Journal of Environmental Science and Engineering B9 (2020) 248-260 D doi:10.17265/2162-5263/2020.06.003 DAVID PUBLISHING

Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Vladimir I. Gugushvili Department of Metallogeny, Al. Janelidze Institute of Geology, Iv. Javakhishvili Tbilisi State University, Jikia 16, Tbilisi 0186, Georgia

Abstract: Phanerozoic geodynamic evolution development of Tethys Ocean, its collision and closing, revealed at the Eurasian active margin in pre- and post-collision stages during convergence of Afro-Arabian and Eurasian continents. Subduction of oceanic slab under continental margin revealed in steady state subduction and steepening of subducting slab provoked the incursion of mantle diapir. The steady state subduction is related with island arc setting whereas steepening provoked incursion of mantle diaper interarc-backarc and minor ocean settings. They are controlled by geological indicators—volcagenic, petrochemical, geochemical, tectonic and metallogenic. Each of them is determined by scale of mantle-crustal influence, controlled by intensity and level of mantle diapir incursion in the crust rising from interarc-backarc to minor oceanic setting. The island arc setting is characterized by blocking, which as others by extension of rifting (interarc-backarc) caused spreading out from zone of volcanic activity and mineralization sialic crusts, whereas minor ocean setting caused by spreading out from zone of volcanic activity and mineralization sialic and basaltic crusts. So mantle crustal influence rising from island arc to minor ocean settings controlled type of volcanism and mineralization in pre-collision development. At the closing of ocean occurred the precollision setting which is transferred in post-collision revealed in orogenesis. It is divided in two stages. The first initial stage occurred in penetration hot fluids from the mantle in sialic crust smelted from in granitoid melt and leached the gold and trace melts Sb, W, Mg and Hg from sialic crust. The latter are geochemical indicators of post-collision setting. The second final stage revealed in shoshonite- volcanism activity occurred with penetrated mantle material into deep volcanic chambers and characterized with increasing of mantle influence than initial stage of post-collision activity.

Key words: Pre- and post-collision settings, crustal-mantle sources, geological indicators.

1. Introduction modern plate tectonic with subduction and spreading of oceanic crust and forming ocean and continents. At the Precambrian after cratonization the Earth crust The collision and closing ocean revealed in forming of is divided by sialic, basaltic and rigid upper mantle continental active margin, as evolution of Tethys and Au and base metals—Pb, Zn and Cu which were ocean at Eurasian margin at pre- and post-collision redistributed within them. Au and Pb contained in stages. Our studied region occurred in the Western sialic, Zn—in basaltic, whereas Cu is rested in mantle segment of Eurasian active margin, within Iran, [1]. In Phanerozoic the plume tectonic is alternated by Caucasus, Turkey and Balcan-Carpaths (Fig. 1). We tried to show in geodynamic development exemplified Corresponding author: Vladimir I. Gugushvili, Ph.D., professor, research fields: volcanology, matallogeny, geodynamic. of this (Fig. 1) region based of plate-tectonic data.

Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, 249 Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 1 Map of the Western Tethysides (Stampfli, et al. [2]) . minor ocean, backarc, marginal Volcanic Massive Sulfide mineralization; subduction related with porphyry, epithermal and kuroko type mineralization; postcollision orogenic and intrusive related lode and porphyry mineralization.

2. Material - volcanic activity, where Au-Pb-Zn-Cu porphyry and Kuroko type stratiform mineralization 2.1 Pre-collision Development are related to calc-alkaline volcanic activity [4]. The In the Caucasus the plate-tectonic study was ore forming process here is controlled by blocking beginning in 1974 [3]. Now the region is studied in related to granodiorite intrusive stocks tumiscenced detail. sea bottom and elevated the islands (Uplifted blocks). The precollision stage of geodynamic development On the islands ignibrite volcanic activity was was revealed by steady state subduction and terminated by cauldron-subsidence (subside blocking). steepening of subducting slab. The initial activity of The blocking at Madneuli, so at Tsiteli-Sopeli steady state subduction began by regional deposits both are synvolcanic. The mineralization as metamorphism and granitization at fluid temperature porphyry, so in Kuroko type deposits’ is related to 350-750 °C. The arising temperature up to granodiorite stocks and volcanic chambers and 1,100-1,200 °C smelting from subducting slab sources of ignimbrite explosion terminated by andesitic magma challenged calc-alkaline volcanic cauldron subsidence [4]. activity of island arc setting. So, volcanogenic indicator here is calc-alkaline The Bolnisi Ore District (Fig. 2) is a good example volcanics related to steady state subduction, of island arc setting, where at the Madneuli and Tsiteli metallogenic—Au, Pb, Zn, Cu mineralization leaching Sopeli gold-base metals porphyry deposits occurred in from sialic, basaltic crust and mantle (the slab was

250 Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 2 Geological map of Bolnisi ore district. I Madneuli cluster, II Bectaqari cluster. deepening inmantle). The tectonic indicator is represented by its two stages. The initial-lower blocking the geochemical cryteria are ratias of St and Campanian stage consists of trachyodacitic volcanic Pb isotopes in the ore bearing rock 87Sr/86Sr = suite intensively alternated by gold-bearing k-fieldspar 0.705-0.715, 208Pb/204Pb = 39 [4]. The similar metasomatites and is not subjected by rifting. The geological indicators were determined in the Pontides subalkal volcanism and alkali alteration must be (Turkey) (Fig. 3), Panaguirishte ore district (Bulgaria) related to initial stage of alkali alteration and must be and Timock region (Serbia), related to island related with initial stage of back arc setting, where calc-alkaline volcanism, porphyry and Kuroko type rifting and spreading out sialic crust from zone of mineralization and synvolcanic tectonics [5] (Fig. 4). volcanic activity was not determined. It is the reason In the Bolnisi ore district neighboring to of low sulfidation gold mineralization and participation Turonian-Santonian clusters of Madneuli occurred of Pb in porphyry ores. Ascending succession of the Campanian Beqtakari cluster. Madneuli and Beqtakari goldbearing Lower Campanian rocks was alternated clusters are divided by regional postvocanic foult (Fig. by Upper Campanian Shorsholety suite of shoshonites 2). The Beqtakari belongs to backarc setting and is alkali olivine and tholeiites [4, 6] (Fig. 5).

Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, 251 Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 3 Geotectonic scheme of Turkey with metallogeny of sulfide deposits after Engin (Engin, [6]. Deposits: 1: Murgul, 2: Madenkoy, 3: Lahanos, 4: Guzelayla, 5: Derekoy (Kircaleli), 6: Cutlalar, 7: Akdagmeni, 8: Bakibaba (Küre), 9: Ashikoy (Küre), 10: Arapchan, 11: Balya, 12: Demirbocu, 13: Altinoluk, 14: Kulakchitligi, 15: Bozkur, 16: Aladag, 17: Hyuilu, 18: Derekoy (Kaizery), 19: Keban (Elazig), 20: Maden (Elazig), 21: Madenkoy (Siirt).

The diabase apophyses of its volcanic chamber that The first stage of rifting is related to consist porphyry mineralization coincided with shoshonite- volcanism. It is in epidote-tcoizite propylitization [4]. Therefore, Achara-Thrialetyi zone at ascending sucsetion Shorsholety suite belongs to second stage of backarc overlined the tholeiite-olivine basalt series and setting. The similar situation (Fig. 4) is known in the belongs to transitional stage of interarc-backarc Panaguirishte ore district, where high sulfidation settings [3]. Its initial stage similarly as island arc Au-Pb-Zn-Cu Chelpech goldbearing deposit is divided setting is characterized by booking tectonics by blocking from Zn-Cu Tsar Asen and Vlaikov Vruh ignimbrite activity, cauldron subsidence and subalkali porphyry deposits [5]. trachyodacite volcanic activity without rifting. The better example of back arc rifting and olivine The minor ocean setting in the studied region is the basalt-tholeiite volcanism and stratiform Volcanic Paleozoic Küre complex (Fig. 3) which consists of Massive Sulfide Cu-Zn mineralization is Hudes group ophiolites type volcanics and dunite-peridotite intrusions. of deposits (Hudes, Urup, Daud) of for Range of The complex contains serpentinized peridotites cumulate North Caucasus [7, 8]. Its genesis may be explained gabbro, pillow lavas intercalated with massive lava by spreading out sialic crust by rifting from zone of flows with lava breccias cut by diabase dikes. Their volcanism and mineralization and represents the oceanic nature is confirmed by geochemistry of second stage of backarc setting. The metallogenic immobile elements, copper-pyrite mineralization and indicator here Cu Zn mineralization, lack of Au and lack of Zn and Pb mineralization in deposits Ashiky Pb, tectonic indicator here extension and rifting. The and Bakibaba [9]. The intensive spreading spread out source of Zn here is basaltic crust, the source of Cu is from zone of volcanism as sialic so basaltic crusts the mantle, diapir caused the rifting. sourced of Au, Pb, Zn and mineralization consisting

252 Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 4 Schematic geological map of the Srednegorie, Timok, Banat and Apuseni region with porphyry and epithermal mineralization, after von Quadt, et al. [5].

Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, 253 Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 5 Lithostratigraphic column of the Bolnisi ore district. 1: Paleozoic crystalline substratum; 2: Intraformation conglomerates; 3: Cenomanian-Turonian Opreti and Didgverdi suites—alternation of rhyo-dacite, tuffs and limestones; 4, 5. Turonian-Lower Santonian Mashavera suite— tuffs, hyaloclastites tephroids, lava flows (4) and ignimbrites (5); 6: Upper Santonian-Campanian Tandzia suite—andesite-basalts and their tuffs; 7, 8. Campanian Gasandami suite—alternation of rhyolitic and rhyodacitic tuffs, -sedimentary rocks and marls (7) ignimbrites (8); 9: Campanian Shorsholeti suite—alkali-olivine basalts and andesite-basalts; 10: Maastrichian Tetritskaro suite-limestones.

254 Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators of only Cu whose source is the mantle, volcanogenic Therefore, the precollision geodynamic development and petrogenic indicators here are ephiolites, was controlled by steady state subduction and steepening dunite-peridotite and serpentinization. The rectonic of subducting slab revealed in various geodynamic indicator is extension and spreading, metallogenic is settings, controlled by geological indicators and only Cu, sialic and basaltic crusts here spread from depending on intensity of mantle diapir incursion into zone of mineralization and volcanism. Earth crust and scale of crustal-mantle participation in In the Bolnisi ore district at the island arc the various geodynamic settings. It is noteworthy that Turonian-Santonian (Tandzia and Mashavera suites) geodynamic development during collision of Tethys and in Campanian backarc (Gasandami and ocean slab at European active margin temporally and Shorsholeti suites) settings the scale of mantle spatially was alternated depending on weakening and material participation revealed by Nd and Sr ratios of strengthening of steepening of subducting slab and isotopes. The 143Nd/144Nd in calc alkaline volcanic of incursion of mantle diapir differently along the Eurasion Mashavera and Tandzia that suites it is 0.51129 and in active margin [4, 10-12]. In the studied region along Gasandami and Shorsholeti suites 0.51278. At the the deepening of subducted slab in the Caucasus same time Sr isotopes ratio decreased from region and Turkey within Paleozoic Jurassic-Cretaceous calc-alkaline to bacarc setting vocanics from 0.706 to and Eocene occurs the temporal alternation steady

0703. The increasing content of K2O from state subduction and steepening of subducted slab, calc-alkaline volcanic to subalkaly and alkiles is expressed in island arc setting temporally and related to mantle diapir incursion [4, 7]. spacially alternate in interarc or backarc (Fig. 6).

Fig. 6 Schematic map reflects the E-W lateral geodynamic transformation of subducted slab above IAES suture, indicate the character of the Eocene volcanic series in the East Pontides and Lesser Cauacasus. 1: Ophyolites; 2: Alkaline olivine basalts and tholeiites of bakarc settings; 3: Eocene calcalkaline volcanic series of island arc; 4: Shoshonite series; 5: Cretaceous calc-alkaline series of island arc. BS: Black Sea, CS: Caspean Sea, GC: Great Caucasus, SSC: Southern Slope of Caucasus, TC: Transcaucasus, AT: Achara-Thrialety, LS: Lesser Caucasus, EP: East Pontides, BSMO: Black Sea Minor Ocean, T: Talysh.

Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, 255 Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 7 Idealized scheme of interrelation of volcanism and mineralization at various stages of subduction of the Tethys ocean slab. I—Steady state subduction and island arc setting, II—Incipient stage of steepening of subducting slab, III—Reinforcement steepening and backarc-interarc setting, IV—Intensive spreading and minor ocean setting. 1: granodiorite stocks, 2: calc-alkaline rhyodacite volcanics, 3: trachy-rhyodacite and alkali olivine basalt and volcanics, 4: olivine basalt and tholeiite volcanics, 5: ophiolite volcanics and dunite-peridotite intrusive bodies, 6: sialic crust, 7: basaltic crust, 8: mantle diapir, 9: Au-Pb-Zn-Cu mineralization, 10: Au-Pb-Zn-Cu mineralization with high grade of gold, 11: Zn-Cu Volcanic Hydrothermal Massive Sulfide ores, 12: Cu-pyrite Cyprus type ores.

Laterally along deepening occurred specially in minor ocean setting [14]. It is noteworthy, that synchronal alternation minor ocean setting with alternation ascending succession is temporally related interarc backarc and farther to island arc setting. It is at one space. The precollision temporally alternation exemplified on eastern transmission of Eocene Black of geodynamic setting of studied region is presented Sea minor ocean in Achara Thrialety interarc on the idealized scheme (Fig. 7). tholeeiites, shosholites and trachyandesite and farther 2.2 Post-collision Development to calc-alkaline island arcal andesite as well as Black Sea Cretaceous minor western transmission in Bulgar The pre-collision development of Eurasian active tholeiite-olivine basalt backarc rifting [13]. The margin was altered by post-collision. The Eocene Caspean minor ocean alternates with Talysh post-collision revealed in orogenesis is related to olivine-basalt backarc [14] (Fig. 6). In opposite the closure of Tethys ocean, convergence and stress Afro Talysh sandstores, was cut by dunite peridotite stocks Arabian on the Eurasian continent. After the ocean and sandstones cut by dunite peridotite stocks and closing the subduction was terminated, however the sandstones evidence of upstarts transmission interarc steepening of subducted slab and continental crust

256 Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators were continuing. Along fault and thrust hot protracted faults and thrusts. Mineralization is associated with Sb, flows from mantle streaming in the thick orogenous W, Mo and Hg (Fig. 8). crust smelted granodioritic magma and leached trace In Turkey, West Anatolides are known postcollision metals Sb, W, Mo, Hg and base metals, forming Au deposits, Cungurlar, Halikoy, Emerly [18], ganodiorite stocks and low sulfidation and porphyry controlled by Cenozoic foulting and associates with mineralization at the initial stage of post-collision trace metals. So, as in Balcan-Carpathian region of development. The granodioritic stocks that controlled Europe, in Rodopean Adatepe porphyry goldbearing porphyry and gold trace metals deposits are deposit [19] and Slovakian Carpaths gold-cooper-base distributed everywhere within studied region in Iran, metal deposit, the mineralization associates with Sb, Caucasus, Turkey and Balkan-Carpathians and their W and Hg [20]. ages everywhere within studied region The gold mineralization with similar geochemical Oligocene-Miocene. So, the first stage of orogenesis is background is known in the various regions of the post-collision development dated as world. The giant gold deposits associated with Oligocene-Miocene, as a granodioritic ctock. mentioned trace metals occur in Tethys Eurasian In the Caucasus the granodioritic stocks and gold metallogenic belt. Here in Altaids (Tianshan) region to trace metal deposits occurred. Main Range and the late stage of Paleozoic relate giant gold deposits of Southern Slope of Caucasus deposites are Zopkhito, Muruntau group associated with Sb, W, Mo and Hg Lukhumi the gold trace metals mineralization as well represented Muruntau, Cumtor, Cholboy [21]. The as in Avadhara, Akhey, Notsarula, Akhahchu similar association of the trace metals in the deposits. postcollision gold deposits occurs in Tombstone gold The low sulfidation gold mineralization coincides belt (Canada) gold mineralization controlled by with antimonite, realgar, sheete, oripiment. The synorgeneous granodioritic stocks and associated with mineralization is controlled as by Oligocene-Miocene Bi, Mg and Mo, W, Sb As well as in the Western dacite extrusions and granodiorite intrusive stocks, so Lachlan Orogeny South-East Australia [22, 23]. So, as by Cenozoic fold thrust zone. postcollision gold deposits are related to orogenesis In the Caucasian mountain range is the known and consist with above mentioned trace metals. Hocrila-Achapara gold trace metal prospect [15]. Here Therefore geochemical background of post-collision the gold is associated with Sb and W. Here occur as settings is represented by trace metals Sb, W, Mo and well trace metal deposit Akhey and Achapara Mercury Hg, metallogenic and geochemical indicators of prospect. postcollision settings. In the Lesser Caucasus occur Kajaran and Agarak The final stage of post-collisuin development was Mo and Zn deposits and Merhadror gold deposits revealed in Pleistocene-Quartenary volcanic activity. associated with trace metals and controlled by It is widespread in our studied region and consists of Cenozoic granodiorites, so fault-thrust structures [16]. calc-alkaline andesite and subalkali shoshonite, alkali The post-collision gold mineralization spread wide olivine basalts and tholeiites [24, 25]. Those are in the Iran (Fig. 8). Here are known Harvana groups similar to pre-collision island arc, interarc and backarc deposits: Miverhud, Astargan, Anderiak, Ganareh and setting volcanics and characterized by geochemical Halphian, in the Sinanjan-Sirgan zone—Muteh, cryteria of precollision rocks. The postcollision setting Zarsheran, Dashkesan and Ahdarek deposits [4]. Here is not characterized by rifting, prevented by thick the gold mineralization is controlled by orogenous crust and lack of mineralization. They are Oligocene-Miocene granodiorite stocks and Cenozoic explosed from deep volcanic chambers which penetrate

Geodynamic Development of Eurasian Active Margin during Closing of Thhetys Ocean, 257 Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators

Fig. 8 Main tectonic elements and Mesozoic-Cenozoic magmatic belts of Iran (after Stöcklin, 1968 and Alavi, et al., 1997) and location of gold occurrences, prospects and mines in Iran. 1: Kharvana, 2: Mianeh, 3: Zarshuran-Agh Darreh, 4: Kervian, 5: Dashkasan-Baharlu, 6: Ahangaran, 7: Astaneh, 8: Zartorosht, 9: Gandy-Abolhassani, 10: Kuh-e Zar, 11: Chelpow, 12: Qal’eh Zari, 13: Shalir (after Moritz, et al. [17]).

258 Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators the mantle material. The volcanic did not consist of sourced by basaltic crust and mantle, the sialic crust trace metals association characterized for the initial spread from zone of volcanism by rifting. Extension stage of postcollision development. The mantle and rifting is tectonic indicator, the volcanogenic influence of initial stage is in proctracted hot fluids indicator is alkali olivine basalt and tholeiite, penetrated from mantle in sialiccrust, whereas at final metallogenic are Zn and Cu, lack of Au and Pb. The stage scale of participation of mantle material volcanogenic indicators of initial and transitional penetrated in deep chambers was significant. So at stages of interarc-backarc settings are subalkaly initial stage occurs mainly crustle influence and at trackyrhyodacite, shoshonite and trachyndesite final stage prevails mantle influence. volcanic activity, the metallogenic indicators are Au, The tectonic indicator of pre-collision development Pb, Zn and Cu. At this stage sialic crust has not yet is blocking at island arcs, extension and rifting at spread out from zone of volcanic activity. The interarc-backarc and spreading at minor oceans. geochemical indicator is 87Sr/86Sr = 0.7036. The minor The tectonic indicator of postcollision stage is ocean setting is characterized by intensive steepening orogenesis and fold-thust zones. and incursion of mantle diapir at highest level and spreading is mostly intensive so from zone of volcanic 3. Discussion and Conclusions activity, sialic spread out, so basaltic crust and sources Geodynamic development of Eurasian active of volcanism and mineralization here is only mantle. margin depended on subduction beneath continent The volcanogenic and petrogenic indicator here is into mantle. Tethys Ocean slab during collision and ophiolite volcanism, dunite peridotite intrusion and closing the ocean at convergence of Afro-Arabian and serpentinization. Geochemical indicator is 87Sr/86Sr = Eurasian continents, occurs in two stages: pre- and 0.7023. The metallogenic indicator is only Cu in post-collision. Cu-pyrite VMS ores. So, from island arc setting to The pre-collision stage developed during steady interarc-backarc and minor ocean setting the mantle stage subduction and steepening of subducting slab influence is arisen and crustal is diminished. coinside and incursion of mantle diapir, determined In the studied regions of Eurasian active margin crustal-mantle influence of forming settings of along deepening of subducting slab temporally and pre-collision development. The steady state spatially the island arc setting alternates with subduction determined the island arc setting. At interarc-backarc in Paleozoic lower Jurassic, Jurassic, steepening of subducting slab and incursion of mantle Cretaceous and Eocene intervals, so laterally to diapir is related with interarc-backarc and minor ocean deepening alternation of setting are spatially settings of Eurasian active margin. The settings are synchronal from minor ocean of Caspean and Black distinguished by influence of crustal-mantle sources Sea to interarc-backarc and island arc settings. As well, determined by geological indicators-volcanogenic, alternation occurs in ascending succession in spatial sourced by sialic, basaltic crusts and mantle occurred units. In Eurasian margin spatial and temporal of calc-alkaline volcanism, synvolcanic blocking Au, alternation is not known everywhere. In some Pb, Zn, Cu metallogeny. The geochemical indicators occasions only island arc setting occur in others only here are Sr and Pb isotopes ratio: 87Sr/86Sr = interarc-backarc without transferring. In one case in 0.705-0.715, 208Pb/204Pb = 39. Volcanism and Turkish Pontides occurs Paleozoic minor ocean metallogeny were here determined mainly by crustal setting—Küre complex with VMS Cu-pyrite influence sourced of Au, Pb and Zn, the source of Cu mineralization, in spite of minor ocean settings in is the mantle. The backarc-interarc settings are studied regions are Cretaceous and Eocene.

Geodynamic Development of Eurasian Active Margin during Closing of Thetys Ocean, 259 Depending on the Scale of Mantle-Crustal Sources Influence at Pre- and Post-collision Settings, Controlled by Geological and Geochemical Indicators So, steepening of subduction crust was alternated metallogenic, hydrothermal activity indicators. spatially and temporally at precollision stage of The forming of giant gold deposits associated with development. above mentioned trace metals, which widespread in So, in island arc setting occurs uplifted blocking, ore bearing rocks, evidenced the geochemical and related with tumescent sea bottom and island uplifting metallogenic criteria of postcollision setting and alternates with ignimbrite explosion and cauldron orogenesis in the world at the post-collision subsidence (subsided blocking). The steepening of geodynamic development. Therefore, the metallogenic subducted slab and mantle diapir incursion occurred indicators of pre-collision development are Au, Pb, Zn on higher level the tectonic indication in rifting. When and Cu, whereas metallogenic indicators of the strengthening of diapir incursion provoked the post-collision development are Au and trace metals Sb, intensive speeding and sialic and basaltic crusts were W, Mo and Hg. spread out, minor ocean setting occurred. At the pre-collision stage scale of the mantle The tectonic indicator of postcollision setting influence as determined by ratio of 143Nd/144Nd which expressed in orogenesis and regional post-collision is increasing from island arc till interarc-backarc faulting. It also depends on mantle-crustal settings in the Bolnisi ore district from 0.51129 till interrelation provoked by stressing Afro-Arabian and 0.51278, coincides with the Bolnisi ore district from Eurasian continents. The subducted slab under 0.51129 till 0.51278, coincides with increasing

Eurasian margin was steepening and intensive content of K2O in the same direction. hydrothermal and granodiorite magmatic activity Acknowledgments provoked at the first stage and olivine basalt and tholeiitic volcanism at the second. At the first stage, The author is very grateful to Prof. Robert Moritz the protracted hot mantle fluids melted the sialic crust and Prof. Richard Goldfarb for collaboration of with granodiorite magmatic activity and extracted investigating the European active margin within trace metals Sb, W, Mo and Hg from thickened sialic studied region boarders (Iran, Caucasus, Turkey and crust with gold and trace metals. Noteworthy, the gold Balkan-Carpaths) and fulfill advising during working, was extracted in tremendous amount and forming the as well as colleagues of Geological Institute of richest gold deposits of Eurasian active margin. The Georgia and Rich Metals Group and Caucasus Mining mentioned trace metals are geochemical indication of Group Companies. postcollision setting. In the second stages, basaltic and References tholeiitic volcanic activity was the result of mantle material incursion in deep volcanic chambers. The [1] Goldfarb, R. G., Groves, D. I., and Gardol, S. 2001. “Orogenic Gold and Geologic Time: A Global Synthesis.” rocks are characterized by geochemical criteria of the Ore Geology Reviews 18: 1-75. same rocks of precollision setting. Therefore, the [2] Stampfli, G. M., Borel, G., Cavazza, W., Mozar, J., precollision and postcollision stages of geodynamic Ziegler, P. A., 2001. Paleotectonic Atlas of the development are estimated by scales of crustal-mantle Perite-Thyan Domain. Windows and Macintosh Compact Disk, p. 89. activity and participation in various settings. For the [3] Adamia, S., Gamkrelidze, I., and Zakariadze, M. 1974. subduction and steepening of subducted slab at the “Achara-Trialeti Trough and Problem of Origin of the geodynamic development, the closure of Tethys Deep Marine Trough Bleck Sea.” Geotectonics 1: 78-94. Ocean depended on crustal-mantle source and scale of [4] Gugushvili, V. 2017. Precollision and Postcollision Geodynamic Evolution of the Tethys Ocean and Its their participation at pre- and post-collision settings Relation with Regional Metamorphism Hydrothermal and was determined by volcanogenic, petrogenic, Activity and Metallogeny along the Eurasian Continental

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