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GEOLOGICA BALCANICA, 32.2-4, Sofia, Decemb. 2002, p. 145-163 Late Cretaceous Apuseni-Banat-Timok-Srednogorie (ABTS) Magmatic and Metallogenic belt in the Carpathian-Balkan orogen 1 2 3 4 Petko Popov , Tudor Berza , Alexander Grubic , Dumitru Ioane 1 University of Mining and Geology, Studentski grad, S ofia, IIOO, Bulgaria, e-mail: [email protected] 1 Geological Institute of Romania, Caransebes Str. No I , Bucharest, R0-78344, Romania, e-mail: [email protected] J University of Belgrade, Dusina 7, Belgrad, IIOOO, Yugosla via , e-mail: grubic@infosky. net ' Geological Institute of Romania, Caransebes Str. No I, Bucharest, R0-78344, Romania, e-mail: [email protected] II. Ilonoe, T Eep3a, A . Tpy6u'l, f{ Homte Abstract. The Apuseni-Banat-Timok-Srednogorie (ABTS) fl030fleMeA060U Ma2MamU<IeCKUU U MemaAA02efiU Magmatic and Metallogenic Belt can be traced from the 'leCKUU naRc AnycceHbl - EaHam - TuMoK - Cpeoflo Apuseni Mountains in the north, through the western zopue (ABTC) 6 Kapnamo-EaAKafiCKOM opo2e11 e. part of the South Carpathians (Banat) in Romania, the MarMaTI1lfeCKI1H 11 MeTa.nJioreHI1lfecKI1H nolle AnyceHhi Timok region in East Serbia, the Srednogorie zone oaH aT - T11MOK - Cpe~ Horop11e (ABTC) Halfi1HaeTCll c (Bulgaria) and continues in Turkey through the Black AnyceHCKHX rop ( c cesepa), npoxo~ I1T qepe3 Jana~HYIO Sea. lfaCTb IOlKHbiX KapnaT (EaHaT - s PyMhiH1111), qepe3 The basement belongs to the southern margin of the T11MOKCKHH pai1oH (s socTOlfHOH Cep61111) 11 ~a.nee , oxsa European continent. The ABTS Belt is unconformly TbiBall Cpe~ HoropcKyiO JOHY (EoJirap11ll), npo~O Ji lKaeTcll superimposed on older structures, including the Early qepe3 qepHoe Mope Ha Tepp11TOp1111 Typ111111. Cretaceous ones. Furthermore, it crosses the Vardar Ero OCHOBaHI1e npHHa~JielKI1T K IOlKHOH 0Kpa11He ophiolite suture in the Mures and Voevodina regions. EsponeH:cKoro KOHTI1HeHTa. ABTC nolle Ha.JIOlKeH Heco These facts indicate a new stage in the alpine evolution macHo Ha 6oJiee ~peBHI1e, BKJI. paHHeMeJIOBhie cTpyKTy which followed the subduction of the Vardar Ocean and pbi . EoJiee TOro - s paH:oHax Mypew 11 Boeso~11Ha OH subsequent collision. This new stage was characterized ne peceKaeT Bap~apcKy!O ocp110JII1TOBYIO JOHy. 3To noKa- by an extensional geodynamic regime. The ABTS arcuate 3biBaeT, 'ITO o6pa30BeHI1e nOliCa CBll3aHO C HOBb!M rift was formed as a result of postcollisional orogenic JTa llOM aJibnHHCKOH JBOJIIOL\1111, HaCTyni1BWI1M llOCJie collapse. cy 6~ yKL\1111 Bap~apcKoro OKeaHa 11 nocJie~osasweH: 3a The Late Cretaceous magmatic activity with submarine Heif KOJIJII1311eH . 3TOT HOBh!H :nan npOTeKaJI B ycJIOBI1liX volcanic rocks and comagmatic intrusions began during 3K CTeHCI10HHOf0 reO~ I1HaMI1lfeCKOfO pelKI1Ma, a nOliC the Cenomanian and ended during the Maastrichtian. ocpopMJieH B pe3yJihTaTe nOCTKOJII13110HHOfO o6pyweHI1ll Volcanic and associated predominantly flysch-typ e oporeHHOH nocTpOHKI1. sedimentary deposits form a 2-3 to 7-8 km thick pile. The XapaKTepHall ~Jill nollca no3~HeMeJioBall MarMaTI1- magma generation in ABTS extensional belt was realized yecKall aKTI1BHOCTb c ee cy6aKsaJibHbiMI1 syJIKaHI1lfeCKI1- in different depth level, which determines differences of :\111 nopo~aMI1 11 KOMarMaTI14eCKI1MI1 11HTPY311liMI1 Halfa melt compositions. Rock association of calc-alkaline, Jia Cb s ceHoMaHe 11 JaKOH411JiaCb s MaacTp11xTe. ByJIKa tholeitic, subalkaline and alkaline series are established. HHlfeCKI1e nopO~hl H aCCOL\1111py!Oll\He C HHMI1 OCa~OlfHhie The petrologic features of the alkaline and subalkaline OTJIOlKeHHll npe11MymecTseHHO Q>JI11wesoro THna cJia rocks and several Sr isotope analyses show the mantle ra!OT pa3pe3hl MO!l\HOCTbiO B 2-3 ~0 7-8 km. reHep11- origin of the parent magma. The calc-alkaline magma was pOB aHHe MarMbi s ABTC nollce ocymecTBJiliJIOCh Ha generated predominantly around the boundary between pa3HblX my6HHax, 'ITO 11 onpe~eJIHJIO pa3JII1411ll B COCTaBe mantle and lower crust. pacnJiasos. AccOL\11al\1111 nopo~ np11Ha~JielKaT K 113BeCT Porphyry copper and copper massive sulphide KO Bo-meJIOlfHOH, TOJiei1TOBOH, cy6meJIOlfHOH 11 meJIOlf deposits are the most important. Some of them have an HOH cepHliM . IleTpoJIOrHlfeCKI1e oco6eHHOCTI1 meJIOlfHhiX economical content of gold and/or molybdenum. There 11 cy6meJI04HbiX nopo~ 11 ~ a HHbie no Sr-1130TonaM yKa- are skarn arrd vein type copper deposits, too. Other 3biBa!OT Ha MaHTHHHhlH reHe311C pacnJiaBOB. l-iJBeCTKOBO important deposits are iron, tungsten-molybdenum and ll\eJIOlfHhie MarMhl reHep11posaJII1Cb npe11MymecTseHHO B lead-zinc skarn deposits. Besides, small hydrothermal 30He MelK~Y MaHTHeH 11 HHlKHeH KOpOH. base metal-gold, barite, porphyry gold, silver and CaMhiMI1 BalKHhiMH ~Jill nollca liBJiliiOTCll cyJibcpi1~Hbie volcano-sedimentary iron-manganese deposits are M e~Hhle opy~eHeHHll (BKpanJieHHble 11 MaCCI1BHhle) opy known. The plutonic, subvolcano-plutonic, volcano ~ eHeHI1ll. HeKOTOpbie 113 HHX co~eplKaT npoMhiWJieHHbie plutonic, volcano-subvolcanic and volcanic ore-bearing 19 Geologica Balcanica, 2-4/2002 145 KOJIH'ieCTBa JOJIOTa H/HJIH MOJIH6,neHa. KpoMe Toro structures are distinguished. The geochemical asso YCTaHOBJieHbl Me,nHb!e MeCTOpO)I(,neHHH CKapHOBOrO H ciations show the predominance of mantle sources of the )I(HJibHoro THna. Ba)I(HOe JHa'ieHHe HMeiOT )l(eJieJHbie, ore-forming fluids. OJIOBHHO - MOJIH6,neHOBble H CBHHUOBO-UHHKOBbie CKapHOBblbie MecTopo)l(,neHHH. KpoMe TOro B o6xsaTe no.Rca paJMel.l.(eHbi He6oJibWHe noJIHMeTaJIJIH'ieCKHe - 30JIOTbie, 6apHTOBbie, BKpanJieHHbie 30JIOTble H cepe6pH Hhle, a TaK)I(e syJIKaHoreHHO-oca,no'iHbie )l(eJieJo-Map raHuesbre MecTopo)l(,neHHH. BbiHBJieHbi nnyTOHH'ieCKHe, cy6ByJIKaHH'feCKHe·nJiyTOHH'ieCKHe,ByJIKaHH'ieCKHe·nJiy TOHH'ieCKHe H BYJIKaHH'ieCKHe py.nosMel.l.(aiOI.l.(He cTpy KTYPbi. reoxHMH'feCKHe accouHaUHH yKaJbiBaiOT Ha npeHMyl.l.(eCTBeHHO MaHTHHHbie HCTO'iHHKH py,noreHe pHpylOI.l.(HX 4JJilOH,nOB. Popov, P., Berza, T., Grubic, A., Ioane, D. 2002. Late Cretaceous Apuseni-Banat-Timok Srednogorie (ABTS) Magmatic and Metallogenic belt in the Carpathian-Balkan orogen Geologica Bale., 32, 2-4; 145-162. Key words: Late Cretaceous; magmatic and metallogenic belt; Carpathian-Balkan orogen. Introduction The presence of Cretaceous igneous rocks in Later this magmatic belt has been referred to as the Carpathian-Balkan orogen is mentioned in Banat-Srednogorie belt or zone (Popov, 1981, the middle and second half of the l91h century. 1987; Bogdanov 1983), as well as Banatitic belt Breithaupt (1861) has given a name "timochite" (province) (Giusca et al. 1966; Russo-Sandu to the hornblende andesite in the Timok region, lescu, Berza, 1979; Berza et al., 1998) or as while Cotta (1864) has described the intrusive Laramian belt (Cioflica, Vlad, 1973). This rocks in the South Carpatians as "banatite", magmatic belt is also expressed in distinct named after the region of their occurrence. tectonic and metallogenic features. In this Petrascheck (1942) points out the unity of the paper we suggest to call it the "Apuseni-Banat Late Cretaceous magmatic rocks within the so Timok-Srednogorie (ABTS) Magmatic and called "Subbalkan zone", extending from Metallogenic Belt" because this name entirely Bourgas to Maidanpek (Fig. 1). Giusca et al. covers its geographic extent and geological (1966) emphasized the similarities between the meaning. This belt is about 1 000 km long and Upper Cretaceous igneous rocks from Apuseni from 30 to 120 km wide (Fig. 2) and represents Mountains and the South Carpatians with those an integral part of the Carpathians and of the Timok region and the Srednogorie zone. Balkanides (Fig. 2). The ABTS Belt can be traced from the Apuseni Mountains in the North, to the western part of the South Carpa thians (Banat) in Romania, Timok region and Ridanj-Krepoljine zone in Eastern Serbia, then it curves to the East, where it comprises the Bulgarian Srednogorie and (by geophysical data) continues in the south-western part of the Black Sea. A northwestern branch of the belt is buried under the Tertiary deposits in Voevodina (Kemenci, Canovic 1975). Its magmatic and metallogenic characteristics will be elaborated in the following sections. Pre-Late Cretaceous geology The Pre-Late Cretaceous basement of the ABTS Belt is characterized by continental crust Fig. 1. Position of Apuseni-Banat-Timok-Srednogorie with 35-45 km thickness (Dobrev and Shchukin Magmatic and Metallogenic Belt in SE Europe 1974). It is composed of various rocks from 146 0 Post-Cretaceous sediments [OJ Post-volcanic Upper Cretaceous sedments [2lJ Upper Cretaceous intrusion G"vv J Upper Cretaceous volcanic, volcano-sedimentary rocks - Pre-volcanic Upper Cretac~ous sediments ~ Pre- Upper c retaceous rocks I/ ] main faults j..c Z:J ore regions Ore deposits + Fe-Ti magmatic • Cu or Au-Cu massive sulphide • Fe skarn (]) Cu (Mo, U), Au-Pb-Zn-Cu vein ~ W-Moskarn ~ Ba stock or vein 0 Cu skarn 8 Au vein or shear zone (} Zn-Pb skarn f) Pb-Zn ~ Porphyry copper (/) Sb vein ® Porphyry gold a Mn-Fe volcano-sedimentary Moesian Platform Fig. 2. Geological sketch of the Apuseni-Banat-Timok-Srednogorie Magmatic and Metallogenic Belt Proterozoic to Lower Cretaceous age (Fig. 3). talline blocks in the northern part of the The largest part of this territory belongs to the Thracian (including the Rhodopian, Serbo active margin of the Mesozoic European conti Macedonian and Central Srednogorie areas) nent. Its structure is formed as a result of a and the eastern part of the Pannonian massifs. number of superposed tectonic