Depth Geological Relations of the Wider Area of Belgrade - Based on the Wells and Geophysical Data

GEOLOŠKI ANALI BALKANSKOGA POLUOSTRVA Volume 81 (2), December 2020, 1–32 – https://doi.org/10.2298/GABP201030009M Original scientiﬁc paper Оригинални научни рад

Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

1 2 orĐE arINovIć jupko uNdIć Đ M & L r Abstract.

2 The subject work covers the Belgrade wider area with a total area of about 2,000 km . The authors integrated the principal geological and geo - physical data provided by surface works and multidisciplinary elements from the fifty-two wells with depths between 33 and 2,733 m. Explicit paleontolo - gical findings of specialized analytists with determinations of macro- and mi - crofauna and flora are presented both from Neogene formations and the older basinal floor. In addition to conventional petrological descriptions of rocks, microscopic determinations of intrusive and extrusive magmatites were also cited. From the enclosed basin space, the mineralization of deep aquifers is also correlative positioned. From the geophysical data for wells deeper than 400 m, records of well logging measurements were used, with markers based Key words: on which valid stratigraphic delimitations were made. Seismic survey sections Stratigraphic elements, were the basis for spatial shaping of Neogene sedimentation and basin floor Neogene, Depth delimitation s, configuration. For in-depth geological interpretations, published and reposi - Geophysical indicators, tory gravimetric and geomagnetic maps of different sizes and years were con - Structural-Paleogeographic sulted. The authors focused primarily on factometric indicators without interpretation. entering into variable and debatable theoretical schematizations, especially orogenically complex of subbasin tectonics, in dissonant relations with the younger disjunctive shaped configuration which is visually shown in the refe - rence cross-sections both vertically and laterally. Апстракт.

2 Предметна референца обухвата простор шире околине Бео - града укупне површине око 2.000 km . Аутори су објединили капиталне геолошке и геофизичке податке обезбеђене површинским истражи - вањима и мултидисциплинарним елементима из 52 бушотин e са дубинама између 33 и 2.733 m. Конкретни палеонтолошки налази спе - цијализованих аналитичара са детерминацијом макро и микрофауне и флоре, презентовани су како из неогених формација тако и из басенске подине. Осим конвенционалних петролошких описа стена цитиране су и микроскопске детерминације интрузивних и екструзивних магматита. Из затвореног басенског простора корелативно су позициониране и ми - нерализације дубинских аквифера. Од геофизичких података за бушоти - не дубље од 400 m коришћени су записи каротажних мерења , са 1 Radnička 41, 21000 Novi Sad, Serbia. маркерима на основу којих су извршена валидна стратиграфска раз - 2 University of Belgrade – Faculty of Mining and Geology, Department of Regional Geology, Kamenička 6, 11000 Belgrade, Serbia. Email: [email protected]

1 ĐoRĐE MaRiNoVić & L jUpKo RUNDić

Кључне речи : Стратиграфски елементи , граничења. Секције сеизмичких испитивања биле су основ за просторно неоген , дубинска разграничења , обликовање неогене седиментације и конфигурације басенске подине. геофизички показатељи, За дубинска геолошка тумачења консултоване су објављене и фондовске структурно-палеогеографска гравиметријске и геомагнетне карте разних година и размера. Аутори су интерпретација се задржали првенствено на фактометријским показатељима не улазећи у променљиве и дискутабилне теоретске шематизације нарочито орогено сложене подбасенске тектонизације, у дисонантном односу са млађом, дисјунктивно обликованом неогеном конфигурацијом која је у референтној графици визуелно приказана и вертикално и латерално.

Introduction

mimicking the configuration of the inherited paleo - relief. The alpine-type tectonized structure is not The wider area of the city of Belgrade includes not identically oriented with the younger disjunctive only its central and highly urban part, but also all the shaped basin structure of Neogene. It is understood peripheral settlements that stretch around that that parts of the more pronounceudN rduIć ptures were re - urban core from both side of the Sava and danube activated during the Neogene ( r et al., 2019). rivers. Within that, so-called the Belgrade danube These facts influenced the authors of this paper meander (Beogradski dunavski ključ), in the nar - to make the basic driving motto has been factome - rower sense, means the area of Belgrade or its east - try, i.e. the desire to present the subsurface struc - ern rim that follows the course of the danube river tures of the wider Belgrade area with much more in the coastal part and low inner hills (višnjica, Slanci, details. veliko Selo) all the way to Mirijevo and vinča. once a Thanks to geological-geophysical research as marginal part of the Belgrade settlement and a space well as performed exploratory drilling, it has long suitable for field trips and professional observationuEs, been known that paleorelief or “old rocks” exposed it has a long tradition of geological research ( B , on the surface of the terrain south of the danube 1840). From that time, numerous studies have been river, build the basis for the Neogene and QETukaotveIr ć - done, hundreds of wells have been drilled and some nary sedNimĐEeLnkotsv Iuć p to 4000 amr ItNhoivcIkć (e.g. p , generally known facts have been established. Many 1951; aIkoLIć , 196a0kS; IMM ovIć , 1970, 1a9N7T1Ić , papers havea bvLeoevnIć publisheduk aobvIoć ut this afateSkr aWrEov rld 197u7L; INć , 19a7d6Iv; oMjEvIć et al. , 19u9N0čI;ć p War I (e.g. p , 1922; L , 1922; L et & d , u1L9Ić 90; r et al ., 2010; d et al., al., 1931). after World War II, the interest of the geo - 2017; d et al., 2019). Having all this in mind, as logical public spread to the other side of the danube, well as the existence of clear discordant relations and with the beginning of hydrocarbon exploration between stratigraphic units and, in that sense, sig - in Banat and beyond, the subsurface geology of the nificant stratigraphic deviations in a smaller area widaerrIN oBveIlć grade area became even more relevant (local unconformities, erosions, pronounced dis - (M , 1959, 1961, 1962). For example, it was junctive tectonics, etc.), the presentation of our re - understand that the subsurface geological composi - sults will contribute to a better understanding of tion of that area is a reflection of the genesis and evo - these processes. lution of the pannonian Basin, pronounced syn- and Considering that nowadays it is difficult to get di - post-rift Neogene tectonics and block structure. This rect data related to exploratory drilling and geo - conditioned the existence of differences in a relatively physical research of the Neogene of vojvodina, and small area, the formation of smaller or larger depres - that subsurface geological models are established sioInkosL Iać s opposeTdEv atoNo dvIićstinct structural elevations mainly on the basis of re-interpretation of existing 2(N , 1976; S , 1977). Neogene sediments data and their further aGepopl. raon.x Biamlk.a ptoilouons,. , a2 0h20u, g81e ( 2d),a 1t–a 32- heterochronously cover the pre-Neogene bedrock, base of geological documents (primarily strati - Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

graphic-paleontological, structural and well-logging deposits with volcanics of the Lower and Middle data), was the key motive for presenting these re - Miocene, marine and marine-brackish Middle Mio- sults to the wider professional and scientific public. cene and caspibrackish to freshwater sediments of Having in mind that the studied area in the northern the upper Miocene to pliocene). due to the large part is completely covered with Quaternary sedi - number of papers regarding this, only those in which ments, the paper especially emphasizes specific and the authors dealt with various aspects of the predo - original interpretations of the distribution and minantlyu MkoivoIcć ene of thaev LaorveIć a are listeadSk acrhErvo no lo - depth relationship of main stratigraphic units as gically ( LaSkarEv , 1922; p EICHE,r 1922B; rLadovIć et al., wAenl lo avs ethreviire mwo ropfh tohsteru gcetuorlaol gfeiactaulres. 19a3r1IN; oL vIć , 1949; W & o ILETIć , 1p9a5jI0ć ; background M ar,I N1o9v6Ić 1, 19E6M2EN, C1I 977, 19T8a2N;G aMčI LovIć -S , 19r S6T1Ić; M & k TEvaNo, 1v9Ić 69; S , 1969I ; koLIć , 1973, 19IL8a5ko; SvIć , 19IH5a7jL, o1 v9Ić75, 19N7E7žE; vNIć - , 19u7M6a; r M uNdI,ć 1986; M aSkovIć & k aTovIć , 1989; Š oLIć & r , 1992NE; žvEvIć a& N IMć , The studied area is shown on the index (to - 1996; drSTIć , 1997, 1998; kCHWarCHa&NS G , 2005, po nyms) map (Fig. 1). It is spatially limited by a 20aN0I8ć ; k et al., 20NĐ1E2L;k SovIć adIvoejEt vaIćl ., 2015; quadrangle: Belegiš–Banatsko Novo Selo–v. Mošta - GovaNoveItć al., 2016; a & r , 2018; nica–Mala ada (Brestovik). It is mainly covered by j et al., 2019). The most important details and thinner or thicker Quaternary deposits of various results of the mentioned research will be discussed genesis (alluvium, river-marsh sediments, river ter - in more detail in the following chapters of this paper. races, deluvial-proluvial deposits, loess-paleosoil se - In the base of Neogene formations, there are the qvukeonvcIć es, etc.), asa re kvoidveIć nced by nuENmaedrIć ous data (e.g. older rocks mostly built of various post-Triassic for - I audEN,y 1I 966; M N,E 1ž9Ev8I5ć ; N et al.,o 2L0jIć11; mations (diabases, serpentinized peridotites, radio - G et al., 2015; k et al., 2018b; T et larites, clays, argiloshists, limestones, sandstones, al., 2014). spilites, andesites, etc.) about which there are puIMb I - lTirsIhjEevdIć data as wEeTlklo (veIć.g. d - NĐELko, v1I9ć 31; p , 1951; aaNovIć ,E 1M9E6N0CI, 1973, 1987; čNEžEvI&ć k , 1988, 1o9L9jI9ć ; k EreItć al., 1994; T uN , 1čI9ć 96; Đ et al., 2010; d - et al., 2017). The stra - tigraphic position of these se dimentary rocks in the area of southern Banat and the Fig. 1. Geographic position of the studied area (a, white rectangle), and a close-up with the Belgrade hills was deter - main toponyms which mark position of the studied boreholes (b). Key: white circle – studied mined on the basis of diffe- deep boreholes; full lines – geological cross-sections (I, II, III). rent maaNcTrIoć - andEć mEriocvrofauna (eN.gEž. EpvIć & Š r, a1G9IN 75; k et al., 1994; B et al., 2011). The genesis, chem - istry features and age of ig - neous rocks were determined Below the Quaternary cover, there is a complex of through their spatial relationships and relations to Miocene and pliocene sediments of different thick - the surrounding rocks or based on geochemical Gneosl.s a nfo. Bramlk.e pdol udous.,r 2i0n2g0 , t8h1 e(2 )e, 1v–o32lution of the pannonian chokaorLacteristics and isotope geochro nology (e.g3. Basin and its southern rim (continental-lacustrine S et al., 2020). ĐoRĐE MaRiNoVić & L jUpKo RUNDić

Material and methods

aNovIć EMENCI taken primarily from č aN&TI ć k EćE(r1o9v 88) and oathNeTIrć pubulLicIć ations (eN.gE.ž EpvIć & Š , 1975; The presentation of the depth geological struc - p & d , 1990; k et al., 1994). However, ture of the Belgrade wider area is the result of the in order to avoid burdening the text with continuous analysis of 15 deep wells on the Banat side of the repetition of the signatories of internal reports or danube river (Fig. 1). In the southern part of studied works of the published paleontological and other area 37 mostly shallow wells were analyzed. It data from the deep wells of Banat, in the chapter should be noted that in the given scale of the gra - „Stratigraphic review“, the corresponding authors phics (Figs. 1 and 10), not all the toponyms men - are grouped as follows: determination of Neogene tioned in the text nor shallow wells could be shown. microfauna - v. Marković, N. Gagic („Naftagas“, Novi The complete list of used wells can be found in the Sad); determination of Mesozoic microfauna - M. ča - Table 1. The collected stratigraphic-paleontological nović („Naftagas“, Novi Sad) and Đ. Mihajlović data, performed well logging and seismic-geological („Geozavod“, Belgrade); determination of Neogene correlations were analyzed by the first signed au - macrofauna - p. janković, Đ. Marinović („Naftagas“, thor (ĐM), as well as a part of the paleontological determination related to Neogene units in the pre - sented deep wells. on the Banat side, the depth ge - ological-stratigraphic demarcations are baarsIeNdo voIćn correlative markers of well logging ( M , 1970, 1971 – see Fig. 2), harmonized with available paleontological, petrological and hydrochemical ele - ments, transferred on the network of reflective seis - mic sections. on the Belgrade side, numerous literature-processed surface data have been supple - mented by a selection of stratigraphically instructive wells and representative geological columns (by Ljr). For the entire area, gravimetric maps of iso - gams (mgl) and vertical gradient (E) were used from the geophysical data – Funds of “Naftagas” (Novi Sad) and “GeozavoIMdI”N (BelgradeIL)I,B wajkhIić ch were par - tiIaLlIlBya pjkuIć blished ( S , 1963; B et al., 1979; B , 1998). In addiItkiooLnIć , geoImMIaN gnetic maps ∆z anomalies ZMp 1954 ( N & S , 1959) and the fund of the Za intensity section were used, except for the areas that were deleted from the competent authorities in due time. Based on all of this, the first signed author con - structed subsurface geological sections of the SW Fig. 2. Synthetic stratigraphic section of the borehole Ov-1 Banat (profiles I, II and III) as well as the map of 2 (compiled by ĐM). The plotted diagram is one of the first geoelec - Neogene base configuration (E = 100 m), which cov - tric measurement in Serbia performed in 1950 with the Schlum - ers an area of about 2,000 km . The depth geological berger apparatus (Zagreb team). Key (generally): 1, serpentinite; model defined in this way is supplemented with 2, conglo-breccia; 3, siltstone & claystone; 4, sandstone; 5, lime - facts that refer to the subsurface and outcrop geo - stone; 6, marl, and 7, sand & gravel. logical data of the wider area of Belgrade, that is south of the danube river (Ljr). 4 determination of the stratigraphic affiliation of Geol. an. Balk. poluos., 2020, 81 (2), 1–32 geological units from the Banat deep wells was Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

Konkisporites

upper Lias (J 1) Novi Sad); determination of microflora – N. pantić sp. were drilled in the BNsj-1 well at (Faculty of Mining and Geology, Belgrade), p. Šeće - a depth of 1901–1908 m (Fig. 6). Stratigraphically, rov and I. dulić („Naftagas“, Novi Sad); petrographic theasNeo vdIeć posiEtMs EcNoCrIrespond taoN TthIć e uLIć analyzes - r. kemenci („Naftagas“, Novi Sad); physi - (č & k , 1988; p & d , 1990). Mirifusus mediodilatatus Pavicingula cal and chemical analyzes of water - a. dekanj and on the other side of the danube river, in the well boesi a. Maksimčev („Naftagas“, Novi Sad); correlative G-1 (Grocka), in adepth interval from 1,300 to 1,378 stratigraphic distinctions - Đ. Marinović (Naftagas, m, the pelites with an abundüaSnT ce of radiolarians Novi Sad). In the area south of the Sava and danube ( aroNa (r ) and rSitvrearst,i tghrea rpefhericen rceevs iaerew cited in Table 1. (p ), less often with spores and NoEthžEevrI ć pa - Belleza decora Semihsuum lynomorphs were drilled (Š. Goričan, in k et Praewilliriedelum robustum Mirifusus Pre-Tertiary basement al., 1994). relatively recently, from dark red radio - dianae Spongocapsula palmera larites from a depth of 1,378 m, thüeS T next radiolarians late middle were identified: (r aTS)u, oka sp . Jurassic a, arrEr (M ), ES SaGNo s.l. ( k ), e p - Parapodocapsa amphitreptera Cingulo - In the studied area, the pre-Tertiary basement which corresponding to the turris carpatica Eucyrtidiellum ptyctum makes the geological and stratigraphic units of , while from a depth of 1,400 m the younger Jurassic Archaeodictyomitra minoensis jurassic and Cretaceous age of different genesis. jurassic association of radiolarianso wrEaMsa dN etermined: Protunuma japonicus uMITrICa (F ), The oldest Jurassic unit Zhamoidellum ovum Hiscocapsa hexagona IEdEL aNFILIpdpo , (r IZuTa&NI S ), aTSuoka ao Upper Jurassic J3- middle Oxfordian to late (M ), uMITrICa M & y , Tithonian is a series of dark to orI d , ultrabasic rocks ( σ) black tectonized clays and argiloshists with sand- (H ). Biostratigraphically, it corresponds to the siltstone intercalations permeated by quartz grains. ErIć ( It was found in the well pč-1 (2,395–2,733 m) and ) ( Đ et al., 2010) (Fig. 6). can be correlated with similar deposits in the close The complex of is repre - vicinity, i.e. with black sericitized claystones with sented by peridotites and serpentinized peridotites sandstone inserts found in the well Crepaja-1 (Figs. 2–4). They were found in the wells Gl-1 (1a,5N9T7Ić –1,603 m) then, generally, with “shiny shales” (below 865 m) and Gl-2 (below 835 m) in the north (p , 1978), as well as with black sericitized of the studied area where they form the pre-Tertiary thiny-bedded claystones, siltstones and sandstones basement. Ophioglosum delectus Cu - of the well padina-1 (1,554.3–1,613.6 m). Based on Somewhat further to south, in the ov-1 well, pressacites minor Protopiceacerina the analysis of the palinospectrum (insight into the compact peridotites at the bottom of the well and Picea Podozamites rotundus original report dated 28.06.1958 byo NLk. BHoavltIeTšIN)a dom - cracked serpentinites at higher levels were drilled Gingko praecuta Leptochylus inated by aLyavkINa B , in the interval 424–454,46 m (Figs. 2, 3). They be - Bennettitales delucidus Lophotrile - oLkHovITINa (M ), oLk long to the masif of peridotite-pyroxene rocks. Mor - tes Selaginella Bothrychium Lycopalium BHovITINa , sp., oLkHovITINa B - phologically, the top of the buried magmatite is lower Jurassic - Lias (J 1) , B oLkHovITINa , located in the narrowest area of ovča, and its the sp., B , longitudinal depth root most probably in the belt of sp., sp., sp., the main tectonic fault, in the area between the Sib - Nannoceratopsis sp., etc. the was deter - nica and Tamiš rivers (Fig.3). an ultramafic complex gracilis Gonyaulacista mined (Figs. 3, 4). was identifNiEeždE vinIć the Sa-2 well, between 352 and Ginkgoales ., Cycadophytes Claystones and clayey siltstones with the asso - 531.5 m ( k et al., 2018a). peridotites and ser - ciation ofL dBiEnroTfI lagellate algae ( cf. pentinized peridotites are degraded, tectonic de - Geol. an. Baalk. poluos., a2n02d0, 81 (2), 1–32 sp.), spores and formed and intersected by a network of cracks. They5 pollen of the type sp sp., are hydrothermally altered (Fig. 3). ĐoRĐE MaRiNoVić & L jUpKo RUNDić

Fig. 3. The geological cross-section Ovča–Pančevo–Dolovo . The stratigraphic units and their boundaries are consistent with geoelectric logs. Comparative review of the nomenclature of depth hydrogeological reonization, according to MArINOvIć (1982).

Masses of similar serpentinized peridotites and on the Belgrade side, similar the compact ser - serpentinites were discovered on the surface north pentine breccias were discovered in well Bt 1-2 and east of avala Mt. (Ljubičica, Bubanj potok, Zuce). (Ljubičica–Bubanj potok) where, in the interval of The Lower Cretaceous (K K1-5 In the well Bt 1-2 (Ljubičica–Bubanj potok) below a 28–38 m depth, they overlie th1,e m1 ass of serpen - 38 m thick seriueNsd oIć f younger rocks, serpentinites tinized peurNiddoIć tites in which drilling was completed were drilled ( r et al., 2019 - Table 1). Similar (92 m) ( r et al., 2019). observations about the appearance of these rocks at ), principally the meanrtoivoInć ed sNitEežsE vhIć ave been omLjIeć ntioned boeLjfIoć re with the characteristics of turbidite, in the segments (er.Igv.I Mć & k , 1985; T , 1996; T & of coarse-clastic flysch, was drilled in the well om- CTreta, c1e9o9u7s ). 1 (omoljica) at a depth of 932–1,905 m (Figs. 4, 6). Spheres are rarely present in the deepest levels of the The coarse clastite complex (K Hedbergella in - B well (laminated siltstones below 1,740 m). above fracretacea that, in the depth interval from 1,566 to 1,569 m, the glauconite siltstones with diabase debris, interbed - Coptocamphilodon fontis Acrop - ) lying over the ded with sandLsatoESnSeNsE rand marls with orella ultramafic rocks was discovered in the wells ov-1 (G ) were found. Breccias similar and Sa-2. It is built of hard breccias, or conglo-brec - the synsedimentary fragments coanTtrauinLI uaS lgal re - cias. The clasts originate mainly from ultramafites, mains of p , predominantly angular pieces of seprentinized peri - sp. which would corresponda tNoo svhIć allowE MfaEcNieCIs Hedbergella dotites (Fig. 3) tightly bound by cement that par - of the Barremian–aptian Stage ( č & k , Lenticulina Textularia tially contains a high percentage of carbonates. The 1988). In deeper levels (1,108–1,495 m), in the suc - Globochaeta alpina thickness of these breccias is from 94 m in the well cession of siltstones, sandstones and partly laminated ov-1 (330–424 m) to over 120 m (229–352 m) in micrites, the presence of foraminifers ( 6the well Sa-2 (Fig. 5). In the ov-1 well, this complex sp., sp., GoeMolB. anr.s d Bpa.l,k e. ptcol.u)o as.n, 2d0 2t0h, e8 1s (p2)h, 1e–r3e 2 is covered by the tectonized flysch sediments. of L was recorded. In the Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

Fig. 4. The geological cross-section Glogonj–Pančevo–Danube (Mala Ada)–Brestovik. For the rest of legend, see Fig. 3.

Cenosphaera Dictiomitra Litho - doz-1 (dolovo) in a depth interval from 1,800 to campe 2,200 m (Fig. 6). They are made of hard siltstones, Hedbergella Bigenerina Tex - marls and micrites with a microfauna of radiolari - tularia ans such as sp., sp., Colomiosphaera Heliosphaera sp., etc. among foraminifers, the pelagic Cadosina-Stomiosphaera sp. and benthic sp. and Globochaeta sp. were found. among microplankton, the alpina representatives of sp., Fig. 5 . Detail of hard, reddish-gray and dark green conglo-breccia sp., association dominate probably of the Lower Cretaceous. Borehole SA-2 (334 m). Photo as well as rare zoospores ( ex. gr by Lj. rundić ). at a depth of 1,980 m and at bottom of the well (2,200 m), synsedimentary spillites and sub - marine basalt outflows were registered. By correla - tion of logging markers, similar the Lower Creta- ceous deposits (Barremian) were found in the well vl-1 (1,222–1,355 m) in vladimirovac. shallowest part, highly tectonized marls and silt - apart from the surface, the Lower Cretaceous stones are without paleontological markings, while formations were previously found in some wells, for the siltstone-sand breccias, micrites and biosparites example, near SkadaroliMjaIć in the centre of Belgrade (997–1,100 m) contain hayNdorvoIzć oas aEnMdE NdCeI tritus of in - (BC-3, 147–321 m; T , 2005), and close to the Tintinoporella carpatica determinate mollusks ( č & k , 1988 ). Faculty ToEfv avNeotevrIć inary Medicine (vF) at a depth of Colomiosphaera heliosphaera Globochaeta In Banatsko Novo Selo, in the well BNs-1 82 m ( S , 1977). recent research and dril - alpina (1,171–1,243 m), marly siltstoneusr GaEnadN ubioImLIpicErSiCtu es ling near the Museum in dedinje, the urgonian lime - with (MoGLEr -F ), stones in the depNEthžE viInć terval of 29–33 m have oMBard (v ), identified (B-11, k et al., 2015). at right bank L , and rare headbergels, textularians of the Sava river, during the construction of the res - and frequent radiolarians were drilled. These rocks idential and business complex “Belgrade Water - coar NreosvpIć ond EtoM EtNhCeI Hauterrivian–Barremian Stage front”, the urgonian limestones and sandstones G(čeol. an. Balk&. p koluos., 202,0 1, 891 8(28), )1.– 3S2 imilar the deep-sea Lo - wNeEržeE ivdIćentified at depths between 60–94,7 m (B-17, wer Cretaceous sediments were found in the well k et al., 2017 – Fig. 7 and Table 1). ĐoRĐE MaRiNoVić & L jUpKo RUNDić

Fig. 6. The geological cross-section Grocka – Banatsko Novo Selo. For the rest of legend, see Fig. 3.

(Fig. 3). Similarly, they have been documented within the tectonized and partially eroded com - Globotruncana arca G. tricarinata pressed synclinal depression near Bavanište (Bav-1, G. concavata Marginotruncana Fig. 6). From a depth of 1,823–1,825 m, a rich asso - coronata Marssonella oxygona Di - ciation of planktonic fourSaHmMianN ifers was determineudE : carinella concavata rosita fornicata rEau (C roTZEN ), (Q - ), oLLI (B ), EuSS (B ), roTZEN (r )L, uM MEr (B ), (p - Fig. 7. Borehole B-1, “Belgrade Waterfront”. The light-gray, ), etc. The association also includes numerous porous limestones of Sarmatian ( right ) overlie the dark-gray globigerinids, lenticu lins, textularians, rotaliadNso, vraIć di - Urgonian limestones (left) at depth of 60 m. It has been visible an Prediscospahera cretacea olEaMrEiaNnCsI and ostracods (det. M. čanović – č & imprint of the Cerastoderma vindobonense (Partsch-Laskarev) Watznaueria barnesae k , 1988). In the depth interval 1,874–1,993 m, mollusk shell. Photo by Lj. rundić Eiffelithus eximius Chiastozygus the calcareous nan noplankton were identified from litterarius Tranolithus orionatus sanrkdHsatoNnGEeLsS kay nd siltstones: LaCk LaCk Zygodiscus elegans (a arNES ), TovEr (B in B and B ), órka (S ), EINHardT (G ), arTNEr r , G , etc. which indicates the Stratigraphically undevided the jurassic-Creta - upper Tu ronian–Senonian (det. Đ. Mihajlović- inter - ceous formations were found in resnik and rakovica nal report of the Naftagas, unpublished). (kGuNkd-1Ić 3 and kGk-15) at 118 and 80 m, respectively on the Belgrade side, the upper Cretaceous fly - (r et al. 201a9SL)a, raEnvdIć in CaeGrIć ak n2e-a4 r rakovica sch sediments were drilled on ada Ciganlija (dNEBž-E1v0Ić , Upper Cretaceous sediments K ,K (BC-3, 42.3 m – M & G ,F 19726). They dis - 21m; dB-9, 24m; dB-8, 60 m; dB-6, 80 m - k cordantly underliethe various Miocene formations. etu Nald. I2ć 012), near Branko’s bridge (upd-1, 127 m - In the base of Tertiary, tectonized flysch-like the r et al. 2011), in New Belgrade at the conflu - ( ) built ma - ence of the Sava and the danube rivers (pduSN-E3 , inly of succession of sandstones, laminated marls ž>E1v2Ić 6 m, paNdIuć S-8, 43m and pduS-13, 128 m - k - and siltstones were documented. In the well ov-1 & G , 2005, 2008). Further to southpa, jtIhć ey (8ovča) they were observed between 166–330 m and wžeordež o fouonMdIć in LeštaneG e(oLl. ean-.I BI)al ka. pt o2lu7os8., 2m020 (, 8S1 (2), 1–3&2 interbedded by the sequences with organic “rot” d -T , 1973). Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

Table 1. Excerpt data of the Neogene basis and the represented Neogene cover of the Belgrade area.

Tertiary

Miocene molasses and shows a discordant relationship to the The early Miocene “pre-Badenian” (Pbt, Pbp) older substratum, i.e. upper Cretaceous flysch. It is described in detail and garraIpNhoivcIćally presented from a lot of daereIpN owveIć lls (eE.gM. EMNCI , 1959, 1961, 1962, 1977; M & k , 1964). In the wells ov-1 Gise otlh. aen .o Bladlke. spto lTuoesr.,t 2i0a2r0y, 8 u1 n(2i)t, 1 f–o3u2 nd in most of the men - (110–166 m), Sa-2 (145–229 m), and G-1 (1,150–9 tioned wells. It is built of terrigenous-subaquatic 1,300 m), multicolored clastites with a predomi - ĐoRĐE MaRiNoVić & L jUpKo RUNDić

nance of greenish and brown-red clays, gray-green permeated with volcanoclastites is known on the gravelly sands and conglomerates, fragments of surface of the terrain and from numerous waevLllosv Iićn Congeria ., Limnaeus Planorbis cherts, serpentinites, carbonates, and carbonate višnjica, TSalNaGnacči,I LvoevliIkć o Selo anda TvoLorlvaIkć area ( p oLIć , Unio concretions were observed (Figs. 3, 6). In the whole 1922; S rSTIć , 1969; p uNdI,ć 1976; d , series, the remains of freshwater molluskan fauna 1997, 1998; k et al., 2012; r et al., 2013). such as sp arINovIć sp., sp., In vicinity of the Slanci village, the well vp-150 up sp. and ostracods ( M , 1962), as well as to 194 m deep, did not enter the bedrock of the fish fragments have beenu pLIoć orly preserved and dif - basin and the pre-oBLaIdć enian series was drilled at a ficult to determinate ( d et al., 2010). Sporadi - depth of 13.6 m ( d , 1997). In other parts of Bel - cally, smaller occurence of coaly clays or thinner grade, drilling has found the equivalents of this old - Pityosporites microalatus Tria - layers of coal can be found. However, based on the est Miocene unit, over which the sediments of the triopollenites quietus Monocolpopollenites analysis of the palynological spectrum in the G-1 marine Badenian mostly lie discordantly. In the B-11 tranqui Polypodiaceos po - well, in which the dominant polleno gT rainFs of cHonifers well (near the May, 25 Museum), the colorful Lower rites maschiensis Leiotriletes mexoides are oToNIé (r. p ) p . et T , Miocene succession was found at a depth of 9 m and oToNIé (p ), near to thNEež dEv. IMć išovirćS THIćospital (B-1) at the depth of llus ( p )u rar nd spores Ed 96 m ( k & k , 2015). In the Bt 1-2 well Marine, archipelago-dispersed sediments of M ., k (Ljubičica–Bubanj potok) similar unit was found, the Badenian (Bd) with the accompanying association of microflora re - where in 21uN mdI ćdepth, it lies under the Badenian car - mainsN,E tžhEev Isć eries corresponds to the Lower Mioce - bonates ( r et al., 2019). ne ( k et al., 1994). Close to ovča, this serie of oxidative genesis localy thickens towards east on a transgressively cover strati - sub- visible morphostructural ridge. However, in the graphically different geological substrates. They were aquatic pelites (Pbp) of reduxing genesis sunken part east of the system of stepped faults, found in wells ov-1 (76–110 m), Sa-2 (112–145 m), within the pančevo depression, there are signifi - G-1 (1,060–1,150 m), Bav-1 (1,596–1,821 m), doz-1 cantly different pre-Badenian, the gray-black (1,479–1,800 m), do-1 (1,515–1,889 m), BNsj-1 (pč-1). (1,350–1,724 m), pč-1 (1,452–1,980 m). Shallowest In two intervals between 2,339 and 2,381 m, the below the surface (76 m), they were drilled in the black to black-gray slightly marly siltstones with Mezosoic ridge near ovča where their thickness is Polypo - thinner transition zones into gray-black fine- only 35 m (Fig. 3), while on the sides of the mor - diaceosporites spiniverrucatus P lusaticus grained, partially and clayey-marly sandstones were phostructures Gloganj–jabuka, omoljica, Banatsko Polyo diaceosporites Laevigatosporites Toro- cored. a scarce Lower Miocene content of the small Novo Selo and vladimirovac they completely wed ged io sporites Tricol popollenites Ephedripites fern and pollen spores was found in them: out. They are the deepest observed in the pančevo Sulbtriporopollenites simplex Triatriopollenites hia - cf. , . cf. , depression (1,980 m), where they transgressively tus Monocolpopollenites sp., sp., and discordantly ovelie the early Miocene rocks and sp., sp., sp., reach up to 550 m thick. Near Bavanište (1,821 m), , dolovo (1,889 m) and Banatsko Novo Selo (1,724 m) , sp., etc. (det. I. dulić - inter - they discordantly overlie the upper Cretaceous or nal report of the Naftagas, unpublished). Lower Cretaceous deposits (Fig. 6). Based on very nu - By correlating of the logging diagrams (Mari - merous fossil remains (mollusks, foraminifers, algae, nović, Maksimčev and janković), the Lower Miocene etc.) three different type of the Badenian facies have interval was simultaneously extended by insight into been identified: a) Basin and the basinal-lagoon, b) sieve samples (Stratigraphic frame 1,980–2,395 m , coaasrtIaNlo avnIć d the shallow water-reef and c) mixed one the Naftagas fund), which indicates that the series (M , 1977). Concerning the differeNnEtž BEvaIdć enian reaches a thickness of over 400 m (central part on facies in thajeIć studied area, also wrNoĐteE LkkovIć eta daIl . the Figs. 3 and 4). v(1oj9E9vI4ć ), G et al. (2008) and a & r - 10 on the right side of the danube river, an early (2018). FindingG eoolf. apn.l aBanlk. tpoolnuoics. , a20n2d0, 8b1e (2n),t 1h–3ic2 Miocene continental-lacustrine “colorful” series foraminif ers in the well do-1 (1.575–1.690 m) such Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

Asteri gerinata planorbis , Cibicides dutemplei , C. ungerianus C. pseudoungerianus Globigerinoides Trilo - d rBIGNy batus) trilobus Glandulina laevigata , as d rBIGNy ( ’o d ) rBIGNy stones were dNiEsžcEovvIeć red arStT 3Ić 0 m depth and are over Cibicides (= Heterolepa) dutemplei Globu - ’o uSHMaN ’o , 60 m thick ( k & k , 2015). at dorćol, near lina gibba Borelis mello EuCSS , d(=r BIGNy the power plant, in the well EC with a total depth of Lucina incrasata Cardium (r ), d rBIGNy ’o 161 m, which did not drill the paulekorveIć lief, Badenian Anadara Ostrea Chlamys Dentalium d rBIGNy ( ’o ICHTEL ), oLL sediments were found at 97 m ( L , 1922). In an badense Lithothamnion ’o , u(FBoIS & M ), unnamed well in kumodraž (here marked as ku – see etc.), mollusks ( d , sp., Table 1), they were discovered at a depth of 149– asrpT.S, CH sp., sp., 333.6 m, while in veliki Mokri Lug (vML) and p , etc.) and red algae sp. žarkovo (S-3) they were discovered frpoamjIć deptžhods žoo f confirm the true marine Ba denian mixed character of 72oM aInć d 76.9 m TtoEv tahNeo evnIć d of the wells ( S & d - the mentioned deposits (det. v. Marković & M. Buljan T , 1973; S , 1977 - Table 1). In the area – “Naftagas” Novi Sad). In terms of facies characteris - of Ljubičica and Bubanj potok, they are already The marine-brackish sediments of the Sarma - tics, in addition to various sandstones, marls and drilled at 8m of depth (Bt 1-2) and are quite reduced ti an (Sm marly clays, typical reef limestones with an abundance in utNhdicIćkness and overlie the pre-Badenian mollase of fossil algae, bryozoans, foraminifers and molluscs (r et al., 2019). have been identified. In the area of the Belgrade danube meander, they ), built of sands, laminated marls, siltstones, were explored on the surface in višnjica, Slanci and clays and partly sandy limestones, were found in the veliko Selo and transgressively overlie the Lowear following wells: ov-1 (70–76 m), ovča c.b. (91 m), vMLioovcIć ene “colourkfouvl Ićseries” oro SLIlć anci Formationu (NpdIć- Sa-2 (103–112 m), pč-1 (1,031–1,452 m), doz-1 , 1922; LCHWar,Z 1H9aN2S2; d , 1997; 19aN9d8I;C r (1,046–1,479 m), do-1 (990–1,515 m), G-1 (620– et al., 2013; S et al., 2015; M et al., 1,050 m), om-1 (749–932 m), Bav-1 (1,067–1,596 m), 2019). Near the confluence of the Sava and danube BNsj-1 (952–1,350 m), BNs-1 (1,053–1,111 m). Simi - rivers, in the wells pduS-9 and pduS-10, the Baden - lar to the Badenian deposits, they have the smallest ian sediments were drilled in the interval 72–84 m thickness in ovča and appear below the surface of depth and were mostly built of the LNeEižtEhvaI ć limestaoNnIć e the terrain at 70 m. From there to the east, towards and a small part of sandstone ( k & G , Bavanište and dolovo, they sank significantly, thick - 2005, 2008). In the pduS-13 well, the similar massive ened in the pančevo depression and reached a thick - limestones are found at depth of 93–128 m and cover ness of 400–500 m (Fig. 3). It is similar in the area of the upper Cretaceous sandstones. on the Srem side, Grocka in the extreme south of the studied area (Fig. i.e. in New Belgrade, the Badenian deposits are also 6). at the structural ridge of omoljica, their thickness present in other wells as shown in Table 1. has been reduced to about 180 m. on the disrupted In the area south of danube river, the Badenian paleohorst of Banatsko Novo Selo (BNs-1), the re - dpeapjIoć sits hžaovdež o beeonM Isć tudied byT EsveavNeorvaIlć authors (e.g. duced Sarmatian layers about 120 m thick, discor - S & d -T , 19N7E3ž;E SvIć aNIć , 1975, 19aN7I7 ć dantly overlying the Lower Cretaceous paleorelief. and references therein; k & G , 2005; G Fossils are not numerous in the Sarmatian deposits, Elphidium macellum et al., 2016). They occupy a significant area near city but their finding clearly indicates a change in the sed - Elphidium hauerinum El. reginum center (kalemegdan, Tašmajdan, dorćol, karaburma, imentation regime and the transition to a reduced- Quinqueloculina acneriana Poroso - konjarnik, kumodraž, Banjica, rakovica, Torlak, etc.) marine environment. In addition to thIeC HsmTEaL ll benotLhL ic nonion granosum Ammonia beccarii or were proven in wells where they are covered by foraminifers ( d rBIGNy (F & Md r), younger Miocene or Quaternary deposits. For exam - BIGNy ( ’o ) d rBIGNy ( ’o - ple, in the well B-1 on ukNadlIeć megdan they were found ), d rBIGNy ’o , Ervilia dissita , Pirenella at a depth of 23 m ( r et al., 2011) while near INNE ( ’o ), ex. gr. picta , Mus culus sarmaticus Ceras - Branko’s bridge, on the Srem side, observed in the (L ), etc.) and numerous ostracods, these depo sits well udp-1 at a depth of 68m (Table 1). In Serdar jola contain the particular assemblageIsC HoWf abLidvalves and GSetorle. aent. Bnaelka. pro tluhoes. , d20.2 M0, 8iš1 o(2v), i1ć– 3H2 ospital, in the well B-1 gastropEoFdrsa NsCuE ch as E aTuEv 11 about 120 m deep, Badenian sands and sandy lime - d (G ), ĐoRĐE MaRiNoVić & L jUpKo RUNDić

toderma vindobonensis Cardium (Cerasto - derma) trans car pa ticum

arTSCH (p rIS)C,H kIEvICH 2017). at the pylon of the ada bridge, the wells arINovIć NEGžEvIć (Fig. 8) dB-6, dB-7 and dB-8 (see Table 1) drilled Sarmatian (MajIć , 1970, 1977; k et al., 1994, 2018a; crumbly, sandy limestones in the depth interval of G et al., 2008). 40–65m which discordantlyN oEvžEevrIlćie the upper Cre - taceous-paleogene flysch ( k et al., 2012). on the čukarica side of the bridge, Sarmatian was drilled shallowly in the same relation to the mentioned fly - sch and was found inN tEhžeEv wIć ells dB-9 (14–24 m), and dB-10 (11–21 m) ( k et al., 2012 – Table 1). In Brackish and caspibrackish sediments of the the part of the terrain around Leštane (Le-II) and ku - Upper Miocene, Pannonian stage s. str. (Pn), modraž (ku), the Sarmatian carbonate sediments reach a significantly greater thickness (Table 1).

known as the Lake pannon deposits have a signifi - Fig. 8. Cardium (Cerastoderma) transcarpaticum Grischkievich cant distribution. Lithologically, they are built of (Ov-1, 70 m). The natural size of the fossil is 14 ×12 mm. marls, sandy marls, siltstones and sands that were Determination and photo by Đ. Marinović. discovered in the following wells: ov-1 (29–59 m), ovča c.b. (30–70 m), Sa-2 (35–93 m), Gl-1 (829–865 m), pč-1 (921–1,031 m), doz-1 (856–1,046 m), do-1 (712–990 m), G-1 (300–620 m), om-1 (540–749 m), Bav-1 (843–1,067 m), BNsj-1 (845–952 m), and BNs-1 (902–1,053 m). The total thickness of these Sarmatian deposits, widely represented in the deposits in the depression south and north of area of the Belgrade danube meander, are present on omoljica is more than 300 m with a decreasing trend the surface in karaburma, Mirjevo, and further to the of thickness towards Banatsko Novo Selo at about Congeria ba - southeast towards vinča, ritopek, Leštani and Gro- 150 m (Fig. 6). Near ovča and Glogonj, they are re - natica C. ramphophora ckTaE, vaabNoouvtI ć which thepraejI ć are previoIuHsaljyL opvuIćblishNedEž dEvaItć a duced to only about 30 m (Figs. 3 and 5). They con - Monodacna viennensis Limnocardium promulti - (S uMa,r 1977u;N SdIć , 1987; NMEžEvIć &aN kIć , tain a rich and diverse fauna of mollusks, among striatum Orygoceras fuchsi Gyraulus . 19uN8d9I;ć Š & r , 1992; k & G , 2008; which are porEerdNoEmS inantly represented: ruSINa preponticus r et al., 2012). In addition, they are known from r. H (Fig. 9ap),p B , Lineocypris reticu - proITkroopv,I ćčukauriNcdaI,ć rakovicaN, LEžeEšvtIać ne, resnik, Grocka EkELIuS p , ITTL lata Serbiella sagitossa Hungarocypris (M uN&dI rć , 1991; k et al., 1994, 2012, j orj,a NovIć raMBErGEr k , cf hieroglyphica Amplocypris subacuta 2017; r et al., 2019). G -k , et al. There are Cyprideis heterostigma obessa Hemicytheria lo - Close to the Sava and danube rivers confluence, also nuEmHEeS rous ostracods such arsS TIć erentheyi Sarmatian sands and sandy limestones were drilled in M , EHES k , aLaNyI the wells pduS-9 (52–72 m) near Branko’s Bridge, M , EuSS Z , pduS-10 (55–84 m) near the old BridNgEež aEnvIdć pduSa-N1Ić3 EHES arINovrIć , pajIć (82–93 m) near the ušće palace ( k & G , uNMdIć , etc. ( MNEžEvIć , 1970, 1977; S , 2005, 2008). Similar thickness of sediments and 19uN8d7I;ć r ITr,o v1I9ć 90; k uNdIć et al., 1994, 2018a; their depth position were found in the wells pduS-3 r & M , 2005; r et al., 2011). (38uN–d5I2ć m) and pduS-7 (52–72 m), upd-1 (60–68 m) South of the Sava and the danube rivers, the pan - (r et al., 2011). In the well B-1, near the Belgrade nonian white and gray marls and silts have a large Tower (“Belgrade Waterfront”), it was determined surface distribution in the area of the city of Bel - that the Sarmatian sandy limestones about 30 m thick grade. They underlie the Quaternary alluvial, prolu - (129–60) transgressively overlie the LNoEžwEevrIć Creta - vial, loess or loess-likIeLG EseTeoIć ld. ainmp. aBejaInćlk.t pso, luaons.d, 2 0or2vS0Te, 8Irć 1l i(2e), 1th–3e 2 ceous sandstones and limestones ( k et al., older Miocene units ( M -S , 1961; k , 1973, Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

lija, near the ada bridge, they were found in wells dB-6, dB-7 and dB-8 in the depth interval of N2E1ž–E6vI5 ć m where they overlie Sarmatian limestones ( k et al., 2012). In New Belgrade, they were drilled di - The Upper Miocene - Pontian stage rectly below the Quaternary deposits at a depth of more than 30 m in wells dBN-4Ež aEnvIdć dB-5 where they reached up to 40 m thick ( k et al., 2012).

TEvaNovIć (s1ensu S 2 , 1990) is divided into two parts: pt and pt . In the wells around pančevo, Bavanište, dolovo and Banatsko Novo Selo, it reaches a total thickness Pontian (Pt ) between 6010–700 m (pč-1, Bav-1, doz-1, BNsj-1, BNs-1), while on the ovča structural ridge it is com - pletely missing (Figs. 3, 5and 6). The older level of the consists of brackish sands, marls and siltstones discovered in the following wells: Gl-1 (640–829 m), pč-1 (573–921 m), doz-1 (460–856 Fig. 9. Pannonian marl with Congeria banatica r. Hoernes and m), do-1 (310–712 m), G-1 (150–300 m), om-1(260– other mollusks (SA-2, 55 m). Photo by Lj. rundić Paradacna abichi 540 m), Bav-1 (450–843 m), BNsj-1 (450–845 m), Didacna otiophorum Lepto - and BNs-1 (574–902 m). Biostratigraphically, the cythere andrusovi Candona (Camptocypria) older pontian was proved on the basis of the finoEdriNnEgS s alata Loxoconchs schweyeri Hemicythe - of caspibrackish mollusrkusS (INa H , ria pejinovicensis Bacunella dorsoarcuata IvEBNTaL ) and ostracods ( NEžEvIć uNdIć aLaNyI L , uZIN 1985; k et al., 1994; r et al., 2011). It was Z , aLaNyI S , a Pontian (Pt 2) also noticed that along the Sava stepped fault, on the LaNyI arINZovIć , NEžEvIć Z - left banku Nodf Itć he Sava river, wNeEržeE vsIuć nk to depths of over , etc.)( M , 1970, 1977; k et al., 50 m ( r et al., 2011; k et al., 2012). on the 1994). right bank of the Sava river, they are often visible on The younger level of concordantly theu NsduIć rface or shallowly below the Quaternary overlies the older pontian and determined in the fol - (r et al., 2011). In the well B-1 (“Belgrade Wa - lowing wells: Gl-1 (381–640), pč-1 (345–573), doz- terfront”), the pannonian gray marls drilled below 1 (175–460), do-1 (155–310), G-1 (0–150), om-1 the Quaternary anthropogenic aNnEždE avIlćluvial deposits (60–260), Bav-1 (125–450), BNsj-1 (130–450), and between 21–29 m of depth ( k et al., 2017). BNs-1 (235–574). It can be seen that in the part of Similar pannonian sedi ments have been found in the trench-depression it reaches a thickness of over Paradacna okrugići other shallow wells in the area of Beli potok, vrčin, 300 m (Fig. 6). Lithologically, it is represented by Caladacna steindachneri Limnocardium Zaklopača, Begaljica and GrockNaE wžEhveIć re they have a sands and sandy clays with admixtures of coal and ochetophorum Zagrabica Pisidium muuNcdhIć greater thickness (e.g. k , 1989, 1990; coal clays. Numerous fossils indicate a freshrwuSaItNea r Candona (Camptocypria) balcanica Candona r , 1990) (Table 1) lake environment (e.g. ruSINa B , (Pontoniella) lotzyi Leptocythere cornuto - In the area of the Great War Island and the conflu - ruSINa B , costata ence of Sava and danube rivers, pannonian gray B , spa.L,a NyI sp., marls were drilled in the wells pduS-9 (30–52 m) aLaNyI Z , near Branko’s bridge, pduS-10 (30–55 m) near the CHWEyEr Z , old bridgNeE žaEnvIdć pduaSN-Ić13 (31–82 m) near the ušće S , etc.). palace ( k & G , 2005, 2008). a similar thick - In the wider Belgrade area, the pontian sedi - Gneosl.s a nw. Baaslk .f opoulunods. , i2n0 2t0h, 8eu1N w(d2)Ie,ć 1ll–s32 pduS-3 (22–38 m) and ments are known from M. Moštanica, avala, Zuc1e3 pduS-7 (30–52 m) ( r et al., 2011). In ada Cigan - and vrčin, and especially from rakovica and the so- ĐoRĐE MaRiNoVić & L jUpKo RUNDić

TEvaNovIć NEžEvIć Pisidium rugosum viviparus di - called Beli potok trench ( S , 1977; k , pannonian marls (Fig. 3). Lithologically, these are va - luvianus Lithoglyphus naticoides 1989 – Tab le 1). Both of the above-mentioned levels rious terrestrial, fluvial-swamp sands, gravels and Candona Scottia of utNhdeI ć pontian TaErvea NwoevIlćl documeunNteddIć faunistically gravel clays with the remains oEfu fMoasysr il gastropods and Pliocene (r , 1990; S , 1990; r et al., 2019). bivalves ( uNTH N , FEIcFfF. Er (k ), (p ) The Pliocene Paludina layers (PS ) viviparus diluvianus 1-3 and freshwater ostracods ( sp., sp., etc.). In the well Gl-1 (Glogonj) at a depth of 100 m, the base of the Quaternary was defineudN bTHased on the fin - – were deter - dings of cf. (k ). – mined only on the Banat side of the studied area. all above that, fluvial-eolian loess-paleosoil sequen - viviparus pannon - the three levels of paludina layers were discovered in ces cover most of the studyE NaardeIać on both sideso oLjfI ćthe icus Glogonj and the pančevo depression (Gl-1, 100 381 danube andau SdaEvNay rI ivers ( N NEežtE avlI.ć, 2011; T et v. bifarcinatus m and pč-1, 140 345 m). In Glogonj, the oldest hori - Salt.,r 2u0c1t4u; rGal-tecteot nali.,c 2 a01n5d; kpaleogeeto agl .,r 2a0p1h8 bic ). zon coErurMeasEpyor nds to the layers with interpretation v. altecarinatus N (295–38IE1L Zm), the middle horizon marks the (B ) zone in the depth of 230– 295 m, and the youngest rounSeIN ha orizon with the index species B was found in a depth interval 100–230 m. Near dolovo only older levels The structural-tectonic interpretation of prima - were found (doz-1, 115–175; do-1, 113–155 m) (Figs. rily Neogene evolution of the Belgrade wider area is 3, 4 and 6). Further to south, towards omoljica, they based on combined geological-geophysical data (cor - completely disappear and also missing north from relations of well logging data and paleontological- viviparus pan - ovča. They were delimited by well logging and the stratigraphic elements transferred on the network of nonicus v. bifarcinatus v. altecari - presence of morphologically different gastropods of reflective-seismic sections, gravimetric and geomag - natus Melanopsis lanceolata the genus vivi parus and other freshwater-lacustrine netic maps, etc.). South of the Sava and the danube valvata Lyrcea Unio Nerodontha and compEleutMealyr freshwater mollusIcEsL Z ( rivers, an abundant literature data and available sur - NruSINa , (B ), cf. EuMayr face outcrops have been supplemented by selected B , M. N , geological columns from the field and an instructive aNkovIć sp., sp.a, rINovIć sp., arINosvpIć.) stratigraphic profiles of wells. (j , 1970, 1977; M et al., 2016; M , Literature data on the presence of pre-Neogene 2017). “paludina layers” in Belgrade and its surround - formations in complex tectonic relations, which are ings south of the danube river are not present, while present in the surface around Belgrade vicinity, to - further to north they aurNed pIć resent in the vicinity of gether with magmato-volcanogenic intrusions and QSruematsekri nkaarly ovci (e.g. r et al., 2016). extrusions of limited size, are not necessary or pos - sible to repeat here. Therefore, on the constructed map (Fig. 10), their outer contours with minor changes as far as the size of the map allowed, are ap - prIoLxoivmaNaotveIlćy framIreIć d according to the regional map by Quaternary deposits of different genesis represent M & ć (1968). the youngest unit of basin filling in the area of SW In order to emphasize the important depth struc - Banat, i.e. the Belgrade city area. In the mentioned tural configuration, the map avoids plotting literary- wells in Banat, they reach a total thickness of over numerous variants (mostly assumed) of mutually 140 m (pč-1) in the pančevo depression. In the south, inconsistent faults of different conceptions, names, towards omoljica, their thickness is reduced to only directions and mutual relations. The routes of the 60 m and further towards the danube river (G-1) they reference mentioned faults fit in organized directions 1h4 ave a very small thickness. on the morphostructural of denser, relatively shorGt ecoul. ravn.e Bda luk. npoifluoorsm., 2 0e2q0u, 8i1d (i2s),t 1a–n32t ridge Belgrade - ovča they discordant ly overlie the distances. The large fault systems are recognizable Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

by distinctly condensed isopaches of the main frac - periclines, is marked by an anomalous geomagnetic tured directions, in principle, an overall disjunc - minimum of a closed oval-funnel configuration, tively shaped neotectonic structures. which indicates a depth absence of ultramafic mas - Taking into account all the above-mentioned, sive. another approach is to slightly decrease the three main structural units were separated in the in - gravimetric values, generally a parallel orientation, vestigated area: Belgrade-Banat Morphostructural south of the center of the Beli potok Neogene trench The Belgrade-Banat morphostructural ridge ridge (BBMr), pančevo-danube Neogene depression and the previously mentioned Zuce, including at the (BBMR) (pdNd) and the West Banat Neogene Belt with the morphologically dominant massif of avala Mt. It edge of regional the Srem depression (WBNB). means that below its cap built of flysch sediments there is no petrologically indeterminate magmatic , in this article, is defined by the eastern pluton, or an ultramafic rock of older alpine mag - side from Crepaja in the north, the lower course of matite of meridional orientation. Contrary, it is an the Tamiš river and the danube riverbed to ritopek, oval-transverse intrusive occurence (acceptable lite - and then across vrčin further to the south. The west - rary as a lacolite) in principle of acidic composition, ern border is marked by a fragmented rim of regional certainly from younger tectonic stage. It corre - the Srem Neogene depression, which continues from sponds to granite-granodiorite, or similar magmatic Moštanica, Surčin and the Zemun polje, through differentiations. This is supported by the once es - kovilovo on the Banat side, to the northeast, encom - tablished occurrences of post-Cretaceous penetra - passing the jabuka and Glogonj massifs (Fig. 10, cen - tion of neutral or neutral-acid apophyses, wires and tral part of the map). phylonites, both at the avala Mt. massif itself and in In the central part of BBMr, the geomagnetic im - the surrounding wider area, partly with a contact pact is most pronounced along the axis: Horst-massif changes, or even later hydrothermal muindoevraIć lization Glogonj–velika humka–jabučki rit–railway sta tion of inI MŠIuTprIljjEav Isć tena and TdEvžaeNvoevrI ć kamen ( G , 1875; ovča–Mirjevo–Mali Mokri Lug–Ljubičica–Zuce and d , 1931; S , 1977). further to kasapovac. The specified route deter - a positive gravimetric anomaly of the E–NE di - mines the belt of pre-Cretaceous penetration of ul - rection is expressed from the elbow of Zavojnica trabasic magmatites of the Cimmerian tectogenesis, river. on surface in the area of Boleč mehana and graphically shown as a sub-basin projection on the Babin vis, the opposite inclinations of Sarmatian reference map of the Neogene base configuration sediments are noticeable, which is indicative of the (Fig. 10). In the meander of the Zavojnica river, near existence of a deep vault that sinks around ritopek Zuce, as well as east of avala Mt. to the south, ser - towards Ivanovo in Banat. pentinized peridotites on the surface are in a re - South of the great meander of danube river, a verse west-vergent relatrikoonv Ić to the Cretaceous gravimetric anomaly of a closed oval configuration deposits they cover ( M , 1985). From the stands out, with a maximum increment below closed maximum geomagnetic anomaly of Zuce, Slanci. However, the geomagnetic influence from through jajinci to kanarevo brdo, the rectilinear lin - Mirjevo, i.e. the axis of the deep fault to the east, is eament to the south decreases sharply, and some - in a trend of continuous decrease, indicative of the what milder in the parallel direction Banjica–Senjak, deficit of ultrabasic masses, within the not deeply with the transverse segment kanarevo brdo–Ban - sunken, an objectively turbidite and Cretaceous fly - jica (Belgrade center). These points to the routes of sch sub-basin structure. on the northeastern wing compensatory-connected the depth faults of dinar - of the morphostructure, within the well v-150, the ides orientation with a droped southwest wing. basin bedrock was not reached to a depth of 194 m, To understanding the area of avala Mt., in the noorL wIć as the deepest well up to 219 m in that area shortest form, it is necessary to combine two mutu - (d , 1997). according to the constructed map here, ally complementary geological-geophysical appro - it would be on a vault at a depth of about 200 m. aches. The first one is that the dome-shape formed To the presence of depth igneous channels from Gaevoal. laan .M Batlk. .( paollut.o s5.,1 2012)0,, b81u (2il),t 1 o–3f2 tectonized terrigenous the basin's floor of high convective heat transfer a1s5 flysch, including the lowest western and southern well as older Miocene effusive breakthroughs is in - ĐoRĐE MaRiNoVić & L jUpKo RUNDić

arINovIć dicated by higher geothermal gradients ( M , Zaklopača wider area i.e. the westerNnE žrEivmIć of the 2019) to the closed anomaly of 0,09 °C/m which is GrNoEcžkEvaI tć rench-depressionuN (dFIić g. 10) ( k uNdIć , 1989; near 40% larger than the gradients of area with the k et al., 1994; r , 1990; r et al., the Badenian sunken Neogene sedimentary column with a domi - 2019). shallow-water ridge of Čubura–Tašmajdan–Ka - nantly conductive heat influence on the eastern, To the north of the discovered tectonized Meso - lemegdan (Belgrade center) Banat side. In this area, thanks to renewed volca - zoic massifs of the Belgrade hills, below the mor - nogenic deposits within the pre-Badenian continen - phologically disparate urban area, talT-ElavacuNostvrIćine series pILaarktolyv Iwć ith crosso-sreIćdimentation (S , 1975; M , 1986; ć , 1992), the point up, with its es - morphostructural elements originally adapted to pecially southern extensions. In that area where the the floor changes were altered by accompanying ex - LoNwEežrE vCorć etaceroSuTIsć rocks build the Neogene basis trusions and additionally disturbed by synchronous (k & k , 2015, during the pre-pontian pleats with fault occurrences, up to local reorienta - overflow-outflow episodes, the various sections of tions in relation to the original structure. pre-Baden - the thin ned, originally more complete sedimentary ian antiform complex with its discordant Badenian column were partially or completely eroded. This cover, along the step ped fault gradually sinks into the refers to the entire area of the flange-separated pa - The Mokri lug Neogene subdepression pančevo depression, and through Mirjevo it is con - leorelief of complex geometry, where the cover built nected to the Belgrade structural units by a shallow of the Neogene sediments are generally less than saddle (Fig. 10). 100 m thick, i.e. there are wedge-shaped, lenticular is dis - and very thin laTyEevarsN owvhIć ich was noNtEicžeEdvI ćby sevaeNrIać l junctively formed within the contour of Zvezdara authors (e.g. NSEžEvIć , 1977; k uN&dI ć G , south–Šumice–Marinkova bara–Miloševac–jajinci– 2005, 2008; k et al., 2015, 2017; r et al., razbojište–kumodraž–kaluđerica (generally, south - 2011). east from Belgrade center, Fig. 10). on the basis of Based on gravimetric measurILeImBaejknItć s, especially combined geoTElovagNicoavlI ć columns pfraojIćm the surface and the map of vertical gradients ( B , 1998), the from wells ( S , 1977; S , 1987) very vari - extension of mentioned structural ridge does not able thicknesses of stratigraphic members were dominate from kalemegdan towards Zemun, but inter preted in ranges: pre-Badenian 50–350 m, continues along the Great War Island along the west - discordantly Badenian 180–200 m, Sarmatian ern side of the rašova river towards kovilovo, with a 150–200 m, pannonian and pontian (partly eroded) pronounced Borča antiform, depth of 400–500 m. Li - 50–180 m but, in the center of the subdepression, teraaSlklayr Eav ccepted the “donji Grad–danube fault” according to the map, with a total average thickness (L , 1949), has its northwestern extension on structural trench Veliko of about 550 m. In the direction to vinča, it is con - the Banat side, specifically along the eastern coast Blato–Krnjača nected to the west-omoljica structural saddle in of rašova river, to the intersection with the segment Banat by a small faulted structural depression. The of the regional fault NW of the BBMG border, form - The Ovča morphostructure discordant basin floor is built by the upper Creta - ing the SW side of the ceous flysch sediments (Le-II, 278 m) with ap alojInć gi - as shown on the map (Figure 10, tuoddižno al obMeIćlt of ultrpaabjIać sic magmatites ( S & central part, north of the danube). d -T , 1973; S , 1987). is slightly inclined With the structural threshold of Torlak–rakovica towards the structural saddle of the višnjica part of village, the subdepression is limitedly connected the Belgrade danube meander, and especially more with the narrowed Beli potok trench of E–W direc - strongly along the NW pericline, i.e. along the length tion and a reduced sedimentary column from the of the fault diagonally formed of its northern flank, pre-Badenian to pontian age (here, the projected approximately along the southern coast of Sibnica depth up to 250 m), and over the nToErvtahNeorvnI ć foothills river. From there, the majority of the pre-Badenian 1o6 f Mt. avala, from Zuce and čot ( S , 1977), content of the structurGee obl.u anil. dBsal ka. p polauoss., t2o02w0,a 8r1d (2s), 1t–h3e 2 it was paleogeographically conected to the vrčin– more stable morphohorsts of jabuka and Glogonj. Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

Fig. 10. The map of Neogene basis configuration (isopache E = 100 m) constructed based on available well data. The dashed line marks an apical axis of the Cimmerian phase of ultramafic rocks (by ĐM). vertical hatching marks the simplified pre-Neogene countours (according to MILOvANOvIć & ćIrIć , 1968 and modified with new data).

on the western side of BBMr, from čukarica and along the SW side, with here predicted Neogene below ada Ciganlija, there is a structural nose of substrate at about 500 m depth (SW part of the map, northwestern orientation, with a subbasin antiform around the Sava river). at a depth of about 200 m. By it closes the struc - Finally, south of the upper Cretaceous-paleogene The Makiš Neogene paleo-gulf depression tural-arched space of the Belgrade geomorphologi - ostružnica flysch horst-massif of orogenic meridian cal amphitheater in the area of Bežanija on the tectonics, a Neogene structural trench was formed, southwest side. in the NW–SE direction, which has a depth of about The Pančevo-Danube Neogene Depression , in 700 m between umka and M. Moštanica and the ex - (PDND) the structural sense, represents the ultimate rim of treme Miocene paleogeographic rim towards Srem - the Batajnica depression. It is a part of the tectonic čica (the extreme SW part of map). trench formed between the fault system Bežanija Ggeoorl.n ajne. Bpalok.l pjeol–ukosn., 2e0ž2e0v, 8a1c (2–)k, 1i–j3e2 vo on the NE side, and extends east of the described BBMG. In th1a7t the fault in the direction Surčin–železnik–orlovača area, the largest morphostructural unit is the pan - ĐoRĐE MaRiNoVić & L jUpKo RUNDić

čevo Neogene depression (Fig. 10, central and NE rogeneously lie directly above the sub-basin tec - part). It has oval contours of 20 15 kilometers, with tonized floor, but not covering the peripheral peaks a bottom of about 2,600 m. The outer contour is of omoljica, jabuka and Banatsko Novo Selo. Mari ne- somewhat elongated from kačarevo to the north to - brackish Sarmatian, of generally transgressive conti - wards Crepaja, and to the south it has a trend of nuity, east of the jabuka horst massif abruptly turning towards Bavanište. The western boundary thickens to the center of the depression (about is marked by a complex Neogene fault system, which 500 m), significantly covering the omoljica horst, and connects from Crepaja to the eastern flank of the sparsely (about 60 m) the extreme NE peripheral jabuka horst massif to the already described the plateau of Banatsko Novo Selo (BNs-1). large longitudinal fault of the eastern BBMG bound - The lacustrine, mostly marly caspibrackish pan - ary. on its SW side, the depression is characterized nonian-pontian sediments, together of the greatest by the inner half-trench bay of Starčevo. The eastern thickness (more than 900 m), are generally directed boundary of the depression was determined by the to centre with a pronounced trend of thinning to - morphostructural series of the sub-basin horst- wards the western edges of the depression, and in massifs Banatsko Novo Selo–dolovo west–Bavanište the zone with stepped faults, with complete extinc - NW (Bav-1, Fig. 6). In the south, it is bordered by the tion of the pontian complex. The limnic-fluvial omoljica horst-massif. „paludina layers“ (pliocene) developed only north The Neogene bedrock in central part of the de - of the central part of the depression. Their thickness pression is formed by tectonized, early jurassic, is about 400 m (Glogonj) with differentiated super - dark to black pelites (sericite clays) (below 2,395 m position members at the crossroads of the pančevo in the well pč-1), thicker than the drilled 338 m, with - and Sefkerin depressions. Quaternary swamp-loess The Grocka trench depression, out the presence of ultrabasic magmatites with de - and aeolian sediment in the central and SE parts of termined direction towards Crepaja (Cp-1, 1,597 m). the depression, variably reaches a thickness of along the length of the western and eastern sides, 150 m. they are building a sub-basin basis predominantly measuring of tecto nized the Lower Cretaceous deposits with 10×5 km, is elongated along the SW–NE axis, from penetrati ons or synsedimentary basic magmatites vrčin, to the crossover of the omoljica horst massif and super positionally limited the upper Cretaceous and the Mala ada (Brestovik) morphostructure on flysch (Bav-1, Fig. 6). The Neogene depression in the danube, up to about 1,300 m deep (extreme S pančevo should not be equated with the eastern and SE part of the map). along the NE extension of trench of depression dolovo selo–Skorenovac– trench, about 10 km long, it sinks abruptly towards Smederevo (further east, outside the map outlines), the morphostructure of Bavanište selo. The basin which is, with its NW segment to the interdepres - bedrock is built by tectonic belts with the meridian sion threshold dolovo west–Bavanište northwest direction of the upper jurassic-lower Cretaceous (Bav-1) included in the constructed map. complex (near Bavanište and with the upper Creta - These oldest Neogene sediments in the center of ceous flysch), entirely without indications of ultra - the depression are about 550 m thick. They were basic magmatites. formed in extremely reduced, subaquatic condi - The Neogene oxidation molasses of uNnEcžeEvrtIćain tions, which is especially emphasized in this paper contours near Grocka up to 200 m thick ( k et due to significant differences in relation to hetero - al., 1994), are covered by discordantly younger, the geneous, a predominant oxidative molasse of the marine Badenian sediments, which thinnen along surrounding areas. Badenian marine sediments, the SW rim and surrounding horst structures. The with the largest thickness up to 600 m, completely marine-brackish Sarmatian from the deeper sunken cover the reducing bottom molasses within the NE sides, thickens inversely to the SW and S, more deepest sunken parts of the depression. on the sides than 300 m and together with the caspibrackish o18 f the depression, including the belt of the interde - pannonian sediments uGpe otlo. a 7n.0 B0al km. p.o Tluohse., 2m02a0r, g81i n(2a),l 1 f–a 32- pression threshold (Bav-1, doz-1, BNs-1), they hete - cies of the pontian on the SW flanks of the subdepres - Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

sion wedged out from Grocka towards Zaklopača, and reflective-seismic indicators, harmonized with and from Brestovik near the danube river towards the data of exploration wells in eastern Srem. Within Begaljica, and significantly thicken on the NE exten - the covered area, east of the ugrinovac-Surčin fault sion of the subdepression trench from Banatski (visible on the map) and the morphostructural ridge Brestovac to Bavanište. The relatively thin Quater - Borča–kovilovo–vrbovski rit, on both sides of the nary cover has not been specifically studied. danube river it reaches depths of about 1,700 m. during the Neogene tectonics, two depressions The internal dimensions average 20×10 km (west - were formed on the northwestern side of BBMG: ern part of the map). a diagonal intra-depression Sef kerin depression, west of the Tamiš river and the fracture, with depths of about 500 m, is noticeable Batajnica depression, partly on the extreme SW part on the stretch Bežanija gornje polje–Zemun polje, The Sefkerin depression of the Banat danube course and partly on the Srem that has NE extension to just mentioned the Borča side of the danube course around Batajnica (NW lineament (west stream of rašova)–kovilovo. part of the map). Between padinska Skela and the eastern pericli - stretches from opovo nal of the Belegiš morphostructure, the depression in the NW and jabučki rit in the SE, about 25 kilo - is structurally associated with the Sefkerin depres - meters long and about 10 km wide, with a maxi - sion. West of Novi Banovci, the peripheral parts of mum depth of about 1,900 m. Between the jabuka the depression are shallower and more complex horst and the NW flank of the ovča massif, it is con - depth configurations. The unincluded area towards nected to the pančevo depression by a structural Nova pazova gradually shifting to a parallel linea - saddle, and in the area of Besni fok–padinska skela ment, the beginning of which is visible in the NW there is a wider communication with the Batajnica part of map, with depth-geological relations that are depression (Fig. 10). The basin bedrock along the Douitsscidues tshieo sn tudied topic. NE flank of the depression is built by the already considered ultrabasites with a cover built of the Lower Cretaceous clastites. under the central part of the depression, the tectonized Cretaceous flysch is prognostically represented. Based on increased The wider Belgrade area has been the subject of geomagnetic influences, especially towards the geological studies for more than a century. In that Belegiš horst, younger Lower Cretaceous complexes sense, the earlier authors, each in their own way, are indicative, possibly with the iron-glauconite contributed to the knowledge of the geological char - clastites. acteristics of this area. However, the impression re - In this area, the older Miocene sediments are mains that these are mostly segmented works that smaller in thickness compared to the pančevo de - dealt with individual aspects of structural-strati - pression, but with an increased clay-marl complex, graphic relations and possible relations of MaivoLcoevnIć e especially within the pannonian–pontian time, and depositusk otovIwć ards theIk ooLlIdć er rocksT E(vea.Ngo. vpIć , an increased thickness of sandy-clay of pliocene de - 19o2LI2ć ; L , 1922; N , 1976; S , 1977; posits. above the inter-depression horst massifs of d , 1997). In Belgrade and its surroundings, it has jabuka and Glogonj, as the mentioned before, the in - been known for a long time that the jurassic-Creta - gressive overflow was achieved at the beginning of ceous rocks are present both on the surface and in pannonian time. From the vrbovsko towards the top some wells. For example, at the Basic Geological of the Belegiš horst on the Srem side, the total thick - Map, sheet Belgrade 1: 100,000, younger jurassic ness of Neogene sediments decreases to about 1,100 limestones, marls and clays have a relatively small The Batajnica depression m. The structural threshold towards the NE part of distribution in the SW part of the map, while the the Batajnica depression was interpreted at a depth Cretaceous carbaorknoavtIeć and flysch deposits are more of 1,500 m (the extreme NW part of the map). widespread ( M et al., 1984). at thvek BoavIsć ic Ge - Geol. an. Balk. poluos., 2020, 81 (2), 1–32 was interpreted on ological Map, sheet pančevo1: 100,000 ( I et a1l 9., the basis of the already cited combined gravimetric 1966), the serpentinites and serpentinized peri - ĐoRĐE MaRiNoVić & L jUpKo RUNDić

dotites and upper Cretaceous flysch deposits are pre - 2) is also quite clear. The clasts originate mainly sented as oases or smaller, elongated belts in the ex - from ultramafics, predominantly angular pieces of treme SW part of the sheet. They have NW–SE seprentinized peridotites tightly bound by cement direction on surface, and so they move to thea vwLeosvtIćern that partially contains a high percentage of carbon - area of the sheet Smederevo, 1: 100,000 ( p et ates. The thickness of these breccias is from 90 m in al ., 1977). It is interesting that in the well Bt 1-2 the well ov-1 (330–424) to over 120 m (229–352) (Bubanj potok, north of avala) under a thin Neogene in the well Sa-2. In the ov-1 well, this complex is cover already at a deputNhd Ioć f 38 m, similar ultramafites covered with the tectonized upper Cretaceous fly - were discovered ( r et al., 2019). Cretaceous sch sediments. No fossil remains were found in it. magmatism and its phenomena in the wider viciniNty Since they are superpositionally located above the ĐoEf LakvovaIlća Mt. ILhoajvEveI ć already boeLejInć described (e.g. a - ultramafites and whose fragments they contain as & M , 1969; T , 1996, 2016). well as they are overlying by the tectonized upper at the beginning, without pretending to talk Cretaceous flysch, their stratigraphic position prob - more about the affiliation of rock deposits from the ably corresponds to the Lower Cretaceous deposits baLsaidnE bNoevdIrć ock to cerutNačinIć large tectonic ouLnjIić ts (see or the so-called para-flysch. M , 1991; d et al., 2017; T et al., on the Belgrade side, similar the compact ser - the 2018, 2019) because we dealt more with the rocks pentinite breccias were discovered in well Bt 1-2 depth, subsurface route of the ultramafic distri - filling the basin, we note that based on the depth de - (Ljubičica–Bubanj potok) where, in the interval of bution marcations and the mutual relationship between 28–38 m depth, they cover a mass of serpentinized the units, we were able to quite accurately locate peuriNddoIć tites in which drilling was completed (92 m) (r et al., 2019). These are conti - in this area (a north-south dashed line, Fig. regarding the depth geological structure of the nental-lacustrine deposits of duoble-natured 10). In this work, it is fully factometrically docu - Neogene-Quaternary cover, it was determined that genesis. mented and has a cle–ar subsurface extension in the the oldest Miocene units lie discordantly over the he - direction plotted on the map (Glogonj–velika hum - te rochronous pre-basin bedrock. ka–jabučki rit–railway station of ovča–Mirjevo–Mali Mokri Lug–Ljubičica Zuce and further along to Šu - This highly interesting geological unit of de - plja Stena–kasapovac). This route within the Banat fined stratigraphic affiliation (Lower Miocene), haas sub-basin belt up to 10 km wide apically determines brIeNeonv Ieć stablished in some weallrsI NmovuIcć h earElMieErN (CeI .g. M - the main depth distribution of intrusive ultrabasic oLIć , 1959, 1961, 1962; M & k , 1969; magmatites, whose root follows the geomagnetic d , 1997, 1998). In the wells ov-1 (110–166 m), deficit of the eastern edge of the belt and as such is, Sa-2 (145–229 m), and G-1 (1,150–1,300 m), in mul - for the first time, clearly marked and graphically ticolored clastites with dominance of greenish and shown on geological cross-sections I and II (Figs. 3 brown-red clays, gray-green gravelly sandstones and and 4). conglomerates, with fragments of chert, serpentinite, Secondly, based on the mutual superpositional Mesozoic carbonates and carbonate concretions, relations in the wells, the character of the boundary there are not many fossil remains or, when found, the oldest Jurassic age between the jurassic sub-basin sediments and other they are poorly preserved and difficult to determine (Lias). rocks, it is evident that dark-black, tectonized clays the remaairnIsN oovf Ifć reshwater mollusk fauna and ostra - and argiloshists in the well pč-1 (2,395–2,733 m) cods ( M uLIć , 1962), fish fragments and pollen represent the rocks of grains ( d et al., 2010). a similar molasses forma - They have visible the processes of alteration tion has been found in dozens of wells in the wider breccias and conglo-breccias of minerals (e.g. sericitization of feldspar), which in - vicinity of Belgrade undoeLrI ćthe name uoNf dSIlćanačka serija (K B) dicate a certain hydrothermal effects. (=N SEžlaEnvIcć i formrSaTtIić on) ( d , 1997; r et al., 2013; Third, the stratigraphic range of the complex of k & k , 2015). 2c0oarse clastites, i.e. due to the lack ofG egolo. aond. B aclkh. rpolunoos.s, t2r02a0t,i 8g1r (a2)p, 1h–i3c2 lying over ultramafites in wells (ov-1 and Sa- benchmarks, it is not easy to give a close strati - Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

graphic determination to this continental series of matian sediments in ovča, which are very shallowly oxidative genesis. Still, other geological characteris - located, thinned and have a thickness of several to tics as well as lithostratigraphic correlation between twenties meters, while in neighboring the pančevo similar continental-lacustrine small basins in Ser - depression they are downlifted to considerable bia, indicate the mentioned mollasse belongs to the depths and have a much greater thickness (up to Lower Miocene. Herein, it corresponds to the Egen - 500 m each). In contrast, on structural elevations or burgian–ottnangian–karpatian regional stages i.e. smaller horsts, some Miocene units are very often time equivalents of the aquitanian anadr IBNuovrIdć igalian completely eroded and remain present only on the stages in generoaLlI ćMiocene division ( M , 1959, flanks of these structures (e.g. omoljica or jabuka 1961, 1962; d , 1997). where Badenian is eroded and the Sarmatian or Pre-Badenian, gray-black sub-aquatic pe- Especially interesting is the stratigraphically syn - pannonian deposits directly overlie the Lower Cre - lites (Pbp) of reduxing genesis chronous series of a completely different genesis, taceous rocks - Fig. 4). on the disrupted paleohorst which was determined within the pančevo depres - of Banatsko Novo Selo (BNs-1), the reduced Sarma - sion. tian sediments about 60 m thick, discordantly over - (pč-1, depth lie the Lower Cretaceous paleorelief at a depth of interval 1,980–2,395 m, see Fig. 3) reach a thickness 1,111 m. of over 400 m. a scarce content of small fern spores a more detailed attempt to interpret the geody - (polypodiacea) was found in them, which indicates namics of the Belgrade IarrIćea during the Neotectonic the Lower Miocene age. In our opinion, this hitherto time was presented by ć (1992). By the author, the unseparated a fine-grained molasses series repre - Neogene period is characterized by radial tectonics. sents the time equivalent of the previously de - Some fault systems are inherited from the Mesozoic scribed the Miocene molasses of oxidative genesis. and reactivated during the Neogene and some others We think that its separation as a particular unit rep - are the product of Neotectonic activity. all of these re - Paludina resents an important contribution of this paper. sulted in the author editing a sketch for a Neotectonic other Miocene units that make up the basin fill- map and showing the main elements, types of faults, in (Ba denian, Sarmatian, pannonian, pontian, plio - volcanic phenomena and Neogene terrains with dif - cene layers) are quite well known. However, ferent degrees and dynamics of sinking. among other in the studied area, they have been completely spa - things, he singled out a few faults important for the tially and temporally correlated by this research. formation of Neotectonic morphostructures, such as Namely, the map of Neogene thicknesses presented the Sava and dana Sukbaer Efav ults (this second one is also The disjunctively shaped space here, indicates a system of morphostructures built of mentioned by L , 1949). So-called the vinča and the resulting structural relationships small or larger depressions separated by structural fault (a right longitudinal strike-slip fault of the NW– saddles and elevations which, logically, gradually pass SE direction) formed in the Mesozoic and reactivated into each other. during the Neogene, which separates this area from have led the velika MoIrraIćva trench at east, is especially impor - to the formation of several significant depressions tant (Fig. 6, ć , 1992). (e.g. pančevo, Sefkerin, Batajnica, Grocka) and horsts Here we would like to note that, regardless of a structures(omoljica, ja buka–Glogonj, Banatsko No - certain contribution of the mentioned paper, the fact vo Selo, etc.) whose existence explains quite differ - is that the fault systems presented are not based on ent stratigraphic relationships in depth and the clear factometric or geophysical data. By our re - present lithostratigraphic content in certain seg - search and by construction of the Neogene thick - ments of this area. This has led to the fact that the ness map and determined structures formed on the relations between the Miocene units are not in ac - basis of wells data, it can be observe in principle the cordance and there are phenomena of local discor - existence of certain faults with significantly cor - dances due to the differential sinking of “blocks” rected direction, size and character of movements G(setorl. uanc.t Buarlke. sp)o,lu eosr.o, 2s0i2o0n, 8 1a (n2)d, 1 –d3e2 nivelation of the exist - (e.g. the Sava fault has a different orientation an2d 1 ing relief. Good examples are the Badenian and Sar - the danube fault has different prolongation). ĐoRĐE MaRiNoVić & L jUpKo RUNDić

the Pančevo depression

an important structural unit on the map is wider Belgrade city area, the aspect of applicability Four hydrogeological systems , located east of the described and use of certain lithostratigraphic units of SW morphostructural ridge and the longitudinal row of Banat and beyond is especially interesting i.e. their sunken horsts of Banatsko Novo Selo–Mala ada depth hydrogeological zoning. (Brestovik). It has a depth up to 2,600 m and N-S di - (HGS I-Iv, see rection (Fig. 10). The observed sharp tectonic Fig. 3) and within them 10 separate complexes boundary of the pančevo depression towards BBMr (a-S), have been defined as the authorized work by on the west side, which has a winding general direc - Đ. Marinović at 1974 and it was pubalrisINhoevdIć for pro - tion of N-S and marked by the flows of the Tamiš and fessional public eight years later ( M , 1982). Sibnica rivers, corresponds to a system of normal, Essentially, this zoning defines how and to what ex - lystric faults (Figs. 3, 4 and 10). our stratigraphic- tent mineralization and aquifer types change within geomagnetic data indicate the sediments of the the basin. This means that the contained mineral - pančevo depression formed in the early Miocene izations of water do not depend on the depth, but syn-rift phase (initial rifting), over which the Middle primarily on the position of the certain layer in re - Miocene sediments of the rift maximum (Badenian– lation not only to the contact floor package but also early Sarmatian) and the post-rift, the middle Sar - to the structural lateral sides, on which the cover matian sediments were deposited all the way to the collector eventually relies. pontian time (Figs. 3–6). as can be seen in the presented profile I, the about the existence of a system of depressions water from ovča from the Sarmatian/pannonian (basins) in suoLIuć thern Banat has been recently re - contact withI aLo djEevpIćth of 91 m has a mineralization of ported by d et al. (2019). among other things, 16.46 g/l ( M , 1960), and the water even from the authors single out the pančevo Basin, which is the eastern side of the pančevo depression, from the one in a series of the so-called pull-apart basins correlatively close pannonian collector depth of formed during the Miocene and whose sediment 1,013 m, has an almost identical mineralization of thickness exceeds 3,700 m. They are genetically re - 16.4 g/l (doz-1). Correlatively slightly younger pan - lated to a complex system of longitudinal faults of nonian layer of the well do-1 with a depth of 839 m, the dinaridic direction along which the space for the has a lower mineralization, specifically 15.5 g/l. a creation of more parallel basins was opened. ac - stratigraphically determined Sarmatian deposits of cording to the authors, these south Banat basins the well doz-1 from a depth of 1,154 m, contain a cor - represent a part of a wider, southern chain of pull- respondingly increased mineralization of 17.85 g/l apart basins developed along the so-called Mora - which is close to the mentioned values from ovča , i.e. vian Corridor. The mechanism of formation of these from the Sarmatian/pannonian contact. Waters structures is relateudL Itć o stresses along regional, lon - from the Badenian reservoirs of the wells doz-1 and gitudinal faults ( d et al., 2019). do-1, depth 1,602 and 1,674 m, have mineralization our research has shown that in a relatively small according to the intra-Badenian “age” by increasing area it is possible to single out several relatively the mineralization from 25.9 to 32.6 g/l, whiacrhk oisv Iićn deep local depressions (e.g. Sefkerin, pančevo) accordance with a modern marine waters ( Š , which have significantly thick Neogene deposits 1973). Finally, water from the Miocene lagoon with (1,900–2,600 m). It should be noted that the mech - an ambientally high mineralization of 51 g/l – was anism of their originin the early Miocene must cer - laterally infiltrated into a fissured collector of the tainly be viewed in the broader context of the entire Lower Cretaceous rocks (Fig. 3). It is worth men - southern rim of the pannonian Basin. Terminologi - tioning that e.g. waters from the pontian sediments cally, for the mentioned area, we are of the opinion (HGS-I, complex d) in kikinda from depths of that is more convenient to use the term depression 1,100–1,400 m, have a mineralization of 4–6 g/l, than basin (e.g. pančevo depression). which is the same as the mineralization of the level 22 Finally, apart from the mentioned historical-ge - of asrigINnoifviIcć ant reductioGne ool. af nc. Baaslkp. pibolruaosc.,k 2i0s2h0, 8c1a (2r)d, 1i–d3s2 ological and structural-tectonic evolution of the (M , 2017). Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

Conclusions

• during the Neogene, by complex fracture s. lato zones and less pronounced fault systems, the de - • The Belgrade wider area includes a segment of pressions and antiform structural units with mu - two morphologically adjacent geotectonic units - the tually different orientations were formed. The most inner dinarides , and the southern rim of the pronounced fault belts, partly with reactivated pre- pannonian Basin, without considering the regional Neogene depth faults, and the zones of less pro - geotectonic interpretations. nounced faults, on the constructed map (Fig. 10) • Within the pannonian Basin, geochronologically are visible in the directions and lengths by differ - and depthly, it differs the sub-basin unit affected by ently condensed isopaches. drawing of these faults an intensive orogenic-fractured tectonization of the is unnecessary. alpine cycle, and, the discordant geological cover, dis - • among the formed morphostructural units, the junctively and compactionally formed during the main depressions stand out: pančevo, Sefkerin, Ba - post-paleogene time. tajnica and Grocka, with a smaller sub-depression • Within the sub-basin structure, the oldest rocks of Mokri Lug. The structural trenches are: Moštanica are a black, schist like, sericited pelites that are pa - (SW corner of the map), Makiš (a bay of the Bataj- lynologically determined as the Early jurassic (late nica depression), krnjača (Belgrade danube river Lias–early doggerian), without the content of ultra - area), Beli potok (foothills of avala Mt.) and Ba - basic magmatites. natski Brestovac (open to the NE). • Serpentinized peridotites of the harzburgite • In the meander of the danube river, there is the type were drilled directly below the Neogene cover Slanci antiform and the smaller one, Babin vis. on (Glogonj), then under the Cretaceous agglomerates the Banat side, the horst massifs ovča, jabuka and (ovča) as well as in the area of Ljubičica–Bubanj Glogonj stand out. The morphostructural row Ba - potok, with an abundance of serpentinite fragments, natsko Novo Selo–vladimirovac–dolovo–Bavanište, cherts and other rocks, comparatively the early Cre - somewhat separates the pančevo depression from taceous age. on the surface, they are already known the Skorenovac–Smederevo depression, the western from the valley of the Zavojnica river, Zuce and the extension of which is visible on the attached map. eastern sides of avala Mt. in a thrust, west-vergent The omoljica horst-massif, with a smaller unit Star - relationship with the Cretaceous flysch. čevo–Ivanovo has a southeastern extension towards • By the analysis of the combined geophysical the antiform structures of Mala ada (Brestovik) and data it is confirmed the possibility of the existence, orešac (outside the map). the pre-Senonian laccolitic intrusions of acidic mag - • Below the Belgrade wider center, there is a matic on avala Mt. The presence of ultrabasite is ex - structural polyfacial antiform, partly reefly row cluded.. čubura–kalemegdan–Borča (extended to padinska • Based on geomagnetic indicators, in this paper, Skela), then a shorter structural nose from čukarica for the first time, the route of ultrabasic break - to Bežanija, and the separated periclinales of os - throughs is presented. on the attached map, it is tružnica in the direction of jakovo and Surčin. specifically plotted as a sub-basin depth p–rojection of • T he oldest Neogene sediments of limited con - the apical axis with a general direction of N–S (Glo - tours are lacustrine-subaquatic, multi-colored hete - gonj –velika humka–jabučki rit–the ovča railway sta - roclastic molasses (interbedded by volcanoclastics) , tion–Mirjevo–Mali Mokri Lug–Ljubičica Zuce). in principle of oxidative genesis. This reference pro - • orogenically tectonized the sub-basin’s geolog - motes the black and gray black, pelitic molasses of ical column of BBMG, generally of meridional orien - reduxing genesis, so far drilled only at the bottom tation, is broken into block systems of different of the pančevo depression, 415 m thick. orientation during pre-Neogene. Besides, it is addi - • The marine and semi-marine sediments (Bade - tionally modified to the disjointed basin floor con - nian, Sarmatian) are discordantly overlying the dif - Gfiegoul. raan.t Bioalnk. paoslu tohs.e, 2 b02a0s, e81 o (2f )a, 1 h–3e2 terochronous Neogene ferent rocks, over which they lie heterochronousl2y3 . cover. Three types can be separated: the basinal-lagoon, ĐoRĐE MaRiNoVić & L jUpKo RUNDić

Geološki s. str anali Balkanskoga poluostrva coastal-reef and mixed one. Each of them has spe - bijanska zona) [paläogeographie und tektonike in - cific lithofacial characteristics and fossil content. esteiles der Innerdinariden (Sumadija - und west ser - • The late Miocene brackish-lacustrine sedi - bische Zone)– in Serbian, German summary]. Geološki anali Balkanskoga ments (pannonian and pontian .) were devel - NĐELkovIć , 27: 103–152. poluostrva oped according to the same ambiental principle, but a , M. 1973. Geologija mezozoika okoline Beo - without the peculiarities of the lagoon and reef type. grada [Geology of Mesozoic of the vicinity of Bel - Geology of the In accordance with the permanently mobile tectonic grade–in Serbian]. surroundings of Belgrade oscillations, according to the disparate geometry of NĐELkovIć , 38: 1–136. NĐELkovIć the floor, the different overflow-outflow relations a , M. 1987. jura [jurassic]. In: a , M. were achieved, including with intraserial discor - (Ed.).Geologija sire okoline Beograda [ dances. – in Serbian]. Zavod za re - • The pliocene lacustrine-fluvial sediments (“pa - gionalnu geologiju i paleontologiju, rudarsko-geo - ludina beds”), were deposited just north of the NĐlEoLškkoiv fIać kultet BeILoogjErvaIdć , 1: 68–86. Surčin–Borča–Tamiš river–pančevo–Bavanište line. a , M. & M , N., 1969. Starost mezozojskog In Glogonj, all the three fossil complexes have been vulkanizma i faze njihovog stvaranja u okolini Beo - paleontologically documented(based on phyloge - grada, sa osvrtom na magmatizam Šumadijske zone Zapisnici SGD za 1964 netic relations of the genus viviparus). [The age of Mesozoic volcanism and the phases of • Quaternary sediments in the pančevo depres - their creation in the vicinity of Belgrade, with refer - sion are estimated to be up to 150 m thick. It is ence to the magmatism of the Šumadija zone – in Ser - goodly correlative with the Glogonj locality, where NĐbEiLakno]v.I ć adIvojEvIć , 65–74. they have been paleontologically determined to a a , F. & r , d. 2018. doprinos poznavanju XvIII kongres geologa Srbije vrnjačka Banja depth of 100 m. facijalne raznovrsnosti badenskih sedimenata Beo - • To all the above, for the practical reasons of grada [a contribution to the knowledge of facial di - usage, it can be added that in the whole vojvodina versity of the Badenian sediments of Belgrade – in basin area, the hydrochemical characteristics of Serbian]. , , water do not depend on depth, but primarily on the ILI2B3aj2 k–Ić 236. XIII Kongres ge - paleoecological elements of the aquifer, including B , p. 1998. Nova saznanja i potencijalne mo - ologa Jugoslavije Herceg Novi lateral infiltrations into the reservoir on which the gućnosti srpske naftonosne provincije [New know - sAtcraktingorawphleicd agqmuifeenr rtes lies. ledge and potential possibilities of the Serbian oil-bearing province – in Serbian].

ILIBajkIć ILIBajkI,ć aNčIć , Iv: 8L4ad1E–N8o5v8Ić . B , p., B , d., j , T. & M , M. 1979.

aLEŠEvIć prilog tumačenju geostrukturnih karakteristika ju - The authors are grateful to N. M (technical goslavije na osnovu regionalnih gravimetrijskih i ge - support of GaBp) for helpo drIuć ring the figures preparation. omagnetnih ispitivanja, s posebnim osvrtom na Special thanks go to S. ć (Geological Survey of aus - jugoslovenski deo panonskog basena [a contribution tria) and an anonymous reviewer for their helpful sug - to the interpretation of the geostructural characteriIsI-I gestions that improved the final version of the tniacsč noif s ykuugpo zsnlaavnisat .o Sna tvh. ez ab ansaifst uo fJ AreZgU ioZnbaol rgnriakv rimadeotvraic , manuscript. Lj. rundić is grateful to the Ministry of Edu - aknjd. Ig, eNoomvia Sgand etic tests, with special reference to the cation, Science and Technological development of the re - yugoslav paErstq oufi tshee g peoanlongoiqnuiaend eB laas iTnu –r qinu iSee Drb´Eiaunro].p e Rpuebfliecr oef nSecrebis a for supporting this research. , ouE 1977, 27–44. B , a. 1840. .

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Резиме

Дубински геолошки односи на ширем подручју Београда : базирано На основу прикупљених геолошко-геофизи - на бушотинским и геофизичким чких података, утврђено је да на Авали нису подацима присутне ултрабазичне стене. Напротив, по- стоји реална могућност присуства лаколитске интрузије киселог типа која је старија од сенона. Преко поменутих ултрамафита, утврђено је да лежи комплекс грубих кластита (бушотине Шири простор града Београда представља Оv-1 и Sa-2). Изграђен је од тврдих, компактних важну геолошку целину смештену у зони кон - бреча и конгло -бреча дебљине и преко 120 m. У такта јужног обода Панонског басена , с једне, и стратиграфском смислу, одговарају вероватно

унутрашњих Динарида у ши2рем смислу, са друге наслагама доње креде јер су у супрепозиционом стране. Овде обухваћено подручје заузима уку - односу испод тектонизованог горњокредног пну површину око 2.000 km . флиша. У оквиру Панонског басена, геохронолошки Орогено тектонизовани подбасенски геоло - и дубински, могу се разликовати две крупне це - шки стуб Београдско-банатске морфострук - лине: а) пренеогена основа (подбасенска цели - турне греде (ББМГ), генералног меридијанског на ) изграђена од различитих мезозојских стена правца, пренеогено је разломљен у блок системе тектонски интензивно орогено и разломно различите оријентације, и додатно модифико - обликованих током старије алпског циклуса , и ван на разуђену конфигурацију подине басена. б) Неогена и квартарна запуна басена – дискор- Током неогена, сложеним разломним зонама дантни геолошки покров, дисјунктивно и ком - и слабије израженим раседним системима, об- пакционо обликован током неогеног периода. ликоване су депресионе и антиформне струк - У оквиру подбасенске целине, најстарије сте- турне целине различитог правца. Најизразитије не су црни, шкриљави серицитски пелити који, раседне зоне , делом са реактивираним пренео - на основу присутне палинолошке асоцијације, геним дубинским разломима, и токови мање одговарају старијој јури (горњи лијас – доњи до - изражених раседања, на карти конфигурације гер ). Утврђени су у Панчевачкој депресији (pč-1, подине неогена су уочљиве по правцима и 2.395–2.733 m). дужинама различито згуснутих изопаха (сл. 10) . Серпентинисани перидотити харцбургитског Из тог разлога, доцртавање разломних траса типа, утврђени су непосредно испод неогеног није било потребно. застора (Глогоњ), затим испод грубокластичног На проучаваном терену, међу морфострук - кредног покрова (Овча) и на потезу Љубичица – турним јединицама истичу се веће депресије Бубањ поток , где је запажено обиље фрагмената попут Панчевачке, Сефкеринске, Батајничке и и класти од серпентинита, рожнаца и других Грочанске, са мањом субдепресијом Мокри Луг. стена несумњиво из старије кредне етаже. На Структурни ровови су: Моштаница (ЈЗ угао површини су од раније познати из долине За - карте), Макиш (залив Батајничке депресије), војничке реке, Зуца и источних падина Авале. На Крњача (београдско подунавље), Бели поток терену показују западно-вергентни однос према (предгорје Авале) и Банатски Брестовац (отво - млађој, флишној креди. рен према СИ). Анализом геомагнетних показатеља, у овом У Београдском дунавском кључу, налази се раду се, по први пут, приказује конкретна траса антиформа Сланци и мања, Бабин вис. На ба - ултрабазичних пробоја. На приложеној карти натској страни, нарочито се истичу хорст-ма - конфигурације базе неогена, уцртана је као сиви Овча, Јабука и Глогоњ. Морфоструктурни подбасенска дубинска пројекција апикалне осе, низ Банатско Ново Село–Владимировац–Доло - генералног правца С–Ј (Глогоњ –Велика хумка – во–Баваниште, разграничава Панчевачку депре - 3Ја0 бучки рит –железничка станица Овча –Мир - сију од депресије СкорGеeoнl.о aвn.а Bцal–k.С pмolеuoдsе., р20е2в0,о 8 1ч (и2)ј, и1– ј3е 2 јево –Мали мокри луг –Љубичица –Зуце ). западни продужетак видљив на приложеној Depth geological relations of the wider area of Belgrade - based on the wells and geophysical data

карти. Омољички хорст-масив, са мањим једи - метара дебљине. Слично је и у грочанској де - ницама Старчево–Иваново има ЈИ продужење пресији, на крајњем југу терена , где достиже према антиформним структурама Мала ада дебљину преко 400 m. Насупрот томе, на струк - (Брестовик) и Орешац (изван оквира карте). турном гребену Омољица, сармат је редукован Испод ширег центра Београда, налази се ан - (око 180 m), а на раседнутом палеохорсту Ба - тиформни структурни и полифацијални (делом натско Ново Село (бушотина BNs-1) има дебљи - спрудотворни) низ Чубура–Калем eгдан–Борча ну око 60 m, и дискордантно належе преко (продужно до Падинске скеле), затим краћи до њокредног палеорељефа на дубини од 1.11 1 m. структурни нос од Чукарице до Бежаније, и раз - У делу терена јужно од Саве и Дунава, баденске двојени периклинални Остружнице на правцу и сарматске наслаге су широко заступљене на Јаково и Сурчин. површини али су добро проучене и у плитким Најстарији неогени седименти (доњи мио - бушотинама на Калемегдану , Ташмајдану , Дор - цен) , ограничених контура , су разнобојне лим - ћолу , Вишњици , Карабурми , Кумодражу , Вели ком ничко-субакватичне хетерокластичне моласе Мокром Лугу, Раковици , Торлаку , Ле штанимаи (прослојене вулканитима), у принципу оксида- др. где имају мању дебљину осим у ретким ционе генезе. Откривене су на површини у ши- случајевима (Гроцка, бушотина G-1 – заједно рем подручју Београда јужно од Дунава (нпр. преко 500 m). Сланци, бушотина vp-150, дебљина моласа је око Најмлађи миоценски бракично-језерски (ка- 200 m). У бушотинама код Овче и Гроцке ( ov-1, спибракични) седименти некадашњег Панон ског 110–166 m; Sa-2, 145–229 m и G-1, 1.150–1.300 m) језера (панон и понт) имају знатно распро - дебљина им је мања . Међутим, на дну панче - страњење и укупно велику дебљину. Обично вачке депресије утврђени су и посебно издво - леже конкордантно преко сарматских наслага јени , синхрони , битно различити сиво-црни или, пак, дискордантно преко ултра мафита и субакватични пелити редукционе генезе дебљи - кредних седимената око Јабучког и Глогоњског не око 415 m ( бушотина pč-1, 1.980–2.395 m) и хорста. У околини Баваништа и Долова, достижу ово представља посебно важан допринос овог укупну дебљину преко 900 m, а утврђени су на рада. дубинама испод 1.000 метара ( pč-1, doz-1, Bav-1, Морски и морско-бракични седименти (сред - BNs-1). У правцу Омољице и даље ка Дунаву доста Па- њи миоцен - баден и сармат), дискордантно и су редуковани (˂ 700 m), код Глогња имају де - лудински хетерохроно належу преко различите подине. бљину око 500 метара док су на потонулој греди Издвојена су три типа развића: басенско-ла - у Овчи знатно редуковани (око 30 m). гунски, приобално-спрудни и мешовити. Сваки Плиоценски, речно -језерски седименти ( појединачно има специфичне литофацијалне слојеви) утврђени су само на банатској карактеристике и фосилну асоцијацију. У пан - страни проучаваног простора , северно од ли - viviparus чевачкој депресији баден је набушен тек на неамента Сурчин–Борча–р. Тамиш–Панчево–Ба - 1.452 m дубине и има велику дебљину (око ваниште. Сва три нивоа палудинских слојева (на 530 m). Слично је и око Долова где дубоко основу присуства различитих морфолошких об - залеже преко доњокредног палеорељефа (бушо - лика филогенетског низа рода ) откри - тина do-1). Најплиће испод површине, баденски вена су код Глогња и у Панчевачкој депресији седименти су набушени код Овче (76 m) где им (бушотине Gl-1, 100–381 m и pč-1, 140–345 m), је дебљина само 35 m, док на боковима хорстова док су око Долова откривени само старији ни - Омољица и Банатско Ново Село потпуно ис - вои ( doz-1, do-1). клињавају. Као и баден , сармат је најтањи око Квартарни седименти различите генезе Овче (свега неколико метара) и појављују се представљају најмлађу јединицу басенске испу- плитко испод површине (70 m). У панчевачкој не. У панчевачкој депресији достижу укупну Gдeеoпl. рanе. сBиalјkи. p оolдuoнsо., 2с0н2о0, 8Д1о (2л),о 1в–3у2 и Баваништу, знатно дебљину преко 140 m ( pč-1 ). У правцу југа, прем3а1 је потонуо и задебљао и достиже између 400–500 Омољици дебљина им се значајно смањује. Код ĐoRĐE MaRiNoVić & L jUpKo RUNDić

АРЧеВИћ viviparus diluvianus Гроцке ( G-1 ) имају симболичну дебљину. У (бушотина doz-1, Ш , 1973). Слично томе, бушотини Gl-1 ( Глогоњ ), на дубини од 100 m, воде из баденских колектора бушотина doz-1 и дефинисана је база кварuтNаTрH а на основу наласка do-1 ( Долово ) дубина 1.602 и 1.674 m, имају cf. (k ). минерализацију саображену интрабаденској Подповршинска геолошка грађа ширег под - „старости“ са повећањем минерализације од ручја Београда још једном указује и на важност 25,9 на 32,6 g/l – сагласно савременим морским примене тзв. хидрогеолошких система (HGS I-Iv), водама . Додатно, вода из миоценске лагуне, ауторизованих још 1974. године од стране Ђ. амбијентално високе минерализације (51 g/l), МаАрРиИнНоОвВИић ћа , а публикованих нешто касније бочно је инфилтрирана у пукотински колектор (М , 1982). Они јасно дефинишу хидро - од доњокредних наслага. Није на одмет додати геолошка својства појединих стратиграфских да нпр. воде из понтских седимента (HGS I, јединица, а с тим у вези, и минерализацију воде комплекс d) у Кикинди из дубина 1.100 –1.400 m, у њима. На пример , вода из Овче са контакта имају минерализацију између 4–6 g/l колика је Manuscript received October 30, 2020 сармат /паноИн ЛдОуЈебВиИнћ е 91m, има минерализацију и минерализација нивоАаР бИиНОтВнИећ редукције каспи - revised manuscript accepted November 26, 2020 16,46 g/l ( М , 1960), а вода са источне бракичних кардида (М , 2017). стране панчевачке депресије , из корелативно блиског панонског колектора дубине 1.013m, има готово идентичну минерализацију 16,40 g/l

32 Geol. an. Balk. poluos., 2020, 81 (2), 1–32