(PDF) Quaternary tectonic and depositional evolution of eastern Srem (northwest Serbia)

GEOLO[KI ANALI BALKANSKOGA POLUOSTRVA 75 43–57 BEOGRAD, decembar 2014 ANNALES GÉOLOGIQUES DE LA PÉNINSULE BALKANIQUE BELGRADE, December 2014 DOI: 10.2298/GABP1475043T Quaternary tectonic and depositional evolution of eastern Srem (northwest Serbia) MARINKO TOLJIĆ1, DRAŽENKO NENADIĆ1, UROŠ STOJADINOVIĆ1,3, TIVADAR GAUDÉNYI2 & KATARINA BOGIĆEVIĆ1 Abstract: The area of eastern Srem is situated in the southern periphery of the Pannonian basin. Its depo- sitional evolution during the Neogene and the Quaternary has been controlled by tectonic processes. Miocene extensional subsidence was followed by the Pliocene-Quaternary inversion of the basin. The latter was accomplished as the result of replacement of the tensile by the compressive stress field. Since the Late Neogene, the regional tectonic activity has been controlled by compressive stress produced by the north- northeastern propagation of the Adria microplate. In the compressive NE–SW-oriented stress field, the recent structural plan of the Pannonian basin and its wider environment, including its southern periphery, was reac- tivated. The youngest tectonic deformations are characterized by positive and negative vertical motions of large intrabasinal segments and basinal periphery, resulting in the final inversion of the basin. The effects of the basinal inversion can be recognized in genetic features of Quaternary sediments and geomorphological characteristics of the relief. Sources of data used for the interpretation of the Quaternary tectonic activity in the area of eastern Srem are of geological, geomorphological, thermochronological, and geophysical charac- ter. The positions of prominent fault structures have been ascertained by remote sensing, interpretations of available geophysical cross-sections, and using the field data. Key words: tectonic activity, Pannonian basin, northwest Serbia, subsidence, basin inversion, eastern Srem, Quaternary. Апстракт: Подручје источног Срема налази се у јужном ободном делу Панонског басена. Његова депозициона еволуција током неогена и квартара била је контролисана тектонским процесима. Ми- оценску екстензиону субсиденцију, прати плиоценско-квартарна инверзија басена. Инверзија басена је изведена као последица смене тензионог напонског поља са компресионим. Касно-неогена и рецентна тектонска мобилност контролисана је компресионим стресом, генерисаним север-североисточном пропагацијом адријске микроплоче. Рецентни структурни план читавог Панонског басена и његовог ширег окружења, укључујући и јужни обод, реактивиран је у домену компресионог напонског поља, оријентисаном по правцу североисток–југозапад. Најмлађе тектонске деформације карактерише по- зитивна и негативна вертикална мобилност значајних унутарбасенских сегмената као и периферије басена, што је резултирало финалном инверзијом басена. Ефекти басенске инверзије препознају се у генетским карактеристикама квартарних седимената, као и у геоморфолошким карактеристикама рељефа. Извори података који су коришћени за интерпретацију квартарне тектонске активности у подручју источног Срема су геолошког, геоморфолошког, термохронолошког и геофизичког карактера. Позиције значајнијих раседних структура утврђене су даљинском детекцијом, интерпретацијом ра- сположивих геофизичких профила и на основу теренских података. Кључне речи: тектонска мобилност, Панонски басен, северозападна Србија, субсиденција, басен- ска инверзија, источни Срем, квартар. 1 University of Belgrade, Faculty of Mining and Geology, Department of Historical and Dynamic geology, Kamenička 6, 11000 Belgrade, Serbia. E-mails:

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2 Geographical Institute „Jovan Cvijić“, Serbian Academy od Sciences and Arts, 11000 Belgrade, Djure Jakšića 9, Serbia, E-mail:

3 Netherlands Research Centre for Integrated Solid Earth Science, VU University Amsterdam, De Boelelaan 1085, 1081 HV Amsterdam, The Netherlands 44 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ Introduction Carpathians. It is filled with Neogene and Quaternary deposits. The basement of the basin is formed by the In the area of eastern Srem during Quaternary peri- tectonic units of both Adriatic and European continen- od tectonic activity has been manifested as a signifi- tal affinity: the Dinarides (as a part of Adria), Tisza cant control factor of deposition and final shaping of and Dacia (as parts of Europe), and also tectono-strati- modern relief (MAROVIĆ et al. 2007). However, tec- graphic contents that belong to the Sava zone (as a tonic evolution of the Pannonian basin has started suture between Adria and Europe, SCHMID et al. much earlier, hence all tectonic structures that have 2008). The territory of Serbia includes the southern- been active in Quaternary, are actually a part of previ- most parts of the Pannonian subsidence area repre- ously existing structural pattern and they belong to the sented by basinal and peribasinal structures, and category of inherited structures. Furthermore, sedi- deeply penetrated towards the south between Dinaric mentation as a dominant process of final phases of and Carpatho-Balkan morphostructures (MAROVIĆ et filling of an inverted depositional basin, took place in al. 2007). Neotectonic movements formed some inter- previously tectonically defined domains (MAROVIĆ et esting structural, depositional, and morphological fea- al. 2002, and other references therein). tures that are different from those in the other parts of During the younger stages of Pliocene and earlier the Pannonian basin. part of Quaternary, after the retreat of Paratethys, the In the recent literature, there are interpretations that area of the southern rim of the Pannonian basin in the southern boundary of the Pannonian basin in whole passed through the terrestrial phase of devel- Serbia is formed by the rivers Danube and Sava, while opment (NENADIĆ et al. 2010, 2011). In that interval the areas south of them, made of Neogene deposits of tectonic shaping of low intensity has been carried out, similar or same composition as those in the Pannonian by which regional morphostructural forms were basin, belong to the peri-Pannonian area. Although finally shaped. Also, tectonically controlled mobility this boundary has a certain geographical and geomor- within basinal segments caused the absence of some phological sense, from the geological point of view it stratigraphical substages of Pliocene, and change of is difficult to place it here, since the basin boundary is facies and thickness of the youngest lithostratigraph- situated further south of the Sava and Danube. ical units (MAROVIĆ et al. 1996, 1998; RAKIĆ et al. Locally, the investigated area belongs to eastern Srem, 2005). limited by the Danube and Sava from the north, east In the southern parts of the Pannonian basin, and south, and by the line Sremska Mitrovica–Neštin Pliocene-Quaternary tectonic activity was manifested from the west (Fig. 1A). in gradual, continuous descending of extensional Identification of structures in the investigated part areas in Posavina toward the interior parts of the of the area, as well as monitoring of their activity dur- Pannonian basin and in uplift of the area of the Fruška ing the youngest tectonic phase, was carried out on the Gora massif, Belgrade promontory and some parts of basis of palaeogeographical, structural, thermochro- Šumadija (MAROVIĆ et al. 2007). This vertical mobil- nological, and geophysical, characteristics of this ity brought significant changes in relief and initiated area. When reconstructing the tectonic evolution, be- the development of exogenic denudation-accumula- side the remote sensing analysis, the data from the tion processes. exploration wells and field data have been used as The postbasinal structural complex, formed in a well as reinterpretation of available seismic sections. post-Neogene phase, is represented by a relatively thick sequence of sediments within which two parts, differing in superposition and origin, can be distin- Material and methods guished (NENADIĆ et al. 2003, 2009). – older, fluvial and fluvio-lacustrine, with relics of The positions of prominent fault structures in the basinal frame, generated by movements on the bound- investigated area have been ascertained by remote ary between Pliocene and Quaternary, which were sensing, interpretations of available geophysical manifested in a poly-phase lowering of the former cross-sections, and using the field data. The field data basin bed and formation of complex alluvial plains of were obtained by the analysis of numerous borehole the pre-Danube and pre-Sava. cores situated in the investigated area. The mineralog- – younger, which corresponds to the fluvio-denuda- ical and petrological composition of these samples has tion system s.s., and which comprises morphological been preliminary analyzed. Remains of molluscs and structures made in the Late Pleistocene and Holocene. ostracodes have been picked out under a binocular microscope and determined to the level of species when it was possible, using the qualitative methods. Geological settings When no fossils were available, the age of deposits has been estimated by the so-called superposition The Pannonian basin is an intracontinental entity principle. situated between the Dinarides, the Alps, and the Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 45 Fig. 1. A, Geographic position; B, Simplified geological map of the study area with localities where samples for new (U-Th)/He apatite thermochronology ages (AHe) werecollected. Results and discussion sphere in the basement of the Pannonian basin, wrin- kled in kilometer-scale folds, was thinned (CLOETINGH Quaternary tectonic mobility et al. 2006). The regional folding of lithosphere was accompanied by vertical mobility of segments of the Quaternary tectonic activity of the southern parts of lithosphere, of different direction and intensity, which the Pannonian basin has been perceived in context of finally resulted in a relatively rapid uplift and denuda- the regional Miocene extensional evolution of the tion of the peripheral parts of the basin and further entire basinal area and its Pliocene-Quaternary inver- subsidence and deposition of the central domains of sion (e.g. HORVATH et al. 2006; MAROVIĆ et al. 2002; the basin. At the same time the existing tectonic pat- MAROVIĆ et al. 2007; MATENCO & RADIVOJEVIĆ 2012 tern was reactivated by local redistribution of com- and other references therein). Miocene extension, pro- pressive stress. This pattern was responsible for the duced by rollback of European lithosphere in the Car- control of tectonic mobility within basinal entities, pathians, was accompanied by rifting, thinning of the such is the area south of Fruška Gora (TOLJIĆ et al. lithosphere and subsidence in the domain of the Pan- 2013). Regionally, in the Pannonian area, to the north nonian basin. A long-term Middle and Late Miocene of the Danube and Sava slow subsidence has been post-rift subsidence, controlled by thermal sag cool- continuing throughout Quaternary, but with smaller ing (HORWATH & CLOETINGH 1996; CLOETINGH et al. velocity than in Neogene and with a constant tenden- 2006), was followed by the Pliocene–Quaternary ba- cy of weakening until recent time. In contrast to this sin inversion, performed in compressive stress field. sinking, peripheral part of the Pannonian basin and The extensive stress field was replaced by compres- intrabasinally situated morphostructure of Fruška sion, which was activated as a result of the final break Gora have been raised. off of the subducted European lithosphere in the do- Quaternary tectonic activity can be identified by main of the Carpathians, on one side, and the north- studying the origin and thickness of sediments. Of northeastern progression of the Adria plate, on the particular significance here are pre-loess fluvial poly- other side (BADA et al. 2007). During Pliocene and cyclic deposits in the southern and deluvial-proluvial Quaternary, both the Dinaric-Carpathian orogen and sediments in the northern part of the area. Geomor- intracontinental Pannonian basin were exposed to phological data, such as hypsometric relationship, po- constant compression, generally oriented towards sition of fluvial terraces, process of erosion, etc., also NE–SW in this region (BADA et al. 2007). Under these point to tectonic changes. Also, information on geo- conditions the lithologically heterogeneous litho- detic measurement and seismic activity are of special 46 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ interest. Furthermore, thermochronology can yield in- compression oriented in general direction NE–SW. formation on the exact timing of the tectonic activity. Recent mobility of the Earth’s crust in the area of the Pannonian basin has been confirmed by geodetic measurements (JOVANOVIĆ 1971, FGS 1972). The ge- Basic geophysical characteristics of the neral model of vertical mobility of the Earth crust in investigated area the domain of the southern parts of the Pannonian ba- sin suggests that the northern periphery of the investi- Seismicity represents one of the most relevant fac- gated area (the area of Fruška Gora) has been raised tors in detecting recent fault activity in the Pannonian by the rate up to +2 mm/year (MAROVIĆ et al. 2002; and peri-Pannonian region (MAROVIĆ et al. 2002). On MAROVIĆ et al. 2007). The peripheral northeastern the basis of existing data it can be concluded that the parts of the Dinarides show a similar trend. Recent Serbian part of the Pannonian basin shows very low subsidence (by the rate of approximately 1 mm/year) seismicity, with exception of the Fruška Gora massif has been ascertained in the area of Srem (Map of re- and the area of eastern Banat. Particularly, these areas cent vertical movements of the Earth’s crust in the are characterized by quakes of magnitudes which do area of SFRJ, FGS 1972, MAROVIĆ et al. 2002, MARO- not exceed M=4.5, except the area of Fruška Gora VIĆ et al. 2007). The most recent geodetic study of the (M=4.5–5) and a part of eastern Banat. In the Serbian Earth’s crust mobility in the southern parts of the part of the Pannonian basin the most seismically active Pannonian basin shows a low level of mobility in the faults are of direction NW–SE, representing structures area of Srem (SUŠIĆ 2013). Isolines map is (Fig. 2) across which there have been transcurrent left move- showing rates of vertical tectonic movement in the ments, with a pronounced reverse component (MARO- area of Srem. Fig. 2. Map of velocities of the recent tectonic movements in the area of Srem (modified after MAROVIĆ et al, 2002). VIĆ et al. 2002). Southern periphery of the Pannonian In the sections of seismic profiles in the area of basin belongs to a seismic active region in Serbia, with Fruška Gora (MATENKO & RADIVOJEVIĆ 2012) in the maximum magnitude M=5,5–6. Southern periphery of south of the mountain an association of faults that the Pannonian basin and its immediate hinterland are form the Vrdnik fault could be recognized (TOLJIĆ et characterized by seismically active, transcurrent right al. 2013). The southern block was primarily gravita- faults of direction NE–SW (ENE–WSW). These two tionally downthrown across this structure, so the systems of conjugated faults are further active in the thickness of Pliocene-Quaternary sediments to the compressive stress field which has an axis of maximum south of the fault exceeds 500 m. The synthesis of the Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 47 data obtained by seismic profiling and deep explora- highlighted. This was accompanied by a rapid erosion tion drilling in this area, also indicates the significant of the uplifted parts and an equally rapid accumula- thickness of Pliocene-Quaternary sediments (MARTI- tion in the neighbouring lowered domains. Conse- NOVIĆ et al. 2010). The greatest thickness is observed quently, recent morphostructural and morphosculptur- between Stara Pazova and Šabac, in the depression al appearance of this massive is a reflection of causal- whose axis lies in the E–W (ENE–WSW) direction. ity and interaction of numerous processes, of both While the Vrdnik fault is situated in the northern endogenic and exogenic origin, so the recent geomor- periphery of the depression, central parts of the area phological features represent the result of complex are controlled by an association of horsts and grabens morphogenesis of this mountain. defined by the faults across which the central part of In the Early Miocene, the metamorphic core of the the Sefkerin depression was downthrown (MATENCO mountain was primary exhumed from the ductile do- & RADIVOJEVIĆ 2012). The southern periphery of the main across the zone of decolman shear, situated at investigated area in seismic section shows a compli- the boundary of metamorphic and underlying Meso- cated tectonic nature of a transitional region between zoic non-metamorphosed tectono-stratigraphical con- the Pannonian basin and its uplifted southern hinter- tents. Further extensional deformations in the brittle land. The Kalemegdan fault (as association of faults) domain were performed in Middle and Late Miocene stands out as a dominant structure. It is a syndeposi- across the gravitational faults, which are now situated tionally active fault(s), across which subsidence of the in the northern and southern slopes of the mountain NW domain has continued to take place in Quater- (TOLJIĆ et al., 2013). Finally, in the Pliocene and the nary, as suggested by the significant thickness of the Quaternary, the Dinaric-Carpathian system entered youngest sediments. This scenario is also indicated by into compression while the Pannonian basin was pro- a relatively small thickness of Pliocene-Quaternary gressively inverted and filled by Plio-Quaternary ter- sediments to the east of this fault. In a planar view, the restrial sediments. Differential vertical motions of association of faults which constitute the Kalemegdan block structures led to intensification of erosional pro- fault consists of echeloned faults with the NE–SW cesses and final modelling of an asymmetrical horst direction that may be followed from Kalemegdan structure surrounded by Quaternary deposits of Srem across Obrenovac and further to SW (Fig. 4). and Bačka plains. The uplift that began at the end of Pontian reached its maximum at the Pliocene/Pleistocene boundary, Geomorphological analysis when across the existing E–W directed faults remobi- lization occurred, characterized by asymmetrical rota- Effects of Quaternary tectonic movements can be tion of the Fruška Gora block. This is recognized in considered by studying morphogenetic characteristics stronger uplift of the southern edge of the massif, re- of the area and sedimentological features of deposits. sulting in high hypsometrical position of the mountain The former include forms of relief, dynamics and ori- range. gin of river valleys, sharp de?ection of river valleys Throughout the Quaternary time, the activities etc., while the later can be obtained by analysis of along these faults continued in the peripheral parts of thickness of facies and types of sedimentation. the recently formed Fruška Gora horst, particularly In the investigated area, three units can be clearly mobile being the zones of the Vrdnik fault, Karlovac distinguished by the shape of relief: 1) hilly northern dislocation and Čortanovci transverse fault. The Da- part, which belongs to the positive morphostructure of nube fault, whose trace coincides with the riverbed of Fruška Gora showing constant uplift trend, 2) transi- the Danube, along with the above mentioned faults, tional part, which corresponds to the higher fluvial played a key role in the formation of the Fruška Gora terraces of Pleistocene age, and 3) the lowland part of horst, around which very specific genetic categories the Sava valley with lower terraces, which are un- of Quaternary sediments were deposited. doubtedly situated in the area of significant, tectoni- After the intensified uplift of Fruška Gora, accom- cally controlled, subsidence. panied by subsequent subsidence of the southern fo- Fruška Gora represents a horst whose tectogenesis othills, a relatively shallow basin was formed, with began as early as Early Miocene, but it was generally axial parts oriented in accordance with the orientation formed in Early Quaternary, and has been permanent- of tectonically active structures (i.e. E–W). Also, it ly modified until recent time (TOLJIĆ et al. 2013). can be considered that these movements were causal- Significant part of primary shaping of morphostruc- ly related to climatic changes at the Pliocene-Pleisto- tures in this massif took place in the Miocene, and it cene boundary, so that the proluvial sediments formed can be recognized in gravitational shear across the in that time have a regional distribution and represent faults of the E–W direction. During Pliocene and the landmark for the drawing of the lower boundary of earlier parts of Quaternary some of these faults were Quaternary in this part of the area. reversely reactivated, by which an antiform and posi- The neotectonic uplift of the Fruška Gora horst tive structural build of Fruška Gora was additionally caused the intensive, but uneven cutting of the Fruška 48 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ Gora watercourses, which on both slopes belong to a megdan fault along the Pannonian part of the section. parallel drainage system, developed at the right angle Its valley in this part also has an asymmetrical charac- to the direction of the peripheral structures and paral- ter, because the loess and alluvial terrace are much lel to the generally N–S oriented structures. Thus more developed on the left, than on the right side of formed river valleys are composite, mainly transverse this watercourse. and consequent. The watercourses that belong to the The dynamic stage of the longitudinal profile of the Sava drainage system have deeply cut and narrow val- Sava river, especially in its lower part to its conflu- leys only in their source parts. In lower parts, because ence with the Danube, is characterized by permanent of gentler slopes and a gradual transition into the sinking, which is manifested in the morphology of the plain, river valleys are wider, watercourses are often river valley, as well as in polycyclic character of sed- ephemeral, and form an alluvial fan, often with water- imentation. Beside the extreme meandering of the logging phenomena. At the northern slopes of the course of this river, numerous deserted meanders are mountain, rivers are deeply cut, of small width, with present, from completely dry, over occasionally to steep valley sides in their upper and middle parts, permanently active. Permanent lowering within the while in the lower parts they expand and form narrow Sava trough is also indicated by a significant increase floodplains. of the thickness of fluvial deposits with thick alluvial Unlike the areas with a steady trend of rising, in the deposits of Late Pleistocene and Holocene overlying lowered regions relatively thick deposits of different them. The younger part of these deposits was formed origin were formed. Among them are products of flu- in conditions of relative rest in this area. vial, swamp, deluvial, and in Late Pleistocene also Also, from the regional point of view the Danube aeolian type of sedimentation. In the areas more low- near Vukovar turns from the meridional direction at the ered by tectonic agents, the watercourses of the Da- angle of almost 90° towards the east, following the nube and Sava have been developed. Vast meanders, faults along the northern foothill of Fruška Gora, all the sharp de?ection of river valleys and apparent asym- way to Stari Slankamen where the watercourse changes metry of their valleys represent distinctive character- its direction and flows to the south. The river valley in istics of watercourses under the influence of neotec- this area is pronouncedly asymmetrical with the mor- tonic and recent tectonic processes. phologically low left valley side and the right side The intermontane valley of the river Sava has been marked by a steep section. This can be explained by the sinking during Quaternary, while the horst of Fruška recent lowering of the area to the north of the fault, fol- Gora and the northernmost parts of Šumadija have lowed by migration of the riverbed to Fruška Gora. been rising. As a result of this trend of movement, From Stari Slankamen to Belgrade the Danube within the young trough a wide river valley was turns twice. The first turning (Stari Slankamen) is formed, whose origin was connected to the tectonical- controlled by the mobility of the faults present on the ly controlled, slow but continuous subsidence. eastern slopes of Fruška Gora, the activity of which Throughout the Early and Middle Pleistocene the tec- led to the separation of the Titel loess plateau from the tonic trough of the Sava river was constantly descend- Srem loess plateau. Both of them were parts of the ing, which was reflected in the increased thickness of same entity before the deposition of the penultimate the deposits and their polycyclic character. Of partic- loess level (GORJANOVIĆ–KRAMBERGER 1921), when ular importance were gravitational movements across they were separated by a fault near Stari Slankamen, the Kalemegdan fault, which controlled the develop- which controlled the turning of the Danube and for- ment of the asymmetrical Sava trough. The depression mation of the recent valley. Another turning is in the axis migrated over time, from NW to SE, which was area of Stara Pazova. It has a distinctive elbow char- followed by migration of the Sava riverbed. From acter, so it may be related to the fault structures that morphological point of view, the valley of this river control the area of uplift to the south of Stari Banovci belongs to the asymmetrical type of river valleys – its (MARTINOVIĆ et al. 2010). At the same time, this is an right side is in constant motion toward SE, while the area of the contact of the Fruška Gora and Zemun left one is quite poorly distinguished and covered by parts of the Srem loess plateau. The valley in this part deluvial deposits. The longer axis of the river valley is also has a pronouncedly asymmetrical character, generally parallel to the extension of the recent wherein its left side makes a vast loess and alluvial depression, with the width amounting to up to 25 km. terrace (Pančevački rit), while the right side forms a Looking at the broader area, a distinctive double very steep loess section, permanently eroded by the sharp de?ection valleys of this river can be observed river. on the line Sremska Mitrovica–Šabac. Namely, under the influence of a great floodplain of the Drina, this river has been shifted towards Sremska Mitrovica, so Lithofacial analysis outside the zone of its influence it turns abruptly towards Šabac, from where it spreads (occasionally Throughout Quaternary in the Serbian part of the meandering) to Belgrade, following mainly the Kale- Pannonian basin, and to a much lesser extent in its Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 49 periphery, a relatively thick succession of genetically occasionally aquatic (swampy) areas, which were different types of sediments was deposited. Of special eroded from the adjacent uplifted structures (Belgrade interest are pre-loess deposits, whose thickness and Promontory). These parts of the area were subsided great distribution indicate that in the wider area of across the cascade systems of faults, indicated by an southern part of the Pannonian basin intensive sinking increased thickness of older Pleistocene deposits. of the terrain was taking place throughout Pleistocene. Deposits of Plio-Pleistocene age (marsh-lacustrine This is particularly indicated by the presence of flu- deposits) were found by deep drilling in the area of vial-lacustrine sediments, whose thickness in some Zemun and Novi Beograd, where their upper bound- places exceeds 200 m. However, despite the great ary is situated at an altitude of about 30,0 m, and thickness of deposits it can be concluded that subsi- lower at –60,0 m; while in some boreholes which are dences were of low intensity compared to those in the even deeper, their lower boundary is not reached, so central parts of this basinal system, such as the Great presumably it could descent to a much greater depth. Hungarian depression, where the thickness of Quater- Taking into consideration that in the area of the nary deposits exceeds 700 m (RONAI 1974). As op- Kvantaš pijaca (meaning Green market) in Zemun the posed to the deposits formed in the subsided regions, Neogene basement was not reached even at the depth deluvial-proluvial sediments („Srem series“, „Kliče- of 260 m, it can be concluded that these deposits have vac Series“, etc.) that have been formed on the slopes a great thickness (Fig. 3). Fig. 3. Map of thicknesses of the pre-loess Pleistocene deposits in the area of Srem (amended after MAROVIĆ et al. 2002). of Fruška Gora and in the peripheral belt of the Pan- A very distinct and relatively extended subsidence nonian basin, especially in its eastern part towards the in the area of Zemun and Bežanija is indicated also by Carpathians (RAKIĆ, 1977), indicate the environment a great thickness of fluvial polycyclic deposits of of inflicted areas between elevated regions. Early Pleistocene, which largely overlie the Plio- According to the thickness of Quaternary deposits, Pleistocene deposits. The faults that caused cascade in particular Pleistocene pre-loess deposits, it can be subsidence in this part of the area, are covered with assumed that in the extreme SE part of Srem (today’s these sediments and other overlying Quaternary territory of Novi Beograd and Zemun) the differentia- deposits. NE–SW directed structures can be followed tion of relief under the influence of vertical tectonic from Kalemegdan to Obrenovac, from where further movements occurred in Early Pleistocene (KNEŽEVIĆ et on, in a planar view, they form a system of echeloned al. 1998; NENADIĆ 1997, 2003; NENADIĆ et al. 2009, faults of similar orientation. 2010, 2011). The lowered parts were then quickly The deposits of the Early Pleistocene age are situ- buried by rapid accumulation of slope deposits in ated in the hilly areas to the south of the Danube and 50 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ Sava rivers (area of the Belgrade Promontory and posited at any height, but their thickness can immedi- around it) on the significant height which is variable ately point to the existent palaeorelief, as well as to and ranges from an altitude of 170–179 m on Zve- the intensity of erosional processes which occurred in zdara, 135–156 m on Mirijevo, 113–130 m on Čubu- the areas where these deposits were sedimented. Con- ra, 69–78 m on Kalemegdan etc. sidering the number of palaeosols and loess horizons The hypsometric position of the fluvial polycyclic and their disturbances, ZEREMSKI (1960, 1961) estab- deposits to the north of the Danube and Sava is signif- lished three phases of tectonic movements of epeiro- icantly lower. In the area of Novi Beograd their lower genic character on the section of the loess plateau boundary begins on an altitude of 35–48 m, and the above the Danube. The oldest movements were fin- upper on approximately 55 m, sometimes over 66 m, ished before the accumulation of loess; the move- so that some recent mollusk shells are found in these ments of the second phase took place during deposi- deposits together with the washed shells of the genus tion of these sediments, while the third phase took Corbicula. The most extensive subsidence was no- place after the accumulation of the last loess horizon, ticed in the area of Zemun, where the lower boundary in younger Neolithic. Movements of two older phases of these deposits descends in some places to an alti- were manifested only in some parts across the profile tude of 25 m. line Stari Slankamen–Zemun, i.e. they have local A significantly decreased thickness of pre-loess character, while the younger ones were manifested on Quaternary sediments in the riparian parts of the Sava the whole profile of the loess plateau. river indicates that subsidence in this region took An example of tectonic activity can be seen near place a little later, in relation to northern parts of the Slankamen (locality Surduk), where beneath two territory. Locally, on the right bank of the river, a mor- upper horizons of loes, which are horizontal, a pack- phologically prominent fault system has been devel- age of deluvial-proluvial deposits is situated, tilted at oped. Across these structures the NW block has been the angle of 8° together with paleosols. On the contact subsided, which brought to development of the Makiš of these two units there are slope debris and pebbles depression. It can be concluded from the mentioned of hard Neogene and Mesozoic rocks. These were data that during Quaternary the overall subsidence in probably formed by the action of proluvial process on the area of the hanging-wall of the Kalemegdan fault the slopes of the Fruška Gora mountain, in the course was approximately 160 m. of which the base across which the water mass was Opposite to the areas of subsidence, the uplifted moving was leveled. In this way, on the horizontal area of the Belgrade promontory and the Fruška Gora surface formed in such way the upper loess complex massif were in the stage of intensive erosion and accu- was deposited in the undisturbed position. This mulation of eroded material, which was transported unconformity between lower and upper horizons, with by colluvial-deluvial processes and then deposited in colluvial gravels, was probably formed at the bound- the environments that were gradually sinking. ary between Middle and Late Pleistocene. In the other In the northern part of the territory (on the slopes of parts of the loess plateau similar elements that would the Fruška Gora massif) the earlier Pleistocene prolu- point to the presence of tectonic activity have not been vial-deluvial deposits were formed by a stronger hyp- observed, since all loess horizons (as well as pale- sometric denivelation of the area on the boundary osols) are horizontal, which was also noted across the between Neogene and Quaternary, i.e. by a prominent visible profiles from Surčin to Stari Slankamen. tectonic activity manifested in the uplift of the core of According to the lithostratigraphic characteristics this massif and subsidence of the outlying foothill of deposits it can be concluded that tectonic activity in areas. In the process of accommodation of the newly Holocene has a similar character as in Pleistocene, i.e. formed inflicted areas between the uplifted and sub- areas of subsidence were marked by fluvial, palustrine sided morphostructures, there was active erosion, de- and swamp deposits, while deluvial and more rarely nudation and filling of these areas with proluvial- deluvial-proluvial deposits were linked to the inflict- deluvial deposits. ed areas toward the uplifted structures. According to the stratigraphic-lithological charac- teristics of Quaternary deposits in the area of eastern Srem, it can be concluded that palustrine-lacustrine Thermochronological data and fluvial polycyclic sediments mark the areas of subsidence, and proluvial-deluvial – inflicted areas (U-Th)/He dating of apatite minerals (AHe) repre- beside the uplifted structures (RAKIĆ 1977; NENADIĆ sents a low-temperature thermochronological tech- 2003; NENADIĆ et al. 2011; NENADIĆ & GAUDENYI nique, which is used for documenting the latest stages 2013). of cooling of rocks as they pass the uppermost levels of During Late Pleistocene great areas of the Pan- the crust, corresponding to the temperatures of ~75 °C nonian basin were covered by loess and loess-like (closure temperature Tc of AHe system, WOLF et al. deposits. Loess deposits cannot be an indicator of tec- 1996). Therefore, this method is frequently used to tonic activities, because they could be primarily de- quantify the time of vertical movements in the upper- Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 51 most ~1–2 km and correlate these movements with deposits (especially deposits of Plio-Pleistocene age) the associated tectonic phases. Two (U-Th)/He single so they are usually not morphologically prominent but grain ages were determined on the two rock samples they represent significant control elements of subsur- collected in greenschist facies metamorphic core, face geological structure. In the peripheral parts of the located in the southern part of the Fruška Gora (Fig. investigated area there are faults which directly affect 1B.). The ages were obtained following standard ana- the morphology of the terrain (for example, the faults lytical procedures available at the VU University by the rim of Makiš, along the Fruška Gora massif, Amsterdam (see STOJADINOVIĆ et al. 2013). etc.). Across the traces of these faults colluvial move- The AHe single grain age of the sericite schist sam- ments of rock masses are common. ple Fg1 is 16.3±1.6 Ma, while the AHe age of chlo- Undoubtedly, the most striking structures are situ- rite-sericite schist sample Fg2 is 2.4±0.9 Ma (Table ated along the northern and southern periphery of the 1). The older age of 16.3±1.6 Ma recorded in sample Fruška Gora massif, and they actually formed this Fg1 reflects a Middle Miocene phase of cooling in the asymmetrical horst surrounded by Quaternary depo- Fruška Gora metamorphic core. It represents the sits. The northern Danubian fault, whose trace gener- result of contemporaneous uplift caused by extension- ally coincides with the Danube riverbed, is covered by al deformations in the brittle domain that occurred a thick package of Quaternary sediments but it is mor- along the gravitational faults along the southern slope phologically very distinct because of a pronounced of the mountain (TOLJIĆ et al. 2013). Hence, temporal- asymmetry of the river valley. In the investigated area, ly it can be well correlated with the main phase of on the southern slopes of the Fruška Gora, Vrdnik Pannonian extension (HORVATH et al. 2006). The fault is situated (TOLJIĆ et al. 2013). Its trace is local- younger, lowermost Quaternary, cooling age of sam- ly observed in the area of Vrdnik, while laterally it is ple Fg2 is 2.4±0.9 Ma, and it is associated with the mostly hidden by loess and pre-loess Quaternary sed- most recent phase of regional tectonic activity. The iments. In the eastern periphery this massif is lateral- obtained age corresponds well with strong uplift at ly limited by the Karlovac and Čortanovci transverse Pliocene/Pleistocene boundary that was recorded in structures. In the south of the investigated area espe- the southern parts of the mountain and was associated cially striking is the Kalemegdan fault, developed reverse reactivation of previously existing E–W ori- along the Pannonian part of the section, extending ented gravitational faults. It represents direct evidence from the SW part of the investigated area across of continuous uplift in the Pliocene and Quaternary, Ostružnica, Železnik and Žarkovo to the confluence followed by intensive, tectonically induced erosion of of the Sava. Across this complex fault its NW block the source area in the Fruška Gora and the fast depo- was downthrown, which was accompanied by deposi- sition of proluvial-deluvial sediments in surrounding tion of a thick package of sediments of Neogene–Qua- domains. This uplift is, again, associated with the con- ternary age. The central parts of the area are covered temporaneous phase of compression that affected the by thick Quaternary deposits, hence fault structures entire region (MAROVIĆ et al. 2002, 2007). are rarely visible on the surface. However, on the Table 1. Apatite (U-Th)/He (AHe) Analytical Data. Bold numbers represent corrected final AHe single grain ages obtained in this study. *Ft is fraction of alphas retained, “corrected ages” are corrected for this effect. Quaternary active faults and structures available seismic sections (MATENKO & RADIVOJEVIĆ 2012) syn-depositionally active faults are recognized, The faults across which movements were perform- across which the axial parts of the Srem depression ed represent inherited structures, primarily formed in were deeply downthrown. the Miocene, as previously interpreted by TOLJIĆ et al. By the analysis of satellite image (1:250 000) infor- (2013). They are mostly covered by Pleistocene mation on spatial position of larger and morphologi- 52 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ Fig. 4. Map of the regional fault setting of the eastern Srem with simplified review of the tectonic blocks structure. cally prominent faults in the area of the eastern Srem to this system, which represent the faults that form the has been obtained (Fig. 4). The basic feature of this periphery of the positive Fruška Gora morphostruc- structure is the existence of several fault systems. In ture. On the diagram in the form of a submaximum a the area of Fruška Gora the most significant faults are system of faults with a statistical direction 150–330 is aligned with the strike of the plicative structures. also observed. The NW–SE directed faults are often These longitudinal structures are oriented in the E–W detected in the central and eastern parts of Fruška (ENE–WSW) direction and associated with the Gora. NW–SE directed faults. Longitudinal structures are Geodetic measurements confirm that the Fruška large regional ruptures of deca-kilometre dimensions, Gora block has been uplifted in recent times at the among which the Vrdnik fault and Kalemegdan fault velocity of 0–1 mm/year (MAROVIĆ et al. 2002). are particularly prominent. Across them the down- throw of central parts of the eastern Srem was per- formed (Eastern Srem Block), opposite to the uplift of Eastern Srem block the Fruška Gora Block in the north and Šumadija Block to the south of the investigated area (Fig. 4). On the north it is limited by the Vrdnik fault, and on According to the determined positions of large the south by the Kalemegdan fault. This block is com- faults, difference in spatial distribution of internal pletely covered by Quaternary sediments, which ham- structures, as well as the lithofacial characteristics of pered geometrical analysis of fault structures. Still, the investigated deposits, 3 structural-depositional careful analysis of the satellite image made it possible environments can be singled out in this area: Fruška to define spatial position of a part of dislocations Gora block, Eastern Srem Block and Šumadija block developed in this area. The data on the fault structures (Šumadija–Belgrade hills, Fig. 4). were measured, statistically processed and shown on the diagram R1 (Fig. 4). On the rosetta a conspicuous maximum marks ruptures with a medium strike direc- Fruška Gora block tion of 150–330. These structures are found on the eastern periphery and in center of the block. The sub- It represents an area limited by the Danube fault on maximum with a medium direction 30–210 corre- the north and the Vrdnik fault on the south. By statis- sponds to the faults detected in the SW part of the tical data processing on spatial positions of the faults block. Part of the fault setting developed in the of this block, a maximum has been obtained with the domain of this block is also comprised of faults with direction 90–270 (diagram R1, Fig. 4). The majority the direction 90–270, which are situated in the area of ruptures developed in this block generally belong between Sremska Mitrovica and Pazova. Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 53 The available geodetic measurements indicate that these parts there are also domains characterized by the block of the central Srem subsided at the velocity permanent late Neogene and Quaternary subsidence. up to –2 mm/year (MAROVIĆ et al. 2002). Intensity of the subsidence is lower compared to the central parts of the Pannonian basin. Relatively high- ly hypsometrically uplifted blocks of Fruška Gora and Šumadija Block (Šumadija–Belgrade hills) northern parts of Šumadija have been developed on the periphery of the downthrown areas, in the area of The northwestern boundary of this block makes the Srem, during Late Neogene and Quaternary. complex Kalemegdan fault, while the southern one is Simultaneous existence of neighboring domains, poorly defined and beyond the investigated area. The which are uplifted and subsided in a compression stress results of analysis of the faults are represented on the field, can be explained by flexion banding of the litho- rosetta R1 (Fig. 4). Detected structures are uniformly sphere (CLOETINGH et al. 2005; DOMBRÁDI et al. 2010), oriented. On the diagram the faults that belong to the followed by reactivation of the large existing faults complex Kalemegdan fault have a statistical strike which are in the same time boundaries between the seg- direction of 60–240. These faults are developed in the ments with a different character of vertical movement. domain of the Sava river and they could be followed Different character and intensity of vertical mobility of from Zemun on NE to Obrenovac and Debrec on SW. the lithosphere in the southern parts of the Pannonian Geodetic information confirms that this area has basin have been, throughout Quaternary, the control been slowly uplifted at the velocity of 1 mm/year factors of the origin and thickness of deposited sedi- (MAROVIĆ et al. 2002), whereas more to the south the ments. A significant control factor of the Quaternary velocity of uplift is increased up to 4 mm/year. depositional environment were the faults on the south- Generally speaking, by the analysis of obtained ern slopes of Fruška Gora and to the southeast of the data it can be observed that in the blocks of Fruška Sava river. The internal mobility and outline of the de- Gora and Šumadija Block, as well as at their periph- pressions are controlled on the east by the faults (from ery, the E–W (ENE–WSW) directed faults dominate, Sremski Karlovci, across Slankamen and Belegiš to while in the Eastern Srem Block the NW–SE faults Zemun), while the basin is open towards the west. prevail. The reasons for such discrepancies probably The central parts of the investigated area are gener- lie in the fact that the central block is covered by rel- ally characterized by a slow, permanent tectonically atively thick Quaternary deposits, which masked controlled subsidence, distinctive also in the recent older structures of this area, so their remote sensing is time. The peripheral parts of the Šumadija-Belgrade disabled in that way. hills and Fruška Gora horst have been in younger Neogene and Quaternary permanently and relatively slowly, uplifted. The (U-Th)/He cooling age obtained Conclusion in the metamorphic core of the Fruška Gora horst, provides a direct evidence for the continuous uplift at Quaternary tectonic activity in southern parts of the the transition from Pliocene to Quaternary, which is Pannonian basin genetically corresponds to the stress the result of the ongoing compression. As a result of field, established earlier, at the end of Miocene (TOLJIĆ accommodation of uplift and following erosion of the et al. 2013). As a consequence of the northward move- uplifted blocks, in the domain of active faults relative- ment of the Adria microplate and final abruption of a ly thick deposits of proluvial-deluvial character have segment of the subducted lithosphere in the Carpathian been formed. In the subsided areas, thick deposits of domain (MATENKO & RADIVOJEVIĆ 2012), the whole different genetic origin have been formed. Among Pannonian basin was exposed to permanent compres- them the most prominent are lacustrine, alluvial, pa- sion. In the border area between the Dinarides and lustrine, and in younger Pleistocene aeolian deposits. Pannonian basin, the axis of maximum compression is In all tectonically subsided parts the flows of major NE–SW oriented (BADA et al. 2007). In this stress field rivers (Danube and Sava) have been developed. Their lithologically and structurally complex and thinned river valleys are situated in areas of faults in which lithosphere of the basement of the Pannonian basin was during Quaternary gravitational movements of high folded in regional fold structures of low amplitudes. intensity have been performed. These faults in the Folding has been accompanied by vertical mobility of same time represent main tectonic boundaries of the blocks limited by the existing fault pattern. morphostructural entities developed in this part of the By the analysis of spatial position of faults, their Pannonian basin. kinematic features and origin and mutual relationship of deposits formed in Quaternary, the data were ob- tained for the purpose of reconstruction of Quaternary Acknowledgements tectonic mobility in the area of Srem. The peripheral southern parts of the Pannonian basin have similar This study was supported by the Ministry of Education, evolution as the internal parts of the basinal area. In Science and Technological Development of the Republic of 54 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ Serbia, Project No. 176015. The authors are very grateful to MAROVIĆ, M., DJOKOVIĆ, I., PEŠIĆ, L., RADOVANOVIĆ, S., DMITRIY A. 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The balance between Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 55 orogenic building and subsequent extension during the зиционо и генетски могу разликовати два дела: Tertiary evolution of the NE Dinarides: Constraints from - старији, речни и речно-језерски, са реликтима low-temperature thermochronology. Global and Plane- басенског склопа, генерисан покретима влашке tary Change, 103: 19–38. или валахијске тектонске фазе, манифестујући се SUŠIĆ, Z. 2013. Geodinamička analiza pomeranja zemljine вишекратним спуштањем некадашњег басенског kore regionalnog karaktera, Doktorska disertacija, дна и стварањем сложених алувијалних равни пра- Univerzitet u Novom Sadu, Fakultet tehničkih nauka, Дунава и пра-Саве, и Geodezija i geomatika, 196 pp., Novi Sad. - млађи, који одговара флувиоденудационом си- TOLJIĆ, M., MATENCO, L., DUCEA, M., STOJADINOVIĆ, U., стему у ужем смислу, а који обухвата морфолошке MILIVOJEVIĆ, J. & ĐERIĆ, N. 2013. The evolution of a облике стваране током горњег плеистоцена и key segment in the Europe – Adria collision: the Fruška холоцена. Gora of northern Serbia. Global and Planetary Change, Квартарну тектонску активност јужних делова 103: 39–62. Панонског басена је сагледана у контексту регио- WOLF, R.A., FARLEY, K.A., SILVER, L.T. 1996. Helium налне миоценске екстензионе еволуције басенског diffusion and low temperature thermochronometry of простора и његове плиоценско-квартарне инвер- apatite, Geochim. Cosmochim. Acta, 60: 4231–4240. зије. Миоценска екстензија, продуцирана rollback- ZEREMSKI, M. 1960. Reljef Beogradske i Zemunske posa- ом европске литосфере у Карпатима, била је пра- vine. Zbornik radova Prirodno–matematičkog fakulteta, ћена рифтингом, истањењем литосфере и субси- Geografski institut, 7: 56–98. денцијом у домену Панонског басена (HORVATH et ZEREMSKI, M. 1961. Još jedan prilog holocenskim al. 2006). Дуготрајну средње и горњомиоценску epirogenim pokretima na istočnom delu odseka sremske пострифтну субсиденцију, контролисану са пос- lesne zaravni. Zbornik Matice srpske, serijal prirodnih тупним хлађењем литосфере у домену Панонског nauka, 20: 16 p.. басена (thermal sag cooling, CLOETINGH et al. 2006), пратила је плиоценско-квартарна басенска инвер- зија, изведена у компресионом напонском пољу. Резиме Екстензионо напонско поље је смењено компре- сијом, активираном као последица финалног отки- Квартарна тектонска и депозициона дања (break off) субдуковане европске литосфере у еволуција источног Срема домену Карпата, с једне стране, и север-северо- (северозападна Србија) источне прогресије Адријске плоче, с друге стране. Током плиоцена и квартара, Динарско-Карпатски ороген и интраконтинентални Панонски басен су Током квартара на подручју источног Срема, изложени константној компресији, за ове просторе саставног дела Панонског басена, испољила се генерално оријентисаној по правцу СИ–ЈЗ (BADA et тектонска активност као битан контролни фактор al. 2007). У овим условима је истањена и лито- депозиције и финалних уобличавања савременог лошки хетерогена литосфера у подини Панонског рељефа. Тектонска еволуција Панонског басена је басена, убрана у наборе километарских размера почела знатно раније, тако да су све током квар- (CLOETINGH et al. 2005, 2006). Регионална литосфер- тара тектонски активне структуре део раније по- на убирања су била праћена вертикалном мобилно- стојећег предцртежа и спадају у категорију насле- шћу сегмената литосфере, различитог смера и ин- ђених и реактивираних структура. Седиментација, тензитета, што је као финалну последицу имало као доминантан процес финалних фаза запуњава- релативно брз аплифт и денудацију периферијских ња инвертованог депозиционог басена, вршила се делова басена и даљу субсиденцију и депозицију у раније тектонски дефинисаним доменима. централних басенских домена. При томе је локал- Током млађих одељака плиоцена и старијег квар- ном редистрибуцијом компресионог стреса реак- тара, након повлачења Паратетиса, област јужног тивиран постојећи тектонски предцртеж, који је био обода Панонског басена у целини пролази кроз у функцији контроле тектонске мобилности унутар копнену фазу развоја. У том интервалу обављена су басенских ентитета, какав је био простор јужно од тектонска обликовања ниског интензитета, којима Фрушке Горе. су финално уобличени регионални морфострук- На секцијама сеизмичких профила Фрушке Го- турни облици. Такође, тектонски контролисана мо- ре (MATENKO & RADIVOJEVIĆ 2012) може препозна- билност унутар басенских сегмената проузроковала ти асоцијација раседа који чине Врднички расед је недостатак неких стратиграфских подкатова пли- (TOLJIĆ et al. 2013). По овој структури је примарно оцена, промену фација и дебљина најмлађих лито- гравитационо спуштен јужни блок, при чему је стратиграфских целина (MAROVIĆ i dr. 1996, 1998). дебљина плиоценско-квартарних седимената јуж- Постбасенски седименти, депоновани током но од раседа и преко 500 m. Такође синтеза пода- квартара, представљени су релативно дебелим па- така сеизмичког профилирања и дубоких истраж- кетом седимената у оквиру кога се суперпо- них бушења изведених у овом подручју, упућује 56 MARINKO TOLJIĆ, DRAŽENKO NENADIĆ, UROŠ STOJADINOVIĆ, TIVADAR GAUDÉNYI & KATARINA BOGIĆEVIĆ да је дебљина плиоценско-квартарних седимената Саве налазио се у константном спуштању, што се значајна (MARTINOVIĆ i dr. 2010). Највећа дебљина и одразило на повећану дебљину наслага и њихов седимената је између Старе Пазове и Шапца, у полициклични карактер. При томе су посебно од депресији чија оса се пружа правцем И–З значаја била гравитациона кретања по Калемег- (ИСИ–ЗЈЗ). На северној периферији депресије се данском раседу, која су контролисала развој аси- налази Врднички расед, централне делове по- метричног Савског рова. Оса депресије је вре- дручја контролише асоцијација хорстова и ровова меном мигрирала, од северозапада ка југоистоку, дефинисаних раседима по којима је дубоко спу- што је било праћено и миграцијом речног корита штен централни део Сефкеринске депресије реке Саве. (MATENCO & RADIVOJEVIĆ, 2012). Јужна периферија Током квартара у српском делу Панонског ба- проучаваног простора на сеизмичким секцијама сена, а у знатно мањој мери на његовом ободу, показује сложену тектонску природу прелазног наталожена је релативно дебела сукцесија ге- подручја између Панонског басена и његовог из- нетски различитих типова наслага. Посебан значај дигнутог јужног залеђа. Као доминантна структу- при том су имале прелесне наслаге, чија дебљина ра се препознаје Калемегдански расед, синдепози- и велико распрострањење упућује да су се на ционо активни расед, по коме је субсиденција ширем подручју јужног дела Панонског басена северозадног домена била активна и током квар- током плеистоцена одвијала интензивна спушта- тара, на што упућује значајна дебљина најмлађих ња. На то нарочито указују седименти речно- седимената. На овакав сценарио указује и рела- језерског карактера чија дебљина местимично тивно мала дебљина плиоценско-квартарних седи- прелази и преко 200 m. Насупрот наслагама мената источно од овог раседа. Посматрано у формираним у спуштеним областима, делувијал- плану, асоцијацију раседа који чине Калемегдан- но–пролувијални седименти („сремска серија“, ски расед, чини низ ешалонираних раседа пру- „кличевачка серија“, итд.) који су формирани на жања СИ–ЈЗ који се могу пратити од Калемегдана падинама Фрушке Горе и на ободном појасу Па- до Обреновца и даље ка југозападу (Сл. 4). нонског басена, посебно у источном делу према Фрушка Гора представља хорст чија тектогенеза Карпатима (RAKIĆ 1977), указују на превојна је отпочела још у доњем миоцену, генерално уо- подручја према издигнутим структурама. бличен током раног квартара, перманентно моди- На основу дебљине квартарних, посебно пре- фикован до у рецентно време. За примарно морфо- лесних плеистоценских наслага, може се претпо- структурно обликовање овог масива значајна су ставити да је на крајњем ЈИ делу Срема (да- миоценска обликовања која се могу препознати у нашњем простору Новог Београда и Земуна) гравитационим смицањима дуж раседа пружања долазило до диференцијације рељефа под ути- И–З. Током плиоцена и старијег квартара део ових цајем вертикалних тектонских покрета током раседа је реверсно реактивиран, чиме је додатно старијег плеистоцена (KNEŽEVIĆ i dr. 1998; истакнута антиформна, позитивна стурктурна грађа NENADIĆ 1997, 2003; NENADIĆ i dr. 2009, 2010, Фрушке Горе, што је било праћено рапидном еро- 2011). При томе су спуштени делови затрпавани зијом аплифтираних делова и исто тако рапидном брзом акумулацијом падинских наслага у повре- акумулацијом у околним спуштеним доменима. мено акватичним (забареним) срединама, еродо- После интензивнијег издизања Фрушке Горе, ваних са околних издигнутих структура (београд- праћеног субсеквентном субсиденцијом јужног ског рта). Ови делови терена су дуж каскадних предгорја, долази до формирања релативно плит- система раседа спуштани наниже, о чему наро- ког басена са аксијалним деловима оријентисани чито сведочи повећана дебљина старијеплеисто- сагласно оријентацији тектонски активних струк- ценских наслага. тура пружања И–З. Такође, може се сматрати да су Творевине плио-плеистоцена (барско-језерске ови покрети каузално били повезани са климат- наслаге) су констатоване дубинским бушењем на ским променама на граници плиоцена и плеис- подручју Земуна и Новог Београда, где им је тоцена, те да тада настали пролувијални седи- одређена горња граница на око 30,0 mnv, а доња на менти имају регионално распрострањење и –60,0 mnv, док поједине бушотине и преко те представљају репер за извлачење доње границе дубине нису стигле до његове подине, па је за квартара на овом делу терена. претпоставити да се доња граница ових наслага Интрапланински ситуирана долина реке Саве местимично спушта доста ниже од горе наведене. током квартара тоне, док се хорст Фрушке Горе и Узимајући у обзир да се на простору Кванташке најсевернији делови Шумадије издижу. Као по- пијаце у Земуну није набушена неогена подлога ни следица оваквог тренда кретања, у оквиру младог на дубини од 260 m, за претпоставити је да ове рова формирана је широка долина реке, чија се наслаге местимично имају јако велику дебљину еволуција може везати за тектонски контролисану (Сл. 3). спору, али континуирану субсиденцију. У току Интересантни су и подаци добијени применом старијег и средњег плеистоцена тектонски ров термохронолошке методе. Као што је познато, Tectonic and depositional evolution of the eastern Srem in the Quaternary (northwest Serbia) 57 одређивање старости хлађења апатита кориш- представља подручје ограничено Дунавским ћењем (U-Th)/He термохронолошке методе, пред- раседом на северу и Врдничким раседом на југу. ставља технику која се често употребљава за Блок источног Срема је са севера ограничен Врд- дефинисање времена одвијања вертикалних тек- ничким раседом, а са југа Калемегданским расе- тонских покрета у најплићим нивоима земљине дом. Шумадијски Блок као северозападну границу коре. Ово је омогућено тиме што је температура има сложени Калемегдански расед, док је јужна затварања (U-Th)/He система у апатитима ~75 °C недефинисана и изван подручја истраживања. (WOLF et al. 1996), што би одговарало хлађењу Квартарна тектонска активност у јужним де- стена при њиховом вертикалном кретању кроз ловима Панонског басена генетски кореспондира приповршинске нивое земљине коре (~1–2 km). са напонским пољем успостављеним раније, кра- Две старости хлађења добијене су анализом два јем миоцена. Као последицa кретањa Адријске узорка из метаморфног језгра Фрушке горе (Та- микроплоче ка северу и финалног откидања сег- бeлa 1 и Сл. 1Б., Fg1 16.3±1.6 Ma и Fg2 2.4±0.9 мента субдуковане литосфере у карпатском до- Ma). Старост узорка Fg1 od 16.3±1.6 Ма, пред- мену, цео Панонски басен је изложен перма- ставља резултат хлађења изазваног издизањем нентној компресији. У граничном подручју између метаморфног језгра Фрушке горе током миоцен- Динарида и Панонског басена, оса максималне ских екстензионих деформација дуж гравитацио- компресије је оријентисана правцем СИ–ЈЗ. У них раседа лоцираних на јужном ободу планине овом напонском пољу је литолошки и структурно (TOLJIĆ et al. 2013). Старост узорка Fg2 od 2.4±0.9 сложена и истањена литосфера подине Панонског Ma се, међутим, може корелисати са хлађењем ових басена, убрана у регионалне наборне структуре стена током снажног издизања на граници пли- ниске амплитуде. Убирања су праћена вертикал- оцена и плеистоцена, а која је асоцирана са ре- ном мобилношћу блокова лимитираних постоје- версном реактивацијом већ постојећих гравита- ћим раседним предцртежом. ционих раседа оријентисаних по правцу исток–за- Истовремено егзистирање суседних домена који пад. Старост узорка Fg2 представља директан се издижу и тону у компресионом напонском доказ континуираног издизања метаморфног пољу, могу се објаснити флексионим савијањем језгра Фрушке горе током плиоцена и квартара, литосфере, праћено реактивирањем крупних, што представља последицу компресије која постојећих раседа који су уједно и границе сегме- диктира рецентни тектонски режим читавог ната са различитим карактером вертикалног региона (MAROVIĆ et al. 2002, 2007). кретања. Различит карактер и интензитет верти- На основу утврђених позиција крупних раседа, калне мобилности литосфере у јужним деловима разлика у просторној дистрибуцији интерних Панонског басена су током квартара били кон- структура, као и на основу литофацијалних ка- тролни фактори генезе и дебљине депонованих рактеристика проучаваних депоната, на истражи- седимената. Као важан контролни фактор квар- ваном подручју могуће је издвојити 3 структурно- тарног депозициног простора препознати су ра- депозиционе целине: Блок Фрушке Горе, Блок седи на јужним падинама Фрушке Горе (Врднички источног Срема и Шумадијски блок (шумадиј- расед) и југоисточно од реке Саве (сложени ско–београдско побрђе) (Сл. 4). Блок Фрушке Горе Калемегдански расед).