Ore Geology Reviews 34 (2008) 501–520

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Ore Geology Reviews

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Metallogeny of the Northwestern and Central Dinarides and Southern Tisia

Ladislav A. Palinkaš ⁎, Sibila BorojevićŠoštarić, Sabina Strmić Palinkaš

Faculty of Sciences, Department of Geology, Institute of Mineralogy and Petrology, University of Zagreb, Horvatovac bb, 10 000 Zagreb, Croatia

ARTICLE INFO ABSTRACT

Article history: The Dinaridic metallogenic province is a part of the Alpine–Himalayan orogenic system, developed as a result Received 31 July 2006 of opening and closure of the Tethys Ocean by convergence of the African and Eurasian plates. The northern Accepted 6 May 2008 boundary of the Dinarides is related to the northern African margin (Adria–Apulia). The Tisia mega-unit, a Available online 10 June 2008 small continental block, positioned between the Dinarides and the Carpathians, is genetically related to the South Eurasian edge. Keywords: Magmatism The geology of the Dinarides is constrained by the Alpine Wilson cycle. The major stages of the cycle are: Metallogeny (a) Permian early intra-continental rifting; (b) Triassic advanced rifting; (c) Jurassic oceanization; Wilson cycle (d) Cretaceous subduction; (e) Paleogene collision; and (f) Neogene post-collision and extension followed Alpine by orogenic collapse. Each stage creates characteristic ore deposits related to the specific geological Variscan environments. Stage (a) bears hydrothermal siderite–barite–polysulphide deposits, epigenetic sedimentary Northwestern and Central Dinarides uranium deposits, red bed-type, sabkha-type copper and barite deposits and evaporites. Stage (b) favored Tisia SEDEX and hydrothermal iron–polysulphide–barite–mercury and MVT deposits. Stage (c) developed – Zagorje Mid-Transdanubian zone chromites, asbestos, talc and magnesite deposits. The spatial position of stage (d) remains poorly constrained. The Southern Tisia unit might be a possible candidate for the Tethyan active continental margin with the Cretaceous subduction zone positioned beneath. Absence of voluminous subduction-related magmatism and mineral deposits, however, favors subduction within the Vardar zone (the easternmost Dinarides), adjoined to the Serbomacedonian ensialic terrain with its large Cu-porphyry deposits. Stage (e) was a prelude to the prolific phase (f) with its numerous hydrothermal Pb, Zn and Sb deposits that mostly occur in the western Vardar zone. The geology and metallogeny of Southern Tisia, with medium/high grade metamorphics, I-type, S-type granites, resembles the Middle Austro-Alpine unit, formed during the main Carboniferous collisional stage. This contribution provides a review of the metallogenic characteristics of the Northwestern and Central Dinarides and Southern Tisia mega-units, based on recently-gained knowledge on the regional geology, petrology and genesis of mineral deposits. Establishment of the plate tectonic model several decades ago greatly contributed to an integrated interpretation of ore deposit genesis. In turn, basic research in the field of ore genesis generated new data that can be used to improve the plate tectonic model. © 2008 Elsevier B.V. All rights reserved.

1. Introduction Franke et al., 1995). There is, however, a wide range of interpretations in the nature, position, kinematics and chronology of rifting, drifting Mineral deposits in the southeastern part of Central Europe belong and collisions of the suspected terrains — with their inherited metal- to the two prominent geological mega-units: Northwestern–Central logenies, which were assembled before the final continent–continent Dinarides and Southern Tisia. The Dinarides, an orogenic belt po- collision in the Variscan orogen. sitioned between the Adria microplate to the southwest and the Tisia The ACD loop consists of external units, mainly medium-grade ensialic block to the north, is part of a long suture of the Tethyan metamorphic terrains, namely the “Variscan peri-Mediterranean Ocean, squeezed between the Gondwana and Euroasian continents. metamorphic belt”, and the internally-located, peri-Apulian, fossil- Their common history, however, extends back to pre-Variscan time. bearing, “Noric–Bosnian” terrain. The former incorporates Tisia, and The Alpine–Carpathian–Dinaride (ACD) arcuate orocline comprises the latter the basement and uncovered Paleozoic terrains of the basement units composed of pre-Variscan continental fragments pre- Dinarides (Neubauer and Handler, 1999). The boundary between the viously amalgamated between Baltica and Gondwana (Matte, 1991; two units suggests the presence of a Carboniferous suture, placed between the southern branch of the European Variscids and a Gondwana-derived paleo-Alpine indenter. The geodynamic evolution ⁎ Corresponding author. Tel./fax: +385 1 4605 998. related to continental plate collision involves consumption of the E-mail address: [email protected] (L.A. Palinkaš). intervening ocean basin with obduction of ophiolites, medium/high

0169-1368/$ – see front matter © 2008 Elsevier B.V. All rights reserved. doi:10.1016/j.oregeorev.2008.05.006 502 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 pressure metamorphism, intrusion of I-type granitoids, followed by S- Pamić and Lanphere, 1991; Lanphere and Pamić, 1992; Pamić et al., type granitoids, and deformation of the Gondwana-derived Noric– 1996). Bosnian terrain in Late Devonian/Early Carboniferous time. The The Tisian Variscan basement is overlain by a non-metamorphic boundary was entirely reactivated during Alpine rifting. Mesozoic cover, and the thick Tertiary fill of the Pannonian basin. By Magmatism in the Eastern Alps and the Southern Tisia shows contrast, the Dinarides, underlain by low/medium-grade meta- similar petrochemistry, timing and style of emplacement. South Tisia morphic rocks of the pre-Alpine African crust, with a Cadomian underwent Variscan orogenesis, as evidenced by its crystalline signature, experienced the complete Alpine Wilson cycle from rifting basement with medium/high- grade metamorphic rocks, I-type and to collision in the Mesozoic. S-type granitoids. The granitoids and metamorphic rocks in South Alpine metallogeny of the Dinarides was primarily created by Tisia have been dated by K/Ar, Ar/Ar and Rb/Sr methods. Barrovian- opening and closure of Vardar and Dinaridic branches of the Tethyan type metamorphic rocks in the Slavonian Mts. yielded 568 to 264 Ma, ocean. The Dinarides contain well-developed and preserved tectonos- S-type granites and migmatites, 336 to 300 Ma, and I-type granites in tratigraphic units of the Alpine Wilson cycle, in contrast with the the Slavonian Mts. 339 to 321 Ma (Lanphere et al., 1975; Pamić, 1988; neighbouring Alps where the indentation of Adria obliterated or

Fig. 1. Geological structural scheme of the Dinarides and surrounding area with index-map (modified after Channell and Kozur, 1997; Tomljenović,2002). L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 503 blurred their regular distribution as a result of extensive tectonome- mountains, situated close to the Tisia microplate, are mainly covered tamorphic events. The metallogeny of the Dinarides and Tisia, based by Tertiary fill of the Pannonian Basin and verge to the northwest. The on the principles of plate tectonics, has been upgraded over recent main tectonstratigraphic units of the Central Dinarides display a decades (Janković, 1977, 1986; Petraschek, 1977; Pamić and Jurković, regular zonal pattern from stable Adria to Tisia. The historical division, 1997; Heinrich and Neubauer, 2002; Jurković,2003). ‘External’ and ‘Internal’ Dinarides, predates plate tectonics, but is still A basic framework has been successfully established but difficul- useful to discriminate tectonostratigraphic elements belonging to the ties have arisen from unresolved geological problems such as the passive and active Tethyan continental margins, respectively. boundary between Variscan and Alpine tectogenesis, the existence of The tectonostratigraphic units, products of Tethys opening and one or two oceanic realms, and the position of the subduction zone closure during successive phases of the Alpine Wilson cycle, are as adjacent to Tisia or the Serbomacedonian suspect terrain. Another follows (Fig. 1): (1) Adriatic–Dinaridic carbonate platform (ADCP); source of ambiguity was a lack of fundamental research on ore (2) carbonate–clastic formations of the passive continental margin genesis, and reliable interpretation of ore types in genetic terms. (Bosnian flysch); (3) Dinaridic ophiolites; and (4) units of the active Proper genetic models and ore petrology contribute substantially to continental margin, olistostrom mélange, Sava–Vardar zone. Units understanding the geological evolution of the Dinarides, and wider, (1) and (2) belong to the External Dinarides; (3) and (4) to the Internal along the entire Tethyan belt. This contribution presents a set of new Dinarides. Any consistent distribution is disturbed by regional nappe data on ore petrology, geochemistry and geology of ore deposits, systems, and exhumation of medium-grade metamorphic terrains in which will assist modification of the plate tectonic model. the Mid-Bosnian Schist Mountains (MBSM). The Dinarides as a whole were thrust onto units of the South Tisia in Pliocene time. 2. Northwestern and Central Dinarides The northwesternmost part of the Dinarides does not exhibit the same regular patterns as the Central Dinarides (Fig. 1). Here, the The Dinarides are an orogenic belt stretching 700 km along the Dinarides deflect NE–SW as the Zagorje–Mid-Transdanubian Zone northeastern margin of the Adriatic microplates (Dercourt et al.,1993). (ZMTZ, Pamić and Tomljenović, 1998), between the Zagreb–Zemplin In the north, this highly complex folded, thrusted, and imbricated belt Fault (ZZF) and the Periadriatic–Balatone Fault (PBF). The region is merges with the Southern Alps and; in the southeast it extends into largely covered by the Sava nappe, composed of Upper Palaeozoic and the Hellenides (Pamić et al., 1998). The general strike of the folds, Triassic formations (Mioč, 1984). The ZMTZ, or the Sava composite thrusts and nappes in the Central Dinarides is NW–SE, and the mega-unit (Haas and Kovács, 2001), bears elements of both the transport direction is towards SW. The Northwestern Dinaridic External and Internal Dinarides, and also the Southern Alps. It was Mountains (Prosara, Motajica and Majevica) comprise collisional and squeezed between ZZF and PBF and extruded eastwards by Tertiary syn-collisional granitoids of Early and Middle Eocene age. These indentation of the Adria microplate during formation of the Alps.

Fig. 2. Geological sketch-map of the Central and Northwestern Dinarides and the southwestern parts of Tisia showing the locations of the Paleozoic complexes (gray), and related ore deposits (see Table 1 for description) with index-map (modified after Pamić and Jurković,2002). 504 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520

2.1. Pre-Variscan, Variscan and post-Variscan geodynamics and orogenic Wilson cycles is clearly visible within recent global geodyna- metallogeny of NW and Central Dinarides mic processes. Any firm distinction of metallogenic processes at the transition of The Dinaridic Palaeozoic complexes (PC) occur in the External and Variscan, post-Variscan and at the onset of Alpine tectogenesis is Internal Dinarides (Fig. 2). The geodynamic evolution of the PC highly blurred by the above ambiguities. While the Alpine Wilson pertains to the opening and closure of Rheic and Palaeotethys oceans cycles are easily recognized and classified into early and advanced (e.g., Jurković and Pamić,2001). Rifting processes along North rifting, oceanization, subduction, syn-collision and post-collision, the Gondwana commenced in the Silurian, locally in Cambrian–Ordovi- earlier, Variscan events are less clearly defined. cian time, followed by the Late Silurian/Devonian opening of the The following analysis will try to distinguish formation of mineral Palaeotethys. Subduction processes were initiated along the Laur- deposits linked to both orogenic events, but not with uniform ussian margin by the end of Devonian and the beginning of Carboni- reliability and quality of arguments. The described deposits were ferous. The main Variscan deformation, during collision of Gondwana mined in the past, or are still in production. The main criterion for and Laurussia, continued into Namurian–Westphalian time. introducing certain deposits into the presentation is primarily the The PCs in the External Dinarides, close to or within the carbonate existence of a characteristic genetic model, rather than size or eco- platform, acquired a comparatively autochtonous position relative to nomic importance. Numbering of the deposits is related to their their Mesozoic cover. Within the Sava nappe, PCs are disrupted and position on Fig. 2; description is given in Table 1. allochtonous. They can be equated tectonostratigraphicaly with those in the Southern Alps, and could be related to the Gondwana passive 2.1.1. Pre-Variscan, Variscan and post-Variscan deposits continental margin. The PCs in the Pannonian and Durmitor nappes Autochtonous Upper Carboniferous to Permian formations of the are related to the Paleotethyan oceanic realm, and might be similar to External Dinarides outcrop over a very small area. They occur in the Upper Austroalpine unit of the Alps. The Palaeozoic formations within cores of disrupted anticlines in Gorski Kotar and the Mt. Velebit area carbonate platform or adjacent to it, were not affected by metamorph- (Herak, 1986). In these areas, an unknown Variscan basement is ism. The PCs in the Sava nappe underwent very low and low-grade overlain by Moscovian limestones, Kassimovian sandstones, Auernig metamorphism, and those in the Pannonian and Durmitor nappes beds, Rattendorf limestones and evaporites (Ramovš et al., 1989). No locally achieved epidote–amphibolite grade, while granitoids in the ore deposits are recorded in the post-Variscan formations of the South Tisia reached polymetamorphic-grade with migmatites. This External Dinarides, with exception of barite deposits in the Lika led to the birth of Pangea and foundation of the Variscan basement, region. which was subsequently unconformably overlain by products of the Stratabound barite deposit.No.1Gračac. These deposits are situated new post-Variscan sedimentary cycle in the Late Carboniferous and within the Upper Carboniferous (Auernig beds), fine-grained clastics, Permian. limestones and dolostones of the Lika region. The ore has diagenetic– The possible boundary between Variscan and post-Variscan metal- epigenetic character and a simple paragenesis. The dominant mineral logenic events could be arbitrarily accommodated at the unconfor- is barite; pyrite, galena and sphalerite occur in minor amounts. The mity defined by the deformed Lower Carboniferous metamorphic model lead age (264 Ma) using the single-stage growth model of Doe basement, and Lower–Middle Carboniferous flysch-type deposits, and Stacey (1974) is probably too young (Palinkaš, 1985). Production followed by Upper Carboniferous–Permian molasse-type sediments. yielded close to 450,000 t in total. Post-Variscan and Alpine metallogeny could be separated by the Allochtonous Paleozoic formations occur in three nappes: Sava beginning of Middle–Upper Permian red bed-type clastic sedimenta- nappe, Pannonian nappe and Durmitor nappe (Fig. 2). tion (terrestrial clastic sediments deposited in Permian rifts). The Sava nappe forms the eastern extension of the Southern Alps Finally, the dilemma of the strict discrimination between the two in Slovenia (Mioč, 1984). The nappe is continuous to Samoborska Gora, cycles may become superfluous. Docking of separate blocks in the and southeastwards in the Central Dinarides, most probably as the process of Pangea amalgamation proceeded with delay in time and Durmitor nappe. The Variscan PC of Medvednica Mt. is composed of under variable conditions including continuous and discontinuous greenschist facies metaclastics, marbles, and orthogreenschists of sedimentation. A shift of Variscan metamorphism in the Alps from uncertain age (Silurian–Triassic?). The formation is affected by an west to east is already recorded (Neubauer, 1988). Overlapping of Early Cretaceous metamorphic overprint at 125 Ma (obtained on

Table 1 Characteristics of the pre-Alpine deposits in the Northwestern and Central Dinarides and the southeastern part of Tisia

Geotectonic unit No./deposit Mineralisation Host rocks Ore/industrial minerals Size Carbonate platform basement 1 Gračac Barite stratabound Upper Carboniferous clastitcs Barite ⁎ and carbonates Sava nappe 2 Medvednica Mt. Fe, Mn, Ba SEDEX Silurian–Devonian metamorphics Magnetite, barite o.e. 3 Litija Cu, Pb, Zn, Sb, Hg, Permo-Carboniferous sediments Galena, sphalerite, ⁎ Ba Fe meso-epithermal chalcopyrite 4 Ključ Fe SEDEX magnetite ? Ordovitian–Carboniferous metamorphics Magnetite, chamosite, pyrite o.e. Durmitor nappe 5 Mid-Bosnian Fe, Ba, Cu, Sb, Hg, As, Silurian–Carboniferous metamorphics, ⁎⁎⁎ Schist Mts. (MBSM) Au meso-epithermal Permian metaryolites 6 Vrtlasce, MBSM Fe, Zn, Pb, Sn, Mo, As, Pyrite, barite sphalerite, ⁎ Cu, Bi katathermal galena, siderite 7 Čemernica, MBSM Fe, Sb, Zn, Cu, As, Pyrite, stibnite, sphalerite, ⁎ Hg mesothermal barite 8 Fojnica, MBSM Fe, Sb, As, Ba, Pb, Cu, Pyrite, siderite, gold, ⁎ Au mesothermal tetrahedrite, stibnite 9 Bakovići, MBSM Au, pyrite (Carlin-type) Dolostones–metarhyolites Gold, pyrite ⁎ 10 Hrmza, MBSM Ba, Hg, As epithermal Metaryolites Barite, cinnabar, realgar ⁎ Tisia basement 121 Kaptol, Sivornica, Brusnik Graphite Metamorphics Graphite, meta-antracite ⁎ 122 Papuk Mt. Pegmatites Metamorphics Feldspars, muscovite ⁎ 123 Ninkovača creek U sedimentary Devonian? meta- Coffinite o.e.

⁎⁎⁎ Large, ⁎⁎ medium, ⁎ small, o.e. in exploration. L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 505 several muscovite concentrates by Ar/Ar measurements; Borojević overlain by Permian conglomerates, sandstones, evaporites, covered Šoštarić,2004). K/Ar measurements yielded ages of 122 to 110 Ma by dolostones (rauhwacke)(Jurić,1979). The Banovina–Kordun and (Belak et al., 1995). The PCs are positioned along the Zagreb–Zemplin Sana–Una Palaeozoic units host numerous hydrothermal-metaso- lineament in the Zagorje–Mid-Transdanubian zone as a result of matic Fe–Ba–Pb–Zn deposits, but they are clearly related to the Alpine Tertiary extrusion tectonics. cycle (early intra-continental rifting). Stratiform SEDEX Fe, Mn, Ba deposits. No. 2 Medvenica Mt. The PC The Palaeozoic succession of the Mid-Bosnian Schist Mts. (MBSM) formation at Medvednica Mt. incorporates stratiform ferruginous starts with Silurian metaclastics, with limestones and lydites, quartzites, 1 to 3 m thick, with 15 to 30 wt.% Fe and 0.2 wt.% Mn. The interlayered with metavolcanics — now greenschists and amphibo- ore beds can be traced along strike for 7 km. Greenschists of the same lites, followed conformably by fossiliferous Devonian platform area contain stratified barite, magnetite and stilpnomelane miner- carbonates, which grade into the platy Lower–Middle Carboniferous alisation (Šinkovec et al., 1988). limestones, unconformably overlain by Middle Permian conglomer- The Variscan PC in Slovenia is represented by Middle Devonian ates. In the Late Carboniferous–Early Permian, the region was affected platform limestones, Devonian basinal sediments, Namurian and by widespread calc-alkaline magmatism (rhyolites, colloquially Lower Westphalian metapelites, metapsammites and metaconglome- named quartz porphyries). Evidence for post-Variscan subduction is rates with flysch signature (Mlakar, 1993). Post-Variscan overstep lacking. formations of the Sava nappe consists of Upper Carboniferous An alternative event responsible for magma generation might be metaclastics with conglomerate interlayers containing lydite pebbles post-collisional or early intra-continental rifting. The alkaline char- derived from the Variscan basement (Mlakar, 1986). The Permian beds acter of MBSM quartz porphyries suggests incipient rifting (Palinkaš comprise carbonate and clastic deposits south of the Periadriatic et al., 2001). Basal conglomerates with quartz porphyry pebbles and lineament, but only clastic ones to the north. The Palaeozoic facies coarse detrital clastics of Upper Permian age overlie the Variscan and of the Sava nappe resemble those in the External Dinarides in post-Variscan formations. many respects. It suggests a common palaeogeographic origin at the Post-Variscan epithermal high- and low-sulphidation Fe, Ba, Cu, Sb, northern margin of Gondwana. Numerous ore deposits occur in the Hg, As, Au deposits. No. 5 Mid-Bosnian Schist Mts. Ore deposits of the Litija area. MBSM have been mined since prehistoric time. This was once the Meso-epitermal Pb, Zn, Cu, Hg, Ba, Fe ore deposits. No. 3 Litija. In the major gold producing area of the Roman Empire; gold was mined from wider area of Ljubljana, Permo-Carboniferous dark-grey slate, quartz both primary deposits and placers. The widespread hydrothermal vein sandstone, and quartz conglomerate accommodate concordant and deposits were formed by extrusion and intrusion of rhyolitic magma discordant ore veins. Between Hrastnica (near Medvode) in the west, in the Late Carboniferous to Early Permian. Host rocks are Lower and Pecelj (at Sevnica) in the east, more than 40 mined deposits are Palaeozoic sericite–chlorite–quartz schists, which grade into meta- situated along an 80 km-long belt, mostly within the Litija anticline. sandstones, fossiliferous Devonian carbonates and Lower Carbonifer- The hydrothermal deposits can be classified according to the ous meta-sediments (Jurković, 1957). Different depths of formation dominant minerals in the veins: (1) sphalerite, (2) galena-sphalerite, and distance from the parent magmatic body, as well as erosion level, (3) galena-sphalerite-cinnabar, (4) cinnabar, and (5) stibnite. The Litija gave rise to a variety of mineral parageneses. A zonal distribution of deposit is one of the largest deposits in the Sava nappe and ore has mineral parageneses around the centre of volcanic activity is, how- been mined and smelted since Prehistoric time. The ore reserves of ever, recognized, although a volcanic edifice has not been recon- Litija enabled production of 50,000 t Pb, 1 t Ag, 42.5 t Hg and 30,000 t structed. High-temperature veins with tourmalinization of wall-rocks barite. The paragenesis is galena, sphalerite, chalcopyrite, tetrahedrite, are located in a deeper part of the meta-rhyolite complex. cinnabar, barite and siderite. The δ34S of sulphide is close to 0.0‰, Mineral parageneses in individual deposits are as follow: no. 6 and in barite is between +17 and +23‰. The deposits show vertical Vrtlasce deposit, pyrite, pyrrhotite, sphalerite, galena, siderite, cassiter- hydrothermal zonation of mineral parageneses — barite, Hg, Pb, Zn, Cu ite, molybdenite, arsenopyrite, chalcopyrite, and traces of Pb–Sb- and Bi- and quartz, in succession downwards. The veins were filled before sulphosalts. No. 7 Čemernica deposit, contains an epi-mesothermal deposition of Middle Permian beds, and are related to Lower Permian paragenesis and comprises quartz veins with cinnabar, stibnite, magmatism, which furnished quartz porphyries and keratophyres in sphalerite, antimonite, minor siderite, pyrite, arsenopyrite and Ag- the Eastern Alps. True outcrops of the volcanics have not been found in minerals. No. 8 Fojnica deposit, bears quartz–pyrite–siderite veins with Slovenia, although pebbles are reported from the Permian Val native gold (up to 20 g/t), tetrahedrite, stibnite, arsenopyrite, barite, Gardena beds (Drovenik et al., 1980). galena, chalcopyrite and calcite. No. 9 Bakovići deposit has a gold- Stratifom SEDEX magnetite occurrences. Palaeozoic rocks are bearing pyrite impregnation at the contact between dolostones and represented in the Ključ area by non-fossiliferous slates, phyllites, metarhyolites (Carlin-type). No. 10 Hrmza, Berberuša Mt. deposit, sandstones and lydites of presumed Ordovician–Silurian to Carboni- consists of low-temperature parageneses including barite veins with ferous age. The Variscan formations are unconformably overlain by cinnabar and realgar, cinnabar veins and realgar veins. The major ore the new sedimentary cycle, red sandstones and porous limestone mineral is Hg-bearing tetrahedrite, with distinctly negative δ34S values (Zellenkalk) of probable Late Permian age. Deposit No. 4 Ključ. Stra- (between −5.5 and −15.4‰); siderite is the main gangue mineral. Barite tiform occurrences of magnetite, chamosite and pyrite occur in the from 14 orefields has δ34Sbetween+6.3‰ and +17.2‰ (mean +11.5‰), Palaeozoic rocks of Ključ area, NW Bosnia (Jurković, 1959). which points to the contribution of Permian seawater sulphate or Variscan and post-Variscan formations of the Pannonian and Dur- evaporites. mitor nappes are widespread along the Dinarides. They exist within Fluid inclusion studies on quartz, barite, fluorite, and hyalophane following terrane: 1. Banovina–Kordun; 2. Sana–Una; 3. Mid-Bosnian from the mineralization in Čemernica, Međuvršje, Raštelica, Hrmza, Schist Mts. (MBSM) (Fig. 2); and out of the map, 4. Drina–Ivanjica– Berberuša, and Busovača suggests two end-member fluid sources: Jadar and 5. Foča–Prača. (a) magmatogenic, related to the rhyolite magmatism, determined in

The Palaeozoic Banovina–Kordun terrane is built of Upper Raštelica and Hrmza (highly saline, CaCl2–NaCl–H2O, 24.0 to 32.9 wt.% Palaeozoic non-metamorphosed clastics and carbonates. Devonian– NaCl equiv., TH =180 to 240 °C), and (b) metamorphenic, generated by Carboniferous flysch formation passes into coarse-grained Permian retrogressive metamorphism during Oligocene exhumation of the sediments, unconformably overlain by Val Gardena sandstones. Dinarides (31.2±0.3 Ma, Ar/Ar plateau age on hyalophane, Balogh In the Sana–Una terrane, Devonian non-metamorphosed clastics et al., 1999). Type (b) fluids are aqueous-carbonic fluids in quartz and and carbonates grade into Early–Middle Carboniferous slates, with hyalophane from alpine veins in Busovača, and vein-quartz in limestone and dolostone olistoliths, developed as a wild-flysch facies, Berberuša with low salinity (6.6 to 13.5 wt.% NaCl equiv., Busovača; 506 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520

2 to 4 wt.% NaCl equiv., Berberuša, TH =270 to 330 °C) and the presence the following tectonostratigraphic phases: (1) early intra-continental of vapour-phase CO2 and N2. Associations of primary type (a) and rifting (Middle–Late Permian, thermal doming, incipient magma- secondary type (b) fluid inclusions are determined in quartz from tism); (2) advanced rifting (Middle Triassic, extensive submarine Čemernica, Međuvršje and Kreševo (Palinkaš et al., 2000a; Jurković and subaerial volcanism and plutonism, resulting in emplacement and Palinkaš,2002). of basalts, spilites, keratophyres, gabbros and andesite–diorites); (3) oceanization, generation of ophiolites (Jurassic–Early Cretaceous); 2.2. Alpine geodynamics and metallogeny of NW and Central Dinarides (4) subduction (Late Cretaceous–Paleogene, emplacement of ophio- lites in the accretionary wedge formations, ophiolitic mélange, basalt– Generation of the main tectonostratigraphic units of the Dinarides, rhyolites); (5) collision (Paleogene granites); and (6) post-collisional with their characteristic lithologies, stemmed from the Mesozoic magmatism (Oligocene–Neogene andesite–dacites, granodiorites). evolution of the Dinaridic part of the Tethys. The individual stages of From the metallogenic point of view, phases 1, 2 and 6 were the the Wilson cycles are recognized by specific magmatic formations, and most productive. In the following sections, we describe metallogeny are responsible for formation of numerous mineral deposits and related to the above geodynamic events. Deposits with numbers are occurrences. In the NW and Central Dinarides one can differentiate located on Fig. 3; their characteristics are summarized in Table 2.

Fig. 3. Geological structural scheme of the Dinarides and surrounding area with index-map (modified Tomljenović,2002) and related Alpine ore deposits (see Table 2 for description) with index-map. L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 507

Table 2 Characteristics of the Alpine deposits in the Northwestern and Central Dinarides

Geodynamic environment No./deposit Mineralization Host rock Ore/industrial minerals Size Permian Early intra-continental 11 Rude, Samoborska gora Mt., Fe–Cu–Ba SEDEX, Middle–Upper Permian clastics Siderite, hematite, galena, ⁎ rifting (EIR) NW Croatia meso-epithermal sphalerite 12 Ljubija, Adamuša, Brdo, Fe–Ba–Pb–Zn±F replacement Middle Carboniferous flysch Siderite, ankerite, ⁎⁎⁎ Atlijina kosa limonite, galena 13 Tomašica, Sana–Una Palaeozoic Fe replacement Middle Carboniferous flysch Siderite, ankerite ⁎⁎⁎ 14 Omarska, Sana–Una Palaeozoic Fe replacement Middle Carboniferous flysch Siderite, ankerite, limonite ⁎⁎⁎ 15 Žune (Dolinac), Ba–F mesothermal Middle Carboniferous flysch Barite, fluorite ⁎ Sana–Una Palaeozoic 16 Vidrenjak, Sana–Una Palaeozoic Ba–F mesothermal Middle Carboniferous flysch Barite, fluorite ⁎ 17 Žirovac, Trgovska gora Mt. Fe replacement Carboniferous flysch Ankerite ⁎⁎ 18 Gvozdansko, Trgovska gora Mt. Fe mesothermal Carboniferous flysch Siderite ⁎⁎ 19 Gradski potok, Trgovska gora Mt. Cu–Fe mesothermal Carboniferous flysch Siderite, chalcopyrite ⁎⁎ 20 Majdan, Trgovska gora Mt. Pb–Fe mesothermal Carboniferous flysch Siderite, galena ⁎ 21 Tomašica, Trgovska gora Mt. Fe–Cu–Pb mesothermal Carboniferous flysch Siderite, chalcopyrite, galena ⁎⁎ 22 Kijak, Petrova gora Mt. Ba epithermal Permian sediments Barite ⁎ 23 Gejkovac, Petrova gora Mt. Ba epithermal Permian sediments Barite ⁎ 24 Bukovica, Petrova gora Mt. Fe SEDEX Permian sediments Hematite ⁎ 25 Žirovski Vrh, Slovenia U sedimentary-epigenetic Middle Permian clastics Coffinite, uraninite ⁎⁎⁎ 26 Škofje, Slovenia Cu Kupferschiefer-type Middle Permian clastics Chalcopyrite, chalcocite ⁎ 27 Lokve, Gorski kotar region Ba Sabkha-type Permian–Triassic sediments Barite, pyrite ⁎⁎ 28 Mrzle vodice, Gorski kotar region Ba Sabkha-type Permian–Triassic sediments Barite, pyrite ⁎⁎ 29 Školski Brijeg, Gorski kotar region Ba Sabkha-type Permian–Triassic sediments Barite, pyrite ⁎⁎ 30 Bosanski Novi Gypsum-anhydrite Upper Permian evaporites Gypsum ⁎ 31 Derviši, Bosanski Novi Gypsum-anhydrite Upper Permian evaporites Gypsum ⁎ 32 Petkovac, Bosanski Novi Gypsum-anhydrite Upper Permian evaporites Gypsum ⁎ 33 Bosanska Krupa Gypsum-anhydrite Upper Permian evaporites Gypsum ⁎ 34 Kulen Vakuf Gypsum-anhydrite Upper Permian evaporites Gypsum ⁎ 35 Desnice, Martin Brod Gypsum Upper Permian evaporites Gypsum ⁎ 36 Kaldrma, Srb Gypsum Upper Permian evaporites Gypsum ⁎ 37 Knin Gypsum Upper Permian evaporites Gypsum ⁎⁎ 38 Drniš Gypsum Upper Permian evaporites Gypsum ⁎ 39 Vrlika Gypsum Upper Permian evaporites Gypsum ⁎ 40 Karakašica, Sinj Gypsum Upper Permian evaporites Gypsum ⁎⁎ 41 Kamengrad, Sanski Most Gypsum Upper Permian evaporites Gypsum ⁎ 42 Gornja Sanica, Ključ Gypsum Upper Permian evaporites Gypsum ⁎ 43 Mrkonjić Grad Gypsum Upper Permian evaporites Gypsum ⁎ 44 Jajce Gypsum Upper Permian evaporites Gypsum ⁎ 45 Elezovići, Donji Vakuf Gypsum Upper Permian evaporites Gypsum ⁎ 46 Bistrica, Gornji Vakuf Gypsum Upper Permian evaporites Gypsum ⁎ 47 Prozor Gypsum Upper Permian evaporites Gypsum ⁎ 48 Visoko Gypsum Upper Permian evaporites Gypsum ⁎ 49 Glamoč Gypsum Upper Permian evaporites Gypsum ⁎ 50 Rude Gypsum Upper Permian evaporites Gypsum ⁎⁎ Advanced Tethyan rifting (ATR) 51 Topla, Karavanke Mt. Pb–Zn MVT Anisian carbonates Sphalerite ⁎⁎⁎ 52 Mežice, Karavanke Mt. Pb–Zn MVT Ladinian–Carnian carbonates Galena, sphalerite ⁎⁎⁎ 53 Sv. Jakob, Medvednica Mt. Pb–Zn MVT Triassic? dolostones Galena ⁎ 54 Ivanščica Mt. Pb–Zn MVT Middle Triassic carbonates Galena ⁎ 55 Svinica, Petrova gora Mt. Pb–Zn MVT Middle Triassic carbonates Galena ⁎ 56 Srb, Lika region Pb–Zn MVT Middle Triassic carbonates Galena o.e. 57 Olovo, Central Bosnia Pb–Zn MVT Middle Triassic carbonates Cerussite, smithsonite ⁎⁎ 58 Vareš, Central Bosnia Fe–Ba–Pb–Zn SEDEX Mid-Triassic sediments Siderite, hematite, barite, pyrite ⁎⁎⁎ 59 Srednje, Central Bosnia Pb–Zn–Ba SEDEX Mid-Triassic dolostones Barite, galena, sphalerite ⁎⁎ 60 Borovica, Central Bosnia Pb–Zn–Ba SEDEX Mid-Triassic dolostones Barite, galena, sphalerite ⁎⁎ 61 Rupice, Central Bosnia Pb–Zn–Ba SEDEX Mid-Triassic sediments Barite, galena, sphalerite ⁎⁎ 62 Veovača, Central Bosnia Pb–Zn–Ba SEDEX Mid-Triassic sediments Barite, galena, sphalerite ⁎⁎⁎ 63 Draževići, Central Bosnia Hg epithermal Werfenian sediments Cinnabar ⁎ 64 Čevljanovići, Central Bosnia Mn SEDEX Mid-Triassic sediments Psilomelane, pyrolusite, braunite ⁎ 65 Bužim, W Bosnia Mn SEDEX Mid-Triassic sediments Pyrolusite, psilomelane, manganite ⁎ 66 Ivanščica Mt. Mn SEDEX Mid-Triassic sediments Psilomelane, pyrolusite o.e. 67 Idrija, Slovenia Hg SEDEX, epithermal Carboniferous–Triassic Cinnabar ⁎⁎⁎⁎ sediments 68 Tršće, Gorski kotar region Hg epithermal Permian–Mid-Triassic Cinnabar o.e. sediments Jurassic–Early 69 Ozren Mt., N Bosnia Chromite, magnesite Jurassic ophiolites Chromite ⁎ Cretaceous oceanization 70 Borja Mt., N Bosnia Chromite Jurassic ophiolites Chromite ⁎ 71 Krivaja–Konjuh Mt., Magnesite Jurassic ophiolites Magnesite ⁎ Central Bosnia 72 Banja Luka–Prnjavor, N Bosnia Magnesite Jurassic ophiolites Magnesite ⁎ 73 Kozara–Pastirevo, NW Bosnia Magnesite Jurassic ophiolites Magnesite ⁎ 74 Zlatibor–Varda, N Bosnia Magnesite Jurassic ophiolites Magnesite ⁎ 75 Mušići, Ozren Mt. Talc Jurassic ophiolites Talc ⁎ 76 Žarkovac, Ozren Mt. Talc Jurassic ophiolites Talc ⁎ 77 Bosansko Petrovo Selo, Ozren Mt. Chrysotile asbestos Jurassic ophiolites Asbestos ⁎⁎⁎

(continued(continued on next page) 508 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520

Table 2 (continued) Geodynamic environment No./deposit Mineralization Host rock Ore/industrial minerals Size Jurassic–Early 78 Ribnica, Maglajac, Kamenac, Cu Cyprus-type Jurassic ophiolites Pyrrothite, pentlandite ⁎ Cretaceous oceanization Krivaja vally 79 Čavka Mt. Cu Cyprus-type Jurassic ophiolites Pyrrothite, pentlandite ⁎ Eocene syn-collision 80 Motajica Mt. Kaolin, pegmatites, Eocene granites Quartz, feldspar, muscovite ⁎ aplites, greisens Oligocene–Miocene 81 Srebrenica, Central Bosnia Pb–Zn–Ag mesothermal Rhyolite–dacite volcanics Sphalerite, galena, pyrrothite, ⁎⁎⁎ post-collision pyrite, arsenopyrite 82 Zajača, Boranja Mt., W Serbia Sb mesothermal granitoids Stibnite, Sb-oxides ⁎⁎⁎ 83 Stolice, Boranja Mt., W Serbia Sb mesothermal granitoids Stibnite, Sb-oxides ⁎⁎⁎ 84 Krupanj, Boranja Mt., W Serbia Sb mesothermal granitoids Stibnite, Sb-oxides ⁎⁎⁎ 85 Cer Mt, W Serbia Pegmatite, greisen granodiorites Feldspar, mica ⁎ 86 Tuzla Rock-salt Miocene evaporites Halite ⁎ 87 Lješani, Bosanski Novi Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 88 Babići, Jajce Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 89 Tešani Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 90 Gračanica Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 91 Zvornik Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 92 Poljanska Luka Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 93 Bednja–Šaša Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 94 G. Jelenska Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ 95 Divoselo Bentonite Middle Miocene pyroclastics Montmorilonite ⁎ Deposits related to subaerial 96 Vrace, Lika region Bauxite Upper Triassic Al-oxy-hydroxides ⁎ weathering 97 Kamnik, NW Slovenia Bauxite Upper Triassic Al-oxy-hydroxides ⁎ 98 Vrsar, Istria Bauxite Malm Al-oxy-hydroxides ⁎ 99 Rovinj, Istria Bauxite Malm Al-oxy-hydroxides ⁎ 100 Grmeč Mt, W Bosnia Bauxite Malm Al-oxy-hydroxides ⁎ 101 Hrušica, Slovenia Bauxite Malm Al-oxy-hydroxides ⁎ 102 Žužemberk, Slovenia Bauxite Malm Al-oxy-hydroxides ⁎ 103 Kijak, Dinara Mt., Dalmatia Bauxite Lower Cretaceous Al-oxy-hydroxides ⁎ 104 Vlasenica, NE Bosnia Bauxite Late Lower Cretaceous Al-oxy-hydroxides ⁎⁎⁎ 105 Nikšić, Montenegro Bauxite Lower Upper Cretaceous Al-oxy-hydroxides ⁎⁎⁎ 106 Kordun, Central Croatia Bauxite Senonian Al-oxy-hydroxides ⁎ 107 Bosanska Krupa, Grmeč Mt. Bauxite Senonian Al-oxy-hydroxides ⁎ 108 Jajce, W Bosnia Bauxite Senonian Al-oxy-hydroxides ⁎⁎⁎ 109 Istria Bauxite Early Paleogene Al-oxy-hydroxides ⁎⁎⁎ 110 North Adriatic islands Bauxite Early Paleogene Al-oxy-hydroxides ⁎⁎⁎ 111 Dalmatia, Herzegovina Bauxite Early Paleogene Al-oxy-hydroxides ⁎⁎⁎ 112 Obrovac, Dalmatia Bauxite Late Paleogene Al-oxy-hydroxides ⁎⁎ 113 Drniš, Dalmatia Bauxite Late Paleogene Al-oxy-hydroxides ⁎ 114 Sinj, Dalmatia Bauxite Late Paleogene Al-oxy-hydroxides ⁎ 115 Imotski, Dalmatia Bauxite Late Paleogene Al-oxy-hydroxides ⁎ 116 Central and NW Slovenia Bauxite Oligocene Al-oxy-hydroxides ⁎ 117 Barači, C Bosnia Bauxite Miocene Al-oxy-hydroxides ⁎ 118 Ozren Mt. Ni laterite Lower Cretaceous Ni-clay o.e. 119 Brezik, Tadići, Konjuh Mt. Ni–Co laterite Lower Cretaceous Ni-clay o.e. 120 Gornje Orešje, Medvednica Ni laterite Lower Cretaceous Ni-clay o.e.

⁎⁎⁎ Large, ⁎⁎ medium, ⁎ small, o.e. in exploration.

2.2.1. Permian early intra-continental rifting deposits (EIR) evaporitic pond–lagoon by sedimentation of gypsum–anhydrite, The EIR stage includes deposits related to the incipient thermal events hematite, siderite and barite. Laterally, epigenetic, epithermal barite– of early intra-continental rifting. The latter took place in the Variscan galena veins intersect Upper Permian coarse-grained sandstones. The basement of Pangea. Incipient magmatism caused by thermal doming and deposit is covered by Lower Triassic variegated clastics (Šinkovec, thinning of the continental crust generated numerous hydrothermal cells 1971). The manganiferous gypsum-anhydrite has δ34S between +9 and in the thick piles of the post-Variscan overstep successions. The most +12‰. Vein galena and cogenetic barite (+3‰ and +11.6‰, respec- widespread deposits linked with the EIR are siderite (±ankerite)–barite– tively) were precipitated out of equilibrium, but show a contribution of polysulphide deposits. Stratabound ores occur as lenticular, irregular, Permian seawater affected by evaporation (high Br/Cl ratio in leaches). replacement bodies within limestones and dolostones, or vein-like ones, This infers a Permian age for the deposit. Fluid inclusion studies on intercalated in dark Carboniferous shales and siltites. The siderite–ankerite quartz from the epigenetic veins revealed a NaCl–CaCl2–H2O composi- mineralisation is accompanied by numerous epigenetic barite (±fluorite, tion, salinity between 6.7 and 18.9 wt.% NaCl equiv., and variable TH sulphide) deposits. All deposits are spatially linked with the post-Variscan between 130 and 170 °C. Some measurements, however, record TH at sedimentary complex (flysch-type) constrained by two unconformities, much higher temperature around 260 °C (Palinkaš et al., 2000b). the older Lower Carboniferous unconformity and the younger one related Ljubija hydrothermal-metasomatic Fe–Ba–Pb–Zn deposits. The Lju- to the mid-Permian rift event. bija deposits are located within the Sana–Una, non-metamorphosed Stratabound hydrothermal and stratiform (SEDEX) Fe, Cu, Pb, Zn, Ba Middle Carboniferous formations (interpreted as wild flysch by Grubić deposits. No. 11 Rude, Samobor, epi-mesothermal and stratiform et al., 2000), in the Pannonian Nappe. Siderite–barite–polysulphide SEDEX Fe, Cu, Pb, Zn, Ba deposit is placed in the Sava nappe, at the ore in the Ljubija district occurs as: (1) siderite–ankerite replace- westernmost part of the Zagorje–Mid-Transdanubian zone. It consists ment bodies in limestones and dolostones (±galena and sphalerite); of two ore types, an epigenetic, hydrothermal vein-type beneath a (2) open-space siderite fillings (veins) with quartz and accessory stratiform, SEDEX type (Fig. 4). Epigenetic, epi-mesothermal, quartz– chalcopyrite and pyrite in slates; (3) barite–fluorite veins in dolo- siderite veins with chalcopyrite, galena, sphalerite and barite, cross- stones; (4) barite veins; and (5) secondary limonitic ore as iron hats cut Middle–Upper Permian clastic rocks. The epigenetic part of the over siderite–ankerite bodies or as redeposited ferruginous sediments deposit is a feeder zone of the SEDEX, stratiform ore lenses formed in an (locally named Brand). The major siderite ore deposits are no. 12 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 509

Fig. 4. Cross-section of the Rude deposit (modified after Šinkovec, 1971).

Adamuša, Brdo, Atlijina Kosa, no. 13 Tomašica and no. 14 Omarska. The sulphosalts — no. 21 Tomašica deposit; and (6) epithermal barite veins largest barite–fluorite deposit is no. 15 Žune (Dolinac) and the largest (Jurković, 1962). Fluid inclusion characteristics include temperature of barite deposit is no. 16. Vidrenjak. The replacement ore is represented homogenization (TH) between 90 and 250 °C and salinity in a narrow by two distinctive textures, dark massive siderite and ankerite, and a range between 8 and 11 wt.% NaCl equiv. The fluid chemistry is 2+ ‘zebra’-like texture with rhythmic bedding of light sparry siderite and dominantly NaCl–H2O, although leaches show a contribution of Ca , dark fine-grained siderite. Micro-caverns in the light sideritic laminae and evaporitic trend on the Cl/Br vs. Na/Br plot. The δ34S value of are partly filled by quartz, galena, sphalerite and the alteration barite is between +8.7 and +10.2‰ (Permian seawater), and in phyllosilicate cookeite. Fluid inclusion data in quartz show moderately sulphides between −3.2 and +2.7‰ (Palinkaš et al., 2003). Mining hot ore-forming fluids (TH, 100 to 275 °C), low to high salinity (2 to activity goes back in Roman times. Medieval mining from the 13th to

39 wt.% NaCl equiv.) fluids, and a H2O–NaCl–KCl–CaCl2 fluid che- 15th Centuries was performed by Saxons, followed by Croatian feudal mistry. Fluid inclusion leachates from siderite and quartz plot along nobility (argentiferous galena, around 1000 kg of extracted silver). The the evaporation line in the Cl/Br vs. Na/Br scatterplot (Palinkaš et al., Turkish invasion at the end of the 16th century stopped production. In 2003; BorojevićŠoštarić,2004). The δ34S values of barite lie between Austrian times, copper and iron were the major commodities. Iron +8.5 and +14.5‰. Fluorite from the Žune barite–fluorite deposit mining continued until the mid-1950s. formed in the two-phase region of the hydrothermal convective cell, Petrova Gora epi-mesothermal Ba, Fe deposits. Petrova Gora is a part and that from Ljubija in its lower margin. The depth of formation, as of the Pannonian nappe. Mineralisation is placed within a zone 13 km determined from boiling PTX parameters, is between 200 and 500 m, in length and 4 km wide. There are three types of veins: (1) epithermal depending on whether lithostatic or hydrostatic pressure has been barite veins thick up to 3 m — no. 22 Kijak; (2) mesothermal quartz– applied (Palinkaš, 1988). The annual production of siderite in the siderite veins; (3) mesothermal quartz–sulphide veins — no. 23 period before 1990 (the onset of political turbulence in Bosnia and Gejkovac (Jurković, 1993). The host rocks are coarse-grained Upper Herzegovina) was 4.7 million t/year. Total reserves estimated at more Palaeozoic molasse-type clastic sediments, (quartzite and oligomict than billion tons (Cvijić,2001). conglomerates, equivalents of Permian Trogkofel strata of Alps) Trgovska Gora, epi-mesothermal Fe–Cu–Zn–Pb–Ba deposits. The overlain by red Upper Permian clastics. Fluid inclusion data for ore

Palaeozoic terrain of Trgovska Gora is composed of Lower Devonian quartz give temperatures of homogenization (TH) between 100 and shales, siltites, sandstones, interpreted as turbidites. The same flysch 200 °C, salinity values between 12 and 26 wt.% NaCl equiv. and a NaCl– facies continues into the Carboniferous, with gradually increasing CaCl2–H2O composition. The Cl/Br vs. Na/Br plot shows an evaporation detrital grain size of greywacke and subgreywacke with interbedded trend. The δ34S in barite varies between +5.5 and +11.4‰ (Palinkaš subordinate carbonates (limestones and dolostones). The uppermost et al., 2003). The red sandstone hosting no. 24 Bukovica deposit part of the formation belongs to the Lower Permian, overlain by contains SEDEX hematite beds and lenses (Jurković, 1962). transgressive, coarse-grained Val Gardena sanstones (Jurković, 1993). Mineralization occurs as morphologically different ore types: strata- 2.2.1.1. Deposits related to terresrial and peri-tidal environments. Epi- bound, replacement bodies within limestones and dolostones, genetic, sedimentary uranium deposit. No. 25 Žirovski Vrh. Žirovski Vrh epigenetic veins, imbedded veins and lenticular stocks. Parageneti- is an epigenetic, sedimentary, “red bed”-type uranium deposit, placed cally these occur as: (1) metasomatic ankerites — no. 17 Žirovac in the 1750 m-thick Middle Permian, Val Gardena Formation of the deposit; (2) epi-mesothermal siderite veins — no. 18 Gvozdansko Sava nappe. The sequence lies uncomfortably on Permo-Carboniferous deposit; (3) epi-mesothermal siderite veins with chalcopyrite — strata and underlies Upper Permian dolostones and limestones of the no. 19 Gradski potok deposit; (4) epi-mesothermal siderite veins with Žažar Formation (Skaberne, 2002). It consists of grey, grey-green and galena — no. 20 Majdan deposit; (5) mesothermal siderite veins with red clastics deposited in fluvial, flood plain and tidal-flat environ- chalcopyrite, galena, pyrite, accessory nickel and cobalt sulphides and ments. The peneconcordant, lenticular uranium orebodies are placed 510 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 within grey-green clastic rocks with intercalations of red varieties. The is close to seawater (Palinkaš et al., 1993). The barite was mined major uranium minerals are pitchblende and coffinite cementing exclusively by washing out from the secondary limonite. detrital grains. These are accompanied by pyrite, and accessories like Evaporites. The Upper Permian sediments of the Central Dinarides galena, sphalerite, chalcopyrite, arsenopyrite, and tennantite (Drove- were formed at the margins of epeiric marine basins with general nik et al., 1980). The deposit is formed within braided river sediments regressive tendency and persistant coastal seaward progradation. The by precipitation from oxidizing bicarbonate–sulphate underground formation is promoted by general thermal uplift of Pangea, and waters. The precipitation proceeded at an organic-rich hydrogen- development of rifts. The evaporitization progressed in the three main sulphate geochemical barrier by activity of desulphurizing bacteria peri-tidal facies: (1) carbonate; (2) evaporites with early-diagenetic 34 (Palinkaš, 1986). The δ S value of sulphides attains almost −37‰. The dolomites; and (3) clastics-carbonates (carbonate cavity breccia, deposit was discovered in 1960; known reserves reach 16,000 t U3O8. rauhwacke; Tišljar, 1992). Evaporitic facies produced gypsum, origi- Diagenetic, sedimentary copper deposit (Kupferschiefer-type). No. 26 nated by hydration of syn-sedimentary anhydrite. The carbonate Škofje. The Val Gardena formation with red, green, and grey siltstones, cavity breccias, usually overlying the gypsum and anhydrite layers, are sandstones and shales, close to the Upper Permian transgressive, interpreted as terrestrial features, a weathering crust of tectonically dolostone–limestones (Žažar Formation) incorporates copper occur- disrupted evaporites. The Central Dinaridic evaporates are comparable rences. The dark-grey sandstone, 15 m thick, is the major ore-bearing with evaporates from the Bellerophon Formation in the Southern Alps. horizon. The mineralisation occurs along the belt of 90 km, eastward δ34S values of the evaporates are mostly between +9‰ and +12.5‰ from the Cerkno area. It contains bornite–chalcopyrite–chalcocite– (Jurković and Šiftar, 1995). pyrite minerals as a part of the sandstone cement. The δ34S values Gypsum-anhydrite evaporate deposits. Such deposits are exposed: show depletion on 34Supto−38‰ and wide variations reaching 40‰, (1) along the prominent Neogene, Una–Dalmatia fault zone, which pointing to a bacteriogenic origin for sulphur (Drovenik et al., 1980). extends from Bihač to Knin [no. 30 Bosanski Novi (W Bosnia), no. 31 The position of the mineralisation at the boundary between Val Derviši, no. 32 Petkovac, no. 33 Bosanska Krupa, no. 34 Kulen Vakuf Gardena dark-grey, peri-tidal clastics and overlying trangressive Žažar (along the Una river), no. 35 Martin Brod, Desnica, no. 36 Kaldrma, dolostones suggests a sedimentary, early diagenetic–epigenetic origin, (Srb, Lika region), no. 37 Knin, no. 38 Drniš, no. 39 Vrlika and no. 40 resembling Kupferschiefer-style mineralisation. Sinj, Karakašica (Dalmatia)]; (2) Central Bosnia–Herzegovina evapori- Early-diagenetic, sabkha-type barite deposits. The barite mineralisa- tic zone, from Bosanska Krupa (W Bosnia) [no. 41 Sanski Most, tion in Gorski Kotar has a stratabound character, placed at the contact Kamengrad, no. 42 Ključ, Gornja Sanica, no. 43 Mrkonjić Grad, no. 44 Permian clastics–Lower Triassic dolostones. It is composed exclusively Jajce, no. 45 Donji Vakuf, Elezovići, no. 46 Gornji Vakuf, Bistrica, no. 47 of barite and pyrite, separated into two juxtaposed horizons, pyrite in Prozor and no. 48 Visoko, to Foča area (E Bosnia and N Montenegro)]; the clastics and barite in the dolostones (Fig. 5). The deposits stretch (3) SW Bosnia–Herzegovina, from no. 49 Glamoč (Bosnia) to Ravni for tens of km along the P/T stratigraphic boundary. In 50 years of Kotari (Dalmatia); and (4) Adriatic islands (Olib and Vis). Deposit no. production that terminated in 1988, excavated ore was close to 50 (Rude) is situated on the westernmost part of the Zagorje–Mid- 700,000 t in total. The richest accumulations are in the no. 27 Lokve, Transdanubian zone. There are more than 50 deposits on the territory no. 28 Mrzle Vodice and no. 29 Školski Brijeg deposits. Cryptoalgal of Bosnia and Herzegovina and more than 25 in Croatia. fabrics and other conspicuous sedimentary features, marked by barite cement-like, stromatolitic bioherms and biostromes, club-shaped 2.2.2. Advanced tethyan rifting deposits (ATR) stromatolitic domes, chicken-wire textures, desiccation cracks and Carbonate-hosted, low-temperature, Pb–Zn deposits within the curling of algal mat, etc., constrain a tidal-flat sedimentary environ- carbonate platform formations (Mississippi valley type (MVT)–Bleiberg– ment. The pyrite layer was formed by early, diagenetic, bacteriogenic Mežica type). Carbonate-hosted Pb–Zn deposits are situated in the sulphate reduction in peri-tidal, organic-rich siliciclastic mud. Middle Triassic formations of the External Dinarides, a passive Disseminated barite in the mud was dissolved under these empha- continental margin of Adriatic microplate. The deposits are character- tically reducing conditions. It was subsequently reprecipitated by ized by anomalous modal age of lead (310 to 490 Ma; Palinkaš, 1985), seawater in the overlying, lime-mud layer, and subjected to the very simple Pb–Zn parageneses without Cu, scarce trace element concomitant, widespread process of evaporitic dolomitization. δ34S content and dolomitization as an alteration phenomena. A fluid values of pyrite vary between −15.5 and +20.2‰, and in barite inclusion study revealed the dominance of Ca2+ in ore-bearing fluids, between +17 and +30‰. The composition of fluid inclusions in barite biogenic sulphur in sulphides and low temperature of formation (TH,

Fig. 5. Cross-section of the ore body at Lokve village, Homer locality (modified after Šušnjara and Šinkovec, 1973). L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 511

100 to 200 °C; BorojevićŠoštarić,2004). The geotectonic position in widespread in Dinarides forming a part of the Mid-Triassic volcano- the thick Middle Triassic carbonate successions of the carbonate sedimentary sequences. They are derived from seafloor hydrothermal platform, together with chemistry of fluids and parageneses constrain exhalations in longitudinal throughs formed by advancing Tethyan their origin to deeply seated basinal, connate brines, expelled during rifting. Orebodies lie conformably within tuffs, tuffites, cherts, clastics, Middle Triassic advanced rifting. The position within the carbonate and occasionally limestone and dolostones and the mineralisation is platform, devoted of expressive tectono-magmatic events, explains often interstratified with extrusive submarine volcanics. Emanation of the low temperature of fluids and simple sulphide paragenesis. hydrothermal fluids along rift faults produced differentiated deposi- No. 51 Topla Pb–Zn deposit is situated in the middle part of the tion of “proximal” low-manganese Fe-deposits and “distal” low-iron Anisian carbonate rocks, of the northern Karavanke Alps. The ore is Mn-deposits within the same depositional basin. Local redox condi- characterized by abundant syn-sedimentary structures and textures, tions generated a variety of reducing and oxidizing parageneses, like rhythmic alternation of ore and gangue minerals. Framboidal including pyrite, cinnabar, base metal sulphides and sulphosalts, pyrite, marcasite and sphalerite were formed during early diagenetic barite, siderite, hematite and Mn-oxides. Feeder zones of the strati- stage. δ34S values in sulphides vary between +8 and −24‰ appro- form SEDEX mineralisations occasionally attain a respectable size, as priating to biogenically reduced sulphates (Drovenik et al., 1980). in the Idrija mercury deposit. No. 52 Mežica Pb–Zn deposit in Ladinian and partly Carnian Vareš metallogenic district (Central Bosnia). The Vareš metallogenic carbonate rocks of the northern Karavanke Alps is the most important province is a part of the Durmitor nappe. Advanced rifting magmatism Pb–Zn accumulation. By the volume of metals produced through three produced spilites, ophitic basalts and diabases, and scarce kerato- centuries, it can be ranked among the most important Pb–Zn deposits in phyres, interlayered with Ladinian sedimentary rocks (Pamić, 1984). the Alps. The host rocks are Ladinian formations; Wetterstein Limestone Deposits related to magmatism include cinnabar deposits, Mn-oxide in lagoonal development passing laterally into reef limestones, and deposits, monomineralic and polymetalic barite deposits, and side- Wetterstein Dolomite. The successive Carnian is represented by Rabelj rite–hematite deposits (Ramović et al., 1979). The deposits are placed Shale (Drovenik et al., 1980). The orebodies are both concordant and within a sigmoid-shaped curved belt, 2 to 5 km wide and 25 km long, discordant with irregular shapes and are disposed in the host rocks which stretches from the Srednje–Draževići area in the south to without geological control. This is a stratabound deposit accommodated Vareš–Borovica in the northwest. The zone is built of Lower Triassic in a narrow stratigraphic range within an area of 30 km2; equivalents are shales, sandstones and limestones, Anisian limestones, Ladinian situated at Bleiberg, Austria and Rabelj, on the Italian–Slovenian border. spilites interlayered with pyroclastic rocks, cherts, shales, Fe–Mn Primary ore minerals are galena, botryoidal sphalerite, pyrite and shales, covered in places by Upper Triassic carbonates. marcasite. Wurtzite, arsenopyrite and molybdenite are mineralogical No. 58 Vareš, siderite–hematite SEDEX deposits. The Vareš curiosities. Gangue minerals are calcite and dolomite; fluorite and barite deposits, Smreka, Droškovac and Brezik, are locus typicus mineralisa- are very rare. Wulfenite and secondary Pb–Zn carbonates are more tion of the Mid-Triassic, advanced Tethyan rifting phase (Red Sea frequent in the upper part of the deposit. The δ34S value in Pb–Zn stage). The deposits contain hydrothermal, stratiform siderite– sulphides varies between −1.7 and −21‰ (mean −12‰). hematite–chert beds. The mineralisation form part of the Anisian No. 53 Sv. Jakob, Pb–Zn deposit is situated on Medvednica Mt. in and Ladinian sequences and displays a distinct vertical zoning, the southwestern part of the Zagorje–Mid-Transdanubian zone, and reflecting a gradual change of redox conditions in the depositional is hosted by non-metamorphosed dolostones. The near vicinity of environment. The sequence starts with bituminous, thinly bedded the deposit is at the very contact between the terrain built of shales with pyrite and base metal sulphides, overlain by barite and metamorphic rocks composed of paragreenschists, marbles, and siderite, deposited under reducing conditions. Overlying clastics and orthogreenschists of uncertain age (Silurian–Triassic?) and non- oolithic limestone are suceeded by hematite shale, hematite±chert metamorphosed formations with elements of Mesozoic carbonate beds, deposited in oxidizing environment (Fig. 6). Major minerals are platform. This setting suggests a Triassic age for the host dolostone rocks and mineralisation. The vein-type mineralisation has simple paragenesis: galena, minor sphalerite and pyrite, and quartz and calcite gangue (Šinkovec et al., 1988). Pb isotopes are anomalous, B- type (Doe and Zartman model, 490 Ma; Palinkaš, 1985). Fluid inclu- sions in quartz show the following characteristics: NaCl–CaCl2–H2O composition, 6 to 19 wt.% NaCl equiv., temperature of homogenization 34 (TH, 80 to 230 °C, mean 130 °C). δ S values of sulphides, galena and sphalerite vary between +7 and +10‰ (BorojevićŠoštarić,2004). Pb–Zn occurrences in Middle Triassic carbonates, which have been mined historically, also include no. 54 Ivanščica Mt. deposit in the Zagorje–Mid-Transdanubian zone (Šinkovec et al., 2000), no. 55 Svinica deposit on the eastern slopes of Petrova Gora and the Srb deposit no. 56 in the Lika region. All of these are positioned within units that can be affiliated to the Mesozoic carbonate platform, or External Dinarides. No. 57 Olovo Pb–Zn deposit located in Central Bosnia, within the Durmitor nappe, is hosted by Middle Triassic carbonate rocks (dolomite and limestones), mainly of reef facies. The major ore minerals are Pb and Zn carbonates (predominantly cerussite and minor smithsonite). The cerussite–smithsonite orebodies are asso- ciated with (1) karstic cavities, (2) brecciated carbonate rocks with black and light cerussite, and (3) thin fissures in the carbonate host rocks. The galena is finely disseminated, with sporadic traces of pyrite and sphalerite. Middle Triassic sedimentary-exhalative (SEDEX) Fe, Mn, Ba, poly- sulphide and Hg deposits. Volcano-sedimentary or SEDEX deposits are Fig. 6. Cross-section of the Vareš deposit (after Janković, 1967). 512 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 siderite, manganese-rich hematite, barite, pyrite, marcasite, chalco- No. 63 Draževići cinnabar deposit is situated in Werfenian sand- pyrite, galena, sphalerite, tetrahedrite and Pb-sulphosalts. The δ34S stones, shales and black limestones of Lower Triassic age. Cinnabar values of barite vary from +21 to +29‰ (mean +23‰, Triassic occurs as impregnations and veinlets. Richer ore contains 0.3 to seawater), in sharp contrast with the lower values, around +10‰,of 1.4 wt.% Hg, locally over 2.0%. Cinnabar is the main mineral; pyrite, barite in the Permian siderite–barite–polysulphide deposits, formed calcite and marcasite are scarce (Ramović et al., 1979). during early intra-continental Tethyan rifting. The δ34S in pyrite No. 64 Čevljanovići manganese deposit. The mineralized ore zone is −11‰ (Šiftar, 1988). Fluids in the inclusions represent modified is 5 km long. Manganese ore occurs in form of layers, lenticular bodies seawater with salinity values between 2 and 4 wt.% NaCl equiv., a and pockets. Primary ore minerals are psilomelane, pyrolusite,

CaCl2–NaCl–H2O composition and a moderately high temperature of braunite, rodochrosite and hausmanite. The Mn content in primary homogenization in sphalerite and barite (TH, 110 to 230 °C). Molar Na/ ore is low (10 to 20 wt.%), while chert contributes to the high silica

Cl vs. Cl/Br ratios are close to the seawater (Strmić et al., 2001). content (40 wt.% SiO2). Weathering of the primary ore raises Mn Srednje–Borovica–Rupice–VeovačaPb–Zn–Ba ore-bearing dolostones concentration to 45 wt.%. and intra-formational ore-breccias. Mineralized dolostones and dolo- No. 65 Bužim manganese deposit, NW Bosnia, within the Panno- mitized limestones, 60 to 120 m thick, with tiny intercalations of chert nian nappe of the Internal Dinarides, is a stratiform Mn deposit within and shale, carry ore in deposits no. 59 Srednje and no. 60 Borovica. The Middle Triassic volcanogenic-sedimentary formation represented by ore-bearing volcano-sedimentary complex was formed on the flanks variegated argillaceous sediments. Ore beds and lenticular orebodies of a longitudinal graben-horst structure. Lage, destabilized masses of are interstratified with tuffites and clayey layers. Ore minerals are sediments and ores on the trough slopes initiated gravitational sliding, pyrolusite, psilomelane, manganite, hematite, goethite, braunite, pyrite intra-formational slumping and brecciation, which created massive, and marcasite. irregular orebodies, and/or ore breccia. The major minerals are barite, No. 66 Mt. Ivanščica manganese occurrence. The ore occurrences galena and sphalerite, minor are gel-pyrite and marcasite; accessory are placed within the southwestermost part of the Zagorje–Mid- minerals are arsenopyrite, chalcopyrite, bournonite, tetrahedrite, Transdanubian zone. The deposit consists of small bedded occur- stibnite and cinnabar. Some of the orebodies, 0.5 to 4 m in thickness, rences in Middle Triassic cherts and shales. The major minerals are contain 5 to 10 wt.% Pb+Zn, and 1 to 20 wt.% barite. psilomelane and pyrolusite (Jurković, 1962). No. 61 Rupice deposit consists of massive ore bodies 1 to 20 m No. 67 Idrija mercury deposit. The deposit is the second largest thick, consisting mainly of iron sulfides with 10 to 30 wt.% barite, or mercury deposits in the world, having produced 145,000 t Hg since massive barite bodies (60 to 90 wt.% barite), which contain 1 to 4 wt.% 1490, surpassed only by Almaden, Spain (Mlakar, 1974). Ore grade Zn (Rammelsberg-type). decreased since the early days from 17.0 wt.% Hg to 0.3 wt.% Hg in No. 62 Veovača Pb, Zn, Ba deposit contains ore-breccia or ore- recent times. The Idrija mine stopped production in 1988, and is now conglomerates with dm- to m-sized clasts cemented by barite and Pb– in a conservation stage. The Idrija deposit is placed in the Trnovo Zn sulphides. Microcrystalline dark barite is accompanied with galena nappe, a part of the Sava nappe. It is composed of two types of ores, and sphalerite. The δ34S value of barite from Borovica and Veovača, concordant and discordant. The former is associated with a fault zone (+21‰) is typical for Triassic SEDEX deposits elsewhere in the Dinarides in Permo-Carboniferous to Upper Ladinian formations and occurs as (Šiftar, 1988). veins, open-space fillings, and replacement of carbonate cement in

Fig. 7. Schematic reconstruction of the Middle Triassic through during deposition of the Langobardian sediments (modified after Placer and Čar, 1977). L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 513 clastic rocks. The epigenetic mineralisation is interpreted as a feeder ites, diabases, spilites and younger Tertiary dacites. Podiform chromite zone of the overlying syngenetic, stratiform cinnabar-pyrite beds in bodies are linked to dunites at deposit no. 69 Ozren Mt. the ore the Upper Ladinian organic-rich Sconca Formation, covered by tuff contains between 17 and 37 wt.% Cr2O3. Lesser amount of podiform (Fig. 7). The ore beds are up to 100 m long and 0.5 m thick with the chromite bodies are found on no. 70 Borja Mt. deposit). richest ore containing up to 79 wt.% Hg. Ore minerals are cinnabar, Magnesite deposits. These are placed along the outer rim of the metacinnabar, native mercury, pyrite and scarce barite. The genesis of Ozren Mt. massif at the localities Rječica, Paklenica, Brusnica, Velika the deposit is linked to Ladinian rifting which induced effusive and and Mala Prenja. Their origin is not clarified, but hydrothermal activity explosive bimodal volcanism (tuffs, tuffites, diabases, pillow lavas, associated with Tertiary magmatism seems probable. Magnesite- quartz porphyries). The Idrija failed rift, hosting the mineralisation, bearing areas with deposits of economic interest are also found within was active from Early Scythian to Early Carnian and became an other ultramafic complexes: no. 71 Krivaja–Konjuh, no. 72 Banja isolated basin with stagnant, lacustrine and swamp water (Placer, Luka–Prnjavor, no. 73 Kozara–Pastirevo and no. 74 Zlatibor–Varda. 1982). The Hg-bearing hydrothermal fluids mineralized the trough fill Talc deposits. These are found extensively on the northern flanks of along subvertical faults, pouring out on the swamp floor under Ozren Mt., at no. 75 Mušići and no. 76 Žarkovac. A large talc zone, a few reducing, euxinic conditions. Fluid inclusion data for cinnabar, quartz hundreds to 1000 m in length, and several hundred m wide, is located and barite from the Grubler orebody indicate mineralisation tem- within talcified, silicified and carbonitized serpentinites. Talc is perature between 160 and 220 °C at depth of ~750 m, a low to accompanied by breunnerite (5 to 7 wt.% FeO), which comprises 30 moderate salinity, between 2.1 and 5.8 wt.% NaCl equiv., a CaCl2–NaCl– to 40 wt.% of the total ore mass. The talc ore contains subordinate H2O composition, and a NaCl/CaCl2 ratio between 0.6 to 1.5 (Palinkaš siderite, chlorite (5%), and pyrite (3 to 5%). The talc deposits are et al., 2004). The δ13C and δ18O of carbonates record a fracture- surrounded by magnesite–talc and quartz–magnesite rocks; total controlled hydrothermal system. Large variations in the δ34Sof reserves are estimated at 7 Mt ore. Their close position to dykes of cinnabar, down to the hand-specimen scale, are attributed to different granite–porhyries and syenites of Miocene age suggests a hydro- mixing ratios between magmatic and other sulphur sources (seawater, thermal-metasomatic origin (Pamić and Olujić,1974). evaporites, pyrite and organic sulphur) (Lavrič and Spangenberg, Chrysotile asbestos. No. 77 Bosanko Petrovo Selo, chrysotile 2003). asbestos deposit with 40 Mt of ore (2.5 wt.% asbestos fibre) is the No. 68 Tršće, Gorski Kotar mercury deposit. The Tršće is a mono- largest asbestos deposit in the Dinarides, and is located on the Ozren mineralic, Hg-ore deposit hosted by Permian clastics, sandstones, peridotite massif. The ore is in the form of simple and complex veins, conglomerates and shales, and Lower Triassic dolostones (Šinkovec, veinlets, stringers and reticular vein bodies. 1961). The simple ore paragenesis consists exclusively of cinnabar, Cyprus-type; veins, stockworks and massive sulfide copper deposits. minor pyrite, accessory sphalerite and calcite. Cinnabar replaces Copper mineralization is accommodated in an elongated 80 km long calcitic cement or fills interstices within matrix of the sandstones. zone. This belt is genetically related to gabbros and diabases, asso- Mercury grades rarely pass 0.02%. The mineralization mode of the ciated with ultramafic varieties and can be followed from Konjuh Mt., deposit resembles Idrija in many aspects. It is believed to have formed along the Krivaja river toward Čavka Mt. Copper deposits are found at during advanced Middle Triassic Tethyan rifting. no. 78 Ribnica, Maglajac, Kamenac in the Krivaja river valley, and at more than 30 other localities on no. 79 Čavka Mt. The ore occurs at the 2.2.3. Jurassic–Early Cretaceous oceanization contact between serpentinites, amphibolites and gabbros cross-cut by The ophiolites of the Dinarides are part of a suture zone diabase dykes in two ways: (1) dykes with lenticular bodies of representing the closure of the Tethyan Ocean. This simple inter- pyrrhotite (95 to 97% of ore mass) and pentlandite, surrounded by pretation is correct globally but does not satisfy their complex spatial disseminated and stockwork mineralisation of chalcopyrite, cubanite, distribution, geological structure and petrochemistry, which have led ilmenite, hematite, bravoite and millerite, (crude ore contains 0.6% Cu, to numerous hypotheses on their origin. A simple discrimination is 0.2% Ni, 0.003% Co); and (2) quartz–chalcopyrite veins, veinlets and that there exists a lherzolite belt confined to the Dinarides, sensu stockworks with pyrite, chalcopyrite, arsenopyrite, pyrrhotite and stricto (Dinaridic ophiolites) and a harzburgite–dunite belt placed calcite. Secondary minerals are malachite, azurite, chrysocolle, mostly within the Vardar zone. Some recent interpretations distin- cuprite, native copper, chalcocite, psilomelane etc. (Đurić and Kubat, guish between two dismembered ophiolites belts, the Dinaride 1962). Pyrite–chalcopyrite veins, 0.1 to 0.3 m thick, are located within Ophiolite Zone (DOZ) related to the open-ocean Tethyan realm and the ophiolitic complexes of Mt. Kozara, and Konjuh Mt. The same type the Vardar Ophiolite Zone (VOZ) linked to the associated back-arc of the mineralizations can be followed eastward along the Dinaridic basin (Pamić et al., 2002a). To avoid lengthy discussion for and against ophiolites (Putnik, 1981). such a division, we shall treat the Dinaridic ophiolites and related ore deposits as a unique unit formed by ocean formation in Jurassic–Early 2.2.4. Cretaceous–Paleogene subduction Cretaceous time. The first ophiolite emplacement indicates that the subduction The Dinaridic ophiolites are commonly dismembered or partially stage in NW Dinarides must have started by the end of Late Jurassic. preserved as blocks of basalts, diabases, gabbros, serpentinites and Gradual reduction of the Dinaridic part of the Tethys, accompanied by peridotites. The peridotites and serpentinites form small or large generation of a magmatic arc along the active continental margin, sheet-like bodies (200 to 500 km2 at surface), a few hundred meters to introduced new sedimentary styles in fore-arc and back-arc basins. 2 km in thickness, thrust onto the olistostrome mélange. The Konjuh The trench and slopes were filled with Cretaceous–Paleogene flysch ultramafic massive is underlain by amphibolites with eclogites. sediments, followed by magmatic arc granitoid plutonism and basalt– Gabbros, sheeted diabases, basalt flows and basalt (spilites) pillows rhyolite volcanism. Their products are present in the Požeška Gora, are accompanied in the mélange by greywackes, shales and radio- north of the Neogene Sava depression, as the masses of rhyolites and larites. Amphibolites with peridotites yield K–Ar ages of 160 to 170 Ma basalts. Subduction ceased by the end of Eocene, with the final (Lanphere et al., 1975); lherzolites gave an apparent Sm–Nd isochron emplacement of ophiolites, tectonization of the olistostrome mélange, age of 136 Ma (Lugović et al., 1991). As a rule, however, the number followed by Alpine metamorphism and granite plutonism. and size of ore deposits related to ophiolites diminishes from the From a metallogenic point of view, the Alpine and Dinaridic Hellenides–Albanides toward the Alps. subduction processes were sterile in comparison to those of the Podiform chromites. Ozren, Čavka, Ljubić and Borja Mts., ophiolite- Carpathians and Balkans [e.g., the Late Cretaceous Banatitic Magmatic related deposits. The ophiolites consist of dunites, feldspatic–perido- and Metallogenic belt (BMMB), extending from Apuseni Mts. in tites, harzburgites, lherzolites, olivine gabbros, amphibolites, doler- Romania through the Ridanj–Krepoljin belt of Serbia into Srednogorie, 514 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520

Bulgaria; Mitchell, 1996; Janković, 1997, Karamata et al., 1997a,b]. The 2.2.6. Oligocene–Miocene post-collisional deposits subduction-related calc-alkaline magmatism, with Cu-porphyry and The Eocene collisional phase was followed by Oligocene transpres- skarn type ores (Cioflica et al., 1996; Janković and Jelenković, 1997; sion along the Sava–Vardar zone with strong dextral strike-slip Berza et al., 1998; Peycheva et al., 2001; Ciobanu et al., 2002; Dupont faulting caused by Apulia indentation. The Sava–Vardar Zone (SZV) is et al., 2002; and others), however, could be envisioned along the presumed to be as an extension of the Periadriatic Fault (PF). Before border between the Vardar and Serbomacedonian zone (a part of the the indentation of Apulia, SZV and PF probably represented a huge Dacian block). Subduction of the Vardar ocean below the Tisia and connected structure about 2,000 km in length, i.e., the collisional Dacia crustal blocks caused their suturing in Early/Mid-Cretaceous suture zone between converging Africa and Eurasia (Pamić,2002). time and formation of the Banatitic magmatic belt in the Late Eocene syn-collisional granite plutonism was proceeded by the Lower Cretaceous (Dallmeyer et al., 1999). The Severin ophiolite belt in the Oligocene magmatism producing granitoids and penecontempora- Carpathians, however, spoils a simple reconstruction scenario (Cioflica neous shoshonites with subordinate high-K, calc-alkaline volcanics et al., 1992). The present sinusoidal outline of the Carpathian orogenic (30.4 to 28.5 Ma; Pamić,2002). Magmatic processes were controlled chain and L-shape of the BMMB is a result of post-collisional tectonics by subducted Mesozoic–Lower Paleogene Tethyan oceanic crust, within the sutured Tisia–Dacia block during the Tertiary (Csonzos, probably by a “slab break off” model (von Blankenburg and Davis, 1995; Heinrich and Neubauer, 2002). 1995). Geochronologically, petrologically and geochemically, Lower The syn- and post-collisional granites, andesites and dacites Oligocene plutonism and volcanism corresponds to the Periadriatic in the Eocene and Miocene, however, were highly productive, tonalitic and shoshonitic volcanism in the adjacent Alps (Pamić and producing numerous Pb–Zn–Ag, and Sb, hydrothermal and skarn Palinkaš, 2000; Palinkaš and Pamić,2001). deposits along the northern margin of the Dinarides in Eastern Pb–Zn-polysulphide hydrothermal deposits. No. 81 Srebrenica Pb– Bosnia, Western Serbia and Vardar zone in the Central/Southern Zn-polysulphide hydrothermal deposits. The Srebrenica region com- Serbia. prises Lower and Middle Carboniferous meta-sediments, with inter- calations of limestones, surrounded with Triassic, Jurassic and 2.2.5. Eocene syn-collisional deposits Cretacous formations and large masses of dacitic–andesitic tuffs and Deposits related to the Eocene syn-collisional granites. The geological propylitised dacites. The ore-bearing zone is several km long. The setting of Motajica Mt., and Prosara Mt., N Bosnia, is dominated by richest ore is emplaced in fault breccias and as open-space fillings in Eocene syn-collisional granitoids. Granitoids of Motajica Mt. outcrop veins; replacements and ore impregnations are less frequent. The across an area of 50 km2 that intruded Upper Cretaceous–Paleogene thickness of the veins and vein-stringers is from the cm-scale up to 20 flysch. Prosara Mt. granitoids are in the form of numerous sills and to 25 m. The orebodies are differentiated as: (1) tourmaline veins and dykes which intruded the same sedimentary formation (48.7 Ma K–Ar stockworks, (2) quartz–pyrrhotite–chalcopyrite veins, (3) quartz– age; Pamić and Lanphere, 1991). The intrusives are S-type with pyrhotite–galena–sphalerite veins with accessory stibnite, cubanite, transition to S–I-type granite families classified on the basis of δ18O proustite etc., (4) siderite–marcasite–galena–sphalerite veins, (5) quartz– and 87Sr/86Sr initial values. They were fractionated as monzogranite, stibnite veins, and (6) pyrite–marcasite–löllingite. The mineral paragen- granodiorite, monzodiorite and quartz–diorite (Pamić and Balen, esis comprises sphalerite, galena, pyrrothite, pyrite, arsenopyrite, 2001). marcasite, safflorite, siderite, boulangerite, stibnite, pyrargyrite, enargite, Pegamtites and aplites.No.80MotajicaMt.Basedonthe proustite, quartz and calcite. The ore contains 6.2% Pb and 8% Zn, 80 to classification of Černy (1991), deposits of Motajica Mt. belong to LCT 100 g/t Ag, 1 g/t Au, 0.01 to 0.03% Cd, 0.04 to 0.1% Cu, 0.06 to 0.46% As, 0.5 family (Li, Cs, Ta) with their geochemical signature Be–B–Li–F–Mo– and0.7%Sb.Oreproductionin1990was400,000t.Reserveswere W–Sn–Bi–Cs–Rb–Sr–U–Th–Ta, low-P, Abukuma metamorphic envir- estimated to be 15 Mt (Ramović et al., 1979). The history of mining goes onment, and emplacement in the interior of granites. The paragenesis back to the Roman, Slavic, Saxon, Turkic and Austrian periods. The most comprises quartz as major mineral, with subordinate microcline, recent production period terminated along with the existence of orthoclase, albite, muscovite, beryl and tourmaline; beryl is present in Yugoslavia in 1991. variable quantities. Veins with 10 to 50% beryl (beryllites) occur in Kaolin deposits. Alongside metal-rich deposits, extensive hydro- some parts of the deposit. Accessory minerals are scheelite, pyrrhotite, thermal activity in Srebrenica area developed wide hydrothermal zircon, apatite, magnetite, ilmenite, titanite, molybdenite, epidote, alteration zones within sanidine-dacite and Palaeozoic schists with garnet and rutile. Feldspar and quartz are minerals of economic value huge kaoline deposits. The largest of these was Bratunac, with (Jurković,2004). The greisenisation belt at Motajica Mt. is 2 km long production of 12,000 t annually prior to 1991. and 100 m wide. Greisenisation affected granite, leucogranite and West Serbian antimony deposits. One of the most significant aplitic granite. Pneumatolitic metasomatism includes intense silifica- antimony producing area of Europa relates to granitoids of Boranja tion, muscovitisation and sericitisation of feldspars. Greisens have a Mt., West Serbia of Lower Oligocene age (33.7 to 29.6 Ma; Pamić, simple mineralogy with major minerals: quartz, muscovite and 2002). The antimony-bearing region of Podrinje has a complex sericite. Minor minerals are zircon, apatite, microcline and biotite. geological structure with predominance of Carboniferous, Permian Ore minerals are wolframite, scheelite, fluorite and molybdenite. A and Triassic formations (Jadar Formation) and numerous intrusions of number of hydrothermal ore occurrences appear in the surrounding granodiorites, extrusions of dacitic–andesitic volcanics, and large meta-sediments as galena veins with tetrahedrite, hematite, cerussite, masses of pyroclastics and epiclastics. The ore deposits are located covellite and goethite. around the contact aureoles of the granodiorite massif and show a Kaolin deposits. Numerous kaolin deposits are located around clear zonation outwards. The contact zone with Palaeozoic schists and the granitic pluton: Brusnik, Ciganluk, Grebski potok, Kameni potok, carbonates carries magnetite–chalcopyrite skarns; the next zone is Đidovi, Filipovića Kosa and Babin grob. The deposits are autochto- galena–sphalerite surrounded by the widest zone of stibnite, with nous, hydrothermal, but some might have been formed by subordinate galena–sphalerite, and the outermost is the fluorite zone. kaolinitization of all Motajica granitoid types in very late Neogene– The highest Sb concentrations, in replacement orebodies, are Pleistocene times. The major mineral is kaolinite and minor illite, connected with silicified Upper Carboniferous limestones, under quartz, orthoclase, albite, sericite, magnetite and zircon. Total impermeable Upper Carboniferous clastic rocks. The ore also occurs reserves are 1,570,000 t. The Prosara Mt. granitoid does not bear as veins with developed salbands or as fault breccia with stibnite– any mineral occurence of significant economic value. The shallow calcite cement. The largest deposits are no. 82 Zajača, no. 83 Stolice erosion level of the Prosara granitoids opened only small kaolin deposits, (Fig. 8) and no. 84 Krupanj. Mineral parageneses are simple: occurrences. stibnite, Sb-oxides, galena, sphalerite, pyrite, quartz and calcite. The L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 515

Radeša, Žabljak and Trepče deposits; (4) Gračanica, no. 90 Džombe, Kulić and Stražbe deposits; (5) Zvornik, no. 91 Zvornik deposits. The deposits in Croatia are no. 92 Poljanska Luka, no. 93 Bednja–Šaša, no. 94 Gornja Jelenska, (Moslavačka gora Mt.) and no. 95 Divoselo (Lika region).

2.2.7. Deposits related to subaerial weathering Aerial exposures of geotectonic units of the Dinarides resulted in their synchronous and asynchronous uplift during all tectono- magmatic phases. Tectonic events, which intensively reshaped palaeogeography of the Internal Dinarides, caused less pronounced changes in the monotonous sedimentation on the Mesozoic car- bonate platform. Hiatuses due to epeiric rise and low of the sea levels interrupted marine sedimentation and exposed dry land to karstification and bauxitization. Stratigraphic gaps record dry- land episodes documented by numerous bauxite deposits. Eocene collision and uplift, with concomitant tectonics, severely deformed bedrocks, uncovered new karstification terrains, caused disintegra- tion of the carbonate platform and induced molasse-type sedi- mentation. Weathering of ultramafic rocks produced Ni-laterites in short episodes after their aerial exposure as obducted ultra- mafic sheets or olistostrome mélange in Early Cretaceous time, (see deposits related to sub-areal weathering on Fig. 9; description in Table 2.). Bauxite deposits. Such deposits in the Dinarides occur in the vast region extending from Western and Central Slovenia to Croatia (Istria, Lika, Kordun, Adriatic islands, Dalmatia), through Western Bosnia and Fig. 8. Cross-section of the Stolice deposit (after Janković, 1967). ending in Herzegovina and Montenegro. Bauxites were formed from Middle Triassic to Miocene times. The bauxites of each stratigraphic horizon have clear relation to the overlying and underlying layers, Stolice ore contains: 30.8% Sb, 0.13% As, 0.005% Pb, 0.007% Cu and adefined geotectonic position and a wide geographic extent. Ten 0.001% Zn (Janković, 1990). stratigraphic horizons with bauxite deposits were determined in the Pegmatites and greisens, West Serbia. No. 85 Cer Mt. pegmatites Dinarides on the basis of these criteria (Sokač and Šinkovec, 1991). The and greisens. The granitoid complex of Cer Mt. covers a surface area deposits bordered by the map (Fig. 9) are: (1) Upper Triassic, no. 96 of 70 km2. Ore deposits are incorporated within biotite– and Vrace deposit (Lika region), no. 97 Kamnik, Bohinj deposits, (NW biotite–amphibolite granodiorites (22 to 33 Ma; Knežević et al., Slovenia); (2) Malm, no. 98 Vrsar, no. 99 Rovinj deposits; (Istria), 1994). A deep level of erosion exposed pegmatites and greisens. no. 100 Grmeč Mt. deposits; (W Bosnia), no. 101 Hrušica, no. 102 The pegmatite bodies are small, lenticular, or vein-like, with thick- Žužemberk deposits, (Slovenia); (3) Lower Cretaceous, no. 103 Kijak, ness from 0.2 to 2 m, rarely 4 to 5 m. The major mineral content of Dinara deposits, (Dalmatia); (4) Uppermost Lower Cretaceous, no. 104 the pegmatites is simple: quartz, microcline, albite, plagioclase, Vlasenica deposits, (NE Bosnia); (5) Lower Upper Cretaceous, no. 105 with some muscovite, biotite, beryl, tourmaline, zircon and apatite. Nikšić deposits (Montenegro); (6) Senonian no. 106 Kordun deposits, Accessory minerals are epidote, cassiterite, scheelite, columbite, (Central Croatia), no. 107 Bosanska Krupa, Grmeč Mt., (W Bosnia) no. rutile, uraninite, monazite, sphalerite and chalcopyrite. The Li con- 108 Jajce deposits, (Central Bosnia); (7) Lower Paleogene, no. 109 tent is low (45 ppm). Greisens of the Cer Mt. are of quartz–muscovite Istria, no. 110 North Adriatic islands, no. 111 Dalmatia, Herzegovina and quartz–muscovite–tourmaline–fluorite types. Ore minerals are deposits; (8) UpperPaleogene no. 112 Obrovac, no. 113 Drniš, no. 114 cassiterite, tantalo-niobates, bismuthinite, fluorite and scheelite Sinj, no. 115 Imotski (Dalmatia); (9). Oligocene, no. 116 Central and NW (Janković, 1990). Slovenia deposits; (10) Miocene, Sinj deposit, (Dalmatia), no. 117 Salt (halite). In contrast to the numerous Permian gypsum– Barači deposit, (Central Bosnia), Herzegovina deposits, (out of the map anhydrite ores and occurrences in the Dinarides, the only rock-salt area). deposit is situated in no. 86 Tuzla (N Bosnia). This more or less Nickeliferous laterites. No. 118 Ozren Mt. Ni-laterite crust. A crust stratified salt-dome of Miocene age (Burdigalian–Helvetian), the with nickeliferous silicates 0.3 to 2 m thick is developed in the Ozren largest in the Balkan Penninsula, consists of banded halite, anhydrite, massif. It contains 9 to 34% Fe, 1 to 4% MnO, 0.42 to 0.61% NiO and 0.05 dolomite and marls. Major minerals are halite, thenardite–mirabilite, to 0.15% Co. and accessories are northupite and searlesite (Kniewald et al., 1986; Konjuh Mt., Ni–Co laterite crusts. The serptentinite masses of the Bermanec et al.,1987). Tuzlaite, approved as a new mineral and named Konjuh ophiolitic complex were submitted to intensive weathering to honor the occurrence, was discovered as an accessory mineral in in Early Cretaceous time. The Ni-laterites were subsequently re- the assemblage (Bermanec et al., 1994). deposited, acquiring an oolitic and pseudo-oolitic ore-texture. The Bentonites. In the Dinarides and South Tisia, bentonites are Ni-lateritic crusts at locality no. 119 Brezik–Tadići have bedded, related to Miocene pyroclastics. Bentonite clays consist mostly of lenticular forms and the ore is 12 m thick. The ore contains 0.1% Co montmorillonite (95%) with some accessory quartz, calcite, feldspar, and 0.5% Ni. muscovite and biotite. There are more than 22 deposits in Bosnia No. 120 Gornje Orešje, Medvednica Mt. Ni-laterite crusts. Alpine- and Hercegovina, and 4 in Croatia. The deposits are pyroclastic type peridotites with metamorphic fabrics outcrop as two separate sediments generated during Middle Miocene volcanic activity which blocks, 0.4 km2 in surface area, with transitional characteristics underwent devitrification and chemical alteration by seawater. The between supra-subduction zone peridotite and MORB-type perido- deposits in Bosnia are grouped in the areas: (1) Bosanski Novi, no. 87 tites (Lugović and Slovenec, 2004). The Ni-lateritic crust (0.8% Ni) is Lješani deposit; (2) Jajce, no. 88 Babići deposit; (3) Tešani, no. 89 transgressively covered by Upper Cretaceous rudist limestones. This is 516 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520

Fig. 9. Geological structural scheme of the Dinarides and surrounding area with index-map (modified Tomljenović,2002) and deposits related to subareal weathering (see Table 2 for description) with index-map.

the northernmost Ni-lateritic crust recorded in the Tethyan realm deep wells under the sediments of the Tertiary Pannonian basin. (Alpine–Himalayan domain, Palinkaš et al., 2005). Complete Triassic to Late Jurassic–Early Cretaceous sequences display positive lithostratigraphic correlation with Triassic and Jurassic se- 3. The South Tisia megablock quences of the Carpathians and Eastern Alps (Šikić et al., 1975). Bleahu et al. (1994) concluded that the Triassic formations, including volcanic Palinspastically and palaeographically the South Tisia megablock is rocks, metabasalts and metarhyolites, are allochtonous and originated genetically related to the South Eurasion margin. Crystalline rocks of the along the South Carpathians, i.e., the northern Tethyan margin. Late South Tisian megablock crop out in the Slavonian Mts., Moslavačka Gora Cretaceous formations are accompanied by basalt–rhyolite flows with and rarely in Požeška Gora. The crystalline rocks can be separated into pyroclastics and small bodies of A-granites. The Pannonian Neogene two groups: most belong to the Palaeozoic formations which are sedimentary fill overlies the Palaeozoic and Mesozoic basement. unconformably overlain by subordinate Mesozoic formations (Pamić, 1986). Petrologicaly, they show wide variations and are represented by 3.1. Geodynamics and metallogeny of Tisia regional medium-, low-, and very low-grade metamorphic sequences, migmatites and granitoids (S-type and I-type). Mesozoic formations are Tisia represents a fragment of the Eurasian southern margin. Its less common on the surface than within the subsurface, penetrated by regionally metamorphosed successions, migmatites and granitoids L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 517 originated during the Variscan orogenic cycle. The protolith was a in the Dinarides is, in contrast, marked by elements of ultrabasic or Silurian–Devonian sedimentary package interlayered with basalts of subcrustal affiliation (Fe, Cr, Ni, Mn, Cu and Hg). Development of a tholeiitic affinity, which originated via I-type subduction-related thick ensialic lithosphere during the collision–post-collision phase in plutonism along the active Palaeothetyan margin (Pamić and Balen, the Dinarides, enriched their metallogeny with crustal elements such 2001). The main Variscan deformation occurred during the Early Car- as Pb, Zn and Sb. boniferous. Its products are Barrovian-type metamorphic sequences Southern Tisia, as a part of the European plate, shares only a few (greenschists and amphibolites facies), migmatites and S-type gra- characteristics of the Variscan metallogeny. This fact still requires nites. Simultaneously, pre-kinematic subduction-related I-type gran- proper explanation, especially since quite a significant quantity of ites underwent cataclasis. The Variscan complex of Moslavačka Gora Variscan granites are present in the Slavonian Mts. On the whole, experienced the same history, but was subsequently affected by Variscan magmatism in the Penninic and Austro-Alpine domains, and pervasive deformation during the final phases of the Alpine cycle (Late in Tisia itself, did not produce a significant mineralization (Schulz, Cretaceous–Early Paleogene subduction processes). Andalusite and 1983; Finlow-Bates and Tischler, 1983; Ebner et al., 2000). cordierite schists evidence the Abukuma-type metamorphic se- Low mineralisation potential of the Southern Tisia should be quences (Garašić, 1993; Balen, 1999). The Slavonia and Moslavina sought in the metallogeny of the Variscan area sensu stricu. The pre- Variscan crystalline complexes can be correlated with those in Mecsek Mesozoic metallogeny of the Central European Variscides reflects a Mt. in South Hungary and with those in the basement of the Pan- progressive cratonization of the crust. From the Eo-Variscan stage nonian Basin, as well as other complexes of Variscan Europe (Buda, (Cambrian–Silurian), through the Meso-Variscan stage (Devonian– 1981; Lelkes-Félvary et al., 1996; Jurković and Pamić,2001). Early Carboniferous), to the Neo-Variscan stage — which marks the Southern Tisia, as an ensialic block of Eurasian affinity related to end of collision (Late Carboniferous–Early Permian, 345 to 330 Ma), the active Laurasian margin is not rich in ore deposits. The metal- metallogeny gradually evolved from an “ensimatic” to an “ensialic” logeny of the South Tisia is primarily created by Variscan tectono- character. The Neo-Variscan stage is characterized by extensive em- magmatic processes (deposits are numbered on Fig. 2, description can placement of granites and acid-volcanics, interpreted as resulting be found in Table 1). The rare commodities of economic value in South from post-collisional melting, explained by lithospheric delamination. Tisia are part of metamorphic sequences (e.g., graphite), products of This stage corresponds to the main metallogenetic phase in the his- igneous activity (e.g., pegmatites), and sedimentary-epigenetic ura- tory of the Western European Variscids (Collins, 1994; Marignac and nium occurences. Cuney, 1999). The collision stage facilitated development of Barrovian- type metamorphism and water-rich granitic magmas emplaced at 3.2. Variscan deposits depths which precluded significant hydrothermal activity. High heat flow is linked, however, with lithospheric delamination and mantle Graphite deposits. Meta-sediments and graphitic slates from the uprise during orogenic collapse. Those terranes, like Southern Tisia, Barrovian metamorphic sequence in the Psunj Mt. incorporate layers did not experience high stacking of nappes during collision, and of graphite and meta-anthracite, which originated by regional thermal afterwards relaxation and delamination. For that reason Southern metamorphism of coal (Šinkovec and Krkalo, 1994). Ore deposits are Tisia the mineralizing potential became diminished. Southern Tisia no. 121 Kaptol, Sivornica and Brusnik. Total production was about may also owe the scarcity of ore deposits to the deep post-Variscan 22,000 t of ore with 45 to 70% C; reserves are assessed at 60,000 t. The erosion. reserves of ore with low C content can be exploited by flotation; these Rearrangement of the present interfingering collage of microplates reserves, although not assessed, are considered to be large. (Alcapa, Tisia and Dacia) into a Tertiary paleogeography, (Csontos and Pegmatites. No. 122 Papuk Mt. Numerous irregular veins, lenses and Vörös, 2004), gives a plausible solution for the uncertain position of irregular bodies of migmatitic pegmatites cross-cut gneisses, migma- the subduction on the northern margin of the Central Dinarides and tites, and S-type granites in Papuk Mt. The largest pegmatite body is South Tisia. Đukina Kosa; feldspars and muscovite are major minerals. Juvenile Interpretation of Dinaride geology leans on the Alpine Wilson cycle pegmatitic veins, skarns and hydrothermal sulphide veins occur model, which has been gradually upgraded from the early days of within I-type granite. The Barrovian sequence, in its low-grade meta- Peri-Adriatic plate tectonics. A great number of studies of classical morphic part, contains numerous monomineral quartz lenses and outcrop areas, radiometric fission-track dating, paleomagnetic data, veins of syn-kinematic and post-kinematic secretional origin, known paleoclimate reconstruction and palinspastic restoration, have pro- as Alpine-type veins (Jurković, 1962). vided valuable information for understanding the geological evolu- Sedimentary uranium deposit. No. 123 Ninkovačacreek.The tion of the Dinarides and peri-Adriatic orogens (Dimitrijević,1974; Radlovac low-metamorphic series (within the chlorite–sericite– Laubscher, 1975, Laubscher and Bernoulli, 1977; Channell et al., 1979; chloritoid facies), Papuk Mt., contains low-concentration uranium Kovács, 1992; Pamić et al., 1998; Csontos and Vörös, 2004; and others). ore (0.0445% U308); estimated reserves are 15 t U3O8. The epigenetic, The Central Dinarides is one of the best preserved segments of the sedimentary uranium mineralization is placed in the terrestrial part Mesozoic Tethys, with a relatively simple geodynamic history in of the regressive series, marine–sabkha–dry land facies (Devonian?). comparison to the more complex terrains in its neighborhood. It is The primary mineral is coffinite; secondary autinite, uranospathite, considered as a “closed system”, bound to the NW by the Zagreb– uranosilite and heyite are also recorded (Braun et al., 1983). Permian Zemplin fault and to the SE by Golija and Drina–Ivanjica units sediments of the Radlovac Formation do not carry uranium miner- (Dimitrijević, 1982; Pamić and Tomljenović, 1998; Herak, 1996). The alisation — likewise their equivalents in the Mecsek Mt., Hungary. sheltered position of the Central Dinarides is due to the north- Deposits formed during the Alpine cycle are unknown in the South westward indentation of the Adria– (Apulia) block and the westward Tisia mega-unit. indentation of the Moesian block, producing strike-slip faulting along the Periadriatic–Sava–Vardar zone (sensu Pamić et al., 2002b). Due to 4. Concluding remarks the oblique continent–continent collision, the Dinarides and Hele- nides suffered much less shortening in comparison with the Alps and The identity and specialisation of the Variscan and Alpine metal- South Carpathian–Balkans. The result was the array of tectonostrati- logenies differs greatly due to marked differences in their metallo- graphic units from the passive continental margin of Adria toward the tects, in respect to the budget and source of elements. Tin, tungsten, active margin along Southern Tisia, which comprises characteristic ore the so-called “five-element association” and uranium are marker deposits, each with preserved morphologies, textures, structures and elements of the “ensialic” Variscan metallogeny. Alpine metallogeny mineral parageneses. These genetic prototypes might be used as 518 L.A. Palinkaš et al. / Ore Geology Reviews 34 (2008) 501–520 standards for discrimination of ore deposits in the neighboring The plate tectonic evolution of the Dinarides is a necessary basis for geotectonic units which underwent substantially higher-grade meta- the interpretation of metallogeny, but proper ore deposit genetic morphism and associated tectonic defomation. models also represent a beneficial contribution to the upgrading of the The geodynamic evolution of the Dinarides remains, however, a plate tectonic model itself. source of controversy and continued research. The title of the article by Channell and Kozur (1997) “How many oceans? Meliata, Vardar, Acknowledgments and Pindos oceans in Mesozoic Alpine paleogeography”, or just the single one (“Vardar–Meliata–Hallstatt”) referred to by Kovacs (1984) We express our sincere gratitude to Franz Neubauer and an and Haas et al. (1995), demonstrates the problems, both spatial and anonymous reviewer for their valuable suggestions which helped us temporal, that make definition of the early intra-continental rifting in to organize the text and made the paper more transparent. Thanks Tethys in the Permian or Triassic so difficult. Two oceans, the Vardar go to Nigel Cook, whose advice helped us clarify the goals of this and the Dinaridic, are attested to by the presence of three ophiolitic contribution. Our gratitude is also assigned to the Ministry of Sciences, suture zones (Dinaridic, Western Vardar and Central Vardar ophiolitic Republic of Croatia, whose financial support of the project No. 119/ zones) but do not resolve whether oceanization took place in Triassic 098709-1175 enabled preparation of the manuscript. or Jurassic time? Was the Dinaridic ocean the main realm of the Tethys – and the Vardar ocean just an arm of back-arc origin? – or was References the situation vice versa? Was subduction directed towards SW in respect to Adria or Tisia? – or was it directed towards NE? Did a Balen, D., 1999. Metamorphic reactions in amphibolites from Mt. Moslavačka Gora. subduction slab sink beneath Tisia or the Serbomacedonian con- Unpublished Ph.D. Thesis, University of Zagreb, 264 pp. (in Croatian). š – Balogh, K., Palinka , A.L., Bermanec, V., 1999. Alpine retrogressive metamorphism dated tinental block? or even both? Is the Peri-Adriatic lineament the real by K/Ar and Ar/Ar methods on Hylophane, Central Bosnia. 77th Jahrestatung der boundary between African and European tectonic elements stretched Deutschen Mineralogischen Gesellschaft, Wien, vol. 11 (1), p. 24. along Lake Balaton (Hungary) or along the Sava–Vardar strike-slip Belak, M., Pamić, J., Kolar-Jurkovšek, T., Pecskay, Z., Karan, D., 1995. Alpine low-grade regional metamorphic complex of Mt. Medvednica, northwest Croatia. In: Vlahović, zone? The list of open questions is extensive and little concensus I., Velić, I., Šparica, M. (Eds.), Proceedings of 1st Croatian Geological Congress, about the basic interpretative facts has been acheived (e.g., Stampfli Opatija. Geological Survey of Croatia, Zagreb, pp. 67–70 (in Croatian). et al., 1991; Pamić, 1993; Robertson and Karamata, 1994; Dimitrijević, Bermanec, V., Zebec, V., Brajković, Z., 1987. Searlesite from the salt mine Tušanj, Tuzla, ć Š ć ć Yugoslavia. Geološki vjesnik 40, 75–80. 2000; Karamata et al., 2000; Resimi - ari et al., 2000; Pami , 2002; Bermanec, V., Ambruster, T., Tibljaš, D., Sturman, D., Kniewald, B., 1994. Tuzlaite, NaCa ć Pami and Slovenec, 2002; and others). The literature contains a large [B5O8(OH)2]·3H2O, a new mineral with pentaborate sheet structure from the Tuzla number of alternative rearrangements of microplates, and opening salt mine, Bosnia and Hercegovina. American Mineralogist 79, 562–569. and closure of microoceans, and underlines the efforts being made to Berza, T., Constantinescu, E., Vlad, S.N., 1998. Upper Cretaceous magmatic series and associated mineralization in the Carpatho-Balkan orogen. Resource Geology 48, address the problems, but extensive basic geological research, 291–306. including the study of mineral deposits, are still needed. Bleahu, M., Mantea, Gh., Bordea, S., Panin, St., Stefanescu, M., Šikić, K., Kovács, S., Pero, The present contribution is not just a catalogue of ore deposits in Cs., Haas, J., Berczi-Maak, A., Nagy, E., Konrad, Gy., Rálisch-Felgenhauer, E., Török, A., 1994. Triassic facies types, evolution and palaeogeographic relations of the Tisza space and time. Genetic interpretations for the ore deposits are Megaunit. Acta Geologica Hungarica 37, 187–234. critically supported by new data obtained using the state-of-art BorojevićŠoštarić, S., 2004. Genesis of siderite–barite–polysulphide ore deposits within analytical techniques (fluid inclusion studies, microthermometry, Palaeozoic of Internal Dinarides. Unpublished Masters thesis, University of Zagreb, 120 pp. (in Croatian). Raman spectrometry, ion chromatography, stable isotope geothermo- Braun, K., Dravec, J., Slović, V., Crnogaj, S., Valković, V., Makljanić, J., 1983. Uranium ore metry, geobarometry, radiometric dating, REE, etc.). 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