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Mineralium Deposita (1997) 32: 426±433 Ó Springer-Verlag 1997 ARTICLE S. Jankovic The Carpatho-Balkanides and adjacent area: a sector of the Tethyan Eurasian metallogenic belt Received: 3 June 1996 / Accepted: 10 January 1997 Abstract The Tethyan Eurasian metallogenic belt (TEMB) was formed during Mesozoic and post-Mesozoic times in the area of the former Tethyan ocean on the southern margin of Eurasia, with the Afro-Arabian and Indian plates to the south. It extends from western Mediterranean via the Alps and southeastern Europe through the Lesser Caucasus, the Hindu Kush, and the Tibet Plateau to Burma and SW Indonesia, linking with the West Paci®c metallogenic belt. The Carpatho-Balkan region is one of the sectors of the TEMB, characterized by some speci®c features. The emplacement of ore deposits is related to a de®nite time interval, and to speci®c tectonic settings such as: 1. Late Permian-Triassic intracontinental rifting along the northern margin of Gondwanaland and/or fragments already separated. This setting involves volcanogenic and volcano-sedimentary deposits (iron, lead/ zinc, manganese, antimony, mercury, barite), skarn deposits associated with volcano-plutonic complexes of bimodal magmatism, and low temperature carbonate-hosted lead/zinc deposits. 2. Jurassic intraoceanic rifting ± ophiolite complexes: This setting hosts major magmatic (particularly podiform chrome deposits) and volcano-sedimentary deposits, mainly of the Cyprus type. 3. Subduction-related setting involves porphyry copper deposits, lesser skarn deposits (iron, locally Pb-Zn), massive sulphide Cu (e.g. Bor) accompanied locally by Pb-Zn of replacement type, epithermal gold deposits, associated with calc-alkaline igneous complexes of the Early Tertiary-Late Cretaceous, and the Neogene gold/silver and base metals deposits. Editorial handling: DR S. Jankovic Department of Mineral Exploration, The Faculty of Mining and Geology, Djusina 7, 11000 Belgrade, Serbia 4. Post-collision continent-continent setting includes deposits of Pb-Zn, Sb, As, Au-Cu associated with volcano-plutonic complexes of calc-alkaline anity. Several major Alpine metallogenic units are developed in the Carpatho-Balkanides and adjacent area, each characterized by speci®c development, mineral associations, and types of ore deposits. Introduction The Tethyan Eurasian metallogenic belt (TEMB) was formed during Mesozoic and post-Mesozoic in the area of the former Tethyan ocean along the southern margin of Eurasia, ¯anked on the south by Afro-Arabian and Indian plates. This metallogenic belt was ®rst recognized as a separate metallogenic unit by Jankovic (1977a). The TEMB is of global size, almost 10 000 km long, and can be compared with the CircumPaci®c belts, though it diers in many respects, and is characterized by many speci®c metallogenic features. It extends from the western Mediterranean via the Alps and SE Europe over the Pontides and Anatolia, Lesser Caucasus and Central and Northern Iran to west Pakistan, Central and SE Afghanistan passing into the Hindu Kush, southern Pamir and the Tibet Plateau reaching Burma and Sumatra, to link with the West Paci®c metallogenic belt. The TEMB consists of several sectors. Figure 1 shows the main regional metallogenic units of the TEMB. The general geotectonic evolution of the domain where the TEMB was formed is closely connected with the history of Tethys, its opening, development of island arcs and microplates, closing, welding of microplates with Eurasia, subduction of oceanic crust(s), as well as collision of continents, continent-island arc collisions and underthrusting of continental crusts. The development of ore deposits and regional metallogenic units is associated with speci®c tectonic settings within the individual sectors of the TEMB. 427 Ore deposits and tectonic setting The tectonic evolution of the Carpatho-Balkanides and adjacent areas in the Alpine period is dominated by the opening and closure of the Tethys-Paratethys ocean. Since the available space for this study is strictly limited, readers are directed to the interpretation of tectonic events in terms of plate tectonics in this region considered by Dimitrijevic and Grubic (1977), Dewey et al. (1973), Herz and Savu (1974a), Horvath (1974), Radulescu and Sandulescu (1973). This study brie¯y reviews the relations between the Alpine deposits, and tectonic settings in the CarpathoBalkanides and adjacent areas based on plate tectonic concepts. These problems have been discussed by Petrascheck (1942, 1974, 1976, 1977, 1982), Herz and Savu (1974a, b), Ilavsky (1977), Ilavsky et al. (1979), Jankovic (1977b), Jankovic et al. (1974), JankovicÂ, ed. (1977), Raincsak (1988), Tvalchrelidze (1985-based on geosyncline concept). Figure 2 shows the relations between regional metallogenic zones and tectonic settings in the NE Mediterranean domain. 1. Intracontinental rifting The intracontinental rifting along the northern margin of Gondwanaland and/or within already separated fragments was particularly widespread during the Late Permian-Middle Triassic. The lateral spreading of continental crust and commencement of drift produced Fig. 1 The Tethyan Eurasian metallogenic belt: the central and eastern segments (above). The principal metallogenic zones in the central and western segments (Jankovic and Petrascheck, 1987) crustal thinning and formation of the graben ¯oor by deep crustal ¯ow and tensional faulting. These processes in the area of consideration were largely of a short duration and failed to reach the stage of ocean ¯oor development. Locally, sea-¯oor spreading along the rift system continues right to the ocean stage as in the area of Mirdita in the Dinarides (Jankovic 1977b). The intracontinental rifting is often accompanied by volcanoplutonic complexes of calc-alkaline composition, spilite-keratophyre, and, locally, albite syenite, and gabbro. The ore metals originated from the intermediate, ma®c or alkaline magmatic complexes, and/or from hydrothermal mobilization from the surrounding rocks. In some areas volcanic sources at depth supplied only heat to drive hydrothermal systems. There are also intracontinental mineral-bearing basins without volcanic activity, the mineralization of which is associated with shallow-water environment, while the sources of metals are most probably non-volcanics. The following three principal morphogenetic types of deposit and metallogenic environment are distinguished. 1.1. First iron-oxide skarn deposits are associated with hypabyssal intrusions. They occur infrequently (e.g. Tovarnica in the Dinarides Jankovic 1982; Iulia and Cetal Bair in Dobrogea, Ianovici and Borcos, 1982; Vlad, 1984a). 428 1.2. Second, volcanogenic hydrothermal and volcanosedimentary deposits, both syngenetic and epigenetic are related to volcanic/subvolcanic activity, close to/or at the ¯oor of an epicontinental sea. Locally, small ore deposits are associated with shallow intrusives (quartz porphyries, diorite, even gabbro, Jankovic 1986, 1987). Scarcity of major copper deposits is a speci®c feature of such environments. The most signi®cant deposits involve (1) barite and base metal sulphides (Somova in Dobrogea, Vlad 1984a), (2) the proximal and distal volcano-sedimentary lead/zinc deposits, locally accompanied by barite and/or cinnabar, (3) hydrothermal veins and stockwork of lead-zinc sulphides hosted by the volcanics (Jankovic 1982), and (4) manganese volcano-sedimentary deposits. 1.3. Third, low temperature deposits are located along continental margins and represented by carbonate hosted lead-zinc sulphides (the Triassic deposits of the Alps), and syngenetic and/or epigenetic mercury mineralization (the Idrija deposit in the Dinarides). 2. Mineralization associated with ocean-¯oor spreading areas When the lateral spreading of continental crust continues beyond the stage of intracontinental rifting, new Fig. 2 Major Alpine metallogenic units and tectonic settings in the northeastern Mediterranean (Jankovic 1977b; modi®ed) oceanic crust is formed and a mid-oceanic ridge develops. The ¯oor of the Tethys has many tectonic elements that are considered to be settings for ore deposits (e.g. active spreading axes, hot-spots). Among the ore deposits, associated with ophiolite suites, particularly in the Dinarides, the following should be mentioned: a. Chromite deposits: numerous podiform chromite deposits are known in the Dinarides and Albanides b. Ni-Cu-Co sulphides (pyrrhotite-chalcopyrite-pentlandite magnetite association accompanied by gold and silver) are locally found in the serpentinites, Jankovic (1990a) c. Titaniferous magnetite veins/lenses and disseminations occur sporadically in the gabbro, accompanied by traces of pyrite and chalcopyrite (JankovicÂ, 1990a) d. Volcano-sedimentary deposits are of two principal types, sporadically found in the same ophiolite complex: (1) sea-¯oor pyritic copper sulphides of Cyprus type, and (2) bedded ferromanganese deposits associated with pillow lavas and with tuaceous beds. Manganese nodules occur sporadically in the Upper Jurassic-Early Cretaceous deep sea sediments (Jankovic 1990a). 429 3. Mineralization in subduction-related setting The closure of Tethys during the Late Jurassic-Early Cretaceous was followed by the subduction of oceanic ¯oor under the European platform, resulting in the generation of numerous volcano-intrusive complexes of calc-alkaline suites, locally alkaline, situated along the western arcs of the Carpatho-Balkanides (Apusenieastern Serbia-Srednegorie). The Laramian magmatism involves both the Senonian volcanics (andesite, dacite, locally rhyolite; andesite prevails), and the Campanian-Paleocene hypabyssal and plutonic rocks (granodiorite, monzonite, diorite). The intrusions are mostly composite and multistage magmatic complexes. Geochemical features of igneous rocks range from continental margin type to island arc type, indicate a contamination of parent magma by continental crust (the 87Sr/86Sr ratios range from 0.07 to 0.14). The collision of the northern Pannonian microplate with the European continental plate in the Late EoceneLower Miocene was followed by the subduction of oceanic lithosphere in the Middle Miocene (Badenian). In the Late Miocene-Early Pliocene a regional island arc type calc-alkaline volcanism was developed in the eastern and western Carpathians. Volcanics dominate and include rhyolite, rhyodacite, dacite and various types of andesite. The centres of volcanic activity were controlled by deep fractures. The emplacements of subvolcanic granite, granodiorite, quartzdiorite porphyries in the volcanic structures are common. The most important types of mineralization are 1. Skarn deposits, both calcic and less frequently magnesian, are commonly developed in the contact zone of plutonic complexes. The dominant ore constituents are iron and base metals, locally molybdenum, boron minerals a.a. The deposits of this type are of particular importance in Banat, Romania (Ianovici and Borcos, 1982 see also Jenchenoaeva 1997 this issue). 2. Pornhyry copper deposits: several major porphyry copper deposits have been discovered since 1950 in the Carpatho-Balkanides (Majdanpek a.a. in Yugoslavia Jankovic 1990a, b; Medet a.a. in Bulgeria ± Bogdanov 1982; Moldova Nuoa a.a. in Romania ± Cio¯ica and Vlad 1980; Ianovici and Borcos 1982; Recsk in Hungary, Baksa et al. 1980). Ore grade mineralization occurs both in the intrusive host rocks (mainly subvolcanic/hypabyssal facies) and in the surrounding rocks, but porphyry copper deposits in andesite prevail. In some of the porphyry copper hydrothermal systems a vertical zoning of various mineralization styles and mineral assemblages have been recognized (Bor, Jankovic 1990b; Recsk-Baksa et al. 1980). Gold content of porphyry copper ore is variable, from less than 0.1 ppm to 1.0 ppm, but mostly 0.2± 0.3 ppm. Concentrations of Pt-group elements (Pt, Pd) are sporadically found (recovery of Pt and Pd is recorded in Bor). 3. Volcanogenic hydrothermal deposits: these deposits are related to volcano-intrusive complexes of calcalkaline suites. They are commonly located at subvolcanic level, genetically associated with deep-seated magmatic sources. The wall-rocks are both volcanics and surrounding rocks. Mineralization is epigenetic with respect to volcanics, replacement type of mineralization occurs in places as well (JankovicÂ, 1986). The spatial distribution of mineralization is often controlled by the volcanic structures. The major deposits of this group include the following: a. Cupriferous pyrite deposits occur in andesite dacite (Bor in Yugoslavia, Jankovic 1990a; Lahoca/Recsk in Hungary, Baksa et al. 1980; Radtka in Bulgaria, Bogdanov 1980). They are of replacement type formed sporadically on the top of porphyry copper systems. b. Polymetallic massive sulphides with high gold content occur in places in volcanics (CÏoka Marin in Yugoslavia, JankovicÂ, 1990a, b; CÏelopecÏ in Bulgaria, Bogdanov, 1980). c. Conglomerate type is a unique type of copper deposits in the Carpatho-Balkanides (Novo Okno in the Bor ore ®eld, Jankovic 1990b). 4. Lead-zinc sulphide deposits are usually located along fractured zones in volcanics (andesite-dacite), less frequently in surrounding rocks, but often in close connection with caldera structures. 5. Epithermal gold-silver deposits, vein and stockwork type of mineralization, occur at subvolcanic levels of andesite-dacite-rhyolite suites in the Carpathians. The most signi®cant are the Neogene deposits in Transilvania, and Banska SÏtavnica-BoÈhmer, 1982). 4. Mineralization related to magmatic activity in post-collision continent-continent setting Some regional metallogenic units such as the SerboMacedonian-Central Anatolian province are associated with the Oligocene-Miocene/Pliocene calc-alkaline complexes. The origin of these magmatic complexes cannot be unequivocally related to subduction of an oceanic crust and its partial melting, although they are situated in the vicinity of a suture zone, formed after the closure of the Vardar-Izmir-Ankara ocean. It is more likely but still a tentative model, that the widespread calc-alkaline igneous suites resulted from an anatectic partial melting of the lowermost part of continental crust and that locally even some ophiolites were involved (Jankovic 1986). These processes took place during the late Paleogene through early Neogene along the suture Vardar-Izmir-Ankara zone, preceded by uplifting of the central parts of suture zone due to lateral compression (Karamata 1982). 430 The ore deposits were emplaced at hypabyssal and volcanic levels, the latter often associated with caldera structures. Some deposits were formed from submarine brines, syngenetic and/or epigenetic with respect to country rocks; they may represent a speci®c group of deposits developed in this tectonic setting (such as hydrothermal-sedimentary deposits of boron minerals, gold/silver ± lead/zinc Sb/As/Tl a.a.). Some deposits were formed above ophiolites and they contain some elements which were mobilized by hydrothermal solutions passing through ophiolites (gold, PGE, copper). Lead-zinc and antimony are the dominant metals in this tectonic setting. Porphyry copper deposits occur along the contact between two tectonic blocks, the Vardar zone and the Serbo-Macedonian massif (SMM). Molybdenum mineralization as disseminated and/or vein types occurs sporadically; some of them contain large reserves but at low grade (MacÏkatica in Yugoslavia). Hydrothermal-sedimentary magnesite and boron deposits occur in the Neogene basins. Major metallogenic units All Alpine ore deposits are located within several major metallogenic units, each characterized by some speci®c features regarding style of mineralization, associations of elements and minerals, and morphogenetic types of deposit. The principal features of these metallogenic units will be brie¯y presented. The Carpatho-Balkan metallogenic province (Fig. 3) is characterized by abundance of base metals and precious metals (Au, Ag). Epithermal mineralization of low sulphidation type dominates, and is associated with Miocene-Pliocene volcanism, in close connection with volcanic structures (volcanic centres and subvolcanic intrusions of calc-alkaline composition, hydraulic fracturing and extensional fault tectonics, etc). The vein type of mineralization prevails, disseminated and stockwork mineralization is subordinate. The Western Carpathian sub-province includes several metallogenic ore districts such as: Central Slovakian district (Pukanec,, Banska SÏtiavnica ± HodrusÏ a, Kremnica) contains volcanic hosted epithermal gold/silver deposits of low sulphidation type; base metal mineralization; skarn magnetite deposits, and some indications of porphyry copper mineralization. Slanske-Tokaj Mts: the epithermal gold/silver, lead/ zinc and antimony deposits are related to Miocene multiphase volcanics, and diorite porphyry. The most signi®cant deposits are in Hungary (e.g. Telkibanya, Rudabanya and GyoÈgyoÈsorszi) (Morvai 1982) and Slovakia (e.g. Brehov). The large porphyry copper-skarn deposit Recsk is associated with Paleogene volcanics in the Hungarian Central Mts. Fig. 3 The Carpatho-Balkanides: principal metallogenic units (simpli®ed) Beregovo-Begansk district in Ukraine: the mineralization of gold/silver, base metals, locally mercury, TeBi and barite occurs in Miocene volcanics. The most signi®cant deposits are Beregovo and Muzhievo (Naumenko, 1987). The Eastern Carpathians sub-province. Various hydrothermal deposits (gold, silver, base metal i.a.) are associated with the Neogene volcanics, mainly andesite, cut by subvolcanic intrusions. The ore deposits in Romania are reviewed by Ianovici and Borcos (1982). The Oas metallogenic zone contains base metal deposits accompanied locally by Au, Ag and Hg mineralization (Bixad, Geamana-Camirzana). Baia Mare metallogenic zone contains signi®cant deposits of precious and base metals, located along the systems of fractures in the volcanics (e.g. Baia Sprie, Herja). Calimani-Gurguhiu-Hargita metallogenic zone involves hydrothermal mineralization of base metals, accompanied locally by gold/silver, mercury, sporadically by native sulphur, associated with volcanic structures. The Apuseni Mts-Krepoljin sub-province. It is developed along a narrow, regional fractured zone (Ianovici et al. 1977; Ianovici and Borcos 1982; Jankovic 1990a). The Apuseni Mts: the ore deposits related to the Upper Cretaceous-Paleocene volcano-plutonic complexes of calc-alkaline suites (diorite, granodiorite etc). 431 Related metallogeny involves various styles of mineralization (skarn-hydrothermal) of Fe, Pb/Zn, Cu, minor B, Mo, Bi, W, Co, Ni, Au, As, Ba (Folea et al. 1987; Vlad 1984b). Skarns are the dominant type (Mo-Bi ores, Cu-W a.a.). The Metalliferous Mts: the ore deposits (Au, Ag, Te and base metals including porphyry copper mineralization) are associated with the Badenian-Pliocene volcanointrusive complexes. The ore deposits are commonly located in the roots of the volcanic structures. The Banat zone: the ore deposits occur mainly as skarn type, both calcic and locally magnesian; magnetite-hematite (Ocna de Fier) and molybdenite-chalcopyrite associations (Oravita, Moldova Nuoa) occur most frequently. They are related to the Upper CretaceousPaleocene magmatic complexes (granodiorite, diorite). The Krepoljin unit: this is an extension of the previous zone southwards of the Danube. The mineralization is related to the andesite-dacite subvolcanic intrusions: the small replacement type of Pb/Zn-Au/Ag association, skarn base metals accompanied by minor Bi and Mo; veins of Sb-W and replacement of stibnite, as well as copper sulphides in Permian sandstone. The Bor-Srednegorie sub-province. It is related to a riftgraben structure, which is traced from Bozovici in Romania over Bor in Yugoslavia to Srednegorie and Burgas/Black sea in Bulgaria. Copper and gold/silver, locally molybdenum and lead/zinc are the most signi®cant metals. The ore deposits are associated with the Upper Cretaceous volcano-plutonic complexes of calcalkaline suites. The Bor ore district involves several porphyry copper deposits (Majdanpek i.a.) with the large cupriferous massive pyrite/porphyry copper-gold deposit at Bor, and small base metals/gold deposit at CÏoka Marin (Jankovic 1990 a, b). The Panagyurishte ore district contains porphyry copper deposits (Medet, Assarel, Elatsite), and massive sulphide deposits (Radtka, Elshitsa and CÏelopecÏ Bogdanov 1982). The Burgas ore district: the mineralization of vein quartz-chalcopyrite association prevails (Rossen, Zidarevo). Some of them are characterized by the presence of Mo, Co, and Bi minerals (Bogdanov 1982). The Serbo-Macedonian metallogenic province. This regional metallogenic unit is developed along the suture zone of ocean. The Alpine ore deposits are commonly associated with the Oligocene-Miocene, locally the Pliocene volcano-intrusive complexes of calc-alkaline suites (Karamata 1974; Jankovic 1990a, b). The most signi®cant deposits are those of lead/zinc, to some extent copper and antimony, accompanied by gold, silver, arsenic, thallium, bismuth, iron. The major metallogenic units are displayed in Fig 4. They include: (1) the Podrinje ore district with signi®cant lead/zinc (e.g. Srebrenica), and antimony deposits (e.g. ZajacÏa); (2) the SÏumadija-Kopaonik ore district characterized by Fig. 4 The Serbo-Macedonian metallogenic province: principal metallogenic zones (Jankovic 1990a) skarn, hydrothermal replacement and vein types of leadzinc mineralization (e.g. TrepcÏa a.a); (3) the LeceChalkidiki metallogenic zone involving lead-zinc deposits such Lece, Zletovo, Olympias, and porphyry copper deposits (e.g. BucÏim, Skouries etc); (4) the Osogovo metallogenic zone dominated by signi®cant leadzinc deposits (e.g. Sase-Toranica etc); and (5) the KozÏuf ore district with minor copper, and important Sb/As/Tl/ Au deposits (e.g. AlsÏ ar). The Dinaric-Hellenides metallogenic province Mineralization is associated with Triassic intracontinental rifting. Jankovic (1977b, 1987) reviewed the principal types of deposit and major metallogenic units. Figure 5 shows the main Triassic metallogenic districts in the Dinarides: (1) the Ljubija ore district containing carbonate-hosted siderite ore bodies, accompanied sporadically by lead-zinc sulphides; (2) the middle Bosnian Mts with numerous occurrences of Sb, As, Cu, Pb/Zn W, Hg-vein type mineralization, locally minor skarn and/or hydrothermal magnetite deposits; (3) the northern Montenegro metallogenic zone dominated by the lead zinc mineralization (volcanogenic and volcanosedimentary types) in this metallogenic zone (e.g. SÏuplja 432 Fig. 5 The principal metallogenic zones in the Dinario province (Jankovic 198) Stijena, Brskovo); (4) the VaresÏ ore district with iron deposits (e.g. VaresÏ : siderite-hematite-massive sulphides stratiform deposit) and lead/zinc-barite-stibnite-cinnabar mineralization (e.g. VeovacÏa); and (5) the Podrinje ore district containing small lead-zinc ore-bodies hosted by carbonates, and volcano-sedimentary lead/zinc-barite mineralization. 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