Upper Triassic‒Middle Jurassic resedimented toe-of-slope and hemipelagic basin deposits in the Dinaridic Ophiolite Belt, Zlatar Mountain, SW Serbia

In the Dinaridic Ophiolite Belt, small (m-scale) to large (km-scale) blocks of Middle to Upper Triassic, and Middle to Upper Jurassic, more or less silicified bedded limestone are widely present, both as parts of para-autochthonous successions and as redeposited blocks in ophiolitic mélanges. The studied, approximately 230-m-thick succession in the wider area of Zlatar Mountain, is one of the most important para-autochthonous sections in the Serbian part of the Dinaridic Ophiolite Belt. The succession is made up of an alternation of redeposited carbonate toe-of-slope deposits, sand to clay-sized siliciclastic rocks, hemipelagic mudstones and radiolarite–spongiolite basin facies. In the lower part of the sequence, the components of the siliciclastic beds were derived mostly from low- and medium-grade metamorphic rocks. Similar components, together with sand-sized fragments of ophiolitic rocks, were encountered in small amounts in some redeposited carbonate beds. The chronostratigraphic assignment of the succession is based mostly on foraminifers, but age-diagnostic radiolarians and other microfossil groups were also considered. In the lower part of the probably continuous succession, a Norian–Rhaetian assemblage was recognized; a Sinemurian–Pliensbachian assemblage was encountered up-section, whereas the upper part of the succession could be assigned to the Bajocian–Bathonian. Considering the paleogeographic reconstructions and the analogies of age-equivalent sections, the succession records the depositional history of the Bosnian Basin during the Late Triassic to Middle Jurassic period and may contribute to the understanding of the evolution of the Adriatic margin of the Neotethys Ocean in the transition interval from passive to active margin stages.


Introduction
The Dinaridic ophiolite belt (DOB) (Dimitrijević 1997;Karamata et al. 2000;Dimitrijević et al. 2003;Karamata 2006) with the Dinaridic Ophiolite Nappe on top of the nappe stack Electronic supplementary material The online version of this article (https ://doi.org/10.1007/s1034 7-019-0566-3) contains supplementary material, which is available to authorized users. (Gawlick et al. 2016(Gawlick et al. , 2017 is an important segment within the Alpine-Dinarides-Albanides-Hellenides Orogenic System (e.g., Jones and Robertson 1991;Bortolotti et al. 2006;Gawlick et al. 2008;Kilias et al. 2010;Ozsvárt et al. 2012;Kilias et al. 2016). The most conspicuous feature of this belt is a Middle-Upper Jurassic ophiolitic mélange with large gravity slides/blocks of varying origin and huge bodies of ultramafic masses (Dimitrijević et al. 2003;Karamata 2006;Haas et al. 2011;Kovács et al. 2011;Gawlick et al. 2016Gawlick et al. , 2017. Investigations of the rock assemblage, which was first referred to as the "Diabas-Hornstein Formation" or "Diabashornsteinschichten" (e.g., Ampferer and Hammer 1918;Hammer 1923), began in Serbia before the 1920s, the focus of studies being its age-determination (Triassic or Jurassic). It was considered a normal volcanic-sedimentary formation and this opinion persisted for a long time (see in Dimitrijević et al. 2003). Intensive studies were performed during the time of geological mapping for the Basic Geological Map of the SFRY (scale 1:100,000) between 1960 and 1990, when these deposits were called the "Diabase-Chert Formation" (e.g., Živaljević et al. 1983). Dimitrijević andDimitrijević (1973, 1979) summarized the general characteristics of this rock assemblage in the Inner Dinarides, calling it ophiolitic mélange for the first time in the area of SW Serbia, and suggesting its sedimentary origin. Karamata et al. (1999) interpreted an oceanic trench complex as the depositional environment; in contrast with other authors (e.g., Schmid et al. 2008), they supposed a more or less para-autochthonous position of the mélange. Later, Dimitrijević et al. (2003) described a chaotic association of shallow-marine to deep-sea sedimentary rocks and mafic to ultramafic rocks as an olistostrome/mélange and interpreted this block-in-matrix texture as slope sediments. In the above-mentioned papers of Serbian authors, all the ophiolitic rocks were interpreted as large blocks and/or olistoplacae within the mélange. Gawlick et al. (2016Gawlick et al. ( , 2017 distinguished two types of succession within the area of the DOB: (1) the underlying Triassic to Upper Jurassic paraautochthonous sedimentary sequences formed by imbrication and nappe overthrusting within the continental margin, and (2) the overlying Middle Jurassic mélanges (sedimentary mélange mainly with Triassic and Jurassic clastic components) deposited in the foreland basins of the advancing nappe stack formed due to the westward-prograding ophiolite obduction.
Intensive and comprehensive geological investigations and detailed mélange analyses were initiated in the DOB after the first papers of Gawlick et al. (2007Gawlick et al. ( , 2009. These studies revealed the complexity caused by the multiple resedimentation processes and multiphase deformation, leading to different and commonly contradictory interpretations for the genesis of the studied rock assemblages (discussed by Gawlick et al. 2017).
After reconnaissance studies in the vicinity of the town of Sjenica located in the south-easternmost parts of Zlatar Mt. (Gawlick et al. 2009), we carried out detailed field investigations and sampling along a section on the eastern side of the Trijebinska Reka valley (Fig. 1c). The section exposes part of the para-autochthonous basement of the ophiolite mélange. Our investigations permitted the chronostratigraphic assignment and provided data on the lithoand bio-facies characteristics, as well as the sedimentological features of the succession recording a significant part of the history of the Neotethys margin evolution. Since only a few similar exposures are known in the Inner Dinarides, and the number of the detailed, comprehensive studies is very limited, the results are particularly important for the reconstruction of the evolution of the Adriatic margin of the north-western Neotethys Ocean as a whole.

Geological setting and earlier investigations in the Sjenica area
In the central parts of the DOB, especially in the area of Zlatar Mt., the widely exposed ophiolite mélange contains clasts of variable lithology (pelagic carbonates, radiolarites, ophiolitic rocks, albite granites, etc.) and variable size (from millimeter to hundreds of meter) in a shale, radiolaritic marl, and radiolarite matrix. In the neighborhood of the town of Sjenica, this rock assemblage was named the "Sjenica mélange" (Gawlick et al. 2009). More or less silicified, bedded limestones also occur in the same area, either as redeposited blocks in the mélange or as parts of para-autochthonous sedimentary successions (Gawlick et al. 2017).
During the mapping project of Thematic Geological Maps of Serbia (1:50,000), which began in the late 1980s and was based on lithostratigraphic principles, Dimitrijević and Dimitrijević (1991) introduced the name Grivska Formation  (Karamata 2006;Karamata et al. 2000;Gawlick et al. 2017): SMU Serbian-Macedonian Unit, MVZ Main Vardar Zone, KBRU Kopaonik Block and the Ridge Unit, VZWB Vardar Zone Western Belt, JB Jadar Block, DIE Drina-Ivanjica Element, DOB Dinaridic Ophiolite Belt, EBDMU East Bosnian-Durmitor Megaunit. c Geology of the wider surrounding of the town of Sjenica (part of the simplified map by Živaljević et al. 1983). Legend: 1 Alluvial, 2 Neogene sediments, 3 Ophiolitic mélange (3a peridotite and basite), 4 Middle to Upper Jurassic radiolarites with intercalated turbidites and mass transport deposits, 5 Lower Jurassic red limestone, 6 in general Upper Triassic massive and bedded limestones, 7 Middle Triassic limestone, 8a normal fault, 8b supposed fault, 8c erosional boundary, 9 localities: a Krš Gradac b Strmenica c Brajska reka, 10 Trijebinska Reka section (asterisk) Page 4 of 29 for grey, thin-to-medium cherty bedded limestones with thin marl and clayey limestone interlayers. According to their interpretation, it represents a hemipelagic facies and they assigned it to the Ladinian. Later, based only on macroscopic attributes, regardless of their generally unknown age and without any detailed microfacies investigations, the term "Grivska Formation" was used in a confusing and misleading way until the recent work of Gawlick et al. (2017) and Sudar and Gawlick (2018) for all Middle Triassic (Ladinian) to Middle (?Upper) Jurassic grey cherty limestone successions in the DOB (e.g., Dimitrijević 1997;Radovanović et al. 2004;Chiari et al. 2011), and also in the Vardar Zone Western Belt (Toljić et al. 2013). After reinvestigation of the Grivska Formation in its type locality and in adjacent areas of the DOB, a new amended definition was presented by Gawlick et al. (2017) and Sudar and Gawlick (2018). According to the new definition, the Grivska Formation is characterized by radiolarian-and filament-bearing wackestones, without any platform-derived components, Late Triassic (early Carnian to Rhaetian) in age; it is known only as blocks in the ophiolitic mélange. For the other Triassic grey cherty limestones occurring in the DOB and for the Kopaonik area in the Vardar Zone (in the sense of Karamata 2006;Gawlick et al. 2017), new formations were introduced by Schefer et al. (2010), Missoni et al. (2012), Sudar et al. (2013) and Gawlick et al. (2017).
Two new radiolarite units were defined from the Middle and Upper Jurassic para-autochthonous sequences of the DOB (Gawlick et al. 2017). Grey cherty limestones of Jurassic age also occur but they have not yet been differentiated, defined, and reviewed in a lithostratigraphic sense.
In the initial studies of the "Diabase-Chert Formation" (up to the 1980s) in the Sjenica area, the succession of the Trijebinska Reka section (black asterisk in Fig. 1c) was the object of very contradictory opinions. Jovanović et al. (1979) considered it as a limestone-chert series, with rare intercalations of diabase, tuffaceous sediment, siltstone and marl, undoubtedly indicating its volcanic-sedimentary genesis, and did not assign it to the "Ophiolitic mélange". Working on the Geological Map of Serbia (1:50,000), Radovanović et al. (1996) suggested that the exposed bedded limestone sequence should be treated as a separate unit (without suggesting any name) within the complex of the "Diabas-Chert Formation" (i.e., in the Ophiolite Mélange). Radovanović et al. (2004) on the sheet Prijepolje 2 (Geological Map of Serbia, scale 1:50,000), including the area of our study, distinguished the "Ophiolite Mélange" and the "Grivska Formation" as separate units.
Several sections similar to that in the Trijebinska Reka valley occur in the vicinity of the town of Sjenica. One of them is Brajska Reka near the village of Aljinovići (locality c in Fig. 1c) and another is Strmenica on Jadovnik Mt. (locality b in Fig. 1c). In the first section, Jurassic bedded limestones with resedimented bioclasts and lithoclasts of various ages were classified into an individual lithostratigraphic unit (without any specified name), as a member of the "Diabase-Chert Formation" (Jovanović et al. 1994). Preliminary field investigations of the Lower to Upper Jurassic cherty limestone successions were performed by our Serbian-Hungarian team in the year 2008 in the Strmenica locality, Jadovnik Mt. (locality b in Fig. 1c).
West of Sjenica, in the Krš Gradac section (locality a in Fig. 1c), there is exposed a succession occurring below the ophiolitic mélange. It is made up of Upper Triassic platform carbonates, Lower Jurassic shallow-marine to hemipelagic limestones, and Middle to Upper Jurassic radiolarites with turbiditic interbeds (Radoičić et al. 2009;Vishnevskaya et al. 2009;Gawlick et al. 2009Gawlick et al. , 2017. This succession was previously interpreted as a tectonic window or a tectonically incorporated sliver/slice (Gawlick et al. 2009). However, according to the latest interpretation of Gawlick et al. (2017), the exposed Upper Triassic to Upper Jurassic sequence belongs to the para-autochthonous succession that is overthrust by the ophiolitic mélange around the Jurassic/ Cretaceous boundary.
In the later Serbian literature, the Jurassic cherty carbonate successions in the wider surroundings of Sjenica (localities in Fig. 1c) were wrongly assigned to the "Grivska Formation" (e.g., Dimitrijević 1997;Radovanović et al. 2004). The successions exposed in the above-mentioned localities differ significantly in age and litho-and micro-facies characteristics from those of the amended Grivska Formation (in the sense of Gawlick et al. 2017;Sudar and Gawlick 2018). The Upper Triassic-Middle Jurassic or Lower to Upper Jurassic deposits from these localities should be assigned to one or more new formations not yet defined, which like the Upper Triassic Grivska Formation belong(s) to the paraautochthonous basement of the DOB, i.e., occur(s) below the Middle to lower Upper Jurassic ophiolitic mélange and the ophiolite nappes (Gawlick et al. 2017).

Materials and methods
The studied section, traditionally named the Trijebinska Reka section, is situated on the eastern side of the river valley near the installations of the Sjenica water supply system (N 43°14ƍ5.5Ǝ E 19°59ƍ31.4Ǝ;Figs. 1,2).
Sampling for microfacies and micropaleontological studies was carried out in two stages. The measured section with the indication of the sampling points is displayed in Fig. 3. In the course of the first sampling, 87 samples were collected; they are marked by the letter S. This was followed by a second sampling to complement the previous sample series, when 29 samples were collected; they are marked by the letter T. From the red radiolarite in the uppermost part of the studied section, three additional samples (BR3, VL-14, GBR1) were selected. In total, 102 thin-sections 24 × 46 mm in size and 60 thin-sections 50 × 50 mm in size, were analyzed. Based on the thin-sections, ten samples, which were the richest in calcareous microfossils, were treated with glacial acetic acid. Six samples (T7, T10, T29, BR3, VL-14 and GBR1) were dissolved in approx. 3-5% HF (nine parts distilled water and one part concentrated HF (48%), following the standard laboratory procedures of Pessagno and Newport (1972). Thereafter, the samples were treated repeatedly in approx. 1-2% HF; thus samples T29 and BR3 yielded some poorly preserved but determinable radiolarian species.
The preparation and microscopic study of the samples were carried out in the laboratories of the Department of Petrology and Geochemistry and the Department of Paleontology of the Eötvös Loránd University (the MTA-ELTE Geological, Geophysical and Space Science Research Group), where all micropaleontological and sedimentological materials and the thin-sections are stored. The imaged radiolarians and sponge spicules presented herein were taken using a Hitachi S-2600 N type scanning electron microscope at the Hungarian Natural History Museum, Budapest.

General description and subdivision of the studied section
Strongly weathered basalt with several better-preserved pillows in chertified matrix (ophiolitic mélange) occurs at the north-eastern end of the studied section ( Fig. 3a) exposed on the eastern side of the Trijebinska Reka valley. From chertified shale matrix, radiolarians of Late Bathonian Early Callovian (UAZ 7) age were found (Djerić 2002). At present, due to a few meters-thick covered interval, the contact between the mélange and the studied succession is not visible.
Along the valley an approximately 230-m-thick, continuous, steeply dipping monoclinal succession is exposed dasycladaleans are fragmented, generally strongly eroded, rounded, and in some cases they appear as the core of cortoids or within larger lithoclasts. Foraminifers commonly occur but usually in a very small number. The specimens are mostly fragmented and/or corroded. In some cases, the foraminiferal specimens occur as individual grains between other grains, but in others they appear in smaller or larger lithoclasts. Locally, the foraminiferal specimens are preserved as the nucleus of ooids, or with cyanobacterial encrustation around them. The carbonate grains of the above-described redeposited limestone beds were derived from an active carbonate platform; the redeposition took place mostly prior to consolidation of the sediments. In the case of Lf 1, debris flows and grain flows may have been the transporting mechanisms and the toe of a platform foreslope the site of deposition. Lf 2 can be assigned to medium-grained turbidites and may have been deposited in the distal part of the toe-of-slope belt. Lf 3 is a fine-grained turbidite, which may have been deposited in distal toe-of-slope and basinal environments.
Lf 4 Siliciclastic-carbonate rocks; sandstone, siltstone, claystone, marl. The sandstone beds consist of 0.05-0.2 mmsized siliciclasts predominantly derived from metamorphic rocks, although components derived from acidic magmatic rocks are also present. Radiolarians occur in the claystone/ marl beds, which are commonly silicified. This lithofacies type may have been deposited in a hemipelagic basin during periods of intensive terrigenous input.
Lf 5 Carbonate mudstone. There are only a small number of radiolarians, sponge spicules, and very small echinoderm fragments in a micritic matrix; this is hemipelagic to eupelagic basin facies.
Lf 6 Radiolarite, spongiolite. It consists predominantly of radiolarians and/or sponge spicules and is a eupelagic basin facies.
The lithofacies categorization of every studied sample, the occurrences of the age-diagnostic fossils and the siliciclastic components, and the interpretation of the depositional environment are displayed in Fig. 3a, b.
Based on the origin of the grains, two main groups of siliciclast are distinguished (Fig. 3a, b). The first group includes minerals and rock-types of a magmatic-anchimetamorphic part of a normal ophiolitic rock series (serpentinite and microcrystalline chlorite derived from glass alteration), Cr-spinel and strongly altered, chloritized mafic magmatic rocks (variolitic and porphyric basalts, dolerite). Some of the sedimentary-metasedimentary rock types may also belong to an ophiolitic sequence (siltstone, metasiltstone, radiolarite, metaclaystone). The other group of siliciclasts was derived from low-to medium-grade metamorphic rocks: chlorite schist, phyllite, quartzite, chloritic metasandstone, mica schist, muscovite schist, chlorite-bearing mica schist, chlorite phyllite, chloritized biotite, chloritic quartzite, (Figs. 2,3). It starts with a thick limestone bed progressing upward into thin-bedded grey limestone. It is followed by an approximately 30-m-thick darker grey, fine-grained siliciclastic sandstone, siltstone, and shale interval. The higher part of the succession (above 125 m) is made up by an alternation of thick-bedded, fining-upward calcarenitic limestone and thin-bedded or platy limestone, argillaceous limestone, or marl. The latter rock types are commonly silicified; they contain thin layers and lenses of chert and are partially locally dolomitized. Red siliceous shale and chert were found in the uppermost part of the studied section ( Fig. 3a, b).
Lf 2 Medium-grained grainstone to packstone. In addition to bioclasts, larger peloids (0.2-0.8 mm) ooids, cortoids, oncoids, and microbial micritic nodules are the typical carbonate grains. A small amount of sand-sized siliciclastic components commonly occurs, mostly in the basal part of the graded beds.
In all of the redeposited carbonate rocks described above, fragments of echinoderms (crinoids and echinoids) are usually common. Fragments of bivalves and ostracod shells are also present in several samples. Fragments of calcimicrobes (Girvanella-type and Cayeuxia-type, microproblematica (Baccinella sp., Pseudolithocodium and Thaumatoporella sp.) and Solenoporacean red algae commonly occur. From among the dasycladalean green algae, Acicularia sp., Anisoporella sp., Epimastopora sp., Selliporella? sp. and Clypeina sp. were found in small quantities. The gneiss, and biotite. Only a few of these rock fragments (e.g., metasandstone) contain relics of the pre-metamorphic magmatic or sedimentary rocks. Other components such as acidic non-zoned (intrusive) plagioclase, sericitic orthoclase, zircon, tourmaline, and some microcrystalline quartz were probably derived from acidic magmatic rocks (granitoids and rhyolites).

Litho-and bio-facies characteristics and chronostratigraphic assignment
As to its lithofacies characteristics, the whole succession below the red shale and radiolarite unit is rather uniform; it is made up of an alternation of toe-of-slope and basinal facies although, based on biostratigraphic data, it represents a long time-range, from the Late Triassic to the Middle Jurassic. Since we could not assign this succession or segments of it to the previously defined lithostratigraphic units (e.g., Gawlick et al. 2017) and we did not want to define new ones on the basis of a single section, we subdivided the studied section into eight informal units, which are based mostly on the microfacies assemblages (Foraminifera, Clorophycota, Chlorophyta Radiolarians, Porifera, Polychaete, and inceratae sedis) but also taking into account the lithofacies characteristics. The chronostratigraphic assignment of the studied section is based on microfossils. For the biostratigraphic evaluation, the foraminifers were mostly used, but the age-diagnostic value of radiolarians and other microfossil groups was also considered. The fossil assemblage of the toe-of-slope facies is evidently mixed; it may contain both autochthonous and allochthonous (redeposited) elements. This aspect should be taken into account for the age evaluation and interpretation of the habitat of the fossils.
For the characterization of these units, we describe first the lithological features and the most typical siliciclastic components (Figs. 5,6). The microfossils (Figs. 7,8,9,10,11) are listed in descending order of their frequency. For the systematic position, the selected synonymy, the stratigraphic range, and the ecological needs of the mentioned species, see Online Resource 1.
Unit 1 The lowermost bed-set of the measured section (8-18 m; samples S6-13, T1-3) is made up of a thick, carbonate turbidite bed (Lf 2, Lf 3) that is overlain by a thin-bedded brownish grey limestone (Lf 5). In a bioclastic wackestone bed a small serpentinite grain and in a bioclastic, peloidal grainstone bed, several Cr-spinel grains were found.
The foraminiferal fauna indicates a Late Triassic age. The U. andrusovi and the genus itself has been known only from the Carnian (Senowbari-Daryan 2016), while D. schaeferae and A. permodiscoides only from the Norian-Rhaetian. The genus Urnulinella belongs to the "Cucurbita group", which mostly appears in the Carnian, but some representatives lived in the Norian-Rhaetian interval (e.g., Senowbari-Daryan 2016). According to several authors (e.g., Bernecker 2005; Senowbari-Daryan 2016), the organisms, including the foraminifers of the Carnian and the Norian-Rhaetian reef systems, are significantly different. Accordingly, the most probable age of this interval is latest Carnian-Rhaetian.
Unit 2 This is a siliciclastic interval (18-47 m, samples S14-19). The carbonate layers of Unit 1 are overlain by dark brown shale with a sharp boundary. This is followed by a grey, fine-grained siliciclastic sandstone interval that gradually progresses upward into siltstone and shale (Lf 4).
In the basal part of this bed-set, in bioclastic, carbonate lithoclastic wackestone, a few sand-sized fragments of metamorphic quartzite, chloritic quartzite, mica schist, and acidic volcanite (magmatic quartz in microcrystalline quartz matrix) were observed (sample T5). A few small serpentinite and larger Cr-spinel grains, fragments of mica schist, and chloritite were found in the overlying layers.
In the toe-of-slope facies (Lf 1-3), besides fragments of echinoderms, sponge spicules and radiolarians, relatively diverse foraminiferal faunas, and algal associations occur. In the basin facies (Lf 5-6), the microfossil content is very similar to that of the previous interval.
Unit 4 The next interval (52-63 m; samples S25, T7-8) consists of cherty limestone. In the usually strongly silicified rocks, only sponge spicules and radiolarians could be recognized in thin-section. However, the acetolysis of one sample (54 m; T7), provided a relatively diverse foraminiferal fauna. The majority of the specimens are preserved as moulds, which allowed only generic classification. The following, mostly nodosariid forms, were identified Ichthyholaria, Lingulina, Lenticulina, Nodosaria, Glomospira, Pravoslavlevia, and Trochammina. These microfossils indicate a deeper-water environment, but they have no age-diagnostic value.
In a sample taken from a turbiditic bed-set in the lower part of this unit (124-128 m; S50) a 3-mm-large chloritic mica schist clast was observed. Higher up, in an interval (128-190 m), which is characterized by the predominance of the coarser and finer-grained redeposited carbonates, a small amount of mica-schist fragments, small serpentinite (?) clasts, chlorite, and biotite grains were found.
The following radiolarian taxa were identified from the samples T29 and BR3: Praewilliriedellum robustum, which indicates UA Zones 5-7 (late Bajocian to early Callovian). Both samples contain Praewilliriedellum convexum, which is a very common species in entire Middle and Late Jurassic and Archaeodictyomitra whalenae, a species that has been known so far from the early Aalenian to early Oxfordian. Beside them, in the sample T29 Archeodictyomitra prisca (early Aalenian to early Oxfordian), Eucyrtidiellum (?) quinatum (early Aalenian to Bathonian) and Parahsuum carpathicum are also present. Striatojaponocapsa conexa, Transhsuum maxwelli, and Zhamoidellum cf. ventricosum were extracted from sample BR3. This poorly preserved and lowdiversity radiolarian fauna (Fig. 12) suggests late Bajocian to Bathonian age. The Upper Triassic foraminifers found in a limestone interlayer suggest a continuation of redeposition of fine lithoclasts from Triassic limestones.

Interpretation of the history and controlling factors of sediment deposition
The studied succession is made up of an alternation of gravity-induced deposits (mostly turbidites) and hemipelagic/  Based on biostratigraphic constraints, the age of Unit 1 is latest Carnian to Rhaetian; taking into account the aspect of the interpretation of the depositional history of the succession, it is most probably Late Norian. The basal redeposited carbonate bed of this unit contains mixed shallow-marine (reefal) and deep-marine fossils. The toe-of-slope deposits grade upward into basinal carbonates.
The basinal carbonates are overlain by basinal finegrained siliciclastics (Unit 2). This striking change in the lithology reflects enhanced terrigenous input, which was probably the result of a significant climate change (increased humidity). Although no age-diagnostic fossils were found in this unit, a Norian-Rhaetian age-assignment of the overlying Unit 3 suggests that it might be connected with the early Rhaetian Kössen Event (e.g., Berra et al. 2010). Siliciclasts of the sandstone beds were derived predominantly from low-to medium-grade metamorphic rocks. Consequently, Hercynian (or perhaps the pre-Hercynian) ranges may have been the provenance.
Gravity-induced carbonate deposits, akin to those found in the basal part of the section, resume above the siliciclastic unit (Unit 3). Based on the foraminiferal fauna, these beds are still Late Triassic, most probably late Rhaetian in age. The appearance of the toe-of-slope carbonate deposits above the basinal sandstones, shales, and marls suggest decreasing humidity and/or platform progradation.
The overlying cherty limestone (Unit 4), which is rich in radiolarians and sponge spicules, was formed in a relatively deep basin. Following the sea-level lowstand in the latest Triassic, the earliest Jurassic is characterized by rising sea level (e.g., Hallam and Wignall 1999;Hallam 2001;Hesselbo et al. 2004). Accordingly, although no age-diagnostic fossils were encountered here, this striking sea-level rise probably happened in the earliest Jurassic (Hettangian).
In the next interval (Unit 5), which can be assigned to the late Sinemurian-early Pliensbachian, the silty, argillaceous, and siliceous basin facies are dominant, punctuated by thin carbonate intercalations containing redeposited shallow-marine fossil elements. The composition of the scarce siliciclastic material is similar to that in the deeper part of the section. Although in the Early Jurassic sedimentation took place in a relatively deep basin, the intercalations of gravity-induced, fine-grained carbonate deposits indicate the survival of shallow-marine carbonate factories in the neighborhood of the basin.
The next part of the succession (Unit 6) is made up predominantly of carbonates; basin and toe-of-slope facies alternate. Based on the foraminiferal fauna, it is assigned to the Bajocian-Bathonian. Compared to the previous one, the quantity, size, and composition of the siliciclastic material do not change in this interval, indicating relative continuity of the depositional system. However, the predominance of the carbonate lithology and the higher proportion of the redeposited beds suggest a sea-level highstand and related platform progradation.
In the higher part of the succession (Unit 7), carbonate lithoclasts of shallow-marine origin were observed in the redeposited carbonate beds, along with individual ooids, peloids, and bioclasts of shallow-marine biota (Middle Jurassic in age). Some of these sand-size clasts contain Upper Triassic and Lower Jurassic fossils. An actively producing carbonate factory must have been the source of the redeposited individual shallow-marine carbonate grains. The carbonate lithoclasts were derived from the erosion of Upper Triassic and Lower Jurassic rocks. In the uppermost carbonate gravity-flow beds, co-occurring mm-sized fragments of medium-grade metamorphic rocks and lithic components of an ophiolite complex were found, suggesting a remarkable change in the provenance.
Red siliceous shale and radiolarite occur in the topmost part of the measured section (Unit 8) and similar rock types continue upward along the valley. Based on lithological and microfacies characteristics, and considering the result of age determination (Late Bajocian to Early Bathonian), these rocks can be assigned to the Zlatar Formation, amended by Gawlick et al. (2017), referring to previous work of Djerić et al. (2007Djerić et al. ( , 2010. Gawlick et al. (2017) noted that the original underlying rocks of this formation were not known in its type area in the DOB. In the Trijebinska Reka section, the underlying succession is exposed and the transition between redeposited toe-of-slope facies and the radiolarian-rich eupelagic basin facies is also visible.

Comparison with age-equivalent successions
Age-equivalent successions are known in the Krš Gradac area in the neighborhood (see Fig. 1c) of the studied section.
They are overthrusted by the ophiolitic mélange (Gawlick et al. 2017), i.e., they have a structural position akin to that of the Trijebinska Reka section but they show a strikingly different development (see Gawlick et al. 2009Gawlick et al. , 2017.  We must note that Upper Triassic (Carnian to Rhaetian) grey, thin-bedded cherty limestones with marl interlayers commonly occur as blocks in the ophiolitic mélange in other areas of the DOB. They typically exhibit radiolarian wackestone/packstone texture with scarce fragments of thin-shelled bivalves. Very fine grained turbiditic interbeds with shallow-marine debris also occur, but rarely. These successions representing predominantly hemipelagic basin facies were assigned to the amended Upper Triassic Grivska Formation by Gawlick et al. (2017) and Sudar and Gawlick (2018).
South of the DOB, in the Lim Subunit of the East Bosnian-Durmitor Unit (or East Bosnian-Durmitor Megaunit after Gawlick et al. 2017;see Fig. 1b), Lower and Middle Jurassic cherty limestones of basin facies were reported ). In the Pre-Karst Unit and in the Bosnian Zone, Hercegovina and Montenegro, a thick succession (Vranduk Group) of alternating graded calcarenites (mostly oolites) and argillaceous micritic limestones and shales with radiolarite intercalations is known. It was formed during the Late Triassic (?) through the Jurassic to the earliest Cretaceous (e.g., Pamić et al. 1998;Dragičević and Velić 2002;Haas et al. 2011).
From the aspects of reconstruction of the paleogeographic setting and depositional conditions of the studied section, the age-equivalent sections of the Slovenian Basin are particularly important because, along with biostratigraphically well-constrained age-assignments, a number of detailed sedimentological studies were reported from that area (e.g., Rožič et al. 2009Rožič et al. , 2013aKolar-Jurkovšek 2011;Gale et al. 2012Gale et al. , 2013Gale et al. , 2014. This deep basin came into existence between the Adriatic-Dinaridic Carbonate platform (ADCP) and the Julian Carbonate Platform (JCP) in the early Carnian and continued until the Early Cretaceous (Buser 1989;Vrabec et al. 2009). The drowning of the JCP took place in the late Pliensbachian and then it was transformed into a submarine high (Rožič et al. 2017(Rožič et al. , 2018. Since the euphotic conditions did not change significantly on the ADCP, from that time this platform may have been the only source of the redeposited shallow-marine carbonate grains. Accordingly, the Bajocian-Bathonian (?Callovian) limestone breccia (debrite) and graded oolitic, bioclastic limestone successions (Tolmin Formation) of toe-of-slope facies reported from the Slovenian Basin (Rožič and Popit 2006;Rožič et al. 2018) were derived from the ADCP. Similar Middle Jurassic redeposited lithoclastic and oolitic, bioclastic toe-of-slope facies were also described from the Croatian segment of the ADCP foreland (Dragičević and Velić 2002;Bucković et al. 2004).

Paleogeographic setting of the studied section
During the initial stages of the Alpine plate-tectonic cycle, the areas of the South Alpine-Outer Dinaridic-Outer Hellenidic ranges belonged to the Tethyan margin of the North African part of Gondwana, which was broken off from here, later forming the Adria microplate (e.g., Csontos and Vörös 2004;Berra and Angiolini 2014). The westward propagation of the Vardar branch of the Neotethys Ocean reached this domain in the Middle Triassic and led to the disintegration of the previously existing large carbonate ramps; smaller isolated carbonate platforms and interplatform basins were formed on the passive margin (e.g., Haas et al. 1995). As a result of the intense terrigenous influx, some of these basins were filled up and occupied by the extending platforms. However, renewal of the extensional tectonic movements in the early Carnian led to the development of a large basin system, which separated the huge ADCP from a series of smaller to larger isolated platforms (Fig. 13). Among them, the Upper Triassic deposits of the JCP are well preserved and excellently exposed. The JCP is separated from the ADCP by the Slovenian Basin. Records of similar Late Triassic platforms are known in the Sana-Una and Jadar Units from the Vardar Zone and the Drina-Ivanjica Unit in the Inner Dinarides, and most probably also in the Bükk Unit, North Hungary, that reached its present-day position as the result of large-scale Cenozoic displacements (e.g., Csontos andVörös 2004, Kovács andHaas 2010). On the basis of this paleogeographic model, the block containing the Krš Gradac section could have originated from one of these platforms. The data on the foreslope deposits made possible the reconstruction of the ADCP slope toward the interplatform basin-system (Bosnian Basin), but only sporadic records on the internal basin succession are available. The section in the Trijebinska Reka valley representing a significant stratigraphic range is one of them, and that is why the inferences of its study are of particular importance.

Depositional model and provenance analysis
Since the carbonate platforms located along the oceanward belt of the passive margin (see Figs. 13,14) were drowned near the Triassic/Jurassic boundary and in the Early Jurassic, it is highly probable that the ADCP was the source of the platform-derived carbonate grains in the Middle Jurassic beds of the studied section, at least prior to the onset of  The relationship of carbonate platform evolution and terrigenous influx has been the subject of detailed investigations in the Southern Alps (Breda et al. 2009;Breda and Preto 2011;Dal Corso et al. 2015). In this region, the enhanced siliciclastic influx, as a result of the Carnian Pluvial Episode, led to drowning of most of the previously existing carbonate  platforms and the filling of the interplatform basins with redeposited shallow-marine carbonates and terrigenous siliciclastic sediments. In the late Carnian lowstand period, a terrestrial to shallow-marine mixed siliciclastic-carbonate succession was formed under semi-arid conditions (Travenanses Formation). According to the paleoenvironmental interpretations there is a lateral transition and interfingering between the alluvial plain, flood basin, and the lagoonalperitidal internal platform facies of the Dolomia Principale (Breda and Preto 2011). The drainage basin of the small ephemeral streams was southward, i.e., towards the internal part of the Adriatic microplate. Carnian bauxites were reported from the Outer Dinarides, which are covered by an upper Carnian carbonate-siliciclastic succession that is overlain the Dolomia Principale (Celarc 2008;Dozet and Buser 2009).According to the Dolomia Principale facies model of Caggiati et al. (2018), there is a near-continent siliciclastic mudflat behind the internal platform lagoon that is separated by the shelf crest from the gently sloping external platform progressing into the steeper foreslope. Outerplatform carbonate sands, together with slope material, were resedimented via turbidity currents and deposited on the slope apron. Fine carbonates together with minor siliciclastics derived from the mudflats were mostly distributed in the periplatform basin from suspensions of hypopycnal and mesopycnal flows. According to Caggiati et al. (2018) the overall depositional system of the Permian Guadalupian carbonate platform is remarkably similar to that of the Dolomia Principale/Dachstein platform. We basically agree with this statement; the comprehensive summary on the evolution of the Guadalupian platform by Kerans et al. (2013) demonstrated the modes and the controlling factors of bypassing of siliciclastic sediments through the carbonate platform to the slope and shedding into the basin. On the basis of the Guadalupian model, assuming channelized transport, the influx of a significant amount of siliciclastic sediment can also be explained. Taking into account the chronostratigraphic constraints, the deposition of the siliciclastic basin facies of the studied section (Unit 2) can be bound to the Rhaetian humid episode (Kössen Event).
The active margin evolution of the Neotethys Ocean began during the Middle Jurassic, probably in the Bajocian (Gawlick et al. 2017). This is manifested in the disruption of the external belts of the shelf and the development of a westward-propagating nappe stack and the obduction of the ophiolite nappes during the late Middle to Late Jurassic (Schmid et al. 2008;Gawlick et al. 2017). This significant change in the geodynamic setting of the region must be taken into account for the provenance analysis of the Bajocian-Bathonian redeposited sediments. Two options emerged for the interpretation of the results of our observations. According to the first one, the redeposited individual carbonate grains might have originated from those shallow-marine environments, which may have developed above the nappe stack (Fig. 14). The fragments of the Upper Triassic-Lower Jurassic carbonate rocks and the medium-grade metamorphic rocks were derived from the frontal part of the nappe stack, and the ophiolitic components from the overthrusting ophiolite nappes. These lithoclasts were transported first onto the shallow margin of the basin and then redeposited via gravity-driven flows into the deep internal basin. According to the second option, the geodynamic changes did not significantly influence the depositional processes and did not cause a fundamental change in the provenance of the redeposited grains. This means that the ADCP remained the source of the individual carbonate grains. Thus, the Upper Triassic-Lower Jurassic carbonate lithoclasts were derived from the high-angle erosional slope of the ADCP, and both the medium-grade metamorphic and the ophiolitic Fig. 13 Paleogeographic setting of the study area during the Late Triassic. a Position of the western Neotethys region. b Position of the study area (white star) within the western Neotethys region (the map is compiled after Dercourt et al. 1993;Haas et al. 1995Haas et al. , 2009Szulz 2000;Schmid et al. 2008;Berra and Angiolini 2014).

Conclusions
The results of our biostratigraphic studies suggest that along the eastern side of the Trijebinska Reka valley, an approximately 230-m-thick Upper Triassic to Middle Jurassic succession is exposed. It is made up mostly of carbonate rocks, with intercalation of shale and fine siliciclastic sandstone beds representing toe-of-slope and pelagic basin facies. The fine-grained debris flow/grain flow and turbidity current deposits of the toe-of slope facies consist predominantly of carbonate grains (mostly bioclasts) derived from ambient carbonate platform/ramp environments. This means that during the long Late Triassic to Middle Jurassic time range of sediment deposition, active shallow-marine carbonate factories must have existed in the neighborhood of the depositional basin. During the Late Triassic to Early Jurassic period, various amounts of fine siliciclasts, derived predominantly from low-to medium-grade metamorphic rocks, were transported into the basin, leading to the deposition of sandstone and shale bed-sets. A small amount of terrigenous siliciclasts are usually present also in the carbonate debrite/turbidite bedsets. In the redeposited beds in the upper part of the Middle Jurassic succession, the co-occurrence of shallow-marine bioclasts, medium-grade metamorphic rocks, and lithic components of an ophiolite complex were encountered, suggesting multiple episodes of redeposition of components derived from various sources.
Evaluation of the paleogeographic reconstructions and the inferences of sedimentological studies performed in the Slovenian Basin and the age-equivalent sections along the foreslope ADCP led to the conclusion that the section in the Trijebinska Reka valley was probably located in the internal part of the Bosnian Basin. Our studies provide data on the depositional history of this basin and the provenance of the redeposited components.
Since the carbonate platforms, located along the oceanward belt of the passive margin, were drowned by the Early Jurassic, the ADCP should have been the source of the platform-derived carbonate grains in the Middle Jurassic beds of the studied section, at least prior to the onset of the active-margin stage. During the passive-margin evolutionary stage, from the Middle Triassic to the earlier part of the Middle Jurassic, only the Adriatic microplate should have been the source of the siliciclasts. Outer platform carbonate sands, containing generally only minor amounts of terrigenous siliciclasts, were subjected to resedimentation by turbidity currents. However, during the humid episodes a large amount of terrigenous material may have arrived into the deep basins via channelized transport. The chronostratigraphic constraints suggest that deposition of the siliciclastic basin facies found in the lower part of the studied section can be connected to the Rhaetian humid episode.
The active margin evolution of the Neotethys Ocean began during the Middle Jurassic and led to the disruption of the external belts of the shelf, the development of a westward-propagating nappe stack and the obduction of the ophiolite nappes. This significant change in the geodynamic setting of the region must be taken into consideration for the provenance analysis of the Bajocian-Bathonian redeposited sediments.
A significant lithofacies change was recorded in the uppermost part of the studied section, where the predominantly redeposited toe-of-slope facies progresses upward into a radiolarian-rich eupelagic basin facies. This change of facies probably occurred during the Early Bathonian.
The studied section records an approximately 50 Ma-long chapter from the history of the western Neotethys margin. Considering the paleogeographic reconstructions and the analogies of age-equivalent sections, this slice may represent the development of the internal part of the Bosnian Basin, which was located between the ADCP and the Drina-Ivanjica Unit. In the DOB, and within it also in the neighborhood of the studied sections, other slices representing a similar age range but showing a strikingly different development, are known. Further systematic and detailed studies of these slices are required for the proper fitting of the jigsaw puzzle that may lead to the correct reconstruction of the paleogeographic setting and better understanding of the complex geodynamic history of this segment of the Neotethys Ocean.