2023 | 76/3 | 147–156 | 5 Figs. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society 1. INTRODUCTION The Lower Cretaceous sedimentary successions in the area around Belgrade are crucial to understanding the late Mesozoic geodynamic history of the Dinarides, because of their position in the proximity of the plate boundary between the Adriatic (Dinar- ides) and the Moesian plates (Fig. 1a, b). The complex geological setting of the study area is interpreted as a mosaic of continental units (Adriatic or European affinity; SCHMID et al., 2008, 2020 and references therein), which are separated by the so-called Sava suture zone (SCHMID et al., 2020 and references therein), and remnants of domains with oceanic lithosphere (West Vardar and East Vardar ophiolites (sensu SCHMID et al., 2008, 2020; Fig. 1a; Neo-Tethys ophiolites sensu GAWLICK et al., 2009). Previ- ously, there has been no consensus as to which tectonic unit the Lower Cretaceous sedimentary rocks (Paraflysch sequence sensu DIMITRIJEVIĆ & DIMITRIJEVIĆ (1976) belong: the main Vardar Zone (MVB/Z; KARAMATA, 2006; Fig. 1b), the Sava Zone (SCHMID et al., 2008; Fig. 1b), or the Inner Dinarides (Kopaonik ridge and block unit =KBR/U =; Fig. 1c), or to a se- quence with European affinity thrust over the wider Adria plate (TOLJIĆ et al., 2018). This controversy is an ongoing discussion (e.g., TOLJIĆ et al., 2018; BRAGIN et al., 2019; SCHMID et al., 2020). TOLJIĆ et al. (2018) in the latest paper attributed the Para- flysch sequence to be deposited on the outer passive margin of the Moesian plate (Carpatho-Balkanides), and in the oceanic ba- sin between the wider Adria plate to the west (Dinarides) and the Moesian plate (Europe) to the east. TOLJIĆ et al. (2018) interpreted the entire Cretaceous to Pala- eogene sedimentary evolution in the Belgrade area as a fore-arc basin infill, which should have been palaeogeographically situ- Middle Aptian Orbitolinid limestones in Belgrade (Serbia): microfacies and depositional environment Bojana Đorđević 1,*, Hans-Jürgen Gawlick2, Nevenka Djerić1, Felix Schlagintweit3 and Miloš Radonjić1 1 University of Belgrade, Faculty of Mining and Geology, Đušina 7, Beograd, Serbia; (*corresponding author: bojana.dzinic@rgf.bg.ac.rs) 2 Montanuniversität Leoben, Franz Josef-Straße 18, 8700 Leoben, Austria 3 Lerchenauerstr. 167, 80935 Munich, Germany doi: 10.4154/gc.2023.09 Abstract Lower Cretaceous (Aptian) shallow-marine limestones with intercalated polymictic conglomera- tes were investigated with respect to their biostratigraphic age and their microfacies. They are the younger part of the generally carbonate-siliciclastic Lower Cretaceous deep-water (max. few hundred metres) turbiditic sequences (“Paraflysch”) of the so-called East Vardar zone in the Bel- grade area. The biostratigraphic age of the limestones was determined by orbitolinid foramin- ifera: the co-occurrence of Dictyoconus? pachymarginalis SCHROEDER and Mesorbitolina texana (ROEMER) besides various other microfossils suggest a biostratigraphic age of this shal- low-marine limestone succession as middle Aptian (Gargasian). Radiolarite components in the conglomerates are Triassic in age and were derived from the obducted Middle Triassic to Middle Jurassic Neo-Tethys ophiolites and/or their ophiolitic mélanges on the wider Adria plate. From both the first precise biostratigraphic age dating as middle Aptian combined with microfacies analysis of these shallow-marine limestones and the component spectrum in the intercalated conglomerates, it can be concluded that the Lower Cretaceous turbiditic “Paraflysch” succes- sion was deposited on the eastern rim of the Dinarides. The results will allow a better compari- son of the different Lower Cretaceous sedimentary successions deposited on the eastern mar- gin of the Dinarides. ated on the Moesian plate margin (Supragetic nappes according to SCHMID et al., 2008). During the assumed Campanian–Early Palaeogene collision between Moesia and the Dinarides, this fore-arc basin was thrust onto the Adria plate and should mark the suture zone. In the Early Cretaceous “Paraflysch” succession, the shallow-marine Early Cretaceous limestones with conglom- erate intercalations locally should evidence a sea-level lowstand (TOLJIĆ et al., 2018). These shallow-marine limestones contain a rich orbitolinid foraminifera fauna that has not previously been studied. The exact age of these shallow-water limestones is not known, and associated rocks, i.e., intercalated conglomerates with fluvial transported components from a hinterland, are not studied and their hinterland should be according to TOLJIĆ et al. (2018) the Moesian plate. However, due to the occurrence of ra- diolarite and ophiolite components in these conglomerates asso- ciated with the shallow-marine Early Cretaceous orbitolinid- bearing limestones, we disagree with the palaeogeographical interpretation of TOLJIĆ et al. (2018). Cretaceous sedimentary rocks deposited in the wider Bel- grade area are subdivided into the Central and East Belgrade fa- cies, i.e. into different “sub-basins”. The Early Cretaceous “Para- flysch” sensu DIMITRIJEVIĆ (1997) is an overstep sequence above ophiolites/ophiolitic mélange, mainly preserved in the Cen- tral Belgrade facies. In contrast, the East Belgrade facies is in- completely exposed and characterized by late Lower Cretaceous shallow-water limestones which pass into the Urgonian-type ree- fal sedimentary rocks, both interpreted as deposited in a fore-arc basin on the Moesian margin (TOLJIĆ et al., 2018). However, in the Late Cretaceous, rudist-bearing shallow-marine limestones were formed throughout the Adriatic plate (SLADIĆ- Article history: Manuscript received March 15, 2021 Revised manuscript accepted September 04, 2023 Available online October 16, 2023 Keywords: Orbitolinidae, Microfacies, Early Cretaceous, Dinarides G eo lo gi a C ro at ic a Geologia Croatica 76/3148 TRIFUNOVIĆ, 1998), as well as in the wider Belgrade area. They represent the beginning of a new sedimentary cycle, start- ing in the early Late Cretaceous, after the “Mid-Cretaceous” tec- tonic motions, which resulted in the eastern Mediterranean area in a new plate configuration (e.g. CSONTOS & VÖRÖS, 2004). After a long period of exposure and continental weathering of huge areas of the Inner Dinarides after the Tithonian uplift and unroofing (GAWLICK et al., 2020 and references therein), includ- ing the so-called East- and West-Vardar ophiolites (compare SCHMID et al., 2008, 2020), the whole area was flooded and a widespread shallow-water reefal evolution was established with a very limited palaeogeographic meaning. In contrast, BRAGIN et al. (2019) used the findings of Late Jurassic radiolarians to suggest that the Central and East Belgrade facies sensu TOLJIĆ et al. (2018) have an Adriatic affinity. In fact, the recent controversial discussion clearly evidenced that there is Figure 1. a) The tectonic setting of the Adria – Europe collision zone in central Serbia (modified after SCHMID et al., 2020). b) Overview of the terrains/composite units of central Serbia (modified after KARAMATA, 2006). Note that the geographical position of the map is approximately similar to Fig. 1a. c) Geological sketch map of the central area of Belgrade. The qhite circle marks the position of the studied section at the Košutnjak railway station (see Fig. 2). Modified after MARKOVIĆ et al., 1984. G eologia C roatica Đorđević et al.: Middle Aptian Orbitolinid limestones in Belgrade (Serbia): microfacies and depositional environment 149 a great need for additional data from the Early Cretaceous sedi- mentary rocks to answer the still open questions in this area. This issue is crucial geodynamic reconstruction of the Cretaceous and the evolution of the Vardar zone between Moesia and Adria and the Early Cretaceous evolution of the Inner Dinarides, a conti- nental area with erosion during that time span. The Early Creta- ceous erosional products of the Inner Dinarides are well studied in the partially underfilled foreland basins to the west (e.g. MIKES et al., 2008), but practically nothing has been studied in their eastern part, i.e. the “Paraflysch” sequences according to DIMITRIJEVIĆ & DIMITRIJEVIĆ (1976). The sedimentological evolution, i.e. biostratigraphic age dat- ing, microfacies analysis and component analysis of the interca- lated turbidites and mass transport deposits of the Early Creta- ceous sedimentary rocks in the whole area is only roughly constrained (TOLJIĆ et al., 2018 and references therein). Micro- facies analysis of carbonate rocks and component analysis of breccias/conglomerates/turbidites is completely missing. There- fore, there is a need for detailed sedimentological studies and de- tailed biostratigraphic age dating for an exact correlation of the different Cretaceous successions to unravel the depositional re- gime and palaeogeographic position of the “Paraflysch” se- quence. Only on the basis of a precise age and a provenance anal- ysis of the components in the Early Cretaceous succession can a palaeogeographic reconstruction of their depositional area be possible, i.e. the eastern Dinarides, Europe, or an estimated oce- anic domain between Adria and Moesia (Europe). The aim of this study is to present new biostratigraphic age and microfacies data of these Early Cretaceous (Aptian) shallow- marine limestones and to describe some key components (radio- larites) of the associated fluviatile conglomerates. The presented data will allow a better comparison to be made with similar sed- imentary sequences in the wider surroundings, which should re- sult in a better understanding of the geology and evolution of the plate boundary between the Dinarides and Moesia. 2. GEOLOGICAL SETTING In the Belgrade area, the Lower Cretaceous sedimentary rocks, deposited on top of the Upper Jurassic ophiolitic mélange (TOLJIĆ et al., 2018 and references therein; compare BRAGIN et al., 2019) are represented by two distinct facies: 1) sedimentary rocks composed of sandstones, siltstones, marlstones, sandy limestones, and limestones; 2) shallow-water reef limestones and siliciclastics (ANĐELKOVIĆ, 1973; PAVLOVIĆ et al., 1979; FILIPOVIĆ et al., 1979; MARKOVIĆ et al., 1985) (Fig. 1c). These Valanginian to Aptian sedimentary successions of central Serbia are termed “Paraf lysch” by DIMITRIJEVIĆ & DIMITRIJEVIĆ (1976, 1987) with respect to their sedimento- logical features. Similar deposits of comparable age range but a different geotectonic position related to the vergence of the thrust belts are described from the Alps, Dinarides, Albanides and Hel- lenides (e.g., the Schrambach and Rossfeld Formations - MIS- SONI & GAWLICK, 2011a; KRISCHE et al., 2014; Bohinj For- mation – KUKOČ et al., 2012; Vranduk Formation - BLANCHET et al., 1970; MIKES et al., 2008; Vermoshi Flysch - MEÇO & ALIAJ, 2000; MARRONI et al., 2009; Firza Formation – GAR- DIN et al., 1996; Kurbnesh Formation – SCHLAGINTWEIT et al., 2008; Boeotian flysch – NIRTA et al., 2015). In contrast to the “Paraflysch”, these sedimentary successions were deposited west of the obducted ophiolites in Early Cretaceous underfilled foreland basins. Only in northern Greece in a similar palaeogeo- graphic setting to the “Paraflysch” was a practically identical ear- liest Early Cretaceous (Berriasian–Valanginian) sedimentary succession deposited on top of obducted ophiolites/ophiolitic mé- lange (“East Vardar ophiolites” and equivalents) (KOSTAKI et al., 2013 and references therein). However, from all these Lower Cretaceous (Berriasian to Aptian) successions with reworked ma- terial from the wider Adria plate the overlying Upper Barremian, Aptian (and younger) shallow-water deposits with orbitolinid fo- raminifera are practically not described, because they are mostly eroded. Exceptions are only known from the Northern Calcare- ous Alps (SCHLAGINTWEIT et al., 2012b and references therein) or the Albanides (ROBERTSON et al., 2012; SCHLAGINTWEIT et al., 2012a and references therein). In Ser- bia, the occurrence of “Paleodictyoconus arabicus” from the Var- dar zone in the Kopaonik area was reported by ZELIĆ et al. (2010, fig. 5c) without sedimentological or microfacies studies. To fill this gap in knowledge the orbitolinid-bearing shallow-wa- ter limestones from the east Vardar zone are described for the first time. The shallow-marine Barremian–Aptian limestones in the surroundings of Belgrade are attributed to “Urgonian limestones” (e.g., ANĐELKOVIĆ, 1973; DIMITRIJEVIĆ, 1997). In certain places, these sedimentary rocks overlie older rocks in the se- quence or should occur as lenses within the turbiditic sequences (ANĐELKOVIĆ, 1954, 1956, 1973). According to ANĐELKOVIĆ (1973) typical Urgonian carbonates consists of grey reef-type limestones, sandy-marly limestones and siliciclastics rich in a shallow-water fauna (caprinids, orbitolinids, corals, brachiopods, gastropods). 3. METHODS The studied section (Fig. 2) is located in Belgrade, at the Košutnjak railway station (N44 4̊5’26.44 ;ˮ E20˚26’43.77 ;ˮ Fig. 1c). Nine samples were collected from a six metre thick limestone section overlying mainly fine-grained siliciclastic rocks. From these samples, twenty thin-sections were prepared for microfa- cies analysis and biostratigraphic age determination. Twenty, mainly rounded to well-rounded radiolarite pebbles from inter- calated conglomerates were processed with hydrofluoric acid (3%) but contain only undeterminable radiolarian faunas. During the field work orbitolinids and gastropods were detected. 4. RESULTS ANĐELKOVIĆ (1973), first studied this section, and subdivided the Košutnjak carbonate succession into three levels with requie- nids, deposited above the fine- to coarse-grained siliciclastic rocks. Based on palaeontological data (Requienia ammonia GOLDFUSS, Toucasia carinata MATHERON and Orbitolina conoidea discoidea GRAS), ANĐELKOVIĆ (1973) he assigned them an Upper Barremian–Aptian age. The six-metre thick succession studied in detail consists of decimetre to 0.5 metre thick-bedded greyish orbitolinid-bearing shallow-water limestone (Figs. 2A, 2B). These orbitolinid-bear- ing beds consist mainly of bioclastic to thick bedded limestones (wackestones to packstones and grainstones). In the lower part of the shallow-water limestone section polymictic carbonate con- glomerates with exotic components (volcanic clasts, radiolarites) are intercalated. Besides the orbitolinids, smaller benthic fo- raminifera, gastropods and bivalves are distributed throughout the succession. Calcareous green algae are rare and appear in some layers. G eo lo gi a C ro at ic a Geologia Croatica 76/3150 4.1. Microfacies analysis Three main microfacies types (MFT) are distinguished within the shallow-marine limestones of the studied succession (Figs. 2A, 2B). MFT-1: bioclastic wackestone with orbitolinids (Dictyoco- nus? pachymarginalis SCHROEDER, Mesorbitolina texana (ROEMER)) (Figs. 3A–C). Besides the age diagnostic orbitolinid foraminifera, other benthic foraminifera are represented by mil- iolids and textulariids, rare algal remains, gastropods, encrusted stromatoporoids (bacinellid facies – Fig. 3A), and bivalves. Litho- clasts (exotic clasts/radiolarite components) are subangular to well-rounded, vary in size and sorting. According to FLÜGEL (2004) and SUDAR et al. (2008) these kinds of sediments were deposited in a shallow subtidal to intertidal environments. The MFT-1 is the most common in the lower part of the section (Figs. 2A, B). MFT-2: bioclastic wackestone to packstone with abundant orbitolinids (Figs. 3D–G). The MFT-2 is the most common in the middle and upper part of the succession (MFT-2) (Figs. 2A, B). Dictyoconus? pachymarginalis SCHROEDER, Mesorbitolina texana (ROEMER), Paleodictyoconus actinostoma ARNAUD- VANNEAU & SCHROEDER and Daxia minima LAUG & PEYBERNÈS are the age diagnostic benthic foraminifera. Be- sides the orbitolinids, other skeletal grains, small benthic fo- raminifera such as miliolids and textulariids, gastropods and bi- valve’s shells occur. In some thin-sections, ooids (Fig. 3E) and subangular peloidal grainstone intraclasts are present. In sample BDZ 7, together with the orbitolinids, indeterminable lituolinid large foraminifera with a complex inner structure appear. Bio- clastic wacke- and packstones with abundant larger foraminifera (e.g. orbitolinids) are common microfacies types in inner ramp environments. The presence of imperforate foraminifera such as miliolids and agglutinated orbitolinids indicate relatively low wa- ter energy circulation with deposition of abundant carbonate mud in a lagoon (SUDAR et al., 2008; FLÜGEL, 2004). MFT-2 cor- responds to the facies of an inner middle lagoon (e.g., Fig. 9L from MOOSAVIZADEH et al. (2020); Fig. 10 (C, D and E) from Figure 2. (A). The studied section at the Košutnjak railway station. Blue lines mark the intervals of the interpreted carbonate microfacies (MF1-3, SC – siliciclastic sequence). Red lines mark the fault traces and their relative movement. White circles indicate sample positions (see Fig. 3). Photo taken in May 2019. (B). Geologi- cal column and summary of the microfacies types. (C) Biostratigraphic column of the main microfossils from Košutnjak railway station. G eologia C roatica Đorđević et al.: Middle Aptian Orbitolinid limestones in Belgrade (Serbia): microfacies and depositional environment 151 RAHIMINEJAD & HASSANI (2015)). The MFT-2 is overlain by wackestones to packstones with a significant amount of fine- grained siliciclastics (Figs. 3F, G). MFT-3: bioclastic grainstone with large and small unsorted intraclasts, bioclasts (gastropods, bivalves, benthic foraminifera, algae, and other broken skeletal grains) (Fig. 3H) beside aggre- gate grains, intraclasts, small ooids, and skeletal grains. Aggre- gate grains have low degrees of roundness. Small intraclasts are subrounded and rounded and show different sphericity values. Large intraclasts have low roundness and low sphericity values. Sediment sorting is poor. The variations in the roundness and sphericity of grains, the wide range of grain size, as well as their Figure 3. Microfacies of the orbitolinid-bearing sedimentary rocks from the Early Cretaceous (Košutnjak railway station). A: Stromatoporoids encrusted by bacine- lid fabrics, the internal sediment is represented by wackestone with D. pachymarginalis, miliolids and textulariids. Sample BDZ 1. B: Bioclastic wackestone with D. pachymarginalis (p), miliolids and textulariids. Sample BDZ 1. C: Bioclastic wackestone/packstone with orbitolinids. Sample BDZ 2B. D-G: Bioclastic wackestone with Dictyoconus? pachymarginalis (p), Mesorbitolina texana (t) and other benthic foraminifera. Samples BDZ 3, BDZ 4, BDZ 6 and BDZ 8. H: Bioclastic grainstone with coated grains. Sample BDZ 9. G eo lo gi a C ro at ic a Geologia Croatica 76/3152 poor sorting indicate mixing and reworking of the grain popula- tions. Large intraclasts with fenestral fabric suggest a low-energy protected intertidal environment. Roundness and sphericity of intraclasts indicate transport within the depositional environ- ment. Poor sorting, mixing of resediments and the deposition of eroded grains together with finer grains point to deposition within tidal channels. The MFT-3 occurs on top of the studied succes- sion (Figs. 2A, B). In general, all three different microfacies types are charac- teristic of shallow-marine depositional realms with varying dep- ositional energies and hinterland influences. This is indicated by the different organisms including orbitolinid foraminifera, en- crusted stromatoporoids, calcareous algae, ooids beside other or- ganisms and skeletal grains. Open-marine organisms from deeper-water environments are missing. Orbitolinid foraminifera are common in shallow-water limestones (normal salinity and warm water), e.g. in the late Early Cretaceous limestones of the Adriatic Carbonate Platform (VELIĆ, 1988;, 2007 and references therein). The orbitolinid foraminifera are associated with miliol- ids, which showed spectacular expansion in the Middle Creta- ceous, proliferating in mid-latitudes (BOUDAGHER-FADEL, 2008). It is also interesting to note that conical forms of orbitoli- nids thrive in the shallowest water (SIMMONS et al., 2000). The microfacies changes over small-scales and short time frames to- gether with the change in the association of grain types is accord- ing to FLÜGEL (2004) common in platform interiors and in inner to mid-ramp depositional environments, partially influenced by storm-induced currents. These small-scale changes are well de- veloped and commonplace in Jurassic and Cretaceous peritidal limestones of the Adriatic carbonate platform (HUSINEC et al., 2000 and references therein). Coarsening and shallowing-up- wards cycles are the result of an increase in water energy which leads to the formation of grainstones composed of mixed and re- worked grains. The occurrence of abundant orbitolinid foraminif- era is quite common in inner ramp depositional environments. Conglomerates transported by fluvial systems from the hin- terland and intercalated in the shallow-marine orbitolinid lime- stones contain ophiolite and various radiolarite components (Figs. 4A–D). In these conglomeratic layers, most of the rounded to well-rounded radiolarite components of several millimetres to centimetre-size are too small for the preparation of radiolarian faunas. Still, their microfacies characteristics are well preserved. The microfacies of the radiolarite components resemble the mi- crofacies of ribbon radiolarites as known from the sedimentary cover of the Neo-Tethys Ocean floor or the distal continental slope (GAWLICK et al., 2016a, b; GAWLICK & MISSONI, 2015). However, the conglomerates overlying the orbitolinid-bearing limestones have an identical component spectrum, only differing in the larger size range of the clasts. Figure 4. Microfacies of different Triassic radiolarite components associated with the Orbitolina limestones. A: Overview of the reefal limestone with Mesorbitolina texana and a radiolarite component. Sample BDZ 2A. B: Rounded Late Anisian to Ladinian radiolarite with recrystallized radiolarians and filaments (compare GAW- LICK et al., 2016a). Sample BDZ 2B. C: Rounded Carnian ribbon radiolarite component with remnants of organic material and recrystallized and silicified radiolarians (compare GAWLICK et al., 2016b). Sample BDZ 2A. D: Rounded Norian ribbon radiolarite component. Sample BDZ 2A. G eologia C roatica Đorđević et al.: Middle Aptian Orbitolinid limestones in Belgrade (Serbia): microfacies and depositional environment 153 Analysis of the different rounded radiolarite pebbles from these overlying fluviatile conglomerates resulted in identification of very poorly preserved radiolarian faunas due to intense silici- fication, as typical for oceanic ribbon radiolarites. The radiolar- ians are strongly recrystallized and cannot be determined, not even to generic level, but they have a clear Triassic (Late Anisian - Ladinian and Late Triassic) radiolarian habitus (compare Fig. 4). However, despite the differences in microfacies of Triassic and Jurassic radiolarites, both are associated with either the Neo- Tethys Ocean floor or the distal parts of the eastern passive wider Adria margin, are well known and documented (GAWLICK et al., 2009; GAWLICK & MISSONI, 2015 and references therein). Therefore, the microfacies of radiolarites can be roughly used to constrain their age, i.e. Middle Triassic (Late Anisian–Ladinian), Carnian-Norian, Rhaetian or Middle Jurassic. 4.2. Biostratigraphy In the Tethyan realm, the Aptian stage is subdivided into three divisions: Bedoulian (early Aptian), Gargasian (middle Aptian) and Clansayesian (late Aptian) (GRADSTEIN et al., 2020). Some authors (e.g., SCHROEDER et al., 2010) subdivided the Aptian into two divisions (Bedoulian - Early Aptian, Gargasian with Clansayesian - Late Aptian). Figure 5. Microfossils from the Košutnjak railway station. A, B: Dictyoconus? pachymarginalis. Samples BDZ 1, BDZ 3. Axial section. C – G: Mesorbitolina texana. Sam- ples BDZ 3, BDZ 4, BDZ 8. C: axial section, D: tangential section, E–G: transverse section. H: Paleodictyonus actinostoma. Sample BDZ 5. Subaxial section. I: Daxia minima. Sample BDZ 5. G eo lo gi a C ro at ic a Geologia Croatica 76/3154 (e.g., OBRADOVIĆ & GORIČAN, 1988; DJERIĆ et al., 2007; GAWLICK et al., 2020 and references therein, for Dinarides; DE WEVER et al., 1979; MARCUCCI et al., 1994; CHIARI et al., 1996; GAWLICK et al., 2008; 2016a for Albania; OZSVÁRT et al., 2012, for Greece). Also, the overlying fine-grained siliciclas- tic rocks, carbonate sandstones and polymictic fluviatile con- glomerates consisting of exotic material were shed from the west/ southwest and deposited most probably in the late Aptian. These conglomerates consist of volcanic pebbles (most probably ophi- olite derived material) and various rounded radiolarite compo- nents. Determinable radiolarians from the radiolarite components could not be extracted, and a detailed component analysis espe- cially of the volcanic components is lacking. During the Early Cretaceous, large parts of the Dinarides underwent continental weathering and the erosional products were shed either to the west in the remaining foreland basins (e.g., Vranduk or Bosnian basin) or to the east, i.e. the passive continental margin of the re- maining eastern part of the Neo-Tethys Ocean (MISSONI & GAWLICK, 2011b). Triassic to Middle Jurassic ophiolites are only known from the wider Adria plate, i.e. the obducted ophi- olites and their ophiolitic mélanges. These ophiolites obducted in Middle to early Late Jurassic times (for discussion see GAW- LICK & MISSONI, 2019; SCHMID et al., 2020 and references therein), are missing on the Moesian superunit. The provenance area of the ophiolite and radiolarite components is therefore un- doubtedly the wider Adria plate, i.e., the Inner Dinarides. Depo- sition of this Aptian sedimentary succession on the Moesian mar- gin (TOLJIĆ et al., 2018) can therefore be excluded. 6. CONCLUSIONS On the basis of the new data from the Košutnjak railway station section in Belgrade, the following conclusions can be drawn: Deposition of the Early Cretaceous shallow-marine carbona- tes above the deeper-marine “Paraflsch” succession in the Bel- grade area started in the Aptian and not in the Barremian as for- merly estimated. The Gargasian age of the “Orbitolina”-limestones” in the Belgrade area provides the first most accurate biostrati- graphic age data from this carbonate sequence; Radiolarite components from the conglomerates are Triassic in age and derive from the obducted Middle Triassic to Middle Jurassic Neo-Tethys ophiolites and/or their ophiolitic mélanges on the wider Adria plate; The first precise biostratigraphic dating as Middle Aptian combined with microfacies analysis of these shallow-marine limestones and the component spectrum in the intercalated con- glomerates evidence that the Early Cretaceous turbiditic “Para- flysch” succession was deposited on the western shelf of the re- maining Neo-Tethys after Middle to Late Jurassic ophiolite obduction, i.e. on the eastern part of the Jurassic Dinaridic oro- gen. ACKNOWLEDGMENT This manuscript has been written in the framework of the IGCP- project 710 (Western Tethys meets Eastern Tethys). Bojana ĐORĐEVIĆ and Hans-Jürgen GAWLICK gratefully thank the “Central European Exchange Program for University Studies” (CEEPUS) for network mobilities (CEEPUS CIII-RO-0038). Bo- jana ĐORĐEVIĆ would like to thank Montanuniversität Leoben for providing the facilities for this research. The research was supported by the Ministry of Science, Technological Develop- ment and Innovation of the Republic of Serbia, Contract no. 451- 03-68/2022-14/ 200126. We would also like to thank Ioan BU- In the studied section, the Aptian foraminiferal association was analysed in twenty thin-sections yielding Dictyoconus? pa- chymarginalis (SCHROEDER), Mesorbitolina texana (ROE- MER), Paleodictyoconus actinostoma ARNAUD-VANNEAU & SCHROEDER, Daxia minima LAUG & PEYBERNÈS, and Nau- tiloculina broennimanni ARNAUD-VANNEAU & PEYBER- NÈS. Among these, the first two are of biostratigraphic relevance. Dictyoconus? pachymarginalis occurs in samples BDZ 1 and BDZ 3 (Figs. 5A, B). According to SCHROEDER (1964), this species is known from the lower (upper Bedoulian) to the middle Aptian (Gargasian) (Fig. 2C). The species has been reported from many localities of the Neotethyan realm and was originally de- scribed from the Alborz Mountains (SCHROEDER, 1964), and was also successively reported from Central Iran (YAZDI- MOGHADAM & AMIRI, 2010; ROOZBAHANI, 2011; SCHLAGINTWEIT et al., 2013; SCHLAGINTWEIT & WILM- SEN, 2014), from NW Iran (YAZDI-MOGHADAM et al., 2017), and northeast Iran (TAHERPOUR KHALIL ABAD et al., 2013; BUCUR et al., 2019). It is worth mentioning that the species does not appear on the Arabian Plate (Zagros Zone) (SCHROEDER et al., 2010). In Europe, D.? pachymarginalis is reported from NE Spain (MASSE et al., 1992), southern Hungary (SCHLAGINT- WEIT, 1990), and the southern Apennines of Italy (MAN- CINELLI & CHIOCCHINI, 2006). Mesorbitolina texana occurs in all the studied samples ex- cept BDZ 1 (Figs. 5C-G). According to SCHROEDER et al. (2010), M. texana had its first appearance datum (FAD) at the base of the late Gargasian. Compared with Dictyoconus? pachymar- ginalis and Mesorbitolina texana, Paleodictyonus actinostoma ARNAUD-VANNEAU & SCHROEDER (Fig. 5H) has a much wider range, i.e. from the uppermost Hauterivian to the Aptian (CLAVEL et al., 2014) (Fig. 2C). M. texana represents a cosmo- politan species reported from Texas in the West (DOUGLASS, 1960) towards the western Pacific realm, e.g., Japan (IBA et al., 2011). In the Dinaridic realm it has been reported from various localities, e.g., Croatia (HUSINEC et al., 2000). For the wide dis- tribution of mesorbitolinids in the Mediterranean realm see MOULLADE et al. (1985, fig. 2). The co-occurrence of Dictyoconus? pachymarginalis (SCHROEDER) and Mesorbitolina texana (ROEMER) is known from many localities in the Western Tethyan realm up to the Mid- dle East area (e.g., SCHLAGINTWEIT, 1990; MANCINELLI & CHIOCCHINI, 2006; SCHROEDER et al., 2010; SCHLAGINT- WEIT et al., 2013; SCHLAGINTWEIT & WILMSEN, 2014) and indicates an upper Gargasian (Middle Aptian) age for the orbito- linid-bearing beds of the studied section. 5. DISCUSSION In general, the short-lasting deposition of shallow-water “Orbito- lina” limestones above marine siliciclastic sedimentary rocks and below a series of fine grained siliciclastic rocks with intercalated polymictic conglomerates is most probably connected with the long-term falling sea-level during the Aptian (OGG et al., 2004). This would imply that the underlying marine siliciclastics were deposited during the lower Aptian. 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