 1962; Łapcik et al., 2016; Łapcik, 2018 and literature therein). Figures 4 and 5 present palaeogeographic maps, show­ing the palaeotransport directions of detrital material in two flysch lithostratigraphic units: transport from the northern and southern areas during the Early Cretaceous, and dom­inantly from the southern area during the Late Cretaceous (based on Książkiewicz, 1962; Unrug, 1968; Strzeboński et al., 2009). Age of the studied limestones “Štramberk-type limestones” is a field term. These lime­stones are traditionally believed to be the age and facies equivalent of the Štramberk Limestone, which is Tithonian– early Berriasian in age (e.g., Houša, 1990; Houša and Vašíček, 2004; Vašíček and Skupien, 2013, 2014, 2016, 2019; Vašíček et al., 2013; Vaňková et al., 2019), although a latest Kimmeridgian–early Berriasian age was also as­sumed (Houša, 1990; Houša and Vašíček, 2004). Until the 1980s, the Štramberk Limestone was commonly dated as Tithonian. Both recent (Kowal-Kasprzyk, 2014, 2016, 2018) and earlier studies (summarized below; see also the review in Kołodziej, 2015a) showed that most exotic carbonate clasts, traditionally designated the Štramberk-type limestones, are of Tithonian–early Berriasian age. During field studies or even in microscopic studies, it is often impossible to de­termine the age of the Štramberk-type limestones. Recent studies of exotics, which could be in the field classified as the Štramberk-type limestones, revealed that some percent­age of the determinable clasts represent the Oxfordian– Kimmeridgian (Kowal-Kasprzyk, 2016; Kowal-Kasprzyk et al., 2020). Calpionellids are the best stratigraphic markers of the uppermost Jurassic and lowermost Cretaceous deposits. They were determined in the Štramberk-type limestones, including the coral-bearing facies, mainly by Morycowa (1964a, 1988), Ciborowski and Kołodziej (2001) and Kowal-Kasprzyk (2014, 2018), but they were noted also in other works (see Table 1). Generally, the late Tithonian Chitinoidella and Crassicollaria zones, as well as the early Berriasian Calpionella zone are well documented. Younger calpionellid zones were observed in the Kruhel Wielki klippe, where Morycowa (1988) described assemblages of latest Tithonian to early Valanginian age (Crassicollaria to Calpionellites zones). Although Morycowa (1988) did not classify the Valanginian–Hauterivian pelitic limestone blocks (with calpionellids and stomiospherids) from the Kruhel klippe as the Štramberk-type limestones, these lime­stones seem to be analogous to FT 8 of the present authors (see below). In contrast to the Štramberk Limestone (Vašíček and Skupien, 2013, 2014, 2016; Vašíček et al., 2013), well pre­served ammonites are very rare in the exotics. Książkiewicz (1974) described Pseudovirgatites scruposus (Oppel), im­plying an early late Tithonian age for the large limestone boulder at Woźniki. Ivanova and Kołodziej (2010), on the basis of fo­raminifera determined the ages of 30 exotic clasts of the Štramberk-type limestones. Fifteen of them were not older than Tithonian, 13 not older than Berriasian, and at least two of them were Valanginian in age. However, some foraminif­eral species, not known from before the Valanginian, may in fact occur in older strata. Vaňková et al. (2019) recognized that assemblages of the Berriasian peri-reefal limestones at Štramberk contain several taxa previously reported from the Valanginian. Some of the important studies on the shal­low-water foraminifera, which appear also in the Štramberk­type limestones, were based on Lower Cretaceous profiles that did not include the Jurassic–Cretaceous boundary. New data from Romania indicate that Meandrospira favrei (Charollais, Brönnimann et Zaninetti), recognized in the Štramberk-type limestones (Ivanova and Kołodziej, 2010), is not restricted to Valanginian–Hauterivian, but occurs also in Berriasian (Krajewski and Olszewska, 2006; Bucur et al., 2020). Recently, Kowal-Kasprzyk (2016) provided new data on biostratigraphy, based on foraminifera and calcareous dino­flagellate cysts. Some of the earliest Cretaceous foraminiferal taxa have been observed with the late Tithonian calpionellid assemblages. The majority of the foraminifera occurring in the Štramberk-type limestones have relatively wide strati­graphic ranges; some of them occur both before and after the Tithonian–Berriasian interval. Numerous species first appear in the Tithonian, but are also common in the Lower Cretaceous deposits. An exclusively latest Kimmeridgian– Tithonian speciesis Bulbobaculites elongatulus (Dain). Taxa that first appeared before the Tithonian, but disappeared at the Jurassic–Cretaceous boundary (Protopeneroplis striata Weynschenk, Pseudomarssonella? dumortieri (Schwager), Paleogaudryina varsoviensis (Bielecka et Pożaryski)) or in the early Berriasian (Paleogaudryina magharaensis Said et Barakat, Textularia depravatiformis Bielecka et Kuznetsova) are also useful for stratigraphic purposes. Pseudotextulariella courtionensis Brönnimann is a Berriasian taxon. Several taxa (Haplophragmoides cushm­ani Loeblich et Tappan, Haplophragmoides joukowskyi Charollais,BrönnimannetZaninetti, Patellina subcretacea Cushman et Alexander, Hechtina praeantiqua Bartenstein et Brand, Nautiloculina cretacea Peybernes) first appeared in the Berriasian and are also known from younger strata. Calcareous dinoflagellate zones – often interval zones (e.g., Reháková, 2000) – are usually hard to determine in the exotics, because continuous profiles cannot be observed. Moreover, in the deposits of shallow zones, specimens of di­nocysts are not very numerous. The biostratigraphic signifi­cance of calcareous dinoflagellate cysts is undoubted. In the Tithonian–Berriasian exotics, the most common are taxa with relatively wide ranges, such as Crustocadosina semiradiata semiradiata (Wanner), Colomisphaera carpathica (Borza). For this time interval, the most important stratigraphically are Carpistomiosphaera borzai (Nagy), C. tithonica Nowak, Committosphaera pulla (Borza), Parastomiosphaera malmica (Borza), Colomisphaera tenuis (Nagy), C. fortis Řehánek (Kowal-Kasprzyk, 2016). Generally, foraminifera and dinocysts confirm the Tithonian–Berriasian age of the Štramberk-type limestones studied, but the separation of the Tithonian from the Berriasian, based on these fossils, is of-ten problematic. The possibility cannot be excluded that sedimentation of the Štramberk-type limestones (mostly of lagoonal and algal-foraminiferal facies) persisted locally even to the Valanginian (Ivanova and Kołodziej, 2004, 2010), but all available data indicate that the main development of coral reefs (both in the Štramberk Limestone and the Štramberk­type limestones) occurred in the late Tithonian and less extensively in the early Berriasian. Štramberk-type sedi­ments younger than the early Berriasian are not known from the large Kotouč Quarry near Štramberk, but Valanginian shallow-water limestones have already been recognized as pebbles in the Outer Carpathians in the Czech Republic (Soták and Mišík, 1993). Valanginian shallow-water marine carbonates (algal facies) were also recognized recently in the strata drilled in the Carpathian Foredeep (e.g., Matyja, 2009; Urbaniec et al., 2010). Zdanowski et al. (2001) de­scribed Valanginian crinoid-bryozoan grainstones in the Carpathian Foredeep and interpreted them as documenting the transgression maximum. MATERIAL AND METHODS The exotics studied, almost exclusively light- or dark­beige in colour (usually the dark-coloured ones are from deeper facies), are mostly of pebble and cobble sizes (from a few centimetres to ca. 20 cm); more rarely they are blocks, up to 1 m in diameter (Fig. 6). The clasts are largely spher­ical, mostly well-rounded. There are neither macroborings nor encrusting organisms on the surface; only very rare si­liceous crusts occur. The exotics were collected at 36 sites in the area of the Silesian, Sub-Silesian and Skole nappes (Fig. 1, Tabs 2 and 3). Sampling by M. Hoffmann started in the 1980s. The outcrops of exotic-bearing flysch deposits studied are small (Fig. 6A, B). The most effective approach to sampling the exotics, especially the larger clasts, was in streams. Thousands of exotics were examined macroscopi­cally in the field. About 800 thin sections were made from 550 exotics. Most of the thin sections are of standard size (4 × 2.7 cm); about 20 of them are large (6 × 5 cm). The exotics are from the uppermost Jurassic to Oligocene flysch deposits of diverse lithostratigraphic units (Fig. 2; Tabs 2 and 3), but the majority of them are from the Hradiště Formation and the Veřovice Formation (Hauterivian– Aptian), the Istebna Formation (Campanian–Paleocene), and the Ciężkowice Formation and the Hieroglyphic Formation (Eocene) of the Silesian Unit. The exotic-bearing sediments in the study area, more rarely at a particular local­ity, are described or mentioned in the literature references included in Table 3. The samples were studied macroscopically (in the field and in the laboratory using cut and polished slabs) and mi­croscopically. Nearly all the microscopic images on figures are from exotic clasts with a location provided. Some pic­tures are from exotics (collected by the present authors), for which no location is given, but they well document the fa­cies described. The exotics and thin sections are housed in Fig. 6. Field pictures showing exotic-bearing flysch deposits and exotic clasts of the Štramberk-type limestones. A. Clasts in the Piechówka Sandstone Member of the Hradiště Formation, Żegocina (locality 27). B. Żywiec olistostrome, clasts in conglomerate (Hradiště Formation; locality 2). C. Boulder in the Veřovice Formation (co-called “dark exotic-bearing shales”), Barwałd Górny (locality 6). D. Small boulder in a stream, Hradiště Formation, Jastrzębia (locality 10). Table 2 List of localities with the studied exotic clasts of the Štramberk-type limestones, arranged according to their lithostratigraphic and tectonic positions. The number of each locality is in brackets. For the geographic positions, see Figure 1 and Table 3. The names of lithostratigraphic units are according to Ślączka et al. (2006), Cieszkowski et al. (2012), and Łapcik et al. (2016). Unit Formation (age) Locality Vendryně Formation (former Lower Cieszyn Beds, late Kimmeridgian–middle late Tithonian) Zamarski (1) Hradiště Formation, mainly Piechówka Sandstone Member (Hauterivian–Barremian) Żywiec (2), Biskupice (16), Dobranowice (18), Sułów (19), Żegocina (27), Milówka (32), Roztoka (33) Veřovice Formation (Barremian–Aptian) Leśnica (9) Lhoty Formation (Albian–Cenomanian) Jastrzębia (11) Silesian Lower Istebna Formation (Campanian–Maastrichtian) Zarzyce Wielkie (8), Leńcze (12), Izdebnik (13), Krzyworzeka (20), Dzielec (24), Kobylec (25), Rożnów (31) Upper Istebna Formation (Paleocene) Mały Czaniec (3), Targoszów (4), Mucharz (5), Tarnawa (26) Ciężkowice Formation (Eocene) Podole-Górowa (29), Gródek nad Dunajcem (30) Hieroglyphic Formation (Eocene) Lipie (28) Menilite Formation (Oligocene) Skrzydlna (22) Hradiště Formation (Barremian–Aptian) Jastrzębia (10), Sygneczów (15), Wiśniowa (21) Sub-Silesian Veřovice Formation (Hauterivian–Albian) and Gaize Beds (late Aptian–early Cenomanian) Barwałd Górny (6), Woźniki (7), Lusina (= Krzywica) (14), Trąbki (17) Frydek-type marls/Rybie Sandstone (latest Cretaceous–earliest Paleocene) Nowe Rybie (23) Skole Ropianka Formation (Maastrichtian–Paleocene) Wola Rafałowska (35), Lipnik Hill (Wapielnica) (36), Koniusza (37) Babica Clays (late Paleocene) Lubenia (34) the Institute of Geological Sciences, Jagiellonian University in Kraków and in the Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology in Kraków. RESULTS Facies and microfacies General remarks As noted in the section “Age of the studied limestones”, several percent of the exotics, especially if beige in colour, can be confused in the field with the Štramberk-type lime­stones, but in fact they are of Oxfordian–Kimmeridgian age (Kowal-Kasprzyk et al., 2020). These limestones were not described here but are summarized in the chapter “Discussion”. Facies FT 1–FT 8 (Štramberk-type limestones sensu stricto), are considered as being of Tithonian–lowermost Cretaceous age. The age was determined palaeontologically or such age is inferred on the basis of similarities in lithol­ogy with the carbonate clasts, for which the age had been determined. The age of the samples, assigned to the main facies, was based on the work of Ciborowski and Kołodziej (2001) and Ivanova and Kołodziej (2004, 2010) and for the most part that of Kowal-Kasprzyk (2016, 2018). Traditionally, the Štramberk-type limestones are con­sidered to be reefal limestones, but in fact, they represent diverse facies of the carbonate platform and its slope. The names of the facies distinguished here are based on sedimentary characteristics on the scale of clasts (pebbles, cobbles, rarely boulders). For the determination of facies, especially shallow-water facies, it is recommended that clasts at least several centimetres in diameter are studied. Owing to the heterogeneity of shallow-water facies, they show high variability in microfacies (especially coral-mi­crobial boundstones) and are represented by more than one microfacies. Therefore, the study of a single thin-section is not necessarily representative of the facies and will be in­adequate for the study of some facies. Figure 7 shows an exotic ca. 20 cm in diameter, possibly representing coral­microbial boundstones (FT 1), although not in a character­istic development. In different parts of it, four microfaci­es can be distinguished. If only a small fragment of such a clast (one thin-section or a much smaller fragment) were to be studied, the assignment to this facies would be correct only in the case of the part labelled as 1. On the other hand, the microfacies study of the packstone-grainstone matrix of the exotic discussed is necessary, because if this matrix con­tains numerous foraminifera and dasycladalean green algae, the exotic should be assigned to the foraminiferal-algal limestones (FT 5). Table 4 contains a list of recognized, encrusting micro­organisms (microencrusters), their recent biological affilia­tion (they are usually of uncertain genesis) and their relative abundance in four facies (F1–F3, F5). These microencrusters (important for reef construction and/or for the interpretation of the sedimentary environment)are reviewed and literature references are provided in Leinfelder et al. (1993), Schmid (1996), Schlagintweit et al. (2005), Pleş et al. (2013, 2017) and Kaya and Altiner (2015). Table 5 contains a list of main foraminiferal genera, recognized in the various facies. FT 1: Coral-microbial boundstones (Figs 8–10) This boundstone type is defined here as a boundstone, constructed by corals, usually associated with micro­bialites and/or microencrusters. Corals are represented mostly by phaceloid forms (the branching growth type; Figs 8A, B, 9A; see e.g., Morycowa, 1974; Kołodziej, 2003a). Microbialites, commonly only thin crusts, are de­veloped as clotted thrombolite, layered thrombolite, poor­ly structured thrombolite, leiolite, clotted leiolite, micritic stromatolite, and peloidal to agglutinated stromatolite (the frequency of microbialite types was not estimated; Figs 8B, D–F, 9B, D–F, 10E). They are composed mostly of micrope­loids and clotted micrite. The matrix sediment is composed of bioclastic-peloidal packstone to grainstone (Figs 8B, 9B), rarely wackestone, thus this sediment is similar to the peloi­dal-bioclastic limestones (FT 6). Calpionellids and calcare­ous dinoflagellate cysts are present in the micrite-dominated matrix of some samples. Microencrusters include (in order of abundance): Crescentiella morronensis (Figs 10A, E), calcimicrobial crusts with entobian borings (termed here as “Lithocodium”– like structures; Figs 9A–D, 10B, C, F), bacinellid microbial structures (Fig. 10D), calcified sponges (Figs 9B, F, 10E), Iberopora bodeuri (Fig. 10C), Koskinobullina socialis (Figs 9C, 10C), Labes atramentosa (Figs 9F, 10A, F), Thaumatoporella parvovesiculifera, rare Lithocodium aggregatum (Fig. 10B), Radiomura cautica (Fig. 10F) Table 3 Localities (in the order of the numbers marked on Figure 1 and in Table 2) with reference to the literature, in which exotic-bearing sediments in the study area, more rarely a particular locality, are described or mentioned. Most localities have GPS data. No Locality Description Unit Formation Literature 1 Zamarski 6 km N of Cieszyn Silesian Vendryně Formation (former Lower Cieszyn Beds) Król and Decrouez (2002) 2 Żywiec outcrop in Soła River, western part of Grójec Hill (49°40'18.7"N, 19°11'35.8"E) Silesian olistostrome of the Cisownica Shale Member – Hradiště Formation (former Upper Cieszyn Beds) Cieszkowski et al. (2009) 3 Mały Czaniec (Bulowice) 5 km SE of Kęty, clasts from Szybówka stream; area of poor outcrops (around 49°51'38.8"N, 19°15'46.7"E) Silesian Upper Istebna Formation (?) Nowak (1959) 4 Targoszów 10 km W of Sucha Beskidzka, outcrop in Targoszówka stream, close to a road from Kuków to Targoszów (49°45'17.2"N, 19°27'35.3"E) Silesian Upper Istebna Formation Strzeboński et al. (2017) 5 Mucharz 8 km S of Wadowice, outcrop in Skawa River (49°49'15.9"N, 19°32'33.1"E) Silesian Upper Istebna Formation Strzeboński et al. (2017) 6 Barwałd Górny 5 km W of Kalwaria Zebrzydowska, outcrop in tributary of Zakrzówka stream (49°51'04.6"N, 19°37'15.8"E) Sub-Silesian Veřovice Formation Książkiewicz (1951a, b) No Locality Description Unit Formation Literature 7 Woźniki 6 km N of Wadowice, Rędzina stream in Woźniki village Sub-Silesian black shales within the Gaize Beds Książkiewicz (1974), Morycowa (1974) 8 Zarzyce Wielkie 3 km NE of Kalwaria Zebrzydowska, outcrop in landslide niche in Solca za Lasem hamlet (49°52'49.2"N, 19°43'03.7"E) Silesian Lower Istebna Formation Książkiewicz (1951a, b) 9 Leśnica 2 km S of Kalwaria Zebrzydowska, clasts from tributary of Cedron stream (around 49°50'53.2"N, 19°41'09.9"E) Silesian Veřovice Formation 10 Jastrzębia (= Lanckorona) 1.5 km E of Lanckorona, clasts from Jastrzębia stream in Kopań hamlet (around 49°50'26.3"N, 19°44'23.5"E) Sub-Silesian Hradiště Formation Książkiewicz (1951a, b) 11 Jastrzębia 4 km E of Lanckorona, clasts from tributary of Jastrząbka stream between Jastrzębia and Sułkowice villages, poorly outcropped area (around 49°50'30.0"N, 19°46'15.0"E) Silesian Lhoty Formation (?) Książkiewicz (1951a, b) 12 Leńcze 5 km N of Kalwaria Zebrzydowska, stream in Leńcze village Silesian Lower Istebna Formation Książkiewicz (1951a, b) 13 Izdebnik 6 km E of Kalwaria Zebrzydowska, outcrops in tributary of Jastrząbka stream (around 49°52'29.0"N, 19°45'33.1"E) Silesian Lower Istebna Formation Książkiewicz (1951a, b) 14 Lusina (= Krzywica) 7 km W of Skawina, Krzywa stream in Krzywica village Sub-Silesian Veřovice Formation Michalik (1980) 15 Sygneczów 1) 4 km SW of Wieliczka, old pit (49°58'07.4"N, 20°00'35.2"E); 2) 3 km SW of Wieliczka, tributary of Wilga stream in Łysa Góra hamlet (49°57'55.9"N, 20°01'44.9"E) Sub-Silesian Hradiště Formation Burtan (1956), Książkiewicz (1965) 16 Biskupice 6 km SE of Wieliczka: 1) outcrops in a forest gorge (around 49°57'30.2"N, 20°07'01.5"E); 2), tributary of Bogusława stream, north of a gorge (49°57'32.6"N, 20°06'51.0"E) Silesian (Sub-Silesian? see Burtan, 1956, 1984) Piechówka Sandstone Member of the Hradiště Formation Burtan (1956), Burtan et al. (1984) 17 Trąbki 7.5 km SE of Wieliczka, outcrops in small unnamed stream close to Tarnówka hamlet (49°57'33.2"N, 20°08'03.2"E) Sub-Silesian Gaize Beds Burtan (1956) 18 Dobranowice 7 km S of Wieliczka, outcrops in tributary of Sułówka stream between Sułów and Dobranowice villages (around 49°56'51.9"N, 20°07'42.1"E) Silesian (Sub-Silesian? see Burtan, 1956, 1984) Piechówka Sandstone Member of the Hradiště Formation Burtan (1956) 19 Sułów 6 km SE of Wieliczka: 1) Sułówka stream (around 49°57'17.6"N, 20°07'23.8"E); 2) tributary of Zagórzanka stream (around 49°57'10.8"N, 20°06'42.6"E) Silesian (Sub-Silesian? see Burtan, 1956, 1984) Piechówka Sandstone Member of the Hradiště Formation Burtan (1956), Burtan et al. (1984) 20 Krzyworzeka 4.5 km SE of Dobczyce, outrcops in two tributaries of Zagórzanka stream, between Krzyworzeka and Kędzierzynka villages (around 49°52'06.4"N, 20°08'37.7"E and around 49°51'47.3"N, 20°09'03.0"E) Silesian Lower Istebna Formation Burtan (1956), Chodyń et al. (2005) 21 Wiśniowa outcrops in tributary of Krzyworzeka stream in Wiśniowa village (around 49°47'13.5"N, 20°06'09.1"E) Sub-Silesian (Wiśniowa Tectonic Window) Hradiště Formation Burtan et al. (1984), Burtan (1977) No Locality Description Unit Formation Literature 22 Skrzydlna 11 km NE of Mszana Dolna, quarry in Skrzydlna village (49°44'55.9"N, 20°09'57.9"E) Silesian Menilite Formation Burtan et al. (1984), Polak (2000) 23 Nowe Rybie 9 km NW of Limanowa, outcrops in Tarnawka stream (around 49°46'57.7"N, 20°19'49.8"E) Sub-Silesian Frydek-type marls (“grey exotic-bearing marls”)/Rybie Sandstone Burtan et al. (1984) 24 Dzielec 1.5 km N of Stare Rybie, old small quarry and outcrop in tributary of Przeginia stream below the quarry (49°49'03.2"N, 20°19'08.4"E) Silesian Lower Istebna Formation Burtan et al. (1984) 25 Kobylec 2.5 km NW of Łapanów, stream between Syberia and Borówka hamlets (around 49°53'13.8"N, 20°16'57.0"E) Silesian Lower Istebna Formation Burtan et al. (1984) 26 Tarnawa 4 km S of Łapanów, outcrops in tributary of Tarnawka stream (around 49°49'47.5"N, 20°17'09.6"E) Silesian Upper Istebna Formation Burtan et al. (1984) 27 Żegocina old quarry in Żegocina village (49°48'33.2"N, 20°25'14.5"E) Silesian Piechówka Sandstone Member of the Hradiště Formation Malik and Olszewska (1984) 28 Lipie 12 km N of Nowy Sącz, outcrop on bank of Rożnów Lake (49°43'33.2"N, 20°42'55.1"E) Silesian Hieroglyphic Formation Cieszkowski (1992) 29 Podole Górowa 16 km NE of Nowy Sącz, outrcops in tributary of Paleśnianka stream (around 49°44'35.7"N, 20°49'29.4"E) Silesian Ciężkowice Forma­tion/Hieroglyphic Formation Cieszkowski et al. (1991) 30 Gródek nad Dunajcem 14 km N of Nowy Sącz, outcrop on bank of Rożnów Lake (49°43'56.8"N, 20°43'17.2"E) Silesian Ciężkowice Formation Cieszkowski (1992), Morycowa (1968), Leszczyński (1978) 31 Rożnów 16 km N of Nowy Sącz, outcrop on bank of Rożnów Lake (49°45'53.3"N, 20°40'39.1"E) Silesian Lower Istebna Formation 32 Milówka 14 km SE of Brzesko, stream in Milówka village Silesian Piechówka Sandstone Member of the Hradiště Formation 33 Roztoka 19 km SE of Brzesko, outcrop in Roztoka village Silesian Piechówka Sandstone Member of the Hradiště Formation 34 Lubenia 12 km S of Rzeszów, Lubeńka stream in Lubenia village Skole Babica Clays Kropaczek (1917), Bukowy (1957) 35 Wola Rafałowska 15 km SE of Rzeszów: 1) tributary of the Chmielnik stream (49°59'20.0"N, 22°11'0.9"E); 2) gorge of unnamed stream in Wola Rafałowska village (49°59'11.7"N 22°11'05.4"E) Skole Ropianka Formation Łapcik et al. (2016) 36 Lipnik Hill (Wapielnica) 5 km SW of Przemyśl. The locality is in the vicinity of poorly exposed Kruhel klippe Skole Ropianka Formation Bukowy and Geroch (1956), Nowak (1963), Morycowa (1964a) 37 Koniusza 10 km SW of Przemyśl Skole Ropianka Formation Ney (1957), Kotlarczyk (1985), Dżułyński and Kotlarczyk (1988) Table 4 Biological affiliation of microencrusters and their relative abundance in the coral-microbial boundstones (FT 1), microencruster-microbial-cement boundstones (FT 2), microbial and microbial-sponge boundstones (FT 3), and foraminiferal-algal limestones (FT 5). Microencruster present (•); common (••); very common (•••); not recognized (–); uncertain occurrence (?). Microencrusters Biological affiliation Facies FT 1 FT 2 FT 3 FT 5 “Lithocodium-Bacinella” umbrella term ••• ? – ••• Lithocodium aggregatum Elliott ulvophycean green algae • – – ? Bacinellid structures calcimicrobial origin •• ? – ••• “Lithocodium”-like structures calcimicrobial crusts with entobian borings ••• ? – •• Koskinobullina socialis Cherchi et Schroeder incertae sedis: algae? foraminifera? •• – – • Iberopora bodeuri Granier et Berthou incertae sedis: algae? foraminifera? •• – – • Thaumatoporella parvovesiculifera (Raineri) incertae sedis: green algae? cyanophyceans? • – – ••• Crescentiella morronensis (Crescenti) nubeculariid foraminifera ••• ••• ••• • Labes atramentosa Eliášová incertae sedis • ••• • – Radiomura cautica Senowbari-Daryan et Schäfer calcified sponge? • •• – – Perturbatacrusta leini Schlagintweit et Gawlick calcified sponge? • •• – – Terebella lapilloides Münster “worms” • • ••• • Calcified sponges •• •• • • Table 5 Distribution of foraminifera in facies types. Facies type Typical foraminifers FT 1 Benthic calcareous forms (Bullopora, Coscinoconus, Dobrogelina, Lenticulina, Mohlerina, Protopeneroplis, Spirillina, Troglotella, Trocholinidae, Neotrocholininae, Nodosarioidea, miliolids) and agglutinated forms (Gaudryina, Haghimashella, Paleogaudryina, Protomarssonella, Textularia, Uvigerinammina, Valvulina) FT 2 In obvious examples of this facies, foraminifera are rare, difficult to determine and represent allochthonous elements FT 3 Benthic calcareous forms (Bullopora, Lenticulina, Mohlerina, Protopeneroplis, Rumanolina, Spirillina, Neotrocholininae, Nodosarioidea, Epistominidae, Nubeculariidea and rare other miliolids) and agglutinated forms (Glomospira, Haghimashella, Paleogaudryina, Protomarssonella, Reophax, Textularia, Uvigerinammina, Valvulina) FT 4 Foraminifers occur mainly in lithoclasts FT 5 Assemblages rich and diversified; the most typical are larger benthic forms with complex wall structure (Charentia, Everticyclammina, Melathrokerion, Pseudocyclammina) and numerous miliolids; other foraminifers: benthic calcareous and calcareous agglutinated forms (Bullopora, Coscinoconus, Dobrogelina, Lenticulina, Mayncina, Mohlerina, Nautiloculina, Pfenderina, Protopeneroplis, Rumanolina, Siphovalvulina, Spirillina, Troglotella, Trocholinidae, Neotrocholininae, Nodosarioidea), agglutinated forms (Ammobaculites, Coscinophragma, Gaudryina, Haghimashella, Haplophragmium, Paleogaudryina, Pseudomarssonella, Textularia, Uvigerinammina, Valvulina, Verneuilina) FT 6 Benthic calcareous forms (Coscinoconus, Dobrogelina, Everticyclammina, Lenticulina, Mayncina, Mohlerina, Patellina, Pfenderina, Protopeneroplis, Rumanolina, Siphovalvulina, Troglotella, Trocholinidae, Neotrocholininae, Nubeculariidea, Nodosarioidea, Spirillinidae, numerous miliolids), agglutinated and calcareous-agglutinated forms (Arenobulimina, Charentia, Coscinophragma, Glomospira, Haghimashella, Haplophragmium, Haplophragmoides, Melathrokerion, Nautiloculina, Paleogaudryina, Protomarssonella, Pseudocyclammina, Reophax, Textularia, Trochammina, Uvigerinammina, Valvulina, Verneuilina) FT 7 Benthic calcareous forms (Lenticulina, Protopeneroplis, Spirillina, miliolids) and agglutinated forms (Paleogaudryina, Protomarssonella, Reophax, Textularia, Verneuilina) FT 8 Mainly benthic calcareous forms (Lenticulina, Ophthalmidium, Spirillinidae, Nodosarioidea, Nubeculariidea), less commonly agglutinated forms (Protomarssonella, Paleogaudryina) Fig. 8. Exotics representing the coral-microbial boundstones (FT1). A–C. Coral-dominated boundstones. D–E. Microbialite-dominated boundstones. A. Phaceloid (branching) colony of the coral Placophyllia dianthus. B. Phaceloid coral Thecosmilia sp. encrusted by calci­fied sponges (cs) and bored by bivalves (bor); mc – microbial crust; gr – bioclastic-peloidal grainstone; white spots represent Crescentiella morronensis and Labes atramentosa. C. Dense aggregation of encrusting corals (cor 1, cor 2, cor 3). D. Corals (cor), microbialites (mc) and numerous C. morronensis and L. atramentosa (white spots, some are arrowed). E. Microbialite-dominated boundstone with rare corals (cor). Growth cavity(cav) is filled with different generations of the internal sediment, including laminated, dark limestone (arrow). F. Cavity formed by the growth of corals (cor) and microbial crusts (mc) and filled with laminated, peloidal sediment (mostly crustacean microcoprolites Favreina sp.). A, B – Woźniki, C – Leńcze, D, E – Lusina, F – Jastrzębia. Fig. 9. Microfacies of the coral-microbial boundstones (FT 1). A. Corallites of phaceloid pachythecaliine coral Pleurophyllia aff. trichotoma encrusted mostly by calcimicrobial crusts with entobian borings (“Lithocodium”-like structures, arrowed); mc – peloidal­agglutinated microbialite. B. Phaceloid coral Calamophylliopsis sp. encrusted by “Lithocodium”-like structures (L, arrow), calcified sponges (cs) and microbial micropeloidal crust (mc); gr – intra-reef peloidal grainstone. C. Coral encrusted by Koskinobullina socialis (Ks), “Lithocodium”-like calcimicrobial crust (L), ?Lithocodium aggregatum (Lia) and foraminifer Coscinophragma cribrosum (Cc). D. Coral (cor) encrusted by “Lithocodium”-like crust (L), Crescentiella morronensis (Cm) and laminated, micropeloidal, microbial crust (mc). E. Cavity (cav) formed by the growth of corals (cor) and microbialite crusts (mc) filled with multigenerational, internal sediment. The youngest sediment generation (on the left) consists of laminated, micritic sediment. For the original sedimentary position, the image should be rotated 90 degrees in a clockwise direction. F. Growth cavity formed by the microsolenid coral (cor on the right), lined with non-photophilic microencrusters (ch – chaetetids, Pl – Perturbatacrusta leini, La – Labes atramentosa, s – serpulids, cc – cement crusts, mc – microbial crusts). The internal sediment (on the left) consists of peloidal packstone-grainstone, including microcoprolites Favreina. A – Zamarski, B – Leńcze, C – Sułów, D – Gródek nad Dunajcem, E – Lusina, F – Jastrzębia. B. Coral fragmentencrusted by “Lithocodium”-like crust (L) and Lithocodium aggregatum (Lia). C. Thick crust of Iberopora bodeuri with thin intergrowths of “Lithocodium”-like structures (L, arrowed) and Koskinobullina socialis (Ks). D. Microbial crust showing “bacinellid” vesicular fabric. E. L. atramentosa (La), Radiomura cautica (Rc), calcified sponges (cs), microbialite crust (mc) and small coral bioclast (cor). Microfabricresembles this one in the microencruster-microbial-cement boundstones (FT2). F. “Lithocodium”-like crust with boring and cryptic foraminifer Troglotella incrustans. A– Targoszów, B – Podole-Górowa, C – Leńcze, D – Izdebnik, E – Biskupice, F – Zarzyce Wielkie. and Perturbatacrusta leini. “Lithocodium”-like structures are commonly associated with the boring and cryptic fo­raminifer Troglotella incrustans Wernli et Fookes(Fig. 10F; for more examples from the Štramberk-type limestones see Kołodziej, 1997a). An umbrella term, “Lithocodium-Bacinella”, usually had to be used (like commonly in the literature) in micro-facies descriptions, because it was difficult to differentiate between true L. aggregatum (an alga with morphologically different euendolithic, chasmoendolithic, epilithic and ter­minal stages, sensu Schlagintweit et al., 2010) and struc­tures of other origins (see the section “Microencrusters” in the chapter “Depositional and environmental settings”). Other algae are not numerous and are represented by green algae (fragments of dasycladales, Nipponophycus ramosus Yabe et Toyama), rare red algae (“Solenopora”), the prob­lematic Marinella lugeoni Pfender and rivulariacean-like cyanobacteria (Bucur et al., 2005). Podoba (2009) described in a Master’s thesis common, calcified sponges (= hypercalcified sponges, sclerospong­es), mostly millimetres in size (identified in thin sections). It is not clear which facies the species are from. Probably, most of them are from the coral-microbial boundstones, because the microencruster-microbial-cement boundstones are much less common, and in other facies calcified spong­es are rare (Table 3). On the other hand, in the coral-mi­crobial boundstones, calcified sponges are not important in the reef framework, although they are more taxonomi­cally diverse. The calcified sponges, described by Podoba (2009), are represented by chaetetids (?Ptychochaetetes globosus Koechlin, ?Chaetetes ehrenbergi Bachmayer et Flügel and others not determined), Neuropora lusitani­ca Termier, Burgundia astrotubulata Turnšek, Cylicopsis verticalis? Turnšek, ?Cladocoropsis mirabilis Felix, ?Dehornella crustans Hudson, ?Milleporidium reme­si Steinmann, ?Sobralispongia densespiculata Schmid et Werner, ?Calciagglutispongia yabei Reitner,and Calcistella cf. jachenhausenensis Reitner. Apart of the species mentioned above, corals are encrust­ed by annelids (serpulids, Terebella lapilloides), foraminif­era (nubeculariids, Coscinophragma sp.), bryozoans (e.g., Reptomulticava sp., Heteropora sp., ?Ceriocava sp.; Hara and Kołodziej, 2001), and more rarely by ostreid-like bi­valves and small thecideid brachiopods. Microbialites pre­dominate over corals (on the scale of the clast) in some sam­ples. Nevertheless, these clasts are classified as referable to FT 1 because they are assumed to be parts of the coral-mi­crobial patch-reefs. The microencruster-microbial-cement microframework of FT1 can be locally (in the scale of one thin-section) com­posed as in the microencruster-microbial-cement boundstones (FT 2), of non-photophilic (not light-dependent) microen­crusters (Fig. 10F), which makes it resemble the microframe­work of FT2. The intergrowth of corals, microencrusters and microbialite crusts has resulted in the origin of growth cavi­ties, up to several centimetres in diameter. The walls of the cavities (cryptic microhabitat) are encrusted by microbialites and non-photophilic microencrusters (Fig. 9E, F). The cavi­ties are mostly filled with peloidal wackestones-packstones, including crustacean microcoprolites Favreina (Figs 8F, 9F). Age: The Tithonian and earliest Cretaceous age of this facies is confirmed by the occurrence of such stratigraph­ically significant microfossils as the calcareous dinocysts Carpistomiosphaera tithonica, Colomisphaera fortis; C. tenuis, Committosphaera ornata (Nowak), C. pulla; calpionellids: Calpionella alpina Lorenz, Chitinoidella boneti Doben, Ch. elongata Pop, Ch. popi Sallouhi, Boughdiri et Cordey, Crassicollaria intermedia (Durand Delga), C. parvula Remane, and Tintinnopsella carpathica (Murgeanu et Filipescu); and the foraminifers Coscinoconus alpinus (Leupold), Coscinophragma cribrosum (Reuss), Massilina mirceai (Neagu), Protomarssonella hechti (Dieni et Massari), Protopeneroplis ultragranulata (Gorbatchik), and Textularia densa Hoffman. FT 2: Microencruster-microbial-cement boundstones (Fig. 11) Macroscopically, FT 2 is hardly recognizable in hand specimens (but see analogous facies in the Štramberk Limestone: Hoffmann et al., 2017, fig. 5), but is clearly vis­ible under the microscope. This boundstone type consists of a complex intergrowth of microencrusters, microbialite and cement crusts (Fig. 11). Microencrusters are represent­ed mostly by the following species (in order of abundance): Labes atramentosa (Fig. 11A–D), Crescentiella morronen­sis (Fig. 11B–D, F), Perturbatacrusta leini (Fig. 11A, B), Radiomura cautica, calcified sponges (Fig. 11A–E), spicu­lar sponges and Terebella lapilloides. Corals are very rare and are mainly opportunistic microsolenids (with a some­what sponge-like appearance; Fig. 11C). In “typical” exam­ples of FT2, photophilic (light-dependent) microencrusters (e.g., “Lithocodium-Bacinella”), common in FT 1, are not present or are uncertain. Less important for the reef frame­work are microbialite and cement crusts. Microbialites are represented by laminated and non-laminated, micropeloidal crusts (Fig. 11B, D, E).Growth cavities (up to some millime­tres in size) are filled with peloids, pseudo-ooids (Fig. 11F) and cement. Synsedimentary, first cement generation is developed as a thin, brownish cement rim (originally pos­sibly fibrous, isopachous cement; see Schlagintweit and Gawlick, 2008), whereas the second generation is devel­oped as blocky cement (Fig. 11E). Locally, microencrusters are attached to the cement generation 1 (Fig. 11E). Peloidal­bioclastic packstones occur in the matrix. Age: Lack of stratigraphically significant microfossils. Perturbatacrusta leini is a microencruster known from the Kimmeridgian–Berriasian (Pleş and Schlagintweit, 2014; Kaya and Altiner, 2015). Similar boundstones were de­scribed from the upper Kimmeridgian–lowermost Berriasian (Schlagintweit and Gawlick, 2008). They occur also in the Štramberk Limestone (Hoffmann et al., 2017). FT 3: Microbial and microbial-sponge boundstones (Figs 12, 13) FT3 is built of microbialites (Figs 12A, B, 13B) and rem­nants of siliceous sponges (usually calcified; Figs 12C, D, 13C, D) associated with Terebella lapilloides (Fig. 13B), Crescentiella morronensis (Fig. 13A, E), less often Labes atramentosa, and serpulid tubes. The skeletal elements are bound by microbial crusts of diverse microstructures, Fig. 11. Microfacies of the microencruster-microbial-cement boundstones (FT2). A. Intergrowth of Labes atramentosa and ?Crescentiella morronensis (black spots), calcified sponges (cs), Perturbatacrusta leini (Pl) and supposed thin peloidal microbial crusts. Synsedimentary cement is darker (c1; black arrows); late diagenetic cement (c2; white arrows) is lighter. B. Intergrowth of microencrusters (L/C – L. atramentosa or C. morronensis, Pl – Perturbatacrusta leini, cs – calcified sponges). Black arrows indicate supposed synsedimentary cements (c1). C. Microsolenid coral (cor) encrusted by L. atramentosa (La), calcified sponge Neuropora lusitanica (Nl), C. morronensis (Cm) and serpulids (s). D. Intergrowth of microencrusters (mostly L. atramentosa and C. morronensis – L/C and calcified sponges – cs) and microbialites (mc). Growth cavity is filled with peloids and pseudo-ooids (microbial peloids?). E. Growth cavity (filled with sparry calcite cement) within the framework formed by microencrusters and presumably microbialite crust with peloidal fabric (mc). The wall of the intra-framework cavity is encrusted by a thin, dark rim of synsedimentary cement (c1) and filled with two generations of light, late-diagenetic cement (c2). Arrows indicate minute microorganisms attached to synsedimentary cement. F. C. morronensis encrusting synsedimentary cement (arrowed). A, D–F – Woźniki, B – Koniusza, C – Gródek nad Dunajcem. B. Large, Terebella-like burrows in the microbial-peloidal boundstone. C. Siliceous sponge within the microbial-sponge boundstone. White spots are mostly Crescentiella morronensis. D. Siliceous sponge in bioclatstic packstone. White spots are mostly crinoid fragments. A, C – sites unknown, B – Lusina, D – Gródek nad Dunajcem. Fig. 13. Microfacies of FT 3: microbial (A–B) and microbial-sponge boundstones (C–E). A. Peloidal microbialite with Crescentiella morronensis (arrows). B. Numerous worm tubes Terebella lapilloides within dense to peloidal microbialite. C, D. Calcified siliceous sponges from the microbial-sponge boundstones. E. Peloidal packstone to grainstone with C. morronensis (arrows). F–I. Planktonic micro­fossils evidencing age of FT3. F. Calcareous dinoflagellate cyst Parastomiosphaera malmica; Tithonian. G. Chitinoidellid Chitinoidella elongata; lower upper Tithonian. G. Calpionellid Tintinnopsella remanei; middle upper Tithonian. I. Calpionellid Crassicollaria parvula; uppermost Tithonian–lowest Berriasian. A – Sułów, B – Gródek nad Dunajcem, C – Wiśniowa, D – Nowe Rybie, E – Zarzyce Wielkie, F – Rożnów, G – Roztoka, H – Biskupice, I – Zarzyce Wielkie. similar to FT 1. In addition to the largest sponge remnants, individual sponge spicules are common. Other bioclasts rep­resent crinoid plates, ophiuroid vertebrae, echinoid spines, fragments of bivalve, brachiopod and gastropod shells, ostracod carapaces and bryozoan colonies. Microfossils are represented by foraminifera (Table 3), Globochaete alpi­na Lombard, calcareous dinoflagellate cysts; calpionellids were observed in some samples (Fig. 13F–I). Wackestones, packstones and poorly washed grainstones with bioclasts (sponges and other elements typical for this facies; ocas­sionally bioclasts typical for FT 1) and coated grains occur as the matrix. Figure 12B shows a polished slab of an exotic clast containing sections through tubular terebellid-like burrows. These traces are much larger than T. lapilloides (Fig. 13B) and possibly, like similar burrows recently recog­nized in the Upper Jurassic–Lower Cretaceous of Romania, belong to a new ichnogenus (Kołodziej et al., 2017; compare also burrows from the Oxfordian microbial boundstones: Kędzierski et al., 2013, fig. 8c). Age: The Tithonian (and earliest Cretaceous?) age of this facies is confirmed by the occurrence of such strati­graphically significant microfossils as the calcareous di­nocysts Carpistomiosphaera tithonica, Colomisphaera tenuis, Committosphaera sublapidosa (Vogler), C. pulla, C. ornata, Crustocadosina semiradiata olzae (Nowak), and Parastomiosphaera malmica; the calpionellids Calpionella grandalpina Nagy, C. alpina, C. elliptalpina Nagy, Chitinoidella hegarati Sallouhi, Boughdiri et Cordey, Ch. boneti, Crassicollaria brevis Remane, Crassicollaria colo-mi Doben, C. intermedia, C. massutiniana (Colom), C. par­vula, Daciella danubica Pop, Longicollaria dobeni (Borza), Tintinnopsella remanei Borza, and T. carpathica; and the foraminifers Coscinoconus elongatus (Leupold), Mayncina bulgarica Laug, Peybernes et Rey, Protomarssonella kum-mi (Zedler), P. hechti, and Protopeneroplis ultragranulata. FT 4: Detrital limestones (Figs 14, 15) FT4, the most common facies among the exotics, is rep­resented predominantly by lithoclastic-bioclastic and litho­clastic grainstones and rudstones (Figs 14A, B, 15A–C), occasionally packstones. Rarely among the exotics there are detrital limestones, classified here as the matrix-sup­ported breccias (Figs 14C, D, 15D) and the clast-supported (cement-rich) breccias (Figs 14E, F, 15D). Some of these limestones (especially those containing diverse compo­nents, not only reefal components), occur on the scale of the pebble (Fig. 14A). Bioclasts and lithoclasts, diversified in composition, size and roundness, are typical for a shal­low-water carbonate platform. In terms of the main compo­nents, two types of detrital limestones can be distinguished: (1) with common reefal components (coral fragments, bound­stone clasts) and (2) with reefal and non-reefal components. The grainstones include coral fragments, whereas the rud­stones and breccias contain boundstone clasts of FT 1. The clasts – mostly below 30 mm in diameter – are usually angular (especially in limestones dominated by reefal com­ponents), but in some samples they are rounded. Age: These limestones include bioclasts and clasts with stratigraphically significant microfossils of Tithonian and earliest Cretaceous ages, such as the calpionellids Calpionella minuta Houša, C. alpina, C. grandalpina, Chitinoidella carthagensis Sallouhi, Boughdiri et Cordey, Ch. boneti, Ch. hegarati, Ch. popi, Crassicollaria brevis, C. colomi, C. intermedia, C. massutiniana, C. parvula, Dobeniella colomi (Borza), Borziella slovenica (Borza), Praetintinnopsella andrusovi Borza, Tintinnopsella car­pathica, and T. remanei; the foraminifers Anchispirocyclina lusitanica (Egger), Coscinoconus cherchiae (Arnaud-Vanneau, Boisseau et Darsac), Coscinoconus delphinen­sis (Arnaud-Vanneau, Boisseau et Darsac), Coscinoconus histeri (Neagu), Coscinoconus perconigi (Neagu), C. alpinus, Coscinophragma cribrosum, Dobrogelina ovidi Neagu, Hechtina praeantiqua, Massilina mirceai, Mayncina bulgarica, Nautiloculina bronnimanni Arnaud-Vanneau et Peybernes, N. cretacea, Patellina subcretacea, Protomarssonella hechti, P. kummi, Protopeneroplis ultra­granulata, and Textularia densa; and the calcareous dinocysts Cadosina fusca cieszynica Nowak, Carpistomiosphaera tithonica, Colomisphaera fortis, C. tenuis, Committosphaera sublapidosa, C. ornata, C. pulla, Crustocadosina semira­diata olzae, and Parastomiosphaera malmica. FT 5: Foraminiferal–algal limestones (Figs 16, 17) FT 5 is represented by the following microfacies: foraminiferal-algal grainstone, cortoid-oncoid grainstone to rudstone, bioclastic-oncoid wackestone to floatstone. They include relatively numerous larger foraminifera and miliol­ids, and much rarer macrofossil bioclasts. Larger benthic foraminifera, dasycladalean green algae, rivulariacean-like cyanobacteria, “Lithocodium-Bacinella” (Fig. 17D, E) and Thaumatoporella parvovesiculifera (Fig. 17D) are typical for this facies. Bioclasts are commonly micritized and are commonly cortoids. “Lithocodium-Bacinella” may be an important component of this facies (at the scale of the clast; decimetre-size, irregular lumps, Fig. 16C), but they are ob­served only in part of the samples. Usually, they occur as oncoidal envelopes (up to 15 mm) around fragments of cor­als, calcified sponges, gastropods, bivalves and echinoids. Other macrofossils or their fragments are serpulid tubes, ostracod carapaces, and less frequently brachiopod shells, holothurian sclerites, bryozoan colonies, Carpathocancer triangulatus (Mišik, Soták et Ziegler) and Carpathocancer? spp. (both reinterpreted as decapod crustacean appendages by Schlagintweit et al., 2007). Bioclasts are commonly the nucleus of oncoids, rarely of ooids, or they are superficially or fully micritized. T. parvovesiculifera and the foraminifer Troglotella incrustans often co-occur within these structures (cf. Schlagintweit, 2013). Crescentiella morronensis and K. socialis, common in the coral-microbial boundstones, are rare. Non-skeletal grains are additionally represented by small, rounded intraclasts, diverse peloids, and ooids (usually up to 0.7 mm, often superficial). The assemblages of foraminifera (exclusively benthic) are rich in specimens and in the diversity of forms (Ivanova and Kołodziej, 2010; Kowal-Kasprzyk, 2016). The most common genera are Bullopora, Charentia, Coscinoconus (former Trocholina or Andersenolina), Melathrokerion, Mohlerina, Nautiloculina, and Pseudocyclammina, and miliolids – usually hard to determine in detail – are numerous (Table 5; Fig. 17A–C). Dasycladales are represented by 19 species of the genera Salpingoporella, Griphoporella, Petrascula, Linoporella, Campbeliella, Otternstella, Montenegrella, and the relatively rare Aloisalthella sulcata (Alth) (Bucur et al., 2005). Age: The Tithonian–earliest Cretaceous age of this faci­es is confirmed by the occurrence of such stratigraphically significant microfossils as the foraminifers Coscinoconus campanellus (Arnaud-Vanneau, Boisseau et Darsac), C. al­pinus, C. cherchiae, C. delphinensis, C. histeri, C. perco­nigi, Coscinophragma cribrosum, Hechtina praeantiqua, Mayncina bulgarica, Nautiloculina bronnimanni, N. creta­cea, and Protopeneroplis ultragranulata; the calcareous dino­cysts Cadosina fusca cieszynica, Carpistomiosphaera tithon­ica, Committosphaera pulla, C. sublapidosa, Colomisphaera tenuis, and Crustocadosina semiradiata olzae; and rare calpi­onellids: Calpionella alpina, Crassicollaria sp. FT 6: Peloidal-bioclastic limestones (Fig. 18) FT 6 is represented by peloidal-bioclastic and bioclas­tic-peloidal grainstones, less often by wackestones and packstones. Usually, the shape and size of the peloids are diversified; some of them are poorly rounded. These fea­tures indicate that they are micritized grains, small micritic clasts, resulting from the re-working of partly lithified sedi­ment, and possibly also pellets. Additionally, cortoids, small intraclasts, and occasionally small (up to 0.5 mm) ooids are present. Fossil assemblages are composed of dasycladalean green algae, elements of crinoids, echinoids and ophiuroids, serpulid tubes, fragments of bivalve, gastropod and brachi­opod shells, fragments of bryozoans, ostracod carapaces, calcified sponges, unidentified calcimicrobes, and occa­sionally corals and the calcified spicules of siliceous spong­es. The foraminiferal assemblages are rich and diversified (Table 5); additionally, calcareous dinoflagellate cysts, the zoospores Globochaete alpina Lombard, and – in some samples – calpionellids occur. Crescentiella morronensis, Koskinobullina socialis and Thaumatoporella parvovesic­ulifera are common, occasionally Carpathocancer trian­gulatus, “Lithocodium-Bacinella”, Mercierella? dacica Dragastan and Terebella lapilloides occur. Similar deposits fill voids in the framework of the coral-microbial bound­stones. In some cases, the transition of peloidal-bioclastic grainstones to peloidal or micropeloidal microbial crusts was observed. Age: The Tithonian and earliest Cretaceous age of this faci­es is confirmed by the occurrence of such stratigraphically significant microfossils as the foraminifers Coscinoconus alpinus, C. cherchiae, C. histeri, Coscinophragma cribro­sum, Dobrogelina ovidi, Haplophragmoides cushmani, H. joukowskyi, Hechtina praeantiqua, M. mirceai, M. bulg­arica, Protomarssonella hechti, P. kummi, Protopeneroplis ultragranulata, and Textularia densa; the calpionellids: C. alpina, C. grandalpina, C. elliptalpina, Chitinoidella elongata Pop, Ch. boneti, Ch. carthagensis, Ch. hegarati, Ch. popi, Crassicollaria intermedia, C. massutiniana, C. parvula, Dobeniella tithonica (Borza), and Tintinnopsella remanei; and the calcareous dinocysts Cadosina fusca cieszynica, Colomisphaera tenuis, Committosphaera sub­lapidosa, and Parastomiosphaera malmica. FT 7: Ooid grainstones (Fig. 19) Ooid grainstones, ooid-peloidal, and peloidal-ooid grain­stone microfacies can be recognized in this rare facies type. Ooids, less than 1 mm in size, are recrystallized in the major­ity of samples. Two types of ooids were recognized among those that are better preserved: (1) spherical or ellipsoidal, micritized ooids, less than 1 mm in size; with nuclei of small bioclasts or peloids; some of them are less micritized and the concentric structure of the cortex can be recognized; and (2) more diversified in shape and size, sometimes larger than 1 mm, radial and concentric,-radial ooids; compound ooids and superficial ooids also appear; peloids and bio­clasts (fragments of shells, echinoderms, foraminifers) are their nuclei. This facies is poor in fossils. Rare Crescentiella morronensis, echinoiderm elements, fragments of bivalve shells, calcareous and agglutinated benthic foraminifers, and even calpionellids and calcareous dinoflagellate cysts were observed. Age: The Tithonian–earliest Cretaceous age of this facies is confirmed by the occurrence of Calpionella alpina and Colomisphaera tenuis, as well as several other microfossils with wider stratigraphic ranges, but typical of Tithonian– Berriasian assemblages. FT 8: Mudstones-wackestones with calpionellids (Fig. 20) Mudstones and bioclastic wackestones with calpionel­lids (e.g., Fig. 20E, F) and calcareous dinocysts are in­cluded in FT 8. Other bioclasts are less common and are represented by foraminifera, Globochaete alpina and cal­cified sponge spicules, rarely, ostracod carapaces, small fragments of bivalves, holothurian sclerites, echinoid and crinoid fragments, and calcified radiolarians as well as am­monites (Fig. 20D). The foraminiferal assemblages are not C. Packstone with calcified sponges and dasycladalean green algae (arrows). D. Thaumatoporella parvovesiculifera in the centre, and “Lithocodium-Bacinella” meshwork. E. Bioclast encrusted by “Lithocodium-Bacinella”, including “Lithocodium”-like crust with entobian borings (arrowed). A, D, E – Gródek nad Dunajcem, B – Milówka, C – Zarzyce Wielkie. B. Wackestone (lower part) and mudstone with calpionellids. C. Bioclastic wackestone with calpionellids. D. Wackestone with calpi­onellids and ammonites. E. Tithonian calpionellid assemblage (Calpionella alpina, Calpionella grandalpina, Crassicollaria sp.). F. Berriasian calpionellid assemblage (small, spherical Calpionella alpina). A, B, E, F – Żywiec, C – Sułów, D – unknown site between Woźniki and Lanckorona. rich and represented mainly by small, benthic, calcareous forms. Fine, siliciclastic grains, mainly of quartz, appear in some samples. Additionally, wackestones with pelagic mi­crofossils and an admixture of bioclasts of shallow-water organisms can be included in the facies type. Small, calcar­eous, benthic foraminifers dominate in this facies (Table 5); additionally forms of shallower zones (especially miliol­ids) appear. Other fossils occurring as bioclasts are crinoids (e.g., Saccocoma), echinoids, bivalves (including filamen­tous bivalves), brachiopods, gastropods, bryozoans, sili­ceous sponges, and ostracods. Fossils typical of shallow zones (e.g., dasycladalean algae, Crescentiella morronen­sis, Koskinobullina socialis) occasionally occur, as well as small lithoclasts and peloids. Age: The Tithonian and earliest Cretaceous age of this fa­cies is confirmed by the occurrence of microfossils: main­ly the calpionellids Calpionella elliptica Cadisch, C. alpi­na, C. grandalpina, C. elliptalpina, Crassicollaria brevis, C. colomi, C. intermedia, C. massutiniana, C. parvula, Praetintinnopsella andrusovi, and Tintinnopsella carpath­ica; and the calcareous dinocysts Colomisphaera radia-ta (Vogler), C. fortis, C. tenuis, Committosphaera ornata, C. pulla, C. sublapidosa, Crustocadosina semiradiata olzae, and Parastomiosphaera malmica. Microfacies not assigned to main facies (Fig. 21) The microfacies of some exotics cannot be without doubt assigned to the main facies described above, even though they consist of more than one microfacies. They may rep­resent microfacies from the facies described, or they be-long to independent, but rare facies. Worth mentioning are clasts developed as agglutinated, laminated and micro­peloidal stromatolites in M 1 (Fig. 21A, B), oncoid-ooid packstones in M 2 (Fig. 21C), limestones dominated by bivalves or other shells in M 3 (Fig. 21E–G), and echino­derm wackestones in M 4 (Fig. 21D). The Tithonian and earliest Cretaceous age of all these facies is confirmed by the occurrence of stratigraphically significant microfossils, such as the calpionellids Calpionella alpina, C. elliptica, C. minuta, Chitinoidella boneti, Ch. carthagensis, Ch. he­garati, Ch. popi, Crassicollaria colomi, C. massutiniana, C. parvula, Remaniella duranddelgai Pop, Tintinnopsella carpathica; calcareous dinoflagellate cysts: Colomisphaera fortis, C. tenuis, Committosphaera sublapidosa, and Crustocadosina semiradiata olzae; and the foraminifers Patellina subcretacea, Protomarssonella hechti, P. kummi, and Protopeneroplis ultragranulata. Exotics with neptunian dykes (Fig. 22) Three limestone clasts, developed as shallow-water bio­clastic packstones-grainstones, contain thin fissures (up to 35 mm in width). These fissures are filled with dark calci­mudstones-wackestones with ostracods and small burrows (Chondrites?). Frequency of facies The analysis of the frequency of facies is based on 312 exotic clasts of Tithonian–lowermost Cretaceous age from 31 localities (Fig. 23; Kowal-Kasprzyk, 2016). The most common among clasts are limestones that resulted from reef destruction, or, more generally, from the destruc­tion of the carbonate platform. Detrital limestones (FT 4) were observed in ca. 30 % of samples. Coral-microbial boundstones (FT 1) and microbial and microbial-sponge boundstones (FT 3) were observed (each facies) in ca. 15% of samples. FT 7 and FT 8, and especially M 1–M 4 are the least common. These proportions are approximate. Fig. 22. Thin neptunian dykes (filled with dark Lower Cretaceous limestone) within the exotic clasts of the Štramberk-type lime­stones documenting the destruction and drowning of the carbonate platform. A. Polished slab of the exotic clast showing thin, dark neptunian dykes. B, C. Microscopic images of neptunian dykes cutting shallow-water limestones: bioclastic wackestones (B) and grainstone (C). There are numerous, small burrows (Chondrites isp.) in the calcimudstone filling of the dyke. The wall of the dyke in C is possibly coated by a thin, microbial crust. A, B – Jastrzębia, C – site unknown. For example, some samples classified as the bioclastic-litho­clastic grainstones (FT 4) and the peloidal-bioclastic lime­stones (FT 6), can be in fact intra-reef sediment of the cor­al-microbial boundstones (FT1). Owing to the small size of some clasts, the assignment of some microfacies to the main facies is uncertain. This quantitative analysis corresponds in general to the qualitative microscopic analyses of other samples and to observations in the field. DISCUSSION Distribution of the Štramberk-type limestones in the Polish Outer Carpathians The exotics studied here are mostly from the Silesian and Sub-Silesian units. In the Silesian Unit, the Hauterivian– Barremian Hradiště Formation and the Campanian– Paleocene Istebna Formation are the main exotic-bearing beds. In the Sub-Silesian Unit, exotic clasts occur mainly in the Hradiště Formation and less commonly in the Veřovice Formation. Before the reorganization of the Late Cretaceous basin, the Sub-Silesian and Silesian sedimentary series were similar, because sedimentation in the western part of the Proto-Silesian Basin took place in similar basinal con­ditions (Golonka et al., 2006b; Waśkowska et al., 2009). The exotics from the Skole Unit, much rarer than the ex­otics in earlier units, are almost exclusively from the Maastrichtian–Paleocene Ropianka Formation. Currently poorly exposed, but well known from the litera­ture, the Kruhel klippe (near Przemyśl) occurs in the Ropian­ka Formation. The largest occurrence of different sizes of blocks – traditionally known as the Andrychów Klippen or Klippes (Inwałd, Targanice, Roczyny) – of the Štramberk­type limestones as well as the Middle Jurassic, Oxfordian and Palaeogene limestones occur in front of the Silesian Unit. Originally, they were regarded as tectonic klippen, but recently as olistoliths, which slid down into the Silesian Basin during the late Oligocene or early Miocene, and now occur as olistostromes within the Miocene molasse deposits (see Waśkowska-Oliwa et al., 2008; Cieszkowski et al., 2009). Generally, it is hard to recognize any significant trends in facies distribution in particular geographical areas, tec­tonic units or lithostratigraphic units (see also Burtan et al., 1984). The most common facies types are observed almost everywhere, and the majority of less common facies are observed at various localities. However, it is noteworthy that calpionellid mudstones/wackestones (FT 8) occur at only two localities, Żywiec (locality 2) and Żegocina (lo­cality 27). These localities are geographically distant, but at both sites, clasts occur in the Lower Cretaceous Hradiště Formation (Silesian Unit) and the palaeotransport directions indicate input from the south. There is no trend in the relationship between the age of exotics and the age of the flysch deposits. In general, the frequency of the Oxfordian–Kimmeridgian carbonate clasts (Kowal-Kasprzyk et al., 2020) and the Štramberk­type limestones described here (Tithonian–lowermost Cretaceous) is similar in the older (Lower Cretaceous) and younger (Paleocene–Eocene) flysch deposits. The studies of the present authors and the data in the literature indicate that exotics of the Štramberk-type limestones are rare in the Oligocene deposits (Menilite Formation). The litera­ture indicates that they are absent (rare?) in the Oligocene Krosno Formation, in contrast to exotics of crystalline rocks (Ślączka and Wieser, 1962; Mochnacka and Tokarski, 1972; Bąk et al., 2001). Štramberk-type limestones in other tectonic units, as shown by data in the literature, are much rarer and were not studied here. The Jurassic–Cretaceous exotics are poor­ly known from the Fore-Magura group of nappes and the Dukla Nappe, but Burtan and Sokołowski (1956) and Burtan et al. (1984) described Štramberk-type limestones from a locality near Żywiec (Fore-Magura Unit), which probably were derived from the Silesian Ridge. In the Magura Nappe, Štramberk-type exotics were observed only occasionally in the northern part, whereas in the rest of the unit only car­bonate clasts similar to limestones from the Inner Carpathians (Tatra Mts.) and Pieniny Mts. were found (Oszczypko, 1975; Burtan et al., 1984; Krobicki and Olszewska, 2005; Olszewska and Oszczypko, 2010; Oszczypko et al., 2020). Tithonian–Berriasian exotic limestones from the Krynica Subunit (close to the Pieniny Klippen Belt) of the Magura Nappe are represented by limestones with calpionellids (possibly analogous to FT8 of the present study, Hoffmann in Oszczypko et al., 1992; Oszczypko et al., 2006). On the other hand, the Middle Jurassic and Lower Cretaceous (Urgonian) limestones are much more common there than in the northerly located units. Urgonian limestones in the Polish Outer Carpathians were reported almost exclusive­ly from the Magura Nappe (Hoffmann in Oszczypko et al., 1992, Krobicki et al., 2005; Krobicki and Olszewska, 2005; Oszczypko et al., 2006, 2020). Štramberk-type limestones were also noted in the northerly located, folded Miocene of the Stebnik and Zgłobice units (Ney, 1957). The lack of any clear distribution pattern of exotics in terms of the ages of exotic clasts and the ages of flysch de­posits may be related to (1) the complex geological structure of the source areas, (2) the composition of exotics at a given locality reflecting a very local source area, and (3) possible erosion of exotics out of terrigenous conglomerates, com­posed both of older and younger carbonate clasts. Besides, the sampling at different locations was extensive to different degrees and therefore a strictly quantitative analysis of the frequency in different facies and the comparison of exotics from different localities would not be reliable. Depositional and environmental settings The challenge is to decipher the depositional and envi­ronmental characteristics as well as the facies distribution pattern and to propose a depositional model (platform zona­tion), based on exotics, mostly of pebble and cobble size, or even based on the analysis of olistoliths and large blocks, as in the case of the Štramberk Limestone. The following as­pects should be considered in making such interpretations: the small size of the exotics, random source area, the prob­lem with the age determination of particular clasts, their un­certain spatio-temporal relationships, and the rarity or lack of some facies (e.g., marls) due to their low preservation potential. In this chapter, the focus is on biotic components (corals, microencrusters, microbialites), and some facies (detrital facies and the role of synsedimentary cements in boundstones and in clast-supported breccias), which are im­portant for the interpretation of the carbonate platform. Corals The Štramberk Limestone contains the most diversified Tithonian–Berriasian corals in the world (about 120 spe­cies, e.g., Ogilvie, 1897; Geyer, 1955; Eliášová, 1975, 1978, 1981a, 2008 and references therein) with a unique prolif­eration of the suborder Pachythecaliina (= Amphiastreina; about 40 species; e.g., Eliášová, 1975, 1978), representing possibly not Scleractinia-like modern reef corals, but an extinct order, Hexanthiniaria. Corals are also diversified in the Štramberk-type limestones (about 80 species, includ­ing 20 species of Pachythecaliina; see Kołodziej, 2015b and references in Table 1). It should be kept in mind that much more numerous and diversified coral assemblages of the Štramberk Limestone were described from samples, collected in the large, active Kotouč Quarry, that provid­ed many more specimens than the exotics in the Polish Carpathians. The Tithonian coral faunas are much rarer than those in the Kimmeridgian, while Berriasian to Valanginian corals on a global scale are almost unknown (Löser et al., 2021). For comparison, relatively rich coral assemblag­es from the upper Kimmeridgian–Valanginian of Bulgaria (Roniewicz, 2008) and from the upper Berriasian of Austria and Switzerland (Baron-Szabo, 2018) include 72 and 61 species respectively. The proliferation of the pachythecal­iines in the Štramberk Limestone and the Štramberk-type limestones (only in Poland) is in sharp contrast with oth­er Late Jurassic coral assemblages, including those from Poland (Roniewicz, 1966; Morycowa, 2012), although other coral groups may be comparatively diversified. In the present account, the suborder Pachythecallina is dis­tinguished instead of Amphiastraeina and also corals from the Heterocoeniina were included. These suborders are still accepted by some authors (see the discussion in Kołodziej et al., 2012; Kołodziej and Marian, 2021). The superfamily Amphiastraeoidea disappeared completely at the end of the Albian, while the Heterocoenioidea persisted until the end of the Cretaceous (Löser et al., 2013; Löser, 2016). These corals are the most controversial Mesozoic corals, with con­trasting opinions regarding skeleton structure, microstruc­ture and high-rank taxonomy (see the review in Kołodziej and Marian, 2021). Further studies on the sedimentary environment may be helpful in deciphering the palaeoeco­logical constraints on the development of the corals of the Štramberk Carbonate Platform, particularly on the unique diversification of pachythecaliines. Corals have a largely phaceloid (branching) growth form, as in most Late Jurassic reefs. Corals of the subor­der Microsolenina, a coral group with an opportunistic life strategy, occur both in the Štramberk-type limestones and in the Štramberk Limestone, but there is no evidence that they formed microsolenid-dominatedboundstones. Microsolenid reefs, usually constratal reefs (biostromes), were typical of deeper, mesophotic settings and now occur usually at the base of the Upper Jurassic reef sequences on the northern Tethyan shelf (Insalaco, 1996), for example, in the Holy Cross Mts., Poland (Roniewicz and Roniewicz, 1971), but are very rare on the intra-Tethyan carbonate platforms. Corals from the Lower Cretaceous (Barremian–lower Aptian) of the Polish Outer Carpathians, exclusively from the Hradiště Formation, differ both with regard to taxonomy and state of preservation and in that they are not embedded in a carbonate matrix (Morycowa, 1964b; Kołodziej and Gedl, 2000). Microencrusters Studies during the last decades reinterpreted the biologi-cal and taxonomic affiliation and environmental demands of the Jurassic–Cretaceous microencrusters and showed that an understanding of their associations and abundance is crucial to the interpretation of the sedimentary environments and zonation of carbonate platforms (for review, see Leinfelder et al., 1993; Schlagintweit et al., 2005; Schlagintweit and Gawlick, 2008; Pleş et al., 2013; Kaya and Altiner, 2015). Microencrusters in the Štramberk Limestone have been studied by Eliáš and Eliášová (1984) and Eliášová (1981c, 1986). Some of them have been reported only recently and allowed the recognition in the Štramberk Limestone of two contrasting boundstone types (Hoffmann et al., 2017). Bacinellid and “Lithocodium”-like structures (com­monly termed the “Lithocodium-Bacinella” associa­tion), Lithocodium aggregatum, Koskinobullina socialis, Iberopora bodeuri and Thaumatoporella parvovesiculifera are light-dependent taxa/biogenic structures, implying shal­low-water reef, back-reef or lagoonal settings. Other spe­cies, listed in Table 1, have much broader environmental demands, but especially if photophilic microencrusters are absent, they imply fore-reef and slope settings (Leinfelder et al., 1993; Schlagintweit and Gawlick, 2008, 2011; Pleş et al., 2013, 2021; Kaya and Altiner, 2015; Kołodziej and Ivanova, 2021). “Lithocodium-Bacinella”, the most common in shal­low-water facies (FT 1, FT 5), is of particular significance. Microscopic studies of the Štramberk-type limestones and the Štramberk Limestone indicate that Lithocodium ag­gregatum sensu stricto (green alga; Schlagintweit et al., 2010) is rare. This microencruster also appears to be rare in other Upper Jurassic–lowermost Cretaceous shallow-wa­ter limestones, in contrast to the younger (Barremian– Albian) carbonate platform deposits (known worldwide). Instead, “Lithocodium”-like structures, that is, calcimicro­bial crusts with entobian borings (Cherchi and Schroeder, 2010; Schlagintweit, 2010), associated with the cryptic and boring foraminifer Troglotella incrustans (e.g., Schmid and Leinfelder, 1996; Kołodziej, 1997a; Schlagintweit, 2012), are very common in the material studied. This also seems to be the case for other Late Jurassic–earliest Cretaceous carbonate platforms. Structures that are commonly reported from the Upper Jurassic–Lower Cretaceous shallow-water limestones and termed Bacinella irregularis in fact represent calcimicrobial crusts (bacinellid or bacinelloid structures/ fabrics; Schlagintweit and Bover-Arnal, 2013; Granier, 2021). Bacinella irregularis sensu stricto – filamentous structures, not a vesicular meshwork – are microborings of green algae (Schlagintweit and Bover-Arnal, 2013) and as such were very rarely reported in the literature. Labes atramentosa, Perturbatacrusta leini and Radiomura cautica, had broad environmental preferences and are common in boundstones FT 1 and FT 2, but are especially characteristic for the microencruster-microbi­al-cement reefs (FT 2). This type of boundstone is repre­sented in the samples studied but is subordinate to FT 1. Microencruster-microbial-cement boundstones are unique to the intra-Tethyan carbonate platforms (Schlagintweit and Gawlick, 2008; Ivanova et al., 2008; Hoffmann et al., 2008; Pleş et al., 2013, 2016, 2019, 2021; Hoffmann et al., 2017; Krajewski and Schlagintweit, 2018; Kołodziej and Ivanova, 2021). Schlagintweit and Gawlick (2008) were the first to notice in the Kimmeridgian and Berriasian of the Northern Calcareous Alps (Plassen Carbonate Platform) the crucial role of non-photophilic microencrusters and synsed­imentary cements for the reef framework. Microencruster­cement boundstones contain only rare corals, mostly mi­crosolenids. Previously, such reefs were not distinguished among the Late Jurassic reefs (Leinfelder, 1993; Insalaco et al., 1997). This reef type is characteristic of, although possibly not limited to the isolated platforms of the Neo-Tethys (Schlagintweit and Gawlick, 2008; Pleş et al., 2021; Kołodziej and Ivanova, 2021). To recognize the microen­cruster-microbial-cement boundstones, it is necessary to study them in more than in a single thin-section. A similar microframework on the scale of one thin-section can occur in coral-dominated reefs (FT 1), especially on the walls of growth cavities (cryptic habitat), but in these shallow-wa­ter boundstones there are also photophilic microencrusters. An intermediate reef type, showing a framework composed predominantly of the microencruster-microbial-framework, with more (but still subordinate) corals and rare photophilic microencrusters certainly occurred, but such a type is diffi­cult to recognize in pebbles. Riding and Virgone (2020) at­tributed the microencruster-microbial-cement boundstones described by Hoffmann et al. (2017) from the Štramberk Limestone to a type of carbonates with complex genesis and termed Hybrid Carbonates. This type and other hybrid car­bonates are result of in situ abiotic, microbial and skeletal co-precipitates. Reefs described from the Alps were interpreted to be formed in a high-energy setting, at a depth of 10–20 m up to 50 m (upper part of the platform slope), below the cor­al-stromatoporoid reefal zone (Schlagintweit and Gawlick, 2008). This palaeobathymetric interpretation is supported by the lack or scarcity of corals and photophilic micro­encrusters, which are common in coral-dominated reefs. Synsedimentary cements support an assumption of a steep platform margin and high energy at the upper plat­form slope. The upper platform slope was also inferred for boundstone type B (microencruster-cement boundstones) in the Štramberk Limestone (Hoffmann et al., 2017) and similar reefs in the Kimmeridgian of Bulgaria (Moesian Carbonate Platform; Kołodziej and Ivanova, 2021). The presence of the microencruster-cement boundstones onthe Štramberk Carbonate Platform and their absence from platforms located on the Tethyan margin (see the last sec­tion) confirm the conclusion of Schlagintweit and Gawlick (2008) and Kołodziej and Ivanova (2021) that this peculiar facies can be useful in palaeogeographic reconstructions, for deciphering the puzzle of microplates in the Western Neotethyan realm. Other microencrusters – the worm tube Terebella lapil­loides – arecommon inthe microbial and microbial-sponge boundstones (FT 3) and are typical for limestones, deposit­ed in low-energy and dysoxic environments, for example, the microbial-sponge reefs (Kaya and Altiner, 2014). Microbialites Carbonates produced by microbial growth and metabo­lism, as well as the passive mineralization of organic matter (microbially-induced and microbially-influenced carbonate precipitation) are important component of most coral-dom­inated and other types of Late Jurassic reef (e.g., Schmid, 1996; Helm and Schülke, 1998; Leinfelder and Schmid, 2000; Leinfelder, 2001; Dupraz and Strasser, 2002; Olivier et al., 2004; Matyszkiewicz et al., 2012). Leinfelder and Schmid (2000) summarized types and environmental sig­nificance of the Jurassic microbialites. Late Jurassic mi­crobialites were typically restricted to environments with low hydraulic energy. Microbialites are largely lacking in high-energy reefs, but if steep reef margins allowed the ex-port of most of the debris, microbialites were able to sta­bilize the remaining reef debris. Well-developed coral-mi­crobial (especially thrombolite) reefs were largely restricted to settings close to siliciclastic source areas. Even if during reef growth direct siliciclastic influx was minimal, it may be concluded that nutrient availability was elevated, typical for mesotrophic rather than oligotrophic environments. Late Jurassic reef corals, though having developed symbiosis with photosymbionts analogous to modern zooxanthellae, benefited from slightly elevated nutrient levels (Nose and Leinfelder, 1997). The contribution of microbialites to the reef facies of the Štramberk-type limestones was not appreciated before the work of Hoffmann (1992; see also Hoffmann and Kołodziej, 1997, 2008; Bucur et al., 2005), but they are poorly de­scribed and documented. Microbialites are also important in the Štramberk Limestone, as was initially described by Hoffmann et al. (2017), but previous studies did not exam­ine their composition and significance. Eliáš and Eliášová (1984, p. 131) only briefly mentioned “bioliths-bindstones […] bound by algae” occurring in the inner reef flat with the extensive growth of corals. It is unclear whether these algae correspond to microbial crusts in the recent meaning or cor­respond to “Lithocodium-Bacinella”. It is unclear whether agglutinated, laminated and micropeloidal stromatolites, distinguished in this paper as microfacies and not assigned to the main facies (M 1), should be included in the bound­stones facies (rather to FT 1 than to FT 3) or they devel­oped in a restricted lagoonal environment (without corals). The reason is the lack of fossils or structures within these stromatolites of pebble size implying a sedimentary setting. Stromatolites interpreted as lagoonal were reported from the Štramberk Limestone, but were poorly discussed (Eliáš and Eliášová, 1984, pl. 9, fig. 1). Microbialites within exotic clasts, which were recently assigned (based on microfossils) to the Oxfordian-Kimmeridgian, differ in microscopic ap­pearance (Kowal-Kasprzyk et al., 2020). Different varieties of microbialites in the Štramberk-type limestones and the Štramberk Limestone certainly require insightful studies, including geochemical investigations that could provide in­sight into nutrient availability, redox conditions and chang­es in the input of terrigenous siliciclastics (e.g., Olivier and Boyet, 2006; Matyszkiewicz et al., 2012). Synsedimentary cements Hoffmann et al. (2017) recognized the important role of synsedimentary cements in two facies of the Štramberk Limestone: in the clast-supported breccias and in the micro-encruster-microbial-cement boundstones. Microencrusters are attached to the first generation of cement, which implies a synsedimentary origin for this cement, an important com­ponent of the framework reef of FT2 (see also the previous section “Microencrusters”). The reef-derived, clast-support­ed breccia is one of the characteristic facies of the Štramberk Limestone. Clasts are bound by radiaxial-fibrous calcite ce­ment, interpreted to be dominantly synsedimentary, as im­plies examination under cathodoluminescence (Hoffmann et al., 2017). The thick, banded cement crusts show simi­larity to the “evinospongiae” cements in the Middle-Upper Triassic boundstones and breccias of the Alps (e.g., Harris, 1993; Russo et al., 2000). The presence of similar breccias in the Štramberk Limestone implies steepened slopes of the carbonate platform, as was previously suggested by Eliáš and Eliášová (1984), although they did not describe breccias (but see the discussion in Hoffmann et al., 2017, p. 340 on “large ?oncoids”, described by Eliáš and Eliášová, 1984). A similar assumption can be made for the morphology of platforms in the “Polish part” of the Štramberk Carbonate Platform, although this facies is rarely represented in the ex­otic clasts studied, possibly because of less available mate-rial for study. To the knowledge of the present authors, there are no comparable breccias, showing massive synsedimen­tary cementation (“evinospongiae” cement), in other Upper Jurassic–lowermost Cretaceous platform deposits. Detrital facies Diverse detrital limestones are very common, both in the Štramberk Limestone (Eliáš and Eliášová, 1984; Vašíček and Skupien, 2014; Vaňková et al., 2019) and in the Štramberk­type limestones. Except for the preliminary studies of the clast-supported, reef-derived breccias in the Štramberk Limestone (Hoffmann et al., 2017), discussed above in the section “Synsedimentary cement”, detrital limestones were not studied in terms of volume, components and processes, responsible for the breakdown of biota and lithified sedi­ments as well as their redistribution. Coarse-grained faci­es, i.e., matrix-supported and clast-supported breccias, are of particular importance for the interpretation of platform morphology and zonation. Bioclastic debris, apart of reef building macroorganisms (corals, calcified sponges), mi­crobialites and microencrusters, are components of coral reefs. High debris production and small content of micrite are typical for the Late Jurassic reefs of the Tethyan domain, and some of them even have been called coral debris reefs (Leinfelder, 1992; Leinfelder et al., 2005; Rusciadelli et al., 2011; Rusciadelli and Ricci, 2013; Ricci et al., 2018b). The composition and genesis of detrital limestones have implications for the interpretation of the hydrodynamics in different parts of the carbonate platform, the mechanisms of redeposition of detrital material and platform morpholo­gy (gentle vs steepened slope profile) and improvement of the understanding of the dynamics and development of car­bonate platform systems (e.g., Rusciadelli and Ricci, 2013; Harchegani and Morsilli, 2019). If steep reef margins exist­ed, a large volume of the debris could be exported, allowing the export of most of the reef debris, hence microbialites were able to develop and stabilize the remaining reef de­bris forming coral-microbial-debris reefs (Leinfelder, 1992, 2001). However, studies of exotics do not allow to deter­mine whether this reef type (reef debris bound by microbial­ites) was formed on a larger scale. Oxfordian–Kimmeridgian in exotic pebbles During field observations, some exotics could be termed Štramberk-type limestones, but in fact they are Oxfordian– Kimmeridgian limestones and differ from most facies de­scribed here. These exotics were not described in the pres­ent paper, but below the authors briefly characterize them. Oxfordian–Kimmeridgian limestones are represented by three main facies types: (1) light-beige, porous, sponge-mi­crobial limestones, (2) beige, non-porous, oncoid-intraclas­tic-Crescentiella limestones, and (3) dark-grey, fine-grained biodetrital limestones with Saccocoma (Kowal-Kasprzyk et al., 2020). The first facies is composed mainly of two microfacies: sponge-microbial framestones-floatstones and fine-grained, bioclastic wackestones-packstones. The second facies is represented by oncoid-intraclastic float­stones-wackestones and Crescentiella-peloidal wackestones and bindstones. In the third facies, three microfacies types can be distinguished: filamentous-Saccocoma wackestones, spicule-Saccocoma wackestones and crinoid-Saccocoma packstones-wackestones (Kowal-Kasprzyk et al., 2020). These limestones are similar to Oxfordian (mostly) fa­cies types from the northern shelf of the Western Tethys (e.g., extra-Carpathian southern Poland, including the Carpathian Foredeep basement) and are interpreted as being deposited in similar conditions (e.g., Matyszkiewicz, 1997; Krajewski et al., 2011, 2016; Matyszkiewicz et al., 2012). The sponge-microbial limestones are facies of a distal ramp and mid-ramp; they were deposited mostly in a low-ener­gy, nutrient-rich environment, between the fair-weather and the storm wave bases. The oncoid-intraclastic-Crescentiella limestones are related to a mid-inner ramp with moderate water energy. The fine-grained biodetrital limestones with Saccocoma were deposited in an outer-ramp setting. On the basis of foraminifers, calcareous and organic-walled dinoflagellate cysts, the age of the samples studied can be determined generally as Oxfordian and Kimmeridgian, but a precise age determination is usually impossible (Kowal-Kasprzyk et al., 2020). In summary, these limestones originated in a deeper depositional setting than most facies of the Tithonian–ear­liest Cretaceous Štramberk-type limestones. Oxfordian– Kimmeridgian sponge-microbial and oncoid-intraclastic-Crescentiellafacies are very similar to the Tithonian–?earliest Cretaceous microbial and microbial-sponge boundstones (FT 3), described in this paper, and sometimes are distinguishable only micropalaeontologically. It is notewor­thy that the sponge-microbial limestones (sponge megafa­cies) in the Carpathian Foredeep basement (southeastern segment of the Mid-Polish Trough) rangesinageupintothe lowermost Tithonian (Matyja, 2009). Oxfordian–Kimmeridgian clasts in the flysch can be beige in colour, but they can be also dark in colour, more commonly than the colour of the Štramberk-type lime­stones. FT 8 (deeper facies) is much more commonly dark than are the other facies. However, colour is not a sound criterion for distinguishing the Oxfordian–Kimmeridgian clasts or exotics representing the deeper facies. Exotics of Štramberk-type limestones from the uppermost Jurassic Vendryně Formation and from the Hauterivian–Barremian Hradiště Formation (locality Żywiec) are more commonly dark, possibly because of a shorter period of weathering in a subaerial environment. Cieszyn Limestone – a deep-water equivalent of the Štramberk-type limestones The deep-water Cieszyn Limestone (Cieszyn Limestone Formation, part of the Cieszyn Beds) from the western part of the Polish Outer Carpathians are well described in terms of palaeontology and in particular their stratigraphy (Szydło and Jugowiec, 1999; Olszewska, 2005; Olszewska et al., 2008) and especially sedimentologically (e.g., Nowak, 1967; Peszat, 1967; Malik, 1986; Słomka, 1986; Matyszkiewicz and Słomka, 1994, 2004). The uppermost Kimmeridgian Vendryně Formation (formerly the Lower Cieszyn Beds) – the oldest sediments (“pre-flysch”) of the Polish Outer Carpathians – and the Tithonian–lowermost Valanginian Cieszyn Limestone Formation, were deposited in the deeper zones of the Proto-Silesian Basin, now forming mostly the Silesian Unit and locally the Sub-Silesian Unit (Olszewska, 2005; Olszewska et al., 2008). Thus they are deep-water equivalents of the Štramberk Limestone and Štramberk-type limestones. The Vendryně Formation – mainly Tithonian in age – is dominated by dark, marly shales, while the young­er Cieszyn Limestone includes detrital, organodetrital and pelitic limestones, with intercalations of marly shales. The Upper Cieszyn Limestone Formation (debris-flow sedi­ments) contains clasts representing shallow-water reefs (analogous to FT 1 of the present account) and deep-water boundstones (FT2 and/or Oxfordian–Kimmeridgian micro­bial-sponge boundstones; cf. Matyszkiewicz and Słomka, 2004). Coarse-grained debris-flow deposits are more com­mon in the upper part of the Cieszyn Limestone Formation (Berriasian), reflecting the Neo-Cimmerian movements of the Silesian and Sub-Silesian ridges, probably linked to the initial rifting of the Silesian (Proto-Silesian) Basin (Krobicki and Słomka, 1999; Krobicki et al., 2010). In the initial stage, clastic material was delivered mainly from the northern source area, but since the late Tithonian, the southern source area also was active (e.g., Matyszkiewicz and Słomka, 1994). The tectonic activity resulted in the emergence of the Silesian Ridge from west to east (Unrug, 1968; Matyszkiewicz and Słomka, 1994). Detrital limestone is dominant lithotype of the Cieszyn Limestone Formation and occurs as thin layers in the Vendryně Formation. These originated from the destruc­tion of the carbonate platform that had developed along the margins of the basin. They include shallow-water bioclasts and intraclasts, but also clasts of pelitic calpionellid lime­stones (Peszat, 1967; Książkiewicz, 1971a; Matyszkiewicz and Słomka, 1994, 2004). These intraclasts are analogues to the exotics studied, and they also include similar microfos­sils (e.g., Nowak, 1967; Olszewska, 2005; Olszewska et al., 2008). The pelitic calpionellid limestones – the other main lithotype of the Cieszyn Limestone – are analogues to the FT 8 facies, described here. It is noteworthy that the name “Štramberk-type lime­stones” is used here in a broad sense and not exclusively for the shallow-water platform deposits. Therefore, it is hard to put a boundary between the “Štramberk facies” (their deep­er facies types) and the “Cieszyn facies”. Clasts of some detrital or calpionellid limestones can be indistinguishable from the limestones, observed in profiles of the lowest part of the Silesian Unit. In such a situation, they do not meet the strict definition of “exotic” clasts, because their source rocks are exposed. Zonation of the carbonate platform studied and other intra-Tethyan platforms Štramberk Limestone Because of similarities in the age, facies, and coral as­semblages as well as palaeogeographic proximity, it is tempting to apply the zonation of the sedimentary system of the Štramberk-type limestones (Poland) to the proposed platform zonation that is based on studies of the Štramberk Limestone (Czech Republic). As was already highlighted, the limestones of both countries are interpreted here as de­posited on carbonate platforms, attached to intra-Carpathi­an ridges, which are collectively termed the Štramberk Carbonate Platform. This platform is not considered to have been one huge intra-Carpathian carbonate platform, but rather a number of small, narrow platforms, attached to intrabasinal ridges (the largest are the Silesian Ridge and the Baška-Inwałd Ridge) as well as platforms attached to the margins of the Outer Carpathian Basin. At the end of this chapter, the authors present the zonation of the car­bonate platform based on their studies of exotics and data from recent literature on the zonation of other intra-Tethyan carbonate platforms with reefs. Earlier, the authors pres­ent zonations, proposed for the Štramberk reef complex (Štramberk Limestone) and other European Late Jurassic, reef-bearing carbonate platforms. In accordance with a broad definition of a fossil reef (e.g., Wood, 1999; Riding, 2002; Kiessling, 2009), patch-reefs – the inferred dominant type of reef studied here – safely can be classified as a reef. The model presented by Eliášová (1981b) and Eliáš and Eliášová (1984) was based on studies of olistoliths and large blocks. However, it should be verified because since the 1980s, knowledge of the LateJurassic–Early Cretaceous platforms and reefs has increased significantly. Arevised in­terpretation of the sedimentary environments and reef zona­tion of the Štramberk Limestone requires more qualitative and quantitative data concerning the facies, microfacies and composition of the biota within individual olistoliths and blocks. Apreliminary study by Hoffmann et al. (2017) has provided a new insight into the zonation of the Štramberk reef complex and is applied in the interpretation, proposed in the present work. The Štramberk Limestone rarely features in discussions on the intra-Tethyan carbonate platforms (Leinfelder et al., 2002, 2005; Rusciadelli et al., 2011). Recently, in a paper on the Upper Jurassic reefs of Sardinia (passive margin of the Alpine Tethys) the Štramberk Limestone were not included among examples of Upper Jurassic reefs, even though there were references to ten papers on other Tethyan platforms (Nembrini et al., 2021). Hoffmann et al. (2017) discussed the biotic and sedimentary characteristics that the Štramberk Limestone shares with the Late Jurassic platforms of the Tethyan realm. These similarities include: (1) the strongly zoned character of the reef complexes, (2) high or moder­ate, topographic relief at the reef edge, (3) the presence of the microencruster-microbial-cement reefs with some mi­croencruster species, known exclusively from the Tethyan realm, (iv) the reef-building role of calcified sponges, (v) high debris production, and (vi) the subordinate role of mic­rite and terrigenous material (Leinfelder et al., 2002, 2005; Schlagintweit and Gawlick, 2008; Rusciadelli et al., 2011; Ricci et al., 2018a, b). The small sizes of exotic clasts and much reduced availability of samples is why seeing these features in the Štramberk-type limestones is much more difficult. Nevertheless, the common, detritic limestones and reef-derived breccias and the proximity to deep-water ba­sins (pre-flysch of the Cieszyn Beds) support high or moder­ate, topographicrelief at the reef edge of the carbonate plat­forms, part of the Štramberk Carbonate Platform, remnants of which are preserved as the Štramberk-type limestones. The low number of exotic clasts, representing matrix- and clast-supported breccias, is considered to be a result of the much reduced amount of material available (the large, ac­tive Kotouč Quarry, near Štramberk, in the Czech Republic vs the exotic clasts studied here). The microencruster-mi­crobial-cement boundstones (FT2; typical of the intra-Teth­yan carbonate platforms), previously only reported to a mi­nor extent (Hoffmann et al., 2008; Kołodziej et al., 2015), are well represented in the exotics studied, but as in the Štramberk Limestone (Hoffmann et al., 2017), they are sub­ordinate to the coral-microbial boundstones (FT 1). Eliášová (1981b) and Eliáš and Eliášová (1984) subdi­vided the Štramberk reef complex into (1) a fore-reef; (2) a reef core, with (a) a reef front, (b) a reef edge, and (c) an inner reef flat; and (3) a back reef (lagoon). This model was proposed on the basis of a comparison with modern reefs in the Red Sea and the Caribbean region. However, because of the different ecological demands and physio­logical capabilities of the pre-Cenozoic corals (e.g., mod­ern, multiserial, branching Acropora vs Jurassic branching, phaceloid corals), an actualistic approach to ancient reefs should be critical (e.g., Wood, 1999; Leinfelder et al., 2002). The zonation of modern reefs is used in reconstructions of the Cenozoic fossil reefs, but zonations of the Jurassic reefs based on corals are almost non-existent (Lathuiliere et al., 2005, 2021). Phaceloid corals are common both in the Štramberk Limestone and in the Štramberk-type limestones. The distribution pattern of phaceloid corals in the Štramberk reef, inferred by Eliášová (1981b) and Eliáš and Eliášová (1984), requires modification. It was assumed by these au­thors that such corals grew in two zones: (1) on a low-ener­gy inner platform, and (2) in deeper parts of the reef front. The second zone was inferred on the basis of the co-occur­rence with planktonic organisms, which were, however, not well documented enough in terms of their frequency. Calpionellids are typical of limestones deposited in deeper settings (FT 8, FT 3), but in the Štramberk-type limestones studied, they were recognized also in some samples from the shallow-water facies (FT 1, FT 6, FT 7, and even FT 5). Deeper parts of the reef front were assumed by Eliáš and Eliášová (1984) to be the locations of branching corals. However, this is not in agreement with the present inter­pretation of the distribution pattern of the Jurassic phace­loid corals (very rare in modern reefs), which are current­ly assigned to the inner platform (e.g., Leinfelder et al., 1996, 2002; Rusciadelli et al., 2011; Ricci et al., 2018a). Except for the Štramberk Limestone and the limestones studied here, the only proliferation of phaceloid pachythe­caliines was observed in the upper Barremian of Bulgaria. The growth of these corals was considered referable to dis-tal settings of the rudist-dominated, inner carbonate plat­form (Fenerci-Masse et al., 2011) and to the inner carbonate platform (Kołodziej et al., 2012). In the opinion of the pres­ent authors, most of blocks and clasts with phaceloid corals, both in the Štramberk Limestone and in the Štramberk-type limestones, represent the inner platform. Zonation of other European reef-bearing carbonate platforms The zonation models proposed by Lathuiliere et al. (2005, 2021) concerns the Oxfordian reefs representing reefs of the northern Tethyan shelf that differ significantly from the reefs developed on the intra-Tethyan carbonate platforms. The only recent, detailed model (with biotic zonation) of the Tethyan carbonate platform is based on the study of the Upper Jurassic mixed stromatoporoid-coral reef com­plex (Ellipsactinia Limestones) of the Central Apennines (Rusciadelli et al., 2011; Ricci et al., 2018a). According to Rusciadelli et al. (2011), the proposed sedimentary model can be applied to other Tethyan reef complexes. However, the reefs of the central and southern Tethys are stromatoporoid-coral reefs (Turnšek et al., 1981; Leinfelder et al., 2005; Rusciadelli et al., 2011; Ricci et al., 2018a). The present authors assume that this model can rather be a reference model for the Late Jurassic reef complexes of central and southern Tethys, than for those of its northern part (Štramberk Carbonate Platform). Calcified sponges (stromatoporoids and chaetetids) occur in the Štramberk Limestone (Bachmayer and Flügel, 1961a, b) and in the Štramberk-type limestones (Podoba, 2009), but their quantitative significance has not yet been evaluat­ed. Thin, millimetres-sized, calcified sponges are important in the framework of the microencruster-microbial-cement boundstones (FT 2), but they are volumetrically subordi­nate in the coral-microbial boundstones (FT 1). Both pre­vious and recent studies showed that corals out-competed calcified sponges. Nevertheless, calcified sponges are much more common and diversified, in contrast to the situation on the northern Tethyan shelf. For example, on the upper Kimmeridgian carbonate platform of the Holy Cross Mts. in Poland, only chaetetids (locally common) occur in some beds (Kołodziej, 2003b). An analysis of the stromatoporo­id and chaetetid sponges of the Štramberk Limestone, even though their significance is lower than in the reefs of the central and southern Tethys, would be crucial for the in­terpretation of the original position of particular olistoliths and blocks within the reef complex (upper slope, outer and inner platform; Leinfelder et al., 2005; Schlagintweit and Gawlick, 2008; Rusciadelli et al., 2011). Leinfelder et al. (2005) hypothesised that Jurassic reefs with the pre­dominance of calcified sponges developed under olig­otrophic conditions, controlled by oceanic circulation. The Štramberk Carbonate Platform – located in the northern Tethys – in terms of trophic conditions appears to have been intermediate in character between the central and southern, intra-Tethyan platforms and those in the epicontinental seas of the northern Tethyan shelf. Štramberk-type limestones On the basis of an analysis of exotic clasts, previous studies of the Štramberk Limestone and the zonation of other intra-Tethyan carbonate platforms with reefs, the following zonation of the Tithonian–earliest Cretaceous carbonate platform studied is proposed (Fig. 24). Coral­microbial patch-reefs (FT 1) grew in the inner carbonate platform, while the upper slope of the platform was the sed­imentary setting for the microencruster-microbial-cement boundstones (FT 2). In the inner, open part of the platform, with diverse hydrodynamics, foraminiferal-algal (FT 5) and peloidal-bioclastic limestones (FT 6) were deposited. “Lithocodium-Bacinella” possibly formed lone boundstone patches within the foraminiferal-algal facies (cf., Hofmann, 1991). Reef-derived detrital limestones (FT 4; the com­monest facies) and ooid grainstones (FT 7; a rare facies) were formed in a peri-reefal (only FT 4) and on a high-en­ergy margin of the carbonate platform. Detrital limestones with rare or common reef components may indicate hab­itat and microhabitat heterogenity, but presumably reflect mainly distance to the reef, with more reef components occurring in the peri-reefal environment. Clast-supported (cement-rich) and matrix-supported breccias (classified as FT 4) were deposited on the margin of the platform or on the high-energy, upper slope and low energy, upper slope of the carbonate platform, respectively. Calpionellids were not found in the matrix of the second breccia type, but they were recognized in similar matrix-supported breccias in the Štramberk Limestone (Eliáš and Eliášová, 1984; Hoffmann et al., 2017). The origin of both breccia types was facilitated by the distinct topography of the platform margin, by the high energy (in the case of the clast-supported breccias), and by synsedimentary tectonics. Microbial and sponge-micro­bial boundstones (FT 3) and mudstones-wackestones with calpionellids (FT 8) were developed in a deeper setting: in a deeper part of the platform slope and/or in a basinal set­ting. Eliáš and Eliášová (1984) described in the Štramberk Limestone slope deposits with reef-derived clasts and with abundant planktonic organisms in a micrite-dominated Fig. 24. Schematic facies distribution on a lost carbonate platform, based on the study of the Štramberk-type limestones, Polish Outer Carpathians (Hoffmann and Kołodziej, 2008, modified). Main facies types: FT 1: coral-microbial boundstones, FT 2: microencruster­microbial-cement boundstones, FT 3: microbial and microbial-sponge boundstones, FT 4: detrital limestones, FT 5: foraminiferal-algal limestones, FT6: peloidal-bioclastic limestones, FT 7: ooid grainstones, FT 8: mudstones-wackestones with calpionellids (and allodapic pre-flysch Cieszyn Beds, not studied in this paper), ?: supposed sediments of hypersaline and intertidal environments (not present in exotics). Microfacies not attributed to the main facies. M 1: stromatolites; M 2: oncoid-ooid packstones; M 3: limestones dominated by bivalves or other shells; M 4: echinoderm wackestones. matrix. The clasts of FT 8 may have been derived in part from similar deposits. Between carbonate platforms, in tec­tonic grabens, sedimentation of pelagic (equivalent of FT8) and the dominantly allodapic Cieszyn Limestone Formation took place. Restricted (hypersaline and intertidal) facies of the carbonate platform are not known from exotic clasts, possibly in part owing to their scarcity and lower preserva­tion potential. The platforms, on which sedimentation of the Štramberk­type limestones took place, are part of the Štramberk Carbonate Platform, or more precisely, narrow platforms attached to intrabasinal ridges, with morphology deter­mined by Late Jurassic synsedimentary tectonics. Eliáš and Eliášová (1984) estimated that the reef complexes extend­ed for 400 km “from Bečva valley (close to Štramberk – a comment by the present authors) into the eastern Flysch Carpathians”. Štramberk-type limestones in Romania (e.g., Getic Carbonate Platform, Southern Carpathians; Apuseni Mts, Western Carpathians) show a clear similarity to the limestones studied here (Sasaran, 2006; Bucur et al., 2010; Pleş et al., 2013, 2016, 2019; Mircescu et al., 2019). Corals in these limestones were not studied, but preliminary obser­vations of thin sections from the material mentioned above as well as field observations in the Sănduleşti Quarry in the Trascău Mountains (Sasaran, 2006; Bucur et al., 2010) by one of the authors (B.K.), have not revealed numerous pachythecaliine corals, which are so abundant in Czech Republic and Poland. Thin fissures, interpreted as neptunian dykes, in three exotic clasts filled with dark limestones, document the destruction and drowning of the Štramberk CarbonatePlatform. In the Štramberk Limestone (Kotouč Quarry), there are numerous cavities, including fissures, several decimetres to more than 1 m across. Cavities, mainly filled with laminated micritic limestone, are contemporaneouswith the sedimentation of the Štramberk Limestone and younger limestones (Berriasian–Valanginian). They are mostly related to the tectonic activity of the Baška-Inwałd Ridge. The stress-induced environment of these cavities was colonized almost exclusively by the Chondrites trace maker (Uchman et al., 2003). Similar traces were recog­nized in the micritic limestones in fissures, transecting theshallow-water limestones in exotics of the Štramberk-type limestones mentioned above. Comparison to palaeogeographically close platforms of the Tethyan shelf The limestones of the Štramberk Carbonate Platform show clear differences with coeval limestones of the pal­aeogeographically close carbonate platforms on the north­ern Tethyan shelf (Peri-Tethys). During the Late Jurassic (predominantly in the Oxfordian–early Kimmeridgian), carbonate sedimentation in the Polish part of the epiconti­nental Central European Basin took place on a shelf with a ramp configuration. Since the early Kimmeridgian, in some areas this basin was transformed into a well-developed car­bonate platform (Kutek, 1969). The Meta-Carpathian Arch separated structurally and at times palaeogeographically the Central European Basin from basins of the Carpathian (Tethyan) domain in Permian to Cenozoic time (Kutek, 1994). Tithonian coral-bearing facies, in original deposition­al position, are known from borehole data in the central and southern parts of the Carpathian Foredeep, Poland (Morycowa and Moryc, 1976, 2011; Gutowski et al., 2007; Matyja, 2009; Urbaniec et al., 2010; Krajewski et al., 2011; Morycowa, 2012). The Pilzno Coral Limestone Formation was compared by Matyja (2009) with the Štramberk Limestone, but without data on the reef framework and the abundance and diversity of corals. In the only taxonomic paper on corals from the Carpathian Foredeep (Dąbrowa Tarnowska–Szczucin area), Morycowa (2012) described 42 species (only one species from the suborder Pachythecaliina, which is highly diversified in the Štramberk-type lime­stones). Makowiec (2017) and Faka (2017) in their Master’s theses observed only poorly developed microbial and mi­croencruster framework fabrics (well developed in the FT1 facies of the Štramberk-type limestones) in the Tithonian coral-bearing limestones (partly classified as boundstones) from boreholes at Swarzów, near Dąbrowa Tarnowska (southern part of the Carpathian Foredeep). These observa­tions are confirmed by the examination by the present au­thors of thin sections described by the authors mentioned above as well as those described by Morycowa and Moryc (1976) and Morycowa (2012). Similarly, Krajewski et al. (2011), who studied drill-cores from the Kraków-Rzeszów area, stated that there were no large ooid or reef barriers, but rather numerous open-platform shoals. Microencruster­microbial-cement boundstones (= FT2) are not known in the Carpathian Foredeep. Microbial-sponge facies, known from the Oxfordian of the Kraków Upland (e.g., Matyszkiewicz, 1997; Matyszkiewicz et al., 2012; Krajewski et al., 2016) and up to the lower Tithonian in the Carpathian Foredeep (Matyja, 2009), occur quite commonly in exotics in the Carpathians. They are of Oxfordian–Kimmeridgian age (Kowal-Kasprzyk et al., 2020). Similar facies are repre­sented among the Štramberk-type limestones and clas­sified as FT 3. Dinoflagellate cysts and calpionellids ev­idently indicate on the Tithonian–Berriasian age of FT 3. Siliceous sponge reefs were restricted in Europe most­ly to homoclinal ramp settings along the northern Tethys (Leinfelder et al., 2002). Like many carbonate platforms (including coral reefs) on the northern Tethys shelf, platforms recognized in the Carpathian Foredeep were developed within terrigenous­ly influenced settings, evidenced by the presence of marly limestones and marls. Such terrigenous input was common­ly paralleled by an increase in nutrient level and as a con­sequence, an enhancement in the growth of microbialites (Dupraz and Strasser, 2002 and literature therein). Poorly de­veloped microbial crusts in the limestones of the Carpathian Foredeep may be explained by a high sediment supply. The north-eastward continuation of this platform was rec­ognized in boreholes in the Lublin Upland, which is locat­ed on the East European Craton (Platform). In the Lublin Upland, Tithonian deposits are developed among others as the sediments of marginal environments (hypersaline and intertidal) of the carbonate platform (Niemczycka, 1976; Gutowski et al., 2005a). These facies were not recognized in the Štramberk-type limestones. The Babczyn Formation of the SE Lublin Upland is an equivalent of the upper Tithonian–lower Berriasian Niżniów (Nyzhniv) Formation, outcropping along the Dniester River, Western Ukraine (Gutowski et al., 2005b). Izotova and Popadyuk (1996) re­garded limestones at the contact between the Niżniów and the Opary Formations as reefal, but Gutowski et al. (2005b) regarded them as bioconstructed. The Niżniów Formation in the area studied by Gutowski et al. (2005b) is developed mainly as biomicrites, oncomicrites, and pelmicrites with an abundant fauna, dominated by gastropods, hence cannot be classified as reefal facies. Eliáš and Eliášová (1986) compared the carbonate se­quences of the Štramberk carbonate platform with the Brno carbonate platform (autochthonous Jurassic of the Bohemian Massif) and the Pavlov carbonate platform. The Ernstbrunn Limestone (Austria and Czech Republic), less known than the Štramberk Limestone, was deposited on the Pavlov (Ernstbrunn-Pavlov) carbonate platform (epicon­tinental shelf of the Tethys). Traditionally, the Ernstbrunn Limestone has been interpreted as a tectonically detached part of a carbonate succession, which evolved on the rift­ed, passive, Tethyan margins in the Oxfordian–Tithonian. Alternatively, it is interpreted as a pile of carbonate debris, derived from a pre-existing, hypothetical, Tithonian plat­form and redeposited in the Ždánice Basin (the north-east­ward extension of the Sub-Silesian Basin) at a time of eu­static drop in sea level (Eliáš and Eliášová, 1984, 1986; Schneider et al., 2013). Poorly developed, reefal structures, with poorly diversified corals (26 species, only one from the Pachythecaliina), occur in the Ernstbrunn Limestone in the Czech Republic (Eliášová, 1990). The “classical” Ernstbrunn Limestone in Austria is represented by lagoon­al facies, patch-reef facies, and facies of fringing ooid-on­coid bars. About 30 species of corals were determined (but not illustrated) from the Ernstbrunn Limestone in Austria (see Schneider et al., 2013). Generally, the Ernstbrunn Limestone consists predominantly of variable lagoonal fa­cies, whereas the Štramberk Limestone is mainly composed of reef and fore-reef facies. This is evidenced by the fossil content, for example, the rare occurrence of giant gastro­pods at Štramberk (Harzhauser and Schneider, 2014). According to Eliáš and Eliášová (1986), different sedi­mentary conditions on the platforms discussed were heavily constrained by sedimentation in various tectonic settings. The Štramberk Limestone was deposited on the mobile Baška Ridge (= Baška-Inwałd Ridge). The Brno and Pavlov carbonate platforms were located in a tectonically less ac­tive area (part of the epi-Variscan European Platform). The tectonic setting determined the sedimentary and palaeoeco­logical conditions. There was compensation for the sub­sidence of the Baška Ridge by the intensive development of reefal facies. Environmental conditions on the Pavlov carbonate platform favoured the sedimentation of lagoonal facies. These conditions controlled the origin of magnesi­um brines that resulted in dolomitization. Dolomitization is present in coeval limestones of the Carpathian Foredeep (e.g., Morycowa and Moryc, 1976; Krajewski et al., 2011) and occurs in exotics of the Oxfordian–Kimmeridgian lime­stones (Kowal-Kasprzyk et al., 2020). Dolomitization is absent from the Štramberk Limestone (Eliáš and Eliášová, 1986) and very rare in the Štramberk-type limestones. More detailed, comparative studies of limestones de­posited on platforms, collectively termed the Štramberk Carbonate Platform, and palaeogeographically close, north­erly located platforms, are needed to reveal local versus supra-regional controls (tectonic, oceanographic, palaeobi­ological) on sedimentation. Differences in sedimentation on the Brno and Pavlov carbonate platforms on the one hand andthe Štramberk Carbonate Platform on the other were heavily constrained by various tectonic regimes (Eliáš and Eliášová, 1986), and this is also applicable to the limestones in Poland. CONCLUSIONS 1. The Upper Jurassic–lowermost Cretaceous limestones, named Štramberk-type limestones, are the most common among the exotic clasts (exotics), embedded in the upper-most Jurassic–Oligocene flysch deposits of the Silesian, Sub-Silesian and Skole units (nappes) in the Polish Outer Carpathians. About 90 % of determinable carbonate clasts (classified in the field as Štramberk-type limestones) are of Tithonian–Berriasian age and can be compared to the Štramberk Limestone in Moravia (Czech Republic), rep­resenting limestones of the carbonate platform and its slope. 2. Exotic clasts of the Štramberk-type limestones, predom­inantly of pebble and cobble sizes, from the Polish Outer Carpathians, as well as the Štramberk Limestone (large blocks, olistoliths) bore witness to a lost carbonate facto­ry. Narrow carbonate platforms were attached to the in­tra-basinal ridges (the largest are referred to the Silesian Ridge and to the Baška-Inwałd Ridge), with their dis­tribution and morphology determined by Late Jurassic synsedimentary tectonics. In the interpretation of sedi­mentary environments and platform zonation, these plat­forms have been considered collectively as the Štramberk Carbonate Platform. The unique taxonomic composition of coral assemblages from the Štramberk Limestone and the Štramberk-type limestones support linking these plat­forms in a single palaeogeographic unit. 3. Tithonian (mostly)–Berriasian and sporadically pos­sibly also Valanginian, Štramberk-type limestones are represented by eight main facies, which were attributed to different sedimentary environments. Coral-microbial boundstones (FT 1) were formed as patch reefs in the inner platform. The upper slope of the platform was the depositional setting for microencruster-cement bound­stones (FT 2). Microbial and microbial-sponge bound­stones (FT 3) were developed in a deeper setting (the lower part of the slope?). Detrital limestones (bioclas­tic-lithoclastic grainstones to rudstones, matrix- and clast-supported breccias, FT4) developed in a peri-reefal environment and in a high-energy setting of the platform margin. Foraminiferal-algal limestones (FT5) and peloi­dal-bioclastic limestones (FT 6) were developed in the inner platform. Ooid grainstones (FT 7) were developed on the platform margin. Mudstones-wackestones with calpionellids (FT 8) represent a deeper part of the plat­form slope and/or a basinal setting and can be compared with coeval pelagic lithofacies of the Cieszyn Limestone Formation (“pre-flysch”), deposited in tectonic grabens, between ridges with attached platforms. FT4 is the most common facies among the exotics. Peloidal stromatolites (M 1), oncoid-ooid packstones (M 2), limestones domi­nated by bivalves or other shells (M 3) and echinoderm wackestones (M 4) are subordinate, but noteworthy mi­crofacies. They cannot be assigned to the main facies distinguished, even though some facies show high mi­crofacies diversity. Most facies of the Štramberk-type limestones differ from the Oxfordian–Kimmeridgian limestones (not studied here). The latter are much less common among the exotics; in the field, they also would be termed Štramberk-type limestones. They may be com­pared with limestones of the so-called sponge megafaci­es, deposited on a homoclinal ramp of the northern mar-gin of the Tethys. 4. The destruction and drowning of carbonate platforms (Štramberk Carbonate Platform) in the earliest Cretaceous is recorded in a few exotics by neptunian dykes (very thin in the exotics studied and thick in the Štramberk Limestone), filled with dark, deep-water limestones 5. Reefal facies in the exotics studied and the Štramberk Limestone exhibit similarities in several respects (e.g., the occurrence of the microencruster-cement bound­stones) with the reefs of other intra-Tethyan carbonate platforms, but clearly differ from palaeogeographically close reefs and the coral-bearing facies of the Tethyan shelf (e.g., the coeval limestones occurring in the subsur­face of the Carpathian Foredeep and the Lublin Upland in Poland; the Ernstbrunn Limestone in Austria and the Czech Republic). 6. The most important provenance area for the exotic clasts and other detrital material in the Proto-Silesian and Silesian basins was the intra-basinal Silesian Ridge, tradi­tionally called the Silesian Cordillera. It evolved through time from the emerged part of the Upper Silesian Massif (part of the Brunovistulicum Terrane) to an accretionary prism since the Late Cretaceous. Exotic clasts from the Sub-Silesian Unit were derived mostly from the Baška­Inwałd Ridge (till the end of the Early Cretaceous), while the material that accumulated in the Skole Basin mostly came from the Northern (Marginal) Ridge. Most of the exotics studied were collected in the Silesian Unit, where exotics are particularly common in the Lower Cretaceous Hradiště Formation and the Upper Cretaceous–Paleocene Istebna Formation. In the Sub-Silesian Unit, most exotics are from the Hradiště Formation and less commonly from the Barremian–Aptian Veřovice Formation. In the Skole Unit, they are largely in the Maastrichtian–Paleocene Ropianka Formation. The Štramberk-type limestones are much rarer in the Magura and Dukla units as well as in the Stebnik and Zgłobice units (the folded Miocene at the front of the Outer Carpathians) and were not studied here. Acknowledgements The present paper is the outcome of studies by Mariusz Hoffmann and Bogusław Kołodziej, and work by Justyna Kowal-Kasprzyk in part for her PhD thesis, completed at the Jagiellonian University and supervised by Marek Cieszkowski. The manuscript of this pa­per was finalized after the death of M. Hoffmann and B. Kołodziej, the co-author of the preliminary reports, takes full responsibility for any mistakes. B.K. was supported by the Jagiellonian University (ING UJ statutory funds). J.K.K. was supported by the National Science Centre in Poland (Grant No. N N307 057740), the Brian J. O’Neill Memorial Grant-in-Aid for Ph.D. Research 2014, ING UJ statutory funds No. K/ZDS/001463, and AGH Funds No. 16.16.140.315. B.K. thanks Elżbieta Morycowa (Kraków) for help during work on corals from the limestones under investigation. J.K.K. thanks Barbara Olszewska and the late Marek Cieszkowski (Kraków) for helpful suggestions during her study. The authors are grateful to reviewers Ioan I. Bucur (Cluj-Napoca) and Michał Krobicki (Kraków) and editors Michał Gradziński, Ewa Malata, Alfred Uchman (Kraków) for their corrections and construc­tive comments that improved the manuscript. Frank Simpson (Windsor) kindly improved the English of the manuscript. REFERENCES Atasoy, S. G., Altiner, D. & Okay, A. I., 2018. Reconstruction of a Late Jurassic–Early Cretaceous carbonate platform mar-gin with composite biostratigraphy and microfacies analysis (western Sakarya Zone, Turkey): Paleogeographic and tecton­ic implications. Cretaceous Research, 92: 66–93. 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