2019 | 72/2 | 109–128 | 21 Figs. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society

Stratigraphic implications of the Mio-Pliocene geodynamics in the area of Mt. Avala: new evidence from Torlak Hill and Beli Potok (Belgrade, Serbia) Ljupko Rundić*, Meri Ganić, Slobodan Knežević, Dejan Radivojević and Miloš Radonjić

University of Belgrade, Faculty of Mining and Geology, Department of Regional Geology, Kamenička 6, 11000 Belgrade, Serbia; (corresponding author: [email protected]) doi: 10.4154/gc.2019.11

Abstract Article history: Mt. Avala is located on the southern margin of the Pannonian basin (SPB), a border zone be- Manuscript received February 22, 2018 tween the uplifted morphostructures of the Dinarides and Carpathian-Balkanides. Similar to the Revised manuscript accepted February 28, 2019 Pannonian basin, tectonostratigraphic evolution of the Mt. Avala area during the last 23 Ma has Available online June 3, 2019 is characterized by syn- and post-rifting processes as well as tectonic inversion. Here, we pre­ sent the results of field investigations of the Miocene‒Pliocene dynamics that led to different spa- tial positions of the same stratigraphic units (e.g. Badenian and Pannonian) in a relatively small area. These spatial relationships are interpreted in the context of pronounced block structures (Torlak, Beli Potok and Avala). Torlak Hill represents a horst structure with a core composed of Mesozoic rocks and hillsides composed of the Middle Miocene sediments, which are present at the surface at altitudes up to 336 metres. Nearby, there is the Beli Potok asymmetrical trough that was infilled by the late Miocene sediments. The Torlak horst and the Beli Potok trough struc- tures are separated by the Rakovica normal fault. In some places along the fault line, several geological units are vertically displaced more than a hundred metres. For example, in borehole KGK-14, the Upper Miocene Pannonian marls are observed at a depth of 100 metres below the surface. However, only a few hundred metres away to the northeast, similar Pannonian marls are observed at the surface, at an altitude of about 210 metres. Due to the mentioned observed Keywords: Mio-Pliocene geodynamics, Southern Pannonian Basin, Avala and Torlak horsts, Beli vertical movements along the block structures, a composite hilly relief with dominant the Torlak ­Potok trough, Serbia Hill and the Beli Potok Valley was formed.

1. INTRODUCTION 2015). Seven million years later, Lake Pannon was filled with la- Since the early pioneering work of e.g. ROYDEN et al. (1983) and custrine and fluvio-deltaic sediments derived from the surround- HORVÁTH (1984), the following thirty years or so have seen ing orogenic belts (e.g. MAGYAR et al., 2013; RADIVOJEVIĆ publication of a lot of papers concerning the origin and evolution & RUNDIĆ, 2016). At the beginning of the Pliocene, the “caspi- of the Pannonian Basin (PB) and its marginal parts e.g. TARI & brackish” giant Lake Pannon was reduced to the much smaller PAMIĆ (1998); BADA et al. (1999); HORVÁTH et al. (2006); freshwater Paludina Lake (MAGYAR et al., 1999; SZTANÓ et DOMBRÁDI (2012); KOVÁCS et al. (2015); BALÁZS et al. (2017 al., 2015; MANDIC et al., 2015; RUNDIĆ et al., 2016). A similar and references therein). Generally, in these papers a very complex scenario was demonstrated from the southern margin of the Pan- interdisciplinary and multidisciplinary approach has been ap- nonian Basin (RUNDIĆ et al., 2011, 2015, 2017). plied. Although, some of the authors didn’t have similar views to At the beginning of the Miocene, the studied area was rep- the general model of the PB and mechanisms of its genesis, long- resented by continental-lacustrine facies of different ages term investigations led to greater understanding of these pro- (DOLIĆ, 1997, 1998; KRSTIĆ et al., 2012; RUNDIĆ et al., 2013, cesses. Today, the general structural pattern concerning the evo- 2015). During the Middle Miocene (Badenian), a maximum ex- lution of the PB is accepted (e.g. MATENCO & RADIVOJEVIĆ, tension led to Paratethys marine flooding in Serbia as well as in 2012; BALÁZS et al., 2016, 2017 and references therein). It is other countries at the southern margin of the PB (e.g. ĆORIĆ et evident that the Early to Middle Miocene pre- and syn-rift depo­ al., 2009; KOVAČIĆ et al., 2011; PAVELIĆ & KOVAČIĆ, 2018; sits of the PB show a transition from continental alluvial-lacustrine SANT et al., 2018). The Late Middle Miocene to Pliocene post- to fully marine environments (PAVELIĆ & KOVAČIĆ, 1999; HARZHAUSER & PILLER, 2007; HARZHAUSER & MAN- rift thermal stage of subsidence was weak but more extensive DIC, 2008; MAGYAR et al., 2013; SANT et al., 2017). The peak than during the Badenian (MAROVIĆ et al., 1995; 2002; 2007; of extensional tectonics was reached during the Badenian–Sar- RADIVOJEVIĆ & RUNDIĆ, 2016). At the end of the Miocene, matian rifting phase (ca. 16–12 Ma) (e.g. FODOR et al., 2005; Mt. Avala was an elongate island, with lake-margin and swamp RADIVOJEVIĆ et al., 2010; MATENCO & RADIVOJEVIĆ, environments formed along its shoreline. Later, the Pliocene– 2012; RADIVOJEVIĆ & RUNDIĆ, 2016). The long-lived Lake Quaternary tectonic compression reactivated some older faults Pannon was formed at the Middle/Late Miocene boundary (ca. and the Lake Pannon sediments were differentially displaced and 11.6 Ma) as a consequence of the tectonic uplift of the Carpathi­ lost their lateral continuity (e.g. MAROVIĆ & KNEŽEVIĆ, 1985; ans that separated the basin from marine influences (MAGYAR KNEŽEVIĆ, 1989; MAROVIĆ et al., 1995; 2002; 2007; TOLJIĆ et al., 1999; TER BORGH et al., 2013, 2015; SZTANÓ et al., et al., 2014). Consequently, the system of uplifted block structures Geologia Croatica tectonics especially its stratigraphic implications. implications. stratigraphic its especially tectonics Mio-Pliocene of effects distinct the show to evidence phologic geomor and structural biostratigraphic, principal we collected etc.) units, of position same spatial unconformity, sional contact, ero boundaries, tectonic or (normal geological units the between relationship interesting an and relief the in exposure their field, the in sediments of Miocene distribution the from 1). Starting sights about the evolution of(Fig. relatively area this small-scale the regional tectonic setting of Serbia, the older Mesozoic units in in older Mesozoic the units of Serbia, setting tectonic regional the to 1996).According 1985;ANDJELKOVIĆ & ANDJELKOVIĆ (MAROVIĆ & rides and KNEŽEVIĆ, the Carpathian-Balkanides of Dina the morphostructures uplifted the between zone border of PB, the a margin southern the on located is area studied The SETTINGS GEOLOGICAL 2. processes. weathering and erosion to exposed were deposits Pannonian Lake with fault.Note: fault; ZU–Zuce –Kaludjerica fault,KA Traces oftheaforementioned faultsare takenfrom MAROVIĆ etal. 2007). studied outcrops and figure Key: numbers in the text. TO – Rakovica fault; fault; RF – Torlak TR – Beli fault; BP – reka PotokTopčiderska fault; ZR – Zavojnička reka Figure 1.Location (a)andgeological sketch map(b)ofthestudiedarea (modifiedandupgraded IVKOVIĆ after etal., 1966and the 2016).Numbers mark TOLJIĆ, 110 In this study, the research objective was to provide more in more provide to objective was research study, the this In - - - - formation, predominantly) have a relatively narrow distribution distribution have arelatively narrow predominantly) formation, 2). (?Lower Older units continental-lacustrine Miocene Miocene m unconfor units sedimentary Quaternary and Miocene ferent these All 2018). Much later, dif area. al., the in rocks basement et the represent rocks TOLJIĆ 1996; MATOVIĆ, & (VASKOVIĆ rocks these into intruded were thickness of different sills 2018). the Oligocene, During dykes bodies forming magmatic and al., et 2016; TOLJIĆ (TOLJIĆ, deposits flysch and turbiditic Cretaceous Upper and carbonates Cretaceous Upper and Lower Juras to peridotites, belong serpentinized mélange, rocks ophiolitic carbonates, sic oldest 2011).The al., et GANIĆ 2016; 2006, ­p Quaternary and Mesozoic, Tertiary the during formed rocks sedimentary and igneous of various composed is and features al., et 2008). Sava (SCHMID zone the and 1997; 2016) TOLJIĆ,2006, (DIMITRIJEVIĆ, sense wider the in i.e. Vardar zone the Tethys domain, belong the to area oceanic this eriods (MAROVIĆ et al., 1995, 2002, 2007; TOLJIĆ, 1996; TOLJIĆ, 2007; 2002, 1995,al., et (MAROVIĆ eriods ably or (Fig.overlie sediments Cretaceous Jurassic serpentinites The study area represents a region with complex geological with a region represents area study The Geologia Croatica 72/2 - - ­ Geologia Croatica - - 111 Bearing in mind that the area vegetation, is covered by the lack fossils were photographedMiningand of Faculty DepartmentMineralogyPetrology, and of using SEM (JEOL JSM6610LV) at UniversityGeology, the of Belgrade.detailed However, analyses of these taxa are the further subject of investigations. structuralof information in previous research, as as well our own very poor data, the measurements structural of elements were not collected dip angle systematically and dip direction, (e.g. fault traces, geometric and kinematic properties, Scarce individual etc.). measurementsbedding of plane faultor trace were performed and used to support the above-mentioned stratigraphic results with structuraland geomorphologic observations in the The relief. scarce data was supplemented with the terrain DEM and model these interpretationswerefurther connected to the previously pub lished results. In that sense, ideas and some of could conclusions be described as provisional and are based not on real measurements Furthermore, inthefield. co geomorphologic(GPS basic the data ordinates and altitude, topographic map, Google Earth map, etc.) was used in order to pinpoint the mainlandforms andtheir possible relationships towards the main linear structures relief. of 4. RESULTS 4.1. The studied outcrops and sections ?Lower Miocene (Continental-lacustrine)4.1.1. Bučvar clastites In the upper portion of the Bučvar Stream (Bučvar the Potok), left tributary of the Zavojnička Reka River, i.e. Bolečica River, a - olluscs) as as well theirolluscs) biostratigraphic position has been used hotographed by Leica binocular microscope. Some key micro ollected from outcrops the twelve and sections and two shallow pecimenswere subsequently examined under reflected by light Schematic geological column of the pre-Neogene and Neogene-Quaternary column 2. Schematic geological rocks basement and tectonic stages Figure with palaeoenvironments succession 2016). 1966 and GANIĆ et al. et al., after (modified IVKOVIĆ of the studied area Olympus BH2 microscope. Foraminifers and ostracods were ­p for determining the different Miocene units. After cleaning and and cleaning After units. Miocene different the determining for preparation with water and hydrogen-peroxide, the some of ­s ­m ­c boreholes (Fig. 1). Primarily,and they biostratigraphic were used analyses. for Fossil palaeontological macrofauna (mostly 3. MATERIALS AND METHODS the rock of Most been samples have collected from both banks of the Rakovica Stream valley (Rakovički potok) located in the N-NW Other part been samples Avala. Mt. have taken of more toward the north-northeast Beli Potok, (Torlak, Avala Mt. of Leštane, and Vrčin – Fig. 1). All the analyzed samples were (DOLIĆ, 1997; RUNDIĆ (DOLIĆ, Middle1997; et Mioceneal., 2013). marine andmarine-brackish sediments are and been developed have well extensivelystudied (e.g. LUKOVIĆ, EREMIJA, 1922; 1977a, 1987; PETROVIĆ, STEVANOVIĆ, 1995; KNEŽEVIĆ & 1951; ŠUMAR, RUNDIĆ 1994; & KNEŽEVIĆ, Similarly, the 2017). werePannon Lake the „caspibrackish“sediments Mioceneof late the various subject of stratigraphic studies beginning with the and STEVANOVIĆ well-known studies(1931) by PAVLOVIĆ (1972, KRSTIĆbiostratigraphic the articles of by followed (1951), and EREMIJA (1989) 1990), (1985, STEVANOVIĆ 1985), 1973, KNEŽEVIĆ (1989). Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok Geologia Croatica sively overlies the serpentinite (BT1-2). of reddish, sively consist serpentinite They overlies the the Bučvar conglomerate (more that than 7 m thick observed succession) transgres was it tunnel, railway Potok” “Bubanj the BT1-3 and BT1-2 of for the construction drilling exploratory boreholes During near Leštane. in observed was unit similar a study, this in time, same the At d). 3c, (Fig. sedimentation lacustrine pre-Badenian of phase final the represent (2013)clastites these al. (1997, et DOLIĆ RUNDIĆ to 1998)Fig.3a). and According of the part upper of the Torlak in and vicinity Hill the in tites clas of these presence the determined has research More recent area. this in environment of lacustrine the termination and phase (?Lower Miocene, Egenburgian) and they represent the regressive of Series Slanci the member youngest belong the to glomerates ­R ­H (1987). EREMIJA by proposed was interpretation similar A ­B ­a ­t clays which reddish and sandstones greenish to pinkish sand, ­c conglomerates medium-grained the 1).Herein, Fig. in No.3 – youngest member of the Vrdnik Series (Fruška Gora), i.e. the the i.e.Gora), (Fruška Series Vrdnik the of member youngest the with conglomerates those STEVANOVIĆ(1970) equated macrofauna. and micro- abundant by an clays characterized same the to According Stage. Badenian the to Karpatian the at the from the transition “Helvetian to Tortonian Stage”, i.e. from horizon stratigraphic aspecial represent conglomerates these that STEVANOVIĆ fossils. of (1970) barren believed are cally,they ­t clastites Bučvar the called deposits clastic of package thick valley (b),adetailofreddish conglomerates, light-brown sandstones inintercalation coarse-grained withgreen siltandclay (c, d). Figure 3.The continental-lacustrine ?Lower inthearea Miocene of Torlak hill:Panoramic stream towards viewoftheBučvar theNE(a),aviewinsidestream 112 ogether build a heterogeneous series (Fig.3b-d). Macroscopi (Fig.3b-d). series heterogeneous a build ogether ransgressively overlies serpentinites (N 44°45 (N serpentinites overlies ransgressively uthor, they are in tectonic contact with gray, Badenian marine marine gray, Badenian with contact tectonic in are uthor, they onsist of serpentinite clasts, quartzites, cherts, fragments of fragments cherts, quartzites, clasts, serpentinite of onsist udafa conglomerates of Mecsek Mountain in southern Hungary. Hungary. southern in of Mountain Mecsek conglomerates udafa akovica Stream and its tributary (N 44°44 (N tributary its and Stream akovica owever,DOLIĆ(1997, con Bučvar the that 1998) confident is ′ 01 ′ ″ 04 , E 20°30 E , ″ , E 20°31E , ′ 20 ′ 57 ″ – ″ - - - - 1997; al., et RUNDIĆ 2013). ?Lower Miocene ( sediments loured continental-lacustrine varico and reddish overlie previous the transgressively and area this in transgression marine of Badenian the part basal the mark rocks these Stratigraphically, observed. were diameter 1cm to up pebbles of small occurrences rare and no visible fauna, with stone sand yellow-brown thick 0.70m a conglomerates, and gravels (? recognized be could shell imprints fossil of remains indistinct few a clasts, rock different the sides Be 4d). (Fig. dominant are cm) 7 to (up (cobbles)quartzites of clasts larger However, succession. 4c) (Fig. gravel imbricated (pebbles). gravel coarse very and of coarse form the in essentially well-sorted to moderately sandstones, and quartzites of fragments rounded 1998; al., et RUNDIĆ 2013). (DOLIĆ, 1997, content petrological and colour different a has and fossils not contain does unit this sands, and conglomerates gravel, Badenian marine overlying the Unlike rocks. Miocene succession younger lithological the underlies and distribution spatial a large has that distinct a represents this field, the In clay. silty greenish of lenses and sandstones coarse-grained to fine- with alternation in conglomerates coarser green dark and brown composed of gravels and poorly cemented polymictic conglo polymictic cemented poorly of and gravels composed rocks clastic of coarse-grained outcrop an of stream, the portion v m tary (N 44°43 (N tary tribu right its and section stream of Rakovica the part upper the along exposed is deposits marine of Badenian the part basal The deposits Rakovica Badenian) (Marine Miocene Middle 4.1.2. The composed of well-rounded and sub and of well-rounded composed are deposits ica stream erates up to 1.2 m high has been studied (Fig. 4a, b). The Rako b). The 4a, (Fig. studied been has high m 1.2 to up erates ′ 59 ″ platy and discoid clasts indicate an an indicate clasts discoid and platy Abundant , E 20°30 E , ′ 10 ″ – No.4 in Fig. 1). Nearby, the lower lower the Nearby, 1). Fig. in No.4 – Solecurtus Geologia Croatica 72/2 sp.) . Above these . Above these DOLIĆ, DOLIĆ, - - - - ­ ­ - Geologia Croatica

- ­ - - - ­ ­ ). El. cf. 113 Am ex. gr. and oth , Flabel , . are present. sp . Elphidium – in No.7 Fig. 1). ″ 04 ′ sp., Ammonia Xestoleberis sp., etc. Ostrea sp etc.), foraminifer etc.), ( ., and (FICHTEL et MOLL), (FICHTELMOLL), et

sp., Textularia , E 20°30 ″ 38 ′ Borelis macellum Glycymeris pilosus (LINNÉ) . Quinqueloculina sp., – No.8 in Fig. 1) located on the opposite side ″ 54 , Aurila notata (REUSS), ′ ANDRZEJOWSKI) d’ORBIGNY, d’ORBIGNY, (Turritella sp., Hydrobia sp (Turritella sp., sp., Ammonia , E 20°29 (LINNÉ) d’ORBIGNY, El d’ORBIGNY, ″ 45 ′ The second outcrop, is observed in a new large section (N posits ed inboth stream banks. The first is observed on the left bank, An outcrop more than 5 m high and up to 20 m long exposes grey to brownish laminated sand and poorly cemented sand stone in alternation with gray to greenish silty marl (Fig. 7a). Thedip these gentle angle of sediments isvariable andthe at south the end section of reaches degrees up to 13 dipping towards There theNE is 7b). novisible macrofauna. (Fig. Based on the observed foraminifera and ostracod association, this section corresponds to the Lower Sarmatian deposits ( reginum beccarii 44°43 near to the streamthenearto floor 44°43 (N aculeatum Middle4.1.3. Miocene (Marine-brackish Sarmatian) Rakovica de Along the Rakovica Stream some two hundred valley, metres further to the south, two new Sarmatian sections were discove r quartz clasts together with carbonates, quartzites, schists, and cherts. rounded Clasts cm in and are range from size. well 0.4–1 Frequent bivalve remnants ( ers), anders), bryozoan fragments have also been identified(GANIĆ Bryozoanset al., 2016). are represented by branching forms. Ac studythe in Limestone Leitha the (2013) al. et RUNDIĆ tocording area, due to the predominant composition fossil could be catego rized as an algal-foraminifer-bryozoan type limestone. of lipecten besseri ( phistegina Gastropod ­ ------″ 15 ′ Costa Costa , E 20°30 ″ Cletocythereis 46 ′ (REUSS), Elphidium crispumElphidium – No.6 in Fig. 1). It is represented ″ 09 ′ FICHTEL ET MOLL, Cnestocythere truncata ,E 20°30 ″ Ammonia beccarii LINNÉ,Ammonia 44 ′ (REUSS), Borelis melo Borelis (ROEMER) was discovered, (ROEMER) which further addresses Above the previousAbove outcrop, a hundred metresdownstream, A few metresBadeniansuccession,?Upperhigher thetheinfew A LINNÉ), ences The therein). section contains a very rich and diverse r macro- and microfauna including more than 70 species of gas tropods abundant and bivalves, foraminifers and ostracods, echi noids, fishotoliths, etc. that confirmthe marine flooding in this area. In this the study, microfaunal association foraminifers of andostracods ( ( close to the top of the left Rakovica stream banka well-known Badenian sand section (N (Fig. 44°43 5), there is tok) were described by PAVLOVIĆ (1890, 1893) tok) and were 1893) untildescribed (1890, re by PAVLOVIĆ detailedcently, studies about the marine Badenian shallow-water refe and 2016 al., et GANIĆ (e.g. published were sand “seashore” – No. 5 in Fig. 1) up to 10 m high. The first data concerning the the concerning data first The high. m 10 to up 1) Fig. in 5 No. – “Mediterranean fauna” of the Rakovica Stream (Rakovički Po The Badenian basal conglomerates: Small outcrops at the upper part of the Rakovica Stream valley (a, b), a close up of the relatively well-sorted, imbricated well-sorted, part upper the relatively at the of up a close b), (a, valley Rakovica of the outcrops Small Stream conglomerates: basal Badenian 4. The Figure pebbles of the quartzites (c), semi-rounded (d). and sandstones conglomerates Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok haidingeri edwardsii pods and otoliths confirm theshallow-water character of the aforementioned sands (SCHWARZHANS etGANIĆ al., 2015; 2016). et al., anotheras developed was 2012) al., (WIEDLLimestoneet Leitha facies(N 44°43 the depositional environment and paleoecological characteristics the studyof area. The last recent detailed studies gastro fossil of by hard,by poorly bedded and fossiliferous massive limestone, frac tured and partly karstified at the topof the section.It appears in de limestoneTheis 6). (Fig. relief thein blocks large of formthe termined to represent a biocalcarenite. Fossil detritus is mainly composed calcareous of algae, molluscs, echinoids, bryozoans, and large benthic foraminifers. Rare detritus comprises mainly Geologia Croatica Figure 6. The UpperBadenianpoorly-bedded limestone Stream (LeithaoftheRakovica valley (a,b). limestone) at theupperpart and, microfossil typical exgr. beccarri assemblageoftheUpperBadenian(Ammonia LINNE, stream oftheRakovica FigurePersistrombus (a,b), intheupperpart 5.The coronatus UpperBadeniansands:Awell-knownsandsection (c) (DEFRANCE) 114 Figure 7.The Lower ofgrey Sarmatiansection to brownish laminated cemented sandandpoorly sandstone (a)inalternation withgray to greenish (b). marl silty Elphidium crispum(LINNE), Borelis meloFICHTEL&MOLL,etc. (d). Geologia Croatica 72/2 Geologia Croatica

­ - - 115 sp. Bi sp. The

Anomali ex gr. beccarii gr. ex sp., Pirenella Elphidium aculeatumElphidium Heterocythereis mehesi Loxocorniculina Ammonia (FICHTEL ET MOLL), sp., Cerithium (REUSS), LUCZKOWSKA, Calliostoma El. macellum El. Aurila notata cf. dividens TEVANOVIĆ, 1985) Rakovica marls Late4.1.4. Miocene, Lower Pannonian Pannonian (= sensu S theAt Rakovica Stream valley road, near to and the just Avala 200 m downstream of the Sarmatian section mentioned above LASKAREV), ? following foraminifers were determined: (d’ORBIGNY), (LINNÉ). Elphidiums are common within the fossil assemblage and represent the most abundant specimens. Among the ostraco noides des, only a few species were recognized: (ZALANYI), ostratigraphically, the all aforementioned of species correspond to the Sarmatian Lower in age. - - - - (PARTSCH in Ervilia dissita Eich vindobonensis ex gr. gr. ex Cerastoderma revious described Sarmatian section in On Fig. 7. the western- The Lower Pannonian sandy marl (a), sandy marls steeply dipping towards the southeast (b). the southeast sandy marl towards dipping (a), sandy marls steeply Pannonian Lower 9. The Figure The Lower Sarmatian: a large section of gray, silty marl in alternation with grey to brown laminated sandstones (a, b), thin interbeds of platy limestone (a, b), thin interbeds sandstones laminated brown to silty with grey marl in alternation section a large Sarmatian: of gray, Lower 8. The Figure (d). and marls (c) Erviliadissita EICHWALD ­p southwestern part, a small coarse-grained lens of clastics and peb of the Rakovica Stream valley. It exposes a section more long and up thanto m 12 high of the 80light mbrown to yellowish sands and poorly cemented parallel to cross-laminated sandstones inter calated with thin interlayers gray of marls and platy limestones (Fig. 8a-c). Stratigraphically and structurally, it overlies the is interbedded bles inpart the lower the section.of The mean dip angle of the sediments reaches 15 degrees (dip direction is 40°). This measured section contains poor association fossil relatively molluscs,foraminifers of and ostracods. the fossils are of Most poorly preserved and their shells are covered or partly filledby fine-grained sediments and quartz grains. Among them, thefol lowing mollusc species could be identified: 8d), (Fig. wald Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok Geologia Croatica perphoratus ( observed were molluscs E ­Am (MEHES), and 21). such genera as the Among ostracodes, (Figs.9b tilting forthis responsible is which fault Rakovica the of proximity the to related is deformation the suggest southeast to direction (73–75°) dip a marls and the of angle dip steep the Also, boundary. Sarmatian/Pannonian age close the to an cates indi foraminifers of Sarmatian the forms recrystallized scarce Melanopsis (REUSS), (REUSS), locypris r (Fig. 7), an of outcrop seve marls, sandy the Lower Pannonian 116 identified: identified: of Figure 10.The Lower Pontian (sensu STEVANOVIĆ) clastics, gravel predominantly coarse-grained and semiconsolidated conglomerates shells (a, b), recrystallized al metres in height and length, was discovered was length, height and in metres al

sp.Mytilopsis destroyed (c, d)and, (BRUSINA) apartly M. trnskii specimenof (e). 2 plocypris plocypris 0°29 and Candona and ′ 55 Hemicytheria Hemicytheria ″ Cyprideis sp.). A relatively numerous ostracod association and and association sp.). ostracod Arelatively numerous – No.9 in Fig. 1; Fig. 9). Rare fragments of fossil of fragments 9).Fig.1;Fig.Rare in No.9 – KRSTIĆ, KRSTIĆ, Candona (Propontoniella)Candona candeo cf. firmus firmus

predominate. The following species were were following species The predominate. kollmanni kollmanni Herpetocyprella auriculata Herpetocyprella cf. KRSTIĆ, KRSTIĆ, Orygoceras (REUSS), (REUSS), folliculosa KRSTIĆ, KRSTIĆ, A . cf. recta sp., Lymnocardium sp., C . cf. heterostigma Cyprideis (REUSS), (REUSS),

(N 44°43 (N H. ampullata KRSTIĆ (REUSS), (REUSS), , Amp sp., sp., ′ 33 A. A. ″ - ­ ­ , ,

L. KRSTIĆ, siboviki Cypria HEJJAS Candona POKORNY, Xestolebris cf. coarse-grained sand can be observed (N 44°42 (N observed be can sand coarse-grained and gravels sandstones, semiconsolidated of conglomerates, formed long, m 5 than more and high m 2 to up section a lage, Along the road to the Konopljište stream, in the Beli Potok vil S sensu (= Pontian Pannonian Upper Miocene, 4.1.5. Late 10a, lower molluscs scarce such part), as containing (Fig. predominant are sands and sandstones cemented poorly – No.10 in Fig. 1). In the lower ofpart the section, coarse-grained TEVANOVIĆ, 1985) Beli Potok clastic deposits clastic Potok Beli 1985) TEVANOVIĆ,

mülleri KRSTIĆ, KRSTIĆ, servica KRSTIĆ, KRSTIĆ, miscere , Leptocythere(Amnicythere) ( (MEHES), (MEHES), porosa L. L Typhlocypris) lunata (MEHES),Typhlocypris) lunata sp. sp. Candona (Thaminocypris) Candona Loxocorniculina hodonica POKORNY, Loxoconcha granifera

improbus Geologia Croatica 72/2 C. (T.) C. trigonella . cf. rhombovalis ′ 31 ″ , E 20°31E ,

Melanopsis Melanopsis (REUSS), (REUSS), KRSTIĆ, KRSTIĆ, L . ( ′ 42 A ″ ) -

Geologia Croatica - - ­ – ″ 117 15 ′ Cypri­ Lymno , E 20°32 ″ (M.HÖRNES), 11 ′ M.zagrabiensis (BRUSINA). (BRUSINA). Besides molluscs, a a molluscs, Besides (BRUSINA). Hemicytheria josephinae (ZALANYI), , Bakunella, dorsoarcuata (ZALANYI), (M.HÖRNES), L. riegeli (BRUSINA), KRSTIĆ, KRSTIĆ mayeri cf. “Upper Pontian” outcrops up to m 10 thick have been dis triangulata

the surface (Fig. 11a, b). The lower, older part of the section section the of part older lower, The b). 11a, (Fig. surface the

the aforementioned outcrop belongs to the littoral facies of Lake littoralof thefacies to belongs outcropaforementionedthe Pannon. Above these mentioned marls,thick ~1.5m gray silts contain a similar association fossil (large candonids prevailingamong the ostracods – Fig. They 11e). are intercalated (up to 1m thick) withand a graythin interlayer sandy of silts with(10–20cm) silts zagrabiense Lymnocardium very abundant ostracod assemblage was also observed: deis dubokensis H. No.11 inthey However, Fig. 1). exhibitNo.11 a yellow-brown colour on with 4 m, is height a composed of brownish of sandy to gray, d) which containsmarl 11c, rare(Fig. molluscs such as covered thealong ring Generally, they road con near Avala. Mt. graysist of silts and sandy marls (N 44°43 cardium croatica Mytilopsis - - M. M. FUCHS, Mytilopsis FUCHS, Zone i.e. a time interval Melanopsis defensa Limnocardium banaticum Limnocardium BRUSINA, (MÜNSTER), M. trnskii (BRUSINA), 0a, b). Pebbles 0a,arePebbles b). well rounded and poorly sorted, Congeria praerhomboidea Congeria (PARTSCH), 1

The Upper Pontian (sensu STEVANOVIĆ) light-brown, fine-grained laminated sandy marls (a, b) and gray silts with large molluscan remains (c, d). Detailremains (c, molluscan fine-grained silts with large gray sandy marls (a, b) and light-brown, laminated (sensu STEVANOVIĆ) Upper Pontian The HANDMANN M. (= wolfgangfisheri NEUBAUER, HANDMANN M. (= wolfgangfisheri NEUBAUER, Figure 11. Figure assemblage (e). of the ostracod balatonica but therebut is an internal layering and the appearance cross of strat luscs (Fig. congerians is mostly molluscs, Recrystallized ification. of shells ofthe main characteristic of the section molluscs, ((Fig.10c-e). the following Among species the were recognized: ungulacaprae rugosa Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok HARZHAUSER, KROH, GEORGOPOULOU & MANDIC, 2014). Sporadicallywithin fossil fragments the can be observed.these, Above poorly cemented sand, pisoliths withconglomerates and gravelsoccur the with a large number mol of nucleus of Didacna chyzeri Didacna rugosa HARZHAUSER, KROH, GEORGOPOULOU & MANDIC, Biostratigraphically, the2014). section belongs to the “Lower it correspondsi.e. sensu Pontian”, STEVANOVIĆ to the Upper Pannonian between 8–9Nevertheless, Ma 2012). (MAGYAR & GEARY, Geologia Croatica HANGANU, SOKAČ, SOKAČ, dacito-andesites. Rock boulders and cobbles are sub-rounded and and sub-rounded cobbles are and Rock boulders dacito-andesites. quartzites, sediments, Cretaceous of clasts with conglomerates 44°43ʹ44ʹʹ, E No.13– wellas 20°29ʹ28ʹʹ as Fig. (N of1).breccias in consist They discovered were clastics inclined steeply 8),Fig.(see sediments Sarmatian the of section new described for Mt. road Avala the previously near close the to and Stream, sediments. colluvial and delluvial prolluvial- and valley Reka Zavojnička the along out cropping Vrčin)and 12 to up mthick. Resnik, Torlak, (Leštane, products colluvial and landslides old sporadically, and, sequences loess slope clastics, dium-grained covers the section. the covers 1m to up thick deposits proluvial-deluvial yellowish brown to ­c contains which thick), m 2 to (up silt sandy of layer yellow alight is there Above found. were this, fossil remains the where section the in level last the is It STEVANOVIĆ)age. (sensu Pontian” “Upper early an indicate especially) (ostracods fossils Pontoniella ­SU zalanyi Camptocypria 118 No.12 Fig. in 1; Fig. 12). 44°43ʹ44ʹʹ, (N sediments 20°33ʹ27ʹʹ E pre-Neogene – the as well as Miocene Mostly, various cover units. the they stratigraphic older over the widespread 15are to up They m. thickness, small have arelatively sediments Quaternary the area, studied the In deposits 4.1.6. Quaternary loess sediments (3),andtheHolocene delluvial-prolluvial clastites (4)andrecent (5). soilat thetop ofthesection Figure (1)andthe Pleistocene ofthesection delluvial-prolluvial 12.The between theblueish-gray clastites contact serpentinites (2)andslope inthebasalpart arbonate concretions of different sizes. Finally, the Quaternary Quaternary the Finally, sizes. different of concretions arbonate ZIN Above the right bank of the upper part of the Rakovica of Rakovica the part of upper the bank Above right the sediments alluvial by thin represented are Holocene deposits They include the Pleistocene proluvial/deluvial coarse to me to coarse proluvial/deluvial Pleistocene the include They ,

Thaminocypris Amplocypris bacevicae sp ., Lineocypris sp ., Lineocypris Loxoconcha cumsacui KRSTIĆ, KRSTIĆ, sp., Camptocypria sp., ., ., Camptocypria flectimarginata Camptocypria etc. (Fig. 11e). All determined 11e).(Fig. etc. determined All KRSTIĆ, KRSTIĆ, KRSTIĆ, KRSTIĆ, Cypria tocorjescui Serbiella Serbiella sp., L. schweyeri schweyeri L. sp., -

way, for the purpose of a future railway tunnel “Bubanj Potok”. “Bubanj tunnel railway of afuture way, purpose for the E75 high the to close Leštane, near hill ofthe top the at drilled were 1).Fig.(see They BT1-3) (BT1-2analyzed and been have shallow boreholes two additional an sections, and outcrops tioned aforemen the from data surface collected the to exception an As 4.2. Thesubsurfacedata Pannonian. early the during probably were generated clastics These bodies. (e.g. of clastic deposition processes with processes) proluvial gravitational predominant slopes and of steep formation terrain, of a denivelation in resulted which fault, Rakovica the around s vicinity of the Rakovica fault, it can be assumed that their gene their that assumed be it can fault, of Rakovica the vicinity the in found are clasts 13c).these (Fig. Since deposits these in included are fragments Sarmatian and reworked Badenian dant poorly ofa diameter sorted maximum <40 cm (Fig. 13a, b). Abun continental-lacustrine cycle of the early Miocene (DOLIĆ,continental-lacustrine 1997, the represent and thick m 7 to up Fm.) Slanci are (The member sands and ofconglomerates the coarse-grained variegated Bučvar ­Q and overlying Miocene the towards zone transition the ing of fragments different size,which represent serpentinite contain thick, 10m than 27–38 more m) interval depth (atthe breccias ­s The magnesite. with infilled are fractures These fractures. alot of reticulate contain and tectonized are serpentinites the ­p ­3 90 the within recognized were units stratigraphic different few A BT1-2 44°43 (N 4.2.1. Borehole is is related to the tectonic movements of structural blocks movements of structural tectonic the to related is is erpentinites are overlain by a package of hard serpentinized serpentinized of by overlain hard apackage are erpentinites 8–90 m), more than 50 m of dark to greenish serpentinized serpentinized greenish to dark of m 50 than more m), 8–90 eridotites and serpentinites were discovered. In the upper part, part, upper the In discovered. were serpentinites and eridotites uaternary cover. Transgressively on the serpentinized breccias, breccias, cover. serpentinized Transgressively the on uaternary

m of core log (Fig. 14). At the base of the well (depth interval interval (depth log well (Fig. 14). of ofm core the base At the ′ 10 ″ , E20°34 ′ 01 ″ ) Geologia Croatica 72/2 - - ­ - - Geologia Croatica - 119 ) ″ 36 ′ , E 20°34 ″ 19 ′ stone, a thina stone, crustlimestone Finally, of decompositionvisible. is loess-likecementedpoorly of m 6.5 to up core, of top the at the at sediments constitute the last stratigraphic unit. 4.2.2. Borehole (N 44°43 BT1-3 The second borehole, drilled in the vicinity (Fig. of 1), BT1-2 reached the ?Lower Miocene reddish Fig. seriessee – at a 1998 depth of 1997, 47 m DOLIĆ, Fm.; Slanci of Member Bučvar (the Stratigraphically, caneasilythesebecompared wells two15). in their uppermost metres.30 Herein, only three units were recog nized and, practically represents it the upper portions well of - sp., sp.) was Chlamys Lithotamnion sp.) and corallinacean sp.) alga ( arine transgression which occurred in this area. They consist poradically, only fragments mollusc shells could of be visible. epresents the lateral continuation the previously of mentioned Coarse-grained breccias and conglomerates with clasts of Cretaceous sediments, quartzites, dacito-andesites (a, b) and redeposited material from the from material quartzites,dacito-andesites redeposited (a, b) and sediments, Cretaceous of with clasts 13. Coarse-grainedconglomerates and breccias Figure Badenian and Sarmatian deposits (c). of of differentclasts of gravel, sandstones and carbonate rocks. ­S theTypical Leitha limestone with lot of molluscs ( Glycymeris the limethe topof At m. thefoundat depth interval 6.5–15.0 of similar sediments from the Bučvar and Rakovica surface,Middlestreamsthe the below m (see 20.2 at time,same the At 3). Fig. Miocene Badenian basal clastites (5.2 m thick) indicate the ­m 1998). 1998). There are no fossils identified within this unit which ­r Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok Geologia Croatica Many theMany age fossil Badenian confirm ( remains limestone). sandy Leitha the and sandstones and gravel tites, clas (basal unit Badenian marine by the m) represented is 4–43 interval (depthlog core the of BT1-2.part middle However, the Figure 14.Lithostratigraphic logofborehole BT1-2, ofLeštane. inthevicinity 120 Figure 15.Lithostratigraphic log ofborehole BT1-3,ofLeštane. inthevicinity Chlamys sp., Os sp., - ­ silty clays and loess sediments comprise the limestone cover. limestone the comprise sediments clays loess and silty (c.4 portion m), gray yellowish deluvial ofuppermost silts, thick ( tre Lithotamnion a sp., Conus sp.), etc. At the top of the drilled succession, the the succession, sp.), of drilled top Atthe etc. the sp., red algae, bryozoans, corallinacean algae algae corallinacean sp., bryozoans, algae, red Geologia Croatica 72/2 Geologia Croatica . - 2 121 The wider study area occupies approximately 140 km approachwas forced dueto circumstances but,in ourmind, useful. cause the Topčiderska Reka water course flows to the Sava River whereas the Zavojnička Reka runs to the Danube River. manyAt locations, secondaryE–NE directed streams have Morphologically, it canMorphologically, be divided into two parts: a composite hilly landscape consisting of the m) andHill Torlak Mt. (310 m) andAvala surrounding (511 low hilly area (200–250 m) that areboth dissected by theand ZavojničkaNNW–SSE Reka These valleys 16). (Fig. valleys represent striking Topčiderskathe principal drainage systems the study of area. the At same Reka represent Hilltime, a drainage and Avala Mt. Torlak divide be - - - The digital elevation model (DEM) of the studied area with the positions of the two main drainage systems (Topčiderska reka (Topčiderska reka) and Zavojnička as systems drainage main the positions of the two with area (DEM) of the studied model elevation digital 16. The Figure Japan Aerospace by provided data elevation original The 1. see Fig. the legend, of the main faults (1–4). For cross-sections with locations as the topographic well Agency (JAXA). Exploration tion of inclinationtion of layers, stress of as as well the analysis, etc.) morphological diversity the area of were the main reasons for geomorphologic consideration in order to try to identify the po neotectonic of sition active structures. tried to We support and connectpossibly the afore-mentioned stratigraphic results with geomorphologic observations the In relief. of addition, these observations are connected with an estimation the structural of elementsbased terrain ona DEM and model sys general(not analysis lineartematic) of structures. relief In other words, this 4.3. Geomorphology and some structural properties and some 4.3. Geomorphology area and its vicinity of the study The lack of quality informationstructural systematic elements (no measurements the direc of i.e. a small number of measured Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok Geologia Croatica ments of given length (~ 2km) and plotted on a rose diagram diagram rose a on plotted and 2km) (~ length given of ments seg line as measured were structures Recognized references. aforementioned the from taken were area wider the in timing and kinematics fault the measurements, rare authors the to addition In scale. map given atthe recognized were that features linear assump main The and of valleys river 2007). of orientation the control tectonic the was tion al., et MAROVIĆ 1996; TOLJIĆ, 1985; byis supported the facts known (e.g. MAROVIĆ & KNEŽEVIĆ, 17a) Avala (Fig. Mt. of which area wider the of terrain generated of digitally interpretation by the performed was systems fault the thewithin Mioceneunits,differentorientation analysis of the (Figs. 17ments 20). and sedi Miocene Upper the by filled ofsubsidence area the sents edge the defines of northern the Beli Potoktrough which repre Rakovica fault and its (Figs.17segments and 21). structure This Torlak directed E–W the well as as fault SW striking NE– the by controlled probably Torlak was block the of 1).(Fig. Uplift which has been elevated already since the early Upper Miocene of Torlak the by uplift conditioned block are tian-Quaternary Pon evolution during landscape and system drainage that gue (see Figs. 1, 17 controlled 21), ar to and reasonable is it turally Reka and Zavojnička Reka river flowsarethat obviouslystruc al.,et 2007; KOVACS al., et 2015 therein). references and neity or along exhumation the recent inactive faults (MAROVIĆ slopes affected area bythe study in either geological heteroge geologically conditioned of steep the instability suggest cesses (Fig. 12, northeastern slope of Torlak Hill). These sliding pro processes slope i.e.,movements, and/or creeping landslides slope gravitational active currently from sediments colluvial formed by covered recently are of streams the lowerthe parts (Fig. slopes some 16,places, In 1–4). Profiles southern steeper and sides northern dipping gently with valleys asymmetric 122 based onlinearlengthsofapproximately 2km. (1985), TOLJIĆ (1996)andMAROVIĆ etal. diagram (2007);b)Rose plotted from themap oflinearstructures. Measurements oftheorientation offaulttraces were Figure oftheorientation inthebroader oflinearstructures 17.a)Map studyarea. units separated faultsandneotectonic Main according to MAROVIĆ &KNEŽEVIĆ Except for some individual measurement of faults and strata strata and of faults measurement forExcept individual some Topčiderska observed the as well as data relief these on Based ------21). Besides this orientation, faults which were reactivated in the the in reactivated late Miocene or were stage neotectonic (see Fig. which 18), faults exhibit a direction orientation, this 21). Besides and 20 (Figs. developed were movements vertical pronounced with block the structures faults –WSW oriented ENE along these 17a)(Fig. system F1and the from faults older the of dissection for the responsible are They system. this within recognized are Beli Potok (BP) Torlak (RF), and Rakovica the (TO)area, faults study the In 2007). al., et b). (MAROVIĆ inversion tectonic quent (Fig.17a, direction NE-SW subse and regimes by extensional controlled were events These pronounced a with direction WSW ENE- general a reflects orientation system faults (F2) The sin. ba evolution later of Pannonian and the formation the to related et (MAROVIĆ is (F2) reactivated system fault were Fig.second 18).younger, see 2007; al.,The faults these events tectonic later the 2016). (TOLJIĆ, During area study the in formations ogene pre-Ne the in documented best are events these to related tures 2018).al., et Struc (TOLJIĆ Peninsula) Balkan the of part tral obduction, (along cen the – SE strike NW ageneral with and Jurassic Dinarides the post as of units innermost the within interpreted thrusting and faulting scale large classically is collision This 2007). al., et (MAROVIĆ times Paleogene and Cretaceous Late during happened that processes collisional the from inherited a (Figs. reverse character 1, 16, 18 and 21). system is This mainly show and regime compressional the in reactivated were of them belong to this system. Later, time, some from the post-Sarmatian faults (KF) Kaludjerica and (ZF) Reka Zavojnička (TR), Reka Topčiderska the area, fault study 17a,the (Fig. b). In the direction of SE – trends main two the network. First, the (F1) 1985; fault indicates system is generally oriented in a NW 2007) KNEŽEVIĆ, & al., et (MAROVIĆ MAROVIĆ Avala Mt. of area wider the in of water flows,etc.) as wellas the main fault categories separated turns sharp and of slope changes angles, of valleys, river entation (Fig.

1 7b). The statistical interpretation 7b).of (ori the features interpretation The linear statistical Geologia Croatica 72/2 ------Geologia Croatica ------123 New research findings collected in this study have shown shown have study this in collected findings research New matically and spatially correlative with those previously recog nized within the Pannonian basin and its southern margins (e.g. BADA et al. 2007; MATENCO & TOLJIĆ 2018). et al., RADIVOJEVIĆ, 2016; TOLJIĆ, 2012; 5. DISCUSSION AND INTERPRETATION AND DISCUSSION 5. TheMio-Pliocene tectonic framework the study of area is con trolled the by processes at the southern margin the Pannonian of basin (MATENCO & RADIVOJEVIĆ, BALÁZS 2012; et documented al., well processes arethese As 2018). al., et SANT 2016; in the central part the basin of based on subsurface data (HOR VÁTH et al., 2015, MATENCO et al., they could be inferredetc.) 2016, the for area Avala. Mt. of BALÁZS et al., 2017, that the oldest continental-lacustrine sediments Bučvar (e.g. areclastites) present larger over areas than previously known (clastites are found in the vicinity of Leštane insufficient andinformation is there Resnik, however, see study, thisIn 19). Fig. about the sedimentary conditions in which they were formed, especially since these deposits are mostoften destroyed sub by sequent erosion processes (DOLIĆ, 1997). During the well- known Badenianmarine transgression, a Paratethys was bay established in which the wider area Avala Mt. north today’s of includes Torlak, Leštane and its vicinity Mt. (Fig. 17). Avala representssignifi aIts unique1985). KNEŽEVIĆ, & horst(MAROVIĆ Mountain smaj including the block ofSarmatian follow present early when, differentiationthe begins cantin day Ko ing the faults NE-SW of directions, and E-W the subsidence and formation of smaller bays and troughs flooded by the watersof Paratethys were carried out. Such characteristics are reflected in the local structural units in the eastern section the studied of area, i.e., the Ripanj, Ralja and (MAROVIĆ & KNEŽEVIĆ,In Sopot that sense,1985). our findings bays; see Fig. 17 new Sarmatianof sections and outcrops in the area the Ra of streamkovica valley are important to support analogous sce narios in the northwesternpart the study of area. The Beli Potok trough is similar, which subsided later in the late Pannonian and - ­ - - - - In the study area, there is measured no the fault that follows ar orientation NW-SE the large of fault structures observed in Comparative lithostratigraphic columns of the boreholes around Mt. Avala. The data concerning the KGK boreholes are taken from KNEŽEVIĆ (1989, taken from are boreholes the KGK concerning data The Mt. Avala. around of the boreholes columns lithostratigraphic 19. Comparative Figure 1. see Fig. of boreholes, the location 1990). For l siliferous sands and limestones This (Fig. 18). structure with a measured dip direction and dip is angle part the of fault (214/48) the reverseof faults which were reactivated in the NE-SW ori ented compressional stress-field.Faultsof this direction are sta tisticallyrecognized faultfirst linear structurestheas belong that Furthermore, structurethis simi(F1). systemcorrespondsthe to the study area such as the Topčiderska reka and Zavojnička reka faults (Figs. 20 Also, and this21). system of structures is kine similar to the F1 structure and they outline block structures in 21). the studied 17, area 1, (Figs. late Miocene post-rifting subsidence and Pliocene compressional tectonics. a However, nice example is Avala found Mt. inof kmsouthwest 20 Boždarevac (N 17a), Fig. – 20°22ʹ41ʹʹ E 44°32ʹ27ʹʹ, where there is pinpointedfault a along which resultedmovement the Sarmatian of metres) to 2.5 in fos vertical displacement (up The reverse fault within the Sarmatian sediments as a consequence consequence as a sediments fault within the Sarmatian reverse 18. The Figure south Miocene-Pliocene tectonics Boždarevac, (village of Late compressional west of Mt. Avala). west Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok Geologia Croatica (190.8 ­c are findings new these Furthermore, 1985). KNEŽEVIĆ, & r the previous investigations and indicate more than a hundred met ahundred than more indicate and investigations previous the confirm findings new These discovered. were czjzeki Congeria well-known with marls Pannonian younger (210 the m.a.s.l.), sandy marls was discovered (Fig. 20). Some 300 to m east further inclined andsteeplythe sand Lower Pannonian and fine-grained marls laminated Sarmatian slightly dipping the between section Avala transitional the the near road, Stream of Rakovica the bank Namely, Potok of Beli left trough. the the on characteristics and nature the on have emerged but insights new authors, mentioned ed out Figure 20.The generalized geological through cross-section Potok theBeli trough (modifiedandupgraded STEVANOVIĆ, after 1951).Numbers indicate thestudi m and Cretaceous Middle sedi Miocene and Badenian Sarmatian of Torlak The (horst) composed is deposits. Hill Pontian the underlying marls Pannonian of are base Torlakthe there Hill, z overlie Meso the of lower discordantly the Pontian sediments the Mt. Along Avala slightly folded ashallow syncline. are itself, in which Neogene deposits in (1977b), trough itasymmetric is an STEVANOVIĆto According sediments. (1951) EREMIJA and m (310 Miocene Upper with Hill filled Torlak structure and tectonic a.s.l.) local m a a.s.l.) is a.s.l.) (511 m (224 Avala Mt. trough Potok between Beli The situated 20). (Fig. trough Potok Beli STEVANOVIĆ the which (1951)as trough, the distinguishes Torlak the from horst separates locally which noticed was fault the 1931) Rakovica the LASKAREV, so-called the (e.g. structure, of linear alarge existence studies previous the In blocks. cal movements the are differential there lo ofthe faults separating unit Avala the structural within because structure interesting of point view, an is Beli PotokFrom The trough a geodynamic 17).Fig. 1985; see KNEŽEVIĆ, & (MAROVIĆ area derevo Grocka-Sme the towards east, the to directed and reduced was trough Potok Beli the Pontian, the during 17).Fig. Later, 1985; see – 2007 al., et KNEŽEVIĆ, MAROVIĆ & 1990; MAROVIĆ, & (MAROVIĆ DJOKOVIĆ trough Morava Velika the of parts southwestern the in located blocks uplifted of the quence conse STEVANOVIĆ)a 17,(sensu (Figs. was Pontian 20).It 124 es es of vertical movement of the blocks in this area (e.g. MAROVIĆ oic palaeorelief (Fig. 20). at contrast, In part, the in northern rooae wt te rvosy tde brhl KGK-14 borehole studied previously the with orroborated ents. ents. Our research has generally confirmed theview oftheafore confirmed generally has research Our crops that are located neartheprofile line. For thefaultskey, see Fig. 1.Note:Scaleis adapted to better illustrate thegeological relationships.

m a.s.l.) from the Rakovica downstream fault line (Fig.19). ­ - ­ ­ - - - 2007). Due to differential rock uplift in the vicinity of the Beli Beli the of vicinity the in uplift rock differential to Due 2007). boundary Mio-Pliocene the to phase) continued which (the post-rift time post-Badenian in began movements vertical significant the area absolute m 1000 and altitude 900 (KNEŽEVIĆ et al., 1994). between This means i.e. that m, in the 1100 study and 1000 between of Velika the atdepths Morava trough) structure peripheral local (the depression Grocka the in drilled age were of same Rocks the 300m. above altitudes at located are sediments Badenian the of Mt. Avala. part Torlak wider On the in Hill activity tectonic of the evidence as taken be can blocks subsided and elevated the in deposits of Miocene the altitude absolute and position spatial contemporary 2015). The al., et SUŠIĆ 2007; al., et (MAROVIĆ of development phase a continental of Serbia) experienced part Šumadija day (the present realm Peri-Pannonian PB the the and 1985; &KNEŽEVIĆ, (MAROVIĆ MAROVIĆ al., et 2007). area Grocka-Smederevo the in one northern the to connected was Miocene, in the Beli Potok area there was a Lake Pannon bay which Late the STEVANOVIĆ).(sensuduring Palaeogeographically, between the late to occurred trough Pannonian the late “Pontian” Potok Beli the in sedimentation that and Pannonian early the to thathave the confirmed formation ofthe Rakovica fault is related work this within 1989; data Fig. 19). collected KNEŽEVIĆ, The – 110m than more is KGK-14boreholedifference (the in age and the ofon marls marls the surface the Upper Pannonian same of of layers the the of altitude absolute the comparison on based determined movement was this addition, 100 In m. than more is fault Rakovica along the sediments of aforementioned ment the (Fig. 19).?Lowerof Miocene displace the clastites vertical The and the limestone overlie Bučvar marl, Sarmatian the Pannonian sediments Pontian KGK-13(187holethese a.s.l) m Resnik bore near At 19). KGK-15 (Fig. borehole e.g. Pinosava, of area the in rocks overdeposited palaeorelief the ofCretaceous and Jurassic 19). were Fig. sediments Pontian see similar – that discovered it 1989 was Besides, (KNEŽEVIĆ, m 155 about of depth a at sion, succes drilled the of portion lower the in Pannonian Upper the (sensu 105 of and m depth a to Pontian down Lower determined were STEVANOVIĆ) and Upper the of sediments which in Potok Beli trough the out within carried was drilling The During the Pliocene and Quaternary, the southern margin of margin southern the Quaternary, and Pliocene the During

(MAROVIĆ & KNEŽEVIĆ, 1985; al., et MAROVIĆKNEŽEVIĆ, & (MAROVIĆ Geologia Croatica 72/2 - - - ­ Geologia Croatica - - - 125 In respect the geomorphologic of properties the unusual of middle Miocene, represents together block, it with the a Torlak horst structure that extended (MAROVIĆ southwards et al., 2007). The to block, Torlak which is situated Mt. Kosmaj is covered withnorth pre-Badenian Avala, Mt. of and Badenian sediments at about 300m a.s.l. It indicates the upward relative that the block of movements started at the the end Sarmatian of and continues to in recent boreholes nearfew a times (e.g. Leštane) (MAROVIĆ & KNEŽEVIĆ, RUNDIĆ 1985; et al., The presence2017). of the2015, pre-Badenian clastics in a few boreholes in the area of Resnik at depths below 100 m (the west ernmost part the trough) Beli of where Potok the they overlie Mesozoic rocks support this fact KNEŽEVIĆ,(e.g. The 1989). is formedblock the along movements by Rakovica fault system (RF) 20). fault (Fig. and the Torlak we block,Torlak Reka near of the Zavojnička the flow/geometry documented have data.don’t But, based on some observations by MAROVIĆ & KNEŽEVIĆpotentiallyassociatedbe upliftratherwithof couldfast it (1990), (1985) and DJOKOVIĆ & from block the MAROVIĆ Pliocene tothe recent Torlak time. According to DJOKOVIĆ & MAROVIĆ (1990) and TOLJIĆ (2006, 2016) and the documented structural measurements of differentMesozoic the by controlled is Reka units in study the area, Zavojnička the local fault system with its N-NW to S-SE direction. After the “Pontian” cycle of sedimentation (Late Pannonian, Latest Mio Topography was generated from data provided by the Japanese Aerospace Explora the Japanese Aerospace by provided data from generated was Topography ­ - - - - The neotectonic the map study of area constructed in this nts on the slopes of Mt. areAvala “Pontian” clastics which irectly overlie the Mesozoic rocks (Fig. During20). the early me ­d Potok trough,Potok late Miocene sediments located at higher altitudes were destroyed erosion. by The younger and softer sediments, less resistant to abrasion,As a wereconse eroded12). Fig. (see Neotectonic sketch map of Mt. Avala and the surrounding area (modified after DJOKOVIĆ & MAROVIĆ (1990), TOLJIĆ (1996) and MAROVIĆ et al. (2007).TOLJIĆ MAROVIĆ et al. (1996) and MAROVIĆ (1990), & (modified after DJOKOVIĆ area and the surrounding map of Mt. Avala 21. Neotectonic sketch Figure KAfault, – Kaludjerica –ZU and fault Torlak – RekaTO Reka– Zavojnička ZR fault, fault, Topčiderska – TR fault, Rakovica RF – Beli– BP fault, Potok Abbreviations: references. the mentioned taken from of the faults are Traces Note: fault. Zuce tion Agency (JAXA). quence, the youngest Neogene deposits created during the late Pannonian (the latest Miocene, Pontian sensu STEVANOVIĆ) were preserved only at theOngoing Fig. 19). rock peaksuplift 1990; borehole isKGK-16, docu of the lower hills (KNEŽEVIĆ,mented at the peaks around the Zavojnička Reka valley and Leštane, where the Mesozoic ultramafiteswere (e.g. discovered Leštane and its vicinity – unpublished data). This is confirmed within this study, in the analyzed boreholes and BT1-2 BT1-3 where the Bučvar clastites and the Leitha limestone cover the serpentinites. Based on these observations, can it be assumed that a significant part of the ocenestudied and Pliocene sediments. area was covered by different Mi different kinematics thewith from blocks comprisesseveral work prominenttopographicmost The 21). (Fig. present the to Miocene definedis block Avala The Avala. the is studiedareathe featureof by the Topčiderska Reka (TR), Beli Potok (BP) and Zuce faults (ZU).The presence the lateMiocene of sediments theon moun tain slopes suggests that this structural unit was uplifted during Sarmatian times. This is based on the fact that the youngest sedi Rundić et al.: Stratigraphic implications of the Mio-Pliocene geodynamics inthe area of Mt. Avala: new evidence from Torlak Hill and Beli Potok Geologia Croatica of uplift of trend this blocks. Generally, individual as started uplift their and W-SW to Torlak the system fault E-NE by from an horst arated Avala the (Sarmatian) sep horst Miocene Middle late the During place. took deposition troughs–bays, local its and zones horst It highs. marginal e.g.Kosmaj the in and parts, some but in of denudation, area an was the Torlak including structure horst unified the represented it Miocene, early the In activity. showsdifferent Avala Neogene, the the horst through All deposits. Miocene edge of the on and dunites), and peridotite mafites (serpentinite, ultra ofbelt eastern the volcanites), in Tertiary and Cretaceous Upper by up broken (sometimes sediments 2007, al., rassic–Cretaceous et (MAROVIĆ trough Ju pre-Neogene, from 21).mostly Figs.17built and see Morava was It Velika the towards those are striking most of the which phase syn-rift the to related faults sides by extensional all on it constrained is and meridionally, 1985; MAROVIĆ et al., 2007). The Avala horst is oriented almost KNEŽEVIĆ, & (MAROVIĆ south the in Stojnik and Sopot the to north the in rivers Danube the Sava and the from extends zone aforementioned the in structure Avala largest The the as horst (or older faults ones). the remobiled Mio-Pliocene E-W) striking (partially of NE-SW blocks by systems smaller into dissected was unit structural Avala-Orešac the (2007), al. et MAROVIĆ (1996,2016)(1985), and TOLJIĆ KNEŽEVIĆ & MAROVIĆ to & According (MAROVIĆ 2007). al., et structure MAROVIĆ 1985; KNEŽEVIĆ, blocky by characterized unit Torlak hills and Mt. Avala belongs to the Avala-Orešac structural of the area the Serbia, of NW part and of Šumadija settings tonic that can further support these interpretations. these support further can that area studied the within section no seismic is there fortunately, ( Sava half-graben) (e.g.Mt. Gora Fruška of south observed structures similar with correlative spatially and kinematically is trough This time. nonian Pan in late started subsidence the that indicates blocks Superpo bouring Reka. Topčiderska the neigh the and trough the and within sition of Neogene formations the Zavojnička towards flowing of valleys creeks several it comprises Morphologically faults. tok Po Beli and Rakovica by the blocks. It formed is tively uplifted enian sediments are present on the surface at an altitude of around of around altitude atan surface the on present are sediments enian about 210 Atmetres. the same time, at the top of Torlak Hill, Bad of altitude atan surface atthe found are marls Pannonian same foot of atthe Torlak the Hill, northeast, the away towards metres hundred few a However, only metres. 100below altitudes lute at abso marls Pannonian are below there “Pontian” deposits the KGK-14,borehole the in For example, 200m. to up of fault vica Rako the along displacements vertical significant exhibit They geological block structures. important most the are Potok trough n geo Mio-Pliocene the following concerning conclusions the interpretation, well their as as results obtained the all on Based CONCLUSIONS 6. (Fig. 21).established along which new the flowofmation new, the was local structure for the to led Torlak. activity away from This E-NE, the wards the Zavojnička Reka changes its to flowfromandturns SE-NW progressed, TorlakofHill uplift the as time, that 1985).During KNEŽEVIĆ, & (MAROVIĆ began formation relief of phase cene) the Avala between blocks, the fluvial and Torlak structural 126 amics and its consequences can be drawn. be can consequences its and amics From the structural point of view and according to the tec the to according and view of point structural the From In the studied area of Mt. Avala, area Torlak the Beli studied and the horst In rela two these between situated is Potok Beli trough The

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