geology of the coka structure in northern banat

7/28/2019 Geology of the Coka Structure in Northern Banat

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www.geologicacarpathica.sk

GEOLOGICA CARPATHICA, AUGUST 2010, 61, 4, 341352 doi: 10.2478/v10096-010-0020-5

Introduction

For decades, the Neogene Pannonian Basin has been in thecentre of interest of stratigraphers, sedimentologists, struc-tural geologists, geophysicists, and paleontologists. Hydro-carbon explorations resulted in an enormous amount of dataabout the structure, sedimentary fill and evolutionary historyof the Pannonian Basin. Most of the important results fromthe southern, Serbian part of the Pannonian Basin, however,regretfully remained unpublished. The highlight of this pa-per is to present new data on the stratigraphy and tectonics ofthe oka area, in northern Banat of Serbia (Fig. 1), obtainedby subsurface geological methods (reflection seismics, welllogs, cores, cuttings, etc.). The oka structure represents ananticline, which resulted from the Middle-Late Miocene inver-

sion of an earlier extensional structure (within basin high)covered by Middle Miocene to Quaternary sediments.

Geological setting

The Pannonian Basin was formed due to continental colli-sion and subduction of the European Plate under the African(Apulian) Plate during the late Early to Late Miocene times(Horvth & Royden 1981; Royden 1988; Tari et al. 1992; Hor-vth 1995; Kov et al. 1998; Paveli 2002; Fodor et al. 2005).The Pannonian Basin was bordered by the mountain chains ofthe Alps, Carpathians and Dinarides (Schmid et al. 2008).

Late Early Miocene subsidence and sedimentation as aconsequence of the syn-rift extensional phase resulted in the

Geology of the oka structure in northern Banat(Central Paratethys, Serbia)

DEJAN RADIVOJEVI1, LJUPKO RUNDI2 and SLOBODAN KNEEVI2

1NIS Naftagas, Narodnog fronta 12, 21000 Novi Sad, Serbia; [email protected] of Geology, Faculty of Mining and Geology, University of Belgrade, Kamenika 6, P.O. Box 227, 11000 Belgrade, Serbia;

[email protected]; [email protected]

(Manuscript received July 8, 2009; accepted in revised form March 11, 2010)

Abstract: The oka structure is a fault-bounded anticline in northern Banat, in the southern part of the Neogene PannonianBasin. The structure and its vicinity were explored by 24 wells. In addition to well logs, paleontological, sedimentologicaland petrological analyses of cores and 27 seismic sections with different parameters of acquisition and processing wereused for geological investigation of the area. The E-SE dipping pre-Neogene basement consists of Lower Triassic clastics

and, in the NW part of the study area, Paleozoic greenschists. Thin Middle Miocene (Badenian) sediments unconformablyoverlie the basement and pinch out towards the elevated NW part of the study area. They are also missing in some wells onthe apex of the oka structure, probably due to erosion. Badenian sediments were deposited in a shallow marine environment.The late Middle Miocene (Sarmatian) strata are missing and the Badenian is directly overlain by Upper Miocene (Pannonian)sediments. The latter also pinch out towards the NW but in contrast to Badenian sediments, they are present in all boreholeson the oka structure. Pannonian deposition took place in a caspibrackish environment of Lake Pannon, with predominanceof marls and fine-grained clastics. Pannonian sediments are conformably overlain by latest Miocene (Pontian) and Pleistocenelacustrine, alluvial and terrestrial sediments.

Key words: Miocene, Central Paratethys, Serbia, Northern Banat, tectonics, stratigraphy.

formation of numerous grabens filled with relatively thinsyn-rift marine and brackish deposits (Horvth & Royden

1981; Tari 1994; Tari & Pami 1998; Lui et al. 2001;Paveli 2001). The Late Miocene (pre-Pannonian) unconfor-mity is a result of the first early post-rift phase of basin inver-sion that occurred during the Sarmatian (the latest MiddleMiocene; Horvth & Tari 1999). After that, a quiet and slowthermal subsidence took place, combined with an uplift anderosion of the surrounding mountain belt (Horvth & Royden1981; Schmid et al. 2008). That post-rift sinking was com-pensated by intensive sedimentation in the caspibrackishLake Pannon during the Late Miocene (Juhsz 1991; Magyaret al. 1999; Rundi 2000; Fodor et al. 2005). As a result,huge amounts of sediment were supplied, via large fluvial todeltaic systems, into Lake Pannon. The final result is succes-

sions of several thousand meters of post-rift sediments(Brczi et al. 1988; Szentgyrgyi & Juhsz 1988; Juhsz1991, 1994; Vakarcs G. et al. 1994; Magyar et al. 1999;Fodor et al. 2005; Tth-Makk 2007).

At about the Miocene-Pliocene boundary, and locally evenmore intensively in the Quaternary, another compressive phasetook place in the Pannonian Basin (Jamii 1995; Horvth &Cloetingh 1996; Prelogovi et al. 1998; Mrton et al. 2002). Itreactivatied earlier normal faults, into reverse faults, and alsoresulted in folding of Neogene strata (Safti et al. 2003; Fodoret al. 2005; Horvth et al. 2006; Marovi et al. 2007).

The southern part of the Pannonian Basin is underlain bythe Tisza Unit. During the Early and Middle Miocene exten-

sion of this unit was synchronous with that of the ALCAPA(Alpine-Carpathian-Pannonian) unit in the north (Safti et al.


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342 RADIVOJEVI, RUNDI and KNEEVI

2003; Fodor et al. 2005). From the end ofthe Karpatian (end of Early Miocene) sub-sidence of Tisza was coupled with east-ward motion and possible clockwiserotation under a transtensive stress field

(Csontos et al. 1992, 2002; Csontos 1995;Safti et al. 2003; Horvth et al. 2006).The pre-Neogene basement of the

northern Banat of Serbia, is tectonicallybordered by the Trans-Banat-Baka Dislo-cation belt, a complex E-W striking, re-gional dextral strike-slip fault zone thatseparates two major tectonic units in thepre-Neogene basement: the Vardar Zoneand the Tisza-Dacia block to the south andnorth, respectively (Fig. 2). West of theTisa River, the area is bordered by theNorth Baka High with pre-Neogene

basement at depth between 500 to1000 m below the surface. It is an iso-metric plateau formed during youngerMiocene tectonic events. The major Neo-gene tectonic features of the northernBanat are shown in Fig. 2 and include theNorth Banat and Mako Grabens, whichare bounded by NW-SE to N-S strikingnormal faults. The pre-Neogene basementis downthrown to a depth between 2000and 3500 meters with a relatively elevated(20002500 m) Kikinda-Szeged Highwhich trends NESW. The oka structure

is located on the western flank of theNorth Banat Graben (Fig. 2).The Miocene sediments of the northern

Banat unconformably overlie stronglydeformed Paleozoic-Mesozoic basementof magmatic, metamorphic and sedi-mentary rocks.

Materials and methods

The geological model of the oka areapresented here is based on seismic sur-

veys, well logs, and paleontological, petro-logical, and sedimentological analyses ofcore samples.

The oka structure and its vicinity wereexplored by 24 wells. The seismic data-base consisted of 27 profiles with differentparameters of acquisition and processing,the most recent made in 2005.

Our geological model was built in threesteps: data analysis, interpretation, andsynthesis of results. The first step includedanalyses of all available data and checkingof their quality. Data quality was also

controlled (well diameters, and well loginterpretation).

Fig. 1. Location of the study area within the Pannonian Basin System.

Fig. 2. Top pre-Neogene basement structure contour map of northern Banat (Marovi etal. 2007 modified).


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343GEOLOGY OF THE OKA STRUCTURE (SERBIA)

The second phase included determination of lithology andstratigraphy for each well on the basis of cores, cuttings andwell logs, computation of a synthetic seismogram, structuraland stratigraphic interpretation of the seismic sections, andconstruction of structural maps, geological cross-sections and

thickness maps. Well logs were calibrated with core data andused for qualitative lithological interpretation where the coreswere missing. The main lithology suggested by the mud logwas correlated horizontally with gamma ray and spontaneouspotential logs, then to other types (resistivity, sonic and neu-tron), and finally to sidewall cores and cuttings. In caseswhere the lithological interpretation of logs was ambiguous,we returned to the checking of log quality. Stratigraphic inter-pretation was based on paleontological analysis of core sam-ples (molluscs, ostracods, foraminifers, and palynomorphs).Lithological-stratigraphic columns were compiled for eachwell. The nearest well where checkshots were measured wasabout 1112 km east of the oka locality; therefore a synthet-

ic seismogram based on the sonic and density logs of C-9 wascreated in order to convert time-structural interpretations intothe depth domain. Three structural maps were produced based

on interpretation of all seismic sections of the investigatedarea. Three geological cross-sections, intersecting each otherat C-10, were drawn on the basis of the structural maps. Twothickness maps focused on the oka structure were construct-ed according to borehole data; the thickness of Neogene strata

in this area was below seismic resolution.The final step in geological model generation was synthesisof the results obtained in the second phase.

Results

Stratigraphy

In the study area, several boreholes reached the basement ofthe Neogene deposits (Fig. 3). The basement consisted ofbreccias, sandstones, clays and dolomitic limestones. Fossilsin these sediments are rare, so their age is determined by cor-

relation to other localities in northern Banat and northernBaka. The occurrence of the foraminifer Meandrospira pusillaindicates their Early Triassic age.

Fig. 3. Lithostratigraphic columns of representative boreholes of the oka area. The interpretation is based on well logs and paleontologi-cal, sedimentological and petrological analyses of cores and cuttings. Location of the wells is indicated in Figs. 57 and 913.


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In the C-1, the basement wasmetamorphic (greenschist).

In most of the wells, the Neogenesuccession starts with biogeniclimestones of Badenian age. These

include light-grey to white bio-sparudites and biomicrosparitesmade up of microsparite matrix andsmall sparicalcite microfossil shells(detritus made up of molluscs, bryo-zoans, hydrozoas, corallinacean al-gae (Lithothamnion, Lithophylum,etc.), annelids, cidaroids, ostra-codes, microgastropods, and vari-ous benthic foraminifera, such asAsterigerinata planorbis, Rosalinadubia, Elphidium crispum, E. fich-telianum, E. flexuosum, Borelis

melo, Virgulina schreibersiana,Quinqueloculina partschii, Q.heidingeri, Q. contorta, Q. longi-rostra, Q. heidingerii, Adelosinalongirostra, Hansenisca soldanii,Cibicidoides ungerianus, Ammoniabeccarii, Globulina gibba, Glan-dulina laevigata and Sphaeroidinabulloides. Palynological investiga-tions revealed the presence ofspores and pollen grains of gymno-sperms and angiosperms, such asSporites sp., Polypodiaceoisporites

sp., Laevigatosporites haardti, Ca-thayapollenites div. sp., Pinuspolle-nites labdacus, Cathayapollenitesdiv. sp., Monocolpopollenites tran-quillus, Triatriopollenites cory-phaeus , Alnipollenites verus ,Caryapollenites simplex, Poly-poropollenites stellatus, Tri-colpopollenites liblarensis and T.cingulum.

In addition to reef limestones,there are light-grey arkoses, carbon-ate sandstones and siltstones with

the forams Globigerinoides trilo-bus, G. quadrilobatus, Elphidiumcrispum, Globigerina bulloides, G.concinna, Heterolepa dutemplei,Cibicidoidespseudoungerianus, C.floridanus, Pulleniabulloides, Uvi-gerinasemiornata, U. pygmoides,U. aculeata, Sphaeroidina bul-loides, Textulariagramen, T. pala,Gyroidinoides soldanii, Martinot-tiella communi and Glandulina lae-vigata present.

The age of these shallow marine

and reef sediments is Badenian (ear-ly and middle Middle Miocene,

Fig. 4. Chronostratigraphic position of the Neogene to Quaternary succession of the oka area

(time scale, magnetic polarity zones and chronostratigraphic division of the Neogene afterGradstein et al. 2004; Piller et al. 2007 and Harzhauser & Mandi 2008).


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Fig. 4), as indicated by the presence of Asterigerinataplanorbis, Elphidium crispum, E. aculeatum, Borelis meloetc. The maximum thickness of the Badenian in the selectedwells is 19 m (C-8; Fig. 3).

The Badenian is overlain by compact marlstone and marly

limestones with fragments of ostracods, such asAmplocyprissp., Hemicytheria sp., Candona (Lineocypris) trapezoidea,Candona (Caspiolla) labiata, Loxoconchaschweyeri andLeptocythere sp. In light-grey compact marlstones, there isan association of molluscs including Gyrauluspraeponticus,G. dubius, Radixcroatica, Micromelaniastriata, Velutinopsisvelutina, Limnocardium sp. and Orygoceras sp., as well asassociations of spores and microplankton with Cathayapol-lenites div. sp., Pinuspollenites labdacus and Sporites sp.These ostracods and molluscs were endemic to the brackishLake Pannon and indicate the Pannonian (Late Miocene) ageof these sediments (Fig. 4). In some of the boreholes (C-2and C-10) the Pannonian layers directly overlie the Triassic

basement. The maximum thickness of the Pannonian in theselected wells is 87 m (C-8; Fig. 3).The Pannonian sediments and the pre-Neogene basement,

where they former are missing (e.g. at C-1 and C-24), areoverlain by marls with thin intercalations of sandstone andblack clays containing rare ostracods such as Pontoleberispontica, Loxoconcha schweyeri, Leptocythere andrusovi,Candona (Caspiocypris) labiata, Candona (Caspiocypris)alta, Candona (Lineocypris) trapezoidea, Candona (Ponto-niella)paracuminata, Bacunella dorsoarcuata, B. abchazica,Hemicytheriapejinovicensis and the camoebians, includingSilicoplacentina majzoni, S. hungarica, and S. inflata. This

Fig. 5. Structure contour map of the base of the Neogene with location of wells, seismicprofiles and geological cross-sections.

unit is considered to be of Early Pontian

age in the sense of Stevanovi et al.(1990) and Rundi (1997) (Fig. 4). Itsmaximum thickness in the selected wellsis 361 m (C-4; Fig. 3). The overlyingsediments are represented by sand-marlyclays with coals, thin sandstone layers andgrey-greenish marls with the molluscsParadacna cf. abichi and Lymnocardiumsp., ostracods Candona (Pontoniella)paracuminata and Candona sp., and thecamoebians Silicoplacentina majzoni, S.hungarica and S. inflata. These belong tothe Upper Pontian sensu Stevanovi et al.

(1990), reaching a thickness of 303 m(C-4; Fig. 3).Further chronostratigraphic bound-

aries, like the PlioceneQuaternary, havenot been determined, because there is lit-tle material for correct stratigraphic cor-relation. The post-Pontian formations arerepresented by fluvial, lacustrine, marshand terrestrial sediments including fine-grained sandstones and gravels, sandyclays with coals, marly-clayey sand-stones with the molluscs Gyraulus sp.,Lythoglyphus sp., Pisidium sp., and eo-

lian sediments (Figs. 3, 4). Their maxi-mum thickness is 886 m in C-10.

Tectonics

The structure and thickness of individual stratigraphic unitsare presented in structure contour maps (Figs. 57), seismicprofiles (Figs. 8, 9), geological cross-sections (Figs. 1012),

and thickness maps (Figs. 13, 14).Within the study area, the Neogene basement generally dipsfrom northwest to southeast and east in a monoclinal manner(Figs. 5, 8, 1012). The deepest part of the basement lies at adepth of 1800 m in the eastern part of the research area, where-as the shallowest part is in its northwestern corner at a depth of1040 m in C-1 (Fig. 5). The inclination of monocline is gentlein the NW and becomes steeper in the SE, where the basementstarts to sink steeply into the North Banat Graben (Fig. 2).

The basement of the Neogene is mainly represented byLower Triassic clastics and, in the northwestern part of thestudy area, by Paleozoic greenschists (Figs. 5, 8). The meta-morphic rocks were hit only by C-1 (Fig. 10). The contact be-

tween the two rock types is interpreted to be tectonic in thesouth, whereas the Lower Triassic depositionally or erosional-ly pinches out on the elevated Paleozoic basement in the westand east (Fig. 5).

The oka structure is a fault-bounded anticline, situated onthe basement slope (Fig. 5). This structure is shallowest at thelocation of C-10 at 1393 m (Figs. 8, 10). The high is accentu-ated on its west by two clearly recognizable paleodepressionsin the southern and central parts of the study area, respective-ly, at a basement depth of 1500 m (Fig. 5). These depressionsare expressed on structure contour map of the top Badenianand top Pannonian horizons (Figs. 6, 7).


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position of the Pontian sediments on geologicalcross-sections support this statement.

The Badenian strata pinch out towards thenorth and west (Figs. 6, 8, 10, 11). They are theshallowest at the pinch-out point (at about

1250 m), while in the eastern part of the re-search area, they are at a depth of 1800 m.Over the entire oka area they are thin and aremissing from the top of the oka structure (inC-2 and C-10; Fig. 13). Here, their thickness isbelow the seismic resolution and thus could notbe distinguished from the top Triassic reflector(Fig. 9). On the top Badenian structure contourmap, normal faults with north-south and north-west-southeast direction can be noted (Fig. 6).All the faults have small throw (few meters to afew tens of meters).

The Pannonian sediments pinch out to the

northwest and deepen to the east down to1750 m (Fig. 7). They are the shallowest nearthe pinch-out, near C-24 at about 1100 m(Fig. 11). Unlike the Badenian, they are found inall wells above the oka structure (Fig. 14). Thefaults have a small gravitational movement andmost of them have a north-south direction. In thewestern part of the area, there is a large E-Wtrending normal fault (Fig. 7).

Interpretation and discussion

In the oka area, the Badenian represents theoldest Neogene unit; its sediments transgressive-ly overlie the Lower Triassic (Radivojevi 2008).The distribution and thickness of the Badeniansediments, including their lack in C-2, C-10, C-22and C-23, suggest that the Badenian was proba-bly exposed to erosional processes for sometime. This interpretation is strongly supported bythe complete lack of the subsequent Sarmatiansediments in the studied boreholes.

According to Kemenci (1991), the entire Mid-dle Miocene (Badenian and Sarmatian) can becharacterized by significant expansion of the

aquatic environments in the southern PannonianBasin; only restricted areas (the highest parts ofthe paleorelief) escaped marine flooding. If thisinterpretation is correct, then the lack of the Sar-matian and eroded nature of the Badenian in theoka area is probably due to the tectonic inver-sion that took place in the Late Sarmatian or Ear-ly Pannonian and resulted in a widespreadpre-Pannonian unconformity (Horvth & Tari

Fig. 6. Structure contour map of the top Badenian with location of wells, seismicprofiles and geological cross-sections.

Fig. 7. Structure contour map of the top Pannonianwith location of wells, seismicprofiles and geological cross-sections.

In the oka area, several, N-S and E-W trending normalfaults with small movement have been interpreted. All faultspresent in the oka area were probably reactivated during thePontian as inverted faults which is indicated on seismic and

geological cross-sections (Figs. 812). Reflectors above thetop Pannonian horizon which are also nicely folded and the

1999). Tectonic inversion is obvious both, on seismic lines(Figs. 8, 9) and geological cross-sections (Figs. 1012). Allreflectors above the top Pannonian horizon are nicely foldedand some inverted earlier normal faults are present. Position

of Pontian sediments on geological cross-sections also indi-cates basin inversion.


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Fig. 8. Seismic profile 1 across the oka area. The strong reflector to the left of shot point 250 corresponds to the top of the Paleozoic hori-zon. The large difference in the velocity between the Pontian sediments (Triassic, Badenian and Pannonian sediments are completely miss-ing) and the schists caused appearance of a multiple under the top Paleozoic. For location of the profile see Figs. 57.

Fig. 9. Seismic profile 2 across the oka structure. The Pannonian sediments have a low reflective response over almost the entire study

area. The top of the Pannonian on the right side of the profile, however, has a well-defined reflection. This is a typical feature of the topPannonian in northern Banat. For location of the profile see Figs. 57.


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Fig. 10. Geological cross-section AB (for location see Figs. 57). Note the pinch-out trend of the Badenian and Pannonian towards C-1.The Badenian is missing at C-10, probably due to erosion.

Fig. 11. Geological cross-section CD (for location see Figs. 57). The Badenian and Pannonian pinch out towards C-24.

The Sarmatian-Pannonian boundary, roughly correspondingto the Middle-Late Miocene boundary, was marked by a majorregression, which isolated the Central Paratethys from the glo-

bal sea, and transformed it into the large, long-lived, brackishwater body of Lake Pannon (Magyar et al. 1999). The cause of

this regression is still highly debated (Sndulescu 1988;Vakarcs et al. 1994; Horvth & Cloething 1996; Harzhauser &Piller 2004).

A lake-level rise during the Pannonian caused flooding ofpreviously emerged regions in northern Banat (Kemenci


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Fig. 12. Geological cross-section EF (for location see Figs. 57).

Fig. 13. Thickness map of Badenian sediments above the oka structure (based onwell data). The Badenian is missing from the most elevated parts of the structure.

1991), thus the Pannonian strata are transgres-sive at the base and deposited above an uncon-formity over a greater part of the area. ThePannonian sediments in northern Banat have awider distribution than the Badenian; theyoverlie Paleozoic schists and magmatites, Tri-assic, Badenian, and Sarmatian sediments.

In general, the Pannonian is represented bythin sandstones with carbonate matrix in the lit-toral facies, by pelites with presence of micritein the sublittoral facies, and by marls in thedeep-basin facies. The lithology as well as the

molluscan fauna with Radix croatica and Gy-raulus praeponticus in the oka boreholespoint to a sublittoral facies that was widespreadin the region (Stevanovi 1977; Kneevi et al.1994) and represents a transitional zone be-tween the sandy littoral and clayey deep basinalfacies. The Pannonian associations of flora andfauna indicate a low-salinity caspibrackish en-vironment characteristic of Lake Pannon(Steininger et al. 1988; Rgl 1996). Data fromoka area correspond to recent isotope trendsstudies which indicate that Lake Pannon was asimple system of an alkaline lake with steadily

declining salinity (Harzhauser & Piller 2007;Harzhauser et al. 2007).


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Progradation of deltaic clastic systems, shallowing and fi-

nally infilling of the basin during Pontian times was proba-bly caused by deceleration of basin subsidence (Fodor et al.2005; Horvth et al. 2006). The sedimentary complex depos-ited during the Pannonian, Pontian and later, in northern andcentral Banat is very thick, locally it may exceed 4000 m(the Pannonian ranging from several m to several hundred m).In the surrounding areas, such as the southern Banat, FrukaGora Mts, and most of Baka, this complex is much thinner(Kemenci 1991; Radivojevi 2008).

The stratigraphic position of the oldest post-Pannoniansediments that were treated in this paper is quite question-able. Basic lithostratigraphic and paleontological parametersindicate the presence of the Pontians.str., which is known in

the Eastern Paratethys where they represent a regional stage(Stevanovi et al. 1990). From the paleogeographic point ofview, it should be emphasized that area of Eastern Serbiacorresponds to the Miocene and Pliocene developmentwhich exists in Dacian Basin and further to the east, includ-ing the Pontian in such development. In earlier referencesthere are data which confirm these correlations, similaritiesand differences between the Pontian of these basins. Howev-er, as in the past 20 years, few results from these areas thatare internationally recognized were published, the questionof Pontian (none) existence in the Pannonian part of Serbiashould be seriously revised, and verified on outcrops. Thevalidity of the model which is applicable for the western part

of Central Paratethys can only be tested with direct field ob-servations. In that sense, the adjusted Miocene-Pliocene

Fig. 14. Thickness map of Pannonian sediments above the oka structure (based onwell data).

scheme, which includes both the Pannonianand Dacian Basins is used in this paper as acompromise (Harzhauser & Mandic 2008).

ConclusionsThe basement of the Neogene succession

in the oka area is mainly represented byTriassic sediments, except in the northwest-ern corner of the study area where it is repre-sented by Paleozoic schists. The paleoreliefsubsided along normal faults from the NorthBaka High in the northwest to the North Ba-nat Graben in the southeast and east. Theoka structure, which was initiated as awithin-basin high and later inverted into thefault-bounded anticline is neighboured by

two local paleodepressions in the central andsouthern parts of the study area.The shallow marine Badenian sediments

were deposited transgressively on the Paleo-zoic-Triassic basement. They pinch out at themost elevated northwestern part and wereeroded from the top of the oka structure, asindicated by their small thickness (up to afew tens of meters) and by the lack of Sarma-tian deposits.

The sublittoral Pannonian sediments arepresent in all wells testing the oka struc-

ture, but they also pinch-out towards the west. They are

thicker than the erosionally truncated Badenian sequence (upto 100 m). The overlying Pontian to Quaternary succession,represented by lacustrine to alluvial and terrestrial deposits,is thick (10001800 m) and uniform over the entire area.

Acknowledgments: We owe great gratitude to NIS Naftagasfor allowing unlimited access to all data. The authors aregrateful to Imre Magyar (MOL, Budapest) who greatly im-proved the paper by his comments and suggestions. We wishto thank Vladimir Mukinja and Zoran Stojanovski for thegraphic outfit of the paper. In addition, we owe great grati-tude to colleagues: Jordan Kukavica who helped about the

location of pinch-out of the Badenian and Pannonian sedi-ments, Rastko Pealj and Sneana Marjanovi for the givenmaterial and Zorica oki who helped with the interpreta-tion of the well log measurements. We are also grateful toNIS Naftagas employees: Predrag Cviji, Goran Bogieviand Vladislav Gaji who helped with the stratigraphical andpetrological determination. Many thanks to MariannaKovov (Comenius University, Bratislava) for reviewingthe list of pollen grains and spores. We also want to thankCsaba Krzsek (OMV/Petrom, Bucharest) for critical com-ments on the manuscript. Fruitful discussions and commentsof three anonymous reviewers improved the final versionsignificantly. A part of this paper represents the results of the

Project No. 146009 supported by the Ministry of Scienceand Technological Development of the Republic of Serbia.


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