AB STRA CT Radiolarian assemblages of Late Cretaceous age were studied in a carbonate-clastic section from the Cretaceous sedi- mentary cover that unconformably overlies Triassic sediments of the Jadar Block. According to the identifi ed radi- olarian associations, the studied limestone is of Santonian age. Considering the fact that these sediments belong to a broadly defi ned Turonian-Senonian geologic map unit, the obtained data are important for further more detailed bio- stratigraphic assignment of Late Cretaceous rocks in Western Serbia. Moreover, the obtained data are very important for interregional correlations. Keywords: Upper Cretaceous, Radiolaria, Jadar Block, Vardar Zone Western Belt, Western Serbia  Geologia Croatica 67/3 163–170 4 Fig. 1 Tab. 2 Pls. Zagreb 2014 Geologia CroaticaGeologia Croatica New data on the age of an Upper Cretaceous clastic-carbonate succession in Brežđe (Western Serbia)  Nevenka Đerić and Nataša Gerzina Faculty of Mining and Geology, University of Belgrade, Đušina 7, 11000 Beograd, Serbia; (nevenka.djeric@rgf.bg.ac.rs) doi: 10.4154/gc.2014.12 1. INTRODUCTION Brežđe village is situated in Western Serbia, at the foothills of the Maljen Mountain. The geological setting of the area is extremely complicated, considering the fact that this is a contact zone between the continental Jadar Block and the Western Vardar ophiolites (Figs. 1, 2). Both units are over- lain by transgressive Cretaceous sediments. In the wider studied area, Cretaceous sedimentation be- gins with the Albian Cenomanian transgressive sediments (FILIPOVIĆ et al., 1978). Terrigenous-carbonate and car- bonate sedimentation continued to the end of the Upper San- tonian (BRAGINA et al., 2014) or Campanian (GAJIĆ et al., 2011), while the overlying fl ysch sediments were deposited during the Campanian-Maastrichtian (FILIPOVIĆ et al., 1978). According to bivalve species (MARKOVIĆ & ANĐEL- KO VIĆ, 1953) and the identifi ed fossil foraminifers (FI LI- POVIĆ et al., 1978), the age of the studied sediments in the wider surroundings of Brežđe was determined as Senonian, without any further division. On the geologic map of Serbia (FILIPOVIĆ et al., 1977), these sediments are not even sepa- rated from Turonian sediments, but are together marked as a single unit of Turonian-Senonian age. During the last few years, however, radiolarian investigations have been focused on the Struganik locality in the vicinity of Brežđe village. These investigations enabled a more detailed biostratigraphic assignment of the rocks that belong to the Turonian-Senonian map unit. The lowermost part of the clastic-carbonate succes- sion was assigned an Early Senonian age (DJERIĆ et al., 2009). Further investigations enabled a more precise age de- termination (Early Santonian) of these sediments, while the radiolarian associations from the overlying beds indicate a Santonian age (BRAGINA et al., 2014). The data presented in this paper will enable comparison with similar rocks in the wider surroundings, which should be an important contribu- tion to better understanding of geology of Western Serbia. 2. GEOLOGICAL SETTING The studied locality is situated in Western Serbia, 17 km southeast of Valjevo and 7 km south of Mionica, along the Struganik-Brežđe road (GPS N44°11’30’’, E20°04’16.4’’) (Figs. 1, 2). The investigated area is characterized by extremely com- plex geology. On the geologic map of western and south- Geologia Croatica 67/3Geologia Croatica 164 western Serbia, there are two conspicuous, more or less par- allel, NW-SE oriented belts of ophiolitic mélange overlain by large ultramafic massifs. The southwestern belt is known as the Dinaridic Ophiolite Belt (PAMIĆ et al., 2002; KARA- MATA, 2006), the Central Dinaridic Ophiolite Belt (LU GO- VIĆ et al., 1991) or the Ophiolite Belt (DIMITRIJEVIĆ, 1997). The ophiolite belt in the northeast is referred to as the Vardar Zone Western Belt (KARAMATA, 2006), but also referred to under a variety of names such as the Inner Dinar- idic Ophiolite belt (LUGOVIĆ et al., 1991), the External Vardar Subzone (DIMITRIJEVIĆ, 1997, 2001) or simply the Vardar Zone (PAMIĆ et al., 2002). There are opinions that ophiolites in these two belts re- sulted from obduction of just one ocean (PAMIĆ, 1998; PA- MIĆ et al., 2000; CSONTOS et al., 2003; SCHMID et al., 2008). Occurrence of ophiolites in two rather than only one belt is due to out-of-sequence thrusting and later nappe re- folding during Cretaceous and Tertiary orogenic phases (CSONTOS et al., 2003). A majority of Serbian geologists, however, are of the opinion that these ophiolitic belts repre- sent remnants of two different oceanic realms separated by the Drina-Ivanjica continental block (DIMITRIJEVIĆ & DI- MI TRIJEVIĆ, 1973; ROBERTSON & KARAMATA, 1994; KARAMATA et al. 1999, DIMITRIJEVIĆ, 2001). Another continental unit, i.e. the Jadar Block, is situated north of the Vardar Zone Western Belt. It is considered (by the majority of Serbian geologists) to be either an integral part of the Vardar Zone (DIMITRIJEVIĆ, 1997) or an exotic Figure 1: Tectonic sketch of the Dinarides, modified after SCHMID et al. (2008). Figure 2: A simplified and modified geological map of the wider surroundings of the investigated area, based on the Geological Map of SFR Yugoslavia 1:500 000 (SAVEZNI GEOLOŠKI ZAVOD, 1970); VZWB – Vardar Zone Western Belt, JB – Jadar Block, DIE – Drina-Ivanjica Element Đerić and Gerzina: New data on the age of an Upper Cretaceous clastic-carbonate succession in Brežđe (Western Serbia) Geologia Croatica 165 body pushed into the Vardar Zone in the Late Cretaceous (KARAMATA et al., 1994). The present-day tectonic contact between the Drina- Ivanjica and the Jadar Block (Fig. 2) is very steep and with a strong dextral strike-slip component (GERZINA & CSON- TOS, 2003). In the literature, this contact is referred to as the “Zvornik suture” (DIMITRIJEVIĆ, 1997) that is supposed to mark the ophiolitic suture between the Drina-Ivanjica and Jadar Blocks (KARAMATA, 2006). According to SCHMID et al. (2008), the “Zvornik Suture” simply represents the northwestern continuation of the long belt of Senonian fly- sch, which marks the tectonic boundary between the Drina- Ivanjica and the Jadar-Kopaonik thrust sheets. According to recent interpretations, the Drina-Ivanjica and Jadar units structurally underlie Neotethyan ophiolites of Jurassic age that were obducted onto the Adria margin during the Late Jurassic (SCHMID et al., 2008). However, the original position of the Jadar block below the ophiolitic mélange is visible only in the area of Takovo. In other places, however, the Jadar block seems to be thrust over the mélange and ophiolites (south of Valjevo) and partly over the Late Cretaceous sediments (in the area of Poćuta). Such a posi- tion of the Jadar block is probably a consequence of the post- Senonian (Paleogene?) collision-related thrusting and fold- ing (GERZINA & CSONTOS, 2003; CSONTOS et al., 2004). The Late Jurassic to Early Cretaceous transgressive phase, characterized predominantly by alluvial to neritic sed- imentation, started after the obduction and the subsequent erosion in the Dinaridic-Hellenic belt (PAMIĆ et al., 1998; PAMIĆ & HRVATOVIĆ, 2000; SCHMID et al., 2008). In Western Serbia, however, these sediments are absent, pos- sibly due to Early to mid-Cretaceous collisional processes (Schmid et al., 2008). In the wider research area, both Trias- sic sediments of the Jadar Block and Jurassic rocks of oce- anic origin that belong to the Vardar Zone are both uncon- formably overlain by transgressive Albian-Cenomanian clas tic sediments containing redeposited ophiolite fragments. Terrigenous-carbonate and carbonate sedimentation follow ed through the Cretaceous until the Campanian when flysch se- dimentation began (FILIPOVIĆ et al., 1978). 3. MATERIALS AND METHODS The described radiolarian assemblages originate from a sec- tion in Brežđe village (Fig. 3). Four samples, three of which pro duced positive results (BR 1/1, BR 1/2 and BR 1/3) were taken from marly limestone. The samples were treated with 7–15% acetic acid (CH3COOH), utilizing the standard meth- ods. The residues of the acid treatment, which yielded a well preserved fauna, were studied for biostratigraphic purposes. A SEM microscope JEOL JSM-6610LV SEM at the Faculty of Mining and Geology, University of Belgrade was utilized for precise identification of the radiolarians shown in Pls. 1–2. Table 1: Distribution of radiolarian taxa in the studied samples. Species Samples BR1/1 BR1/2 BR1/3 Alievium gallowayi (White) • • Alievium sp. • • Amphipyndax stocki (Cambell & Clark) cf. cf. Amphipyndax sp. • • Cryptamphorella ? sp. • Dictyomitra formosa Squinabol • • • Dictyomitra koslovae Foreman • • • Dictyomitra multicostata Zittel cf. Dictyomitra sp. • • Patellula euessceei Empson-Morin cf. • Patellula helios (Squinabol) sensu O’Dogherty cf. Patellula sp. • • • Praeconocaryomma universa Pessagno cf. cf. Xitus asymbatos (Foreman) • Xitus sp. • Figure 3: A Simplified geological profile in Brežđe village. Geologia Croatica 67/3Geologia Croatica 166 Plate I Santonian radiolarians from the Brežđe section, Western Serbia 1–3 – Alievium gallowayi (White). 4, 5 – Alievium sp. 6 – Patellula sp. cf. P. helios (Squinabol) sensu O’Dogherty 7, 8 – Patellula sp. 9, 10 – Patellula euessceei Empson-Morin 11, 12 – Patellula sp. 13, 14, 15 – Praeconocaryomma sp. cf. P. universa Pessagno. Specimens illustrated in Figs. 1, 2, 4, 7-9, 13, 14 originate from Sample BR 1/1; specimens in Figs. 6, 10 are from Sample BR 1/2; specimens in Figs. 3, 5, 11, 12, 15 are from Sample BR 1/3. Scale bar length for all images is 50μm. Đerić and Gerzina: New data on the age of an Upper Cretaceous clastic-carbonate succession in Brežđe (Western Serbia) Geologia Croatica 167 Plate II Santonian radiolarians from the Brežđe section, Western Serbia 1, 2 – Amphipyndax sp. 3, 4 – Amphipyndax sp. cf. A. stocki (Campbell & Clark) 5, 6 – Xitus asymbatos (Foreman) 7-18 – Dictyomitra formosa Squinabol 19-28 – Dictyomitra koslovae Foreman 29 – Dictyomitra sp. 30 – Cryptamphorella ? sp. Specimens illustrated in Figs. 1-3, 5-10, 18-22, 29, 30 originate from Sample BR 1/1; specimens in Figs. 11-13, 23-25 are from Sample BR 1/2; specimens in Figs. 4, 14-17, 26-28 are from Sample BR 1/3. Scale bar length for images 1-4, 7-24, 26-30 is 50μm; for images 5, 6, 25 is 100μm. Geologia Croatica 67/3Geologia Croatica 168 The micropaleontological material is housed at the Faculty of Mining and Geology in Belgrade (registration numbers BR 1/1, BR 1/2 and BR 1/3). 4. SECTION DESCRIPTION AND BIOSTRATIGRAPHY In the wider area of Brežđe, MARKOVIĆ & ANĐELKOVIĆ (1953) distinguished Albian-Cenomanian, Cenomanian, Turo- nian and Senonian sediments. According to FILIPOVIĆ et al. (1978), Turonian sediments are represented by detrital limesto ne with marlstone interlayers, reddish bedded silicified limestone, marly-sandy conglomeratic limestone and reddish marly claystone. Senonian sediments are best exposed in Stru- ganik village. They are represented by a sequence predomi- nantly made up of thin-bedded limestone, clayey limestone and marlstone (the so-called Struganik Limestone). Chert con- cretions are present throughout the sequence. Based on the identified radiolarian as sociation, the Lower Senonian age of grayish clay intercalations in limestone of the Struganik quarry was determined by DJERIĆ et al. (2009), while BRA- GINA et al. (2014) distinguished several bed-ranked units, ranging from the Lower to the Upper Santonian, in a carbon- ate-flyschoid section near Struganik village. The profile in Brežđe village (Fig. 3) starts with strongly sheared serpentinite in the footwall of slightly metamorphic Triassic platform carbonates. The footwall of the serpenti- nite is not visible along the profile but, according to the ob- servations in the immediate surroundings, serpentinite is in a tectonic contact with the underlying ophiolitic mélange. This original tectonic sandwich was possibly folded and cer- tainly slightly metamorphosed and cleaved prior to the Se- nonian and also strongly folded after the Senonian (GER- ZINA & CSONTOS, 2003). The Triassic carbonates are pre served in synforms, while the serpentinite forms the cores of antiforms. Finally, the whole tectonic assemblage is un- conformably overlain by an Albian-Cenomanian shaley, mar ly and carbonate succession grading to Senonian, which has a shallowing-upward tendency (Fig. 4). The original trans gressive relationships are disturbed by a steep-dipping fault along which Triassic limestone is in contact with Late Figure 4: A Generalized columnar section of the Cretaceous in the studied area. The inset to the right shows the column interval studied for radiolarians, with the sample locations indicated. Đerić and Gerzina: New data on the age of an Upper Cretaceous clastic-carbonate succession in Brežđe (Western Serbia) Geologia Croatica 169 Cretaceous marlstone. The section terminates with shallow- marine carbonates. Four samples were taken for micropaleontological in- vestigations from gray-yellowish limestone, about 10 m thick at the Brežđe section (Fig. 4). Associations of Late Creta- ceous radiolarians are identified from three positive samples (Table 1). All three samples are characterized by the common pres- ence of Dictyomitra formosa Squinabol and Dictyomitra ko- slovae Foreman. The species Dictyomitra formosa Squinabol is distributed from the Albian to the lower Campanian (SCHAAF, 1985; BANDINI et al., 2006). Dictyomitra ko- slovae Foreman is characteristic of the Campanian and the Lower Maastrichtian oceanic sediments (SANFILIPPO and RIEDEL, 1985). It has also recently been reported from the Santonian rocks (KORCHAGIN et al., 2012, BRAGINA et al., 2014). Samples BR 1/1 and BR 1/3 also contain the species Al- ievium gallowayi (White), which is the index species of the synonymous Santonian zone of California (PESSAGNO, 1976). It should be noted that the joint occurrence of radi- olarian species Dictyomitra koslovae and Alievium gallowayi is also known from Santonian strata of the Crimean Moun- tains (KORCHAGIN et al., 2012) and Struganik village in West Serbia (BRAGINA et al., 2014). The radiolarian association from sample BR 1/1 also con tains Cryptamphorella macropora Dumitrica which, ac- cording to the available published data, had its last appear- ance in the Campanian (DUMITRICA, 1970; EMPSON- MO RIN, 1984; URQUHART, 1994), while the radiolarian assemblage in sample BR 1/3 contains Pseudoaulophacus lenticulatus (White) (LAD in the Campanian; PESSAGNO, 1976; URQUHART, 1994). In summary, the samples are certainly Santonian in age, but a more precise dating is difficult to establish with the ex- isting zonations. Beside the radiolarians, the microfauna is surprisingly rich in sponge spicules. Notable amounts of sponge spicule fragments together with abundant radiolari- ans are conspicuous features in all the three studied samples. Monaxones predominate, but hexactines are frequent as well. A significant amount of sponge spicules together with abun- dant radiolarians in the studied samples indicate a relatively proximal slope environment (KIESSLING, 1996). 5. DISCUSSION AND CONCLUSIONS After the Late Jurassic obduction and subsequent erosion in the Dinaridic-Hellenic belt, Cretaceous synorogenic basins were formed and filled with clastic material composed of variable amounts of ophiolitic, terrigenous and carbonate detritus (LUŽAR-OBERITER et al., 2012). Therefore, the obducted ophiolitic sheets of the Dinarides are in many places unconformably overlain with Late Jurassic to Early Cretaceous shallow and/or deep marine sediments (PAMIĆ et al., 1998; PAMIĆ & HRVATOVIĆ, 2000; SCHMID et al., 2008). In Western Serbia, however, early Cretaceous sedi- ments are missing and transgression did not start prior to the end of the Lower Cretaceous, thus both Triassic sediments of the passive margin of the Adria and Jurassic rocks of oce- anic origin are both unconformably overlain by a transgres- sive succession that starts with Albian-Cenomanian clastites. The studied sediments of Santonian age are parts of this Late Cretaceous terrigenous-carbonate sequence which was con- tinuously deposited until the Campanian, when flysch sedi- mentation began and the so-called Ljig Flysch of Campan- ian-Maastrichtian age was formed. In order to enable more detailed stratigraphic division of the Turonian-Senonian terrigenous-carbonate sequence in Western Serbia, Late Cretaceous radiolarians have been ex- tensively studied during the last five years (DJERIĆ et al., 2009; BRAGINA et al., 2014). According to lithostrati- graphic correlation and the identified radiolarian association, the studied limestone corresponds to the Struganik Lime- stone which originated on the continental slope, in a rela- tively proximal slope environment which is indicated by a significant amount of sponge spicules together with abun- dant radiolarians. The Santonian age of the analyzed sediments is based on radiolarians. Similar Santonian radiolarian assemblages are known from deposits of the Mt. Ak-Kaya, Crimean Mountains (KORCHAGIN et al., 2012) and from Struganik village in Western Serbia (DJERIĆ et al., 2009; BRAGINA et al., 2014). Despite the almost identical stratigraphic rela- tionships observed in the Struganik and Brežđe villages, the differences between the radiolarian associations are quite obvious. The Brežđe radiolarian assemblages are far less taxonomically diverse in comparison with the radiolarian assemblages in Struganik. Moreover, the radiolarian asso- ciation in Brežđe is characterized by an absolute predomina- tion of the species Dictyomitra koslovae and Dictyomitra formosa, which are also present also in the Struganik asso- ciations, but in far lesser amounts. Therefore, the radiolarian assemblages from Struganik enabled more detailed biostrati- graphic division of the host sediments (the lower Santonian, uppermost lower Santonian - basal upper Santonian and up- per Santonian; BRAGINA et al., 2014). A Santonian age is established for the studied radiolarians in Brežđe, but the taxonomic composition of the assemblages does not allow any further division. Geographically, the nearest similar radiolarian assem- blages, although younger (Campanian) are known from Ro- mania (VISHNEVSKAYA, 2001) and from southern Cyprus, where they occur in the sedimentary cover of the Troodos ophiolite and the associated mélange units (URQUHART, 1994; BRAGINA & BRAGIN, 1995, 1996, 2006) as well as an assemblage from southern Turkey from Scaglia-type pe- lagic limestones of the Upper Antalya nappes (MOIX et al., 2009). 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Manuscript received March 19, 2014 Revised manuscript accepted September 16, 2014 Available online October 31, 2014