Petrology
Morteza Delavari; Khadijeh Ghorbani; Amir Ali Tabbakh Shabani
Abstract
The Urmieh- Dokhtar magmatic belt (UDMB) lying parallel to the Zagros suture zone is resulted from the subduction of Neotethyan oceanic lithosphere beneath the southern margin of Eurasia. The studied volcanic rocks of the Razan- Avaj area are part of UDMB magmatism. These rocks are composed of olivine-basalts, ...
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The Urmieh- Dokhtar magmatic belt (UDMB) lying parallel to the Zagros suture zone is resulted from the subduction of Neotethyan oceanic lithosphere beneath the southern margin of Eurasia. The studied volcanic rocks of the Razan- Avaj area are part of UDMB magmatism. These rocks are composed of olivine-basalts, basalts and occasional trachyandesites with alkaline nature. The interlayered stratigraphic relationships of volcanic horizons with sediments of Qom Formation implies Oligo-Miocene age. Major and trace element contents of volcanics and chemical modeling are indicative of significant role of olivine + clinopyroxene + plagioclase fractional crystallization (35-45%) in melt compositional trend. Bulk rock chemistry of theses rocks displays LREE/HREE enrichment and lack of HFSE negative anomaly similar to oceanic island basalts (OIB). It seems that after Eocene magmatic flare-up with obvious magmatic arc signatures in UDMB, during the Oligo-Miocene the origin of magmas has shifted to a deeper asthenospheric mantle. Probably, after the initial stages of the Arabian-Eurasian plate collision in the Late Eocene-Early Oligocene and the slab roll-back, an upwelling asthenospheric mantle is injected into the mantle wedge and is weakly affected by the subduction material, which is the source of Oligo-Miocene melts.
Petrology
Zahra Alaminia; Zahra Rahmati; Hossein Azizi
Abstract
The Dorojin granitoid at the northeastern Isfahan is located in the central Urumieh-Dokhtar zone and within the volcano-sedimentary complex. The Dorojin iron deposit is the one of the several ore deposits that Dorojin granitoid body is caused in its surrounding rocks. According to microscopic evidences, ...
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The Dorojin granitoid at the northeastern Isfahan is located in the central Urumieh-Dokhtar zone and within the volcano-sedimentary complex. The Dorojin iron deposit is the one of the several ore deposits that Dorojin granitoid body is caused in its surrounding rocks. According to microscopic evidences, mineral assemblage of wollastonite, garnet, pyroxene (diopside), amphibole, epidote, feldspar, calcite and quartz, Dorojin deposit attributed to the class of calcic skarns that occur during two stages progressive and regressive. Based on electron microprobe analysis, some garnets are andradite (An92-97Gr1-5) in core and andradite-grossular (An53-66Gr30-41Sp2-4) in rim. In the beginning, andradite fluid inclusions with temperature range from 369˚ to 444˚C and salinity range from 11.22 to 12.96 wt.% NaCl eqv., originate from magmatic fluids, while with change in the acidity condition of environment and the opening of system, grandite, epidote and calcite fluids with a temperature between 221˚ and 305˚C and salinity between 0.4 and 10.11 wt.% NaCl eqv., are dominated by mixing and dilution of early magmatic fluids with meteorite waters. Sr isotopic ratio of garnet vary between 0.70760 and 0.70805, suggesting that prominent role of the magmatic fluids for the formation of andraditic garnet.
Economic Geology
Fardin mousivand; Fayeq Hashemi; Mehdi Rezaei-Kahkhaei; Amir Pakizeh
Abstract
The Darreh Amrood Pb (Ag) deposit is located in south of Ghohrood, in the Urumieh-Dokhtar magmatic arc (UDMA). Host rockes to the deposit are Middle to Late Eocene grey-green siliceous tuff and crystal lithic tuff. Geometry of orebodies is stratabound, irregular, and semiconcordant to discordant to layering ...
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The Darreh Amrood Pb (Ag) deposit is located in south of Ghohrood, in the Urumieh-Dokhtar magmatic arc (UDMA). Host rockes to the deposit are Middle to Late Eocene grey-green siliceous tuff and crystal lithic tuff. Geometry of orebodies is stratabound, irregular, and semiconcordant to discordant to layering of the host rocks. Ore structures and textures are dominated by semi-massive to brecciated, banded and vein-veinlets. Main primary minerals are galena, pyrite and chalcopyrite, and secondary minerals are dominated by covelline, goethite and hematite. Gangue minerals are epidote, chlorite, sericite, clay minerals, quartz, calcite and barite. Wall rock alterations are dominated by epidote-chlorite and sericitic. The rare earth element (REE) pattern of ores is not similar to that of volcanic rocks in the footwall and hangingwall that is concordant with sub-seafloor replacement process for ore formation. Also Ce showed negative anomaly that can be attributed to Ce in the seawater. Also based on structural, stratigraphic, petrographic, textures, mineralogical, alteration and geochemical studies, it is inferred that the Pb (Ag) mineralization in the Darreh Amrood area occurred as bimodal felsic- or Kuroko-type volcanogenic massive sulfide (VMS) mineralization, and formed as sub-seafloor replacement. It should be noted that the Darreh Amrood deposit is the first recognition of base metal-rich and poor barite VMS mineralization in the UDMA.
Negin Fazli; Majid Ghaderi; David Lentz; Jianwei Li
Abstract
The North Narbaghi deposit is located approximately 26 km northeast of the city of Saveh in the central part of Urumieh-Dokhtar magmatic arc of Iran. In this area, the Oligo-Miocene intrusive rocks cut the Eocene volcano-sedimentary rocks intruding into the surrounding rocks causing extensive alteration ...
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The North Narbaghi deposit is located approximately 26 km northeast of the city of Saveh in the central part of Urumieh-Dokhtar magmatic arc of Iran. In this area, the Oligo-Miocene intrusive rocks cut the Eocene volcano-sedimentary rocks intruding into the surrounding rocks causing extensive alteration zones such as phyllic, argillic, propylitic and tourmalinization. The intrusive rocks include diorite, monzodiorite, megadiorite with calc-alkaline nature which formed as a result of subduction of the Neo-Tethyan oceanic crust beneath the Central Iranian block. The epithermal Ag-Cu mineralization at North Narbaghi, with vein-veinlet and breccia geometries is mainly hosted in andesite, lithic tuff, diorite and monzodiorite. At the North Narbaghi deposit, ore minerals can be divided into four groups: sulfides (chalcopyrite, pyrite, sphalerite, bornite), sulfosalts (tetrahedrite, tennantite), carbonates (azurite, malachite) and oxides (hematite, goethite). The alteration shows a relative concentration pattern at the North Narbaghi deposit; the argillic, sericitic and calcite alteration types are in close connection with the Ag-Cu mineralization and the propylitic and tourmalinization alteration types occur at the margin of mineralization. The main characteristics of mineralization such as geodynamic environment, host rocks, mineralogy, metal content, geometry, alteration and comparing these features with the characteristics of epithermal deposits, show that the North Narbaghi deposit can be classified as a typical intermediate-sulfidation (IS) epithermal mineralization.
S. M. Tabatabaei Manesh; F. Javadi; F. S Zohouri2
Abstract
The Nabar skarn is located about 35 km southwest of Kashan and within the Urumieh- Dokhtar magmatic belt and is formed along the contact between limestone of Qom formation with a probably middle to upper Miocene intermediate and basic intrusion body. The main minerals forming this skarn are garnet, ...
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The Nabar skarn is located about 35 km southwest of Kashan and within the Urumieh- Dokhtar magmatic belt and is formed along the contact between limestone of Qom formation with a probably middle to upper Miocene intermediate and basic intrusion body. The main minerals forming this skarn are garnet, clinopyroxene, epidote and accessory minerals are vesuvianite, chlorite, tremolite- actinolite, sphene, quartz and calcite. Ore minerals are pyrrhotite, pyrite with smaller amounts of chalcopyrite, sphalerite and magnetite. According to the presence of magnesium minerals like diopside and calcium minerals such as garnet, vasuvianite and epidote the type of host rock is probably calcite-dolomite. Skarn formation and mineralization in this region was occurred during three development stages. Presence of high temperature anhydrous minerals such as grossular and diopside specifies the formation of the first Stage in these rocks. Stage 2 is associated with the formation of andradite and sphene. Stage 3 is specified by replacement of anhydrous minerals at temperatures below 470 ° C by hydrous minerals such as tremolite-actinolite, epidote, chlorite and vesuvianite.
F. ayati
Abstract
In the studied area, the Cretaceous limestone rocks with abundant cracks are located on the Jurassic shales. Skarn producer fluids have influx into these cracks from a long distance and created distal skarns. The presence of a recrystallized and skarnified limestone rock layer within the shale, distinct ...
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In the studied area, the Cretaceous limestone rocks with abundant cracks are located on the Jurassic shales. Skarn producer fluids have influx into these cracks from a long distance and created distal skarns. The presence of a recrystallized and skarnified limestone rock layer within the shale, distinct the studied skarn from the most well-known skarns in Iran and puts it in the category of reaction skarns. There are some lenses of mineral deposites within skarns which is consisting mostly of magnetite and hematite. Iron-rich solutions which are drived from intrusive rocks, have left iron as magnetite in carbonate. In addition to the formation of magnetite by hydrothermal solutions, it can also be created in retrograde step by andradite alteration. These skarn is consisting mostly of pyroxene, garnet, tremolite-actinolite, chlorite and epidote. Skarnification process has occurred in two successive stages: progressive and regressive. In progressive stage, carbonate - silicate anhydrous minerals like garnet and pyroxene have occured. At later stages, because of the atmospheric water influence, garnets are altered to epidote, magnetite, calcite and quartz and pyroxenes are altered to tremolite, actinolite, calcite, quartz and opaque minerals. There are two set of garnet in studied skarn, the first one is massive (in progressive stage) and the other one is as veinlet (in regressive stage with epidote and has been created in quartz- calcit veins along with sulfide mineralization). Garnet compositions in iron deposits of studied area lie in grossular - andradite series. The compositions of studied garnet are the same as garnet compositions in Cu-Fe skarns in worldwide.
S. M. Heidari; M. Ghaderi; H. Kouhestani
Abstract
Arabshah gold deposit formed through hydrothermal activity with an age of ~11 Ma (based on zircon U-Pb dating by LA-ICP-MS), in northwestern Iran. This hydrothermal activity is a part of the Urumieh-Dokhtar magmatic arc (UDMA), leading to mineralization in this area, similar to Zarshouran, Aghdarreh ...
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Arabshah gold deposit formed through hydrothermal activity with an age of ~11 Ma (based on zircon U-Pb dating by LA-ICP-MS), in northwestern Iran. This hydrothermal activity is a part of the Urumieh-Dokhtar magmatic arc (UDMA), leading to mineralization in this area, similar to Zarshouran, Aghdarreh and Sarigunay gold deposits. Host rocks are a series of lower Paleozoic sedimentary sequences, cut by calc-alkaline to alkaline (high potassium) dacitic domes. Gold mineralization is mainly observed as vein-veinlets, open space filling, disseminated and brecciation in the deposit. The mineralization in terms of hydrothermal alteration (decalcification, minor argillic, sulfidization, dolomitization and silicification) and mineralization development process is associated with brecciation and deposition of base metal sulfides, iron, arsenic and antimony, similar to deposits associated with geothermal systems (low sulfidation epithermal) in volcanic arcs, but the host rock here is sedimentary. Sulfide minerals in the ore include pyrite, arsenopyrite, orpiment and realgar, stibnite, galena, sphalerite and minor amounts of chalcopyrite. Gold mineralization occurred in the form of released grains of oxidized pyrite, the tiny (invisible) in the sulfide phases such as arsenian pyrite for solid solution. The Arabshah deposit shows characteristic alteration assemblages and ore minerals (As, Sb, Hg, base metals) of epithermal low sulfidation deposits. It has been formed in relation to the mid-upper Miocene, high-level magmatic-hydrothermal activity within an extensional regime at the last stages of the UDMA activity in northwestern Iran.
Gh Ghadami; M Poosti; F Babai
Abstract
Few More than 5 dacite to andesite volcanic masses with Mio-Pliocene age are exposed to older volcanic rocksat the south and east of the Mozahem volcano, in south-east of Urumieh- Dokhtar magmatic belt, north-east of Shahre-Babak. These rocks show hyaloporphyritic- trachytic texture and consist of pPhenocrysts ...
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Few More than 5 dacite to andesite volcanic masses with Mio-Pliocene age are exposed to older volcanic rocksat the south and east of the Mozahem volcano, in south-east of Urumieh- Dokhtar magmatic belt, north-east of Shahre-Babak. These rocks show hyaloporphyritic- trachytic texture and consist of pPhenocrysts of plagioclase, amphiboles and biotites. Based on geochemical data and multi elements patterns, these rocks are medium to high K calc-alkaline suite and they show LILE and LREE enriched normalized multi-element patterns, and negative Nb, Ti and Ta anomalies. Chondrite normalized REE patterns display a steep decrease from LREE to HREE without any Eu anomaly. They have higher SiO2 and Sr contents and Sr/Y and La/Yb ratios and low MgO, Y and Yb contents than the normal calc-alkaline volcanic rocks. These volcanic rocks are formed in the a subduction zone in an active margin, and showing full complete of HSA(high SiO2 adakites) characteristics. HREE and Y depleted patterns suggest the existence of garnet and amphibole as a residue in the source. The source of these rocks was probably amphibole-eclogite or garnet-amphibolite possibly generated during subduction or slab break of the Neo-Tethyan oceanic slab beneath the Central Iran microplate in Neogene.
F Sarjoughian; A Kananian; A Esna-Ashari; J Ahmadian
Abstract
The Kuh-e Dom intrusion with calc-alkaline nature, in the northeast of Ardestan is located in the central part of the Urumieh-Dokhtar Magmatic Arc and includes the felsic and intermediate-mafic units. The felsic unit consists of monzogranite, granodiorite, quartz monzonite and quartz monzodiorite, whereas ...
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The Kuh-e Dom intrusion with calc-alkaline nature, in the northeast of Ardestan is located in the central part of the Urumieh-Dokhtar Magmatic Arc and includes the felsic and intermediate-mafic units. The felsic unit consists of monzogranite, granodiorite, quartz monzonite and quartz monzodiorite, whereas the intermediate-basic rocks comprise gabbro, diorite, quartz diorite, monzodiorite and monzonite. The acidic dykes intruded this intrusion and its surrounding rocks. The various mafic microgranular enclaves of dioritic, quartz dioritic, monzodioritic and quartz monzodioritic composition exposed in the acidic rocks. The zircon U-Pb dating by the LA-ICP-MS method indicates that the ages of the felsic rocks, intermediate-mafic rocks, acidic dikes and enclaves are 51.1±0.4 Ma, 53.9±0.4 Ma, 49.95±0.64 Ma and 50.3±0.8 Ma respectively. These ages are in good agreement with the lower-middle Eocene age of the intrusive body, which is simultaneous with subduction of the Neotethys oceanic crust underneath the Central Iran. This result is in agreement with the previous geochemical result.
Gh Ghadami; A Moradiane Shahre Babaki; S.M Mortazavi
Abstract
More than 20 tonalitic to granodioritic plutonic domes, Oligo-Miocene in age, have intruded into the older volcanic rocks, in southeast of Urumieh- Dokhtar Magmatic Belt, northwest of Shahr-e-Babak. These rocks have granoporphyritic texture and consist of Phenocrysts of plagioclase, amphiboles and biotites. ...
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More than 20 tonalitic to granodioritic plutonic domes, Oligo-Miocene in age, have intruded into the older volcanic rocks, in southeast of Urumieh- Dokhtar Magmatic Belt, northwest of Shahr-e-Babak. These rocks have granoporphyritic texture and consist of Phenocrysts of plagioclase, amphiboles and biotites. The geochemical data show calc-alkaline affinities of these rocks , which formed in volcanic arc (I type) of an active continental margin. These data also show LILE and LREE enriched normalized multi-element patterns, and depleted of HFSE (Nb, Ta and Ti). Primitive mantle-normalized REE patterns display a dramatic decrease from LREE to HREE without any Eu anomaly. They have higher SiO2, Al2O3 and Sr content and Sr/Y and La/Yb ratios and lower MgO, Y and Yb contents than the normal calc-alkaline rocks, which reveal their adakitic characteristics. The high content of Sr, LREE enrichments, absente of Eu anomaly, HREE depletion, Y and Yb depletion pattern suggest the existence of garnet, amphibole and absence of plagioclase in the source rocks. Our data suggest that the plutons produced by partial melting of amphibole-eclogite or garnet-amphibolite, due to the subduction of Neotethys oceanic slab under the Central Iran continent.
S.M Heidari; M Ghaderi; H Kouhestani; M Hosseini
Abstract
The Touzlar epithermal gold deposit formed within the high-K calc-alkaline (shoshonitic) andesitic volcanic units in northwestern Iran. The volcanic complex is in fact a part of magmatism related to the Urumieh-Dokhtar Magmatic Belt crosscutting northeastern rim of the Sanandaj-Sirjan Metamorphic-Magmatic ...
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The Touzlar epithermal gold deposit formed within the high-K calc-alkaline (shoshonitic) andesitic volcanic units in northwestern Iran. The volcanic complex is in fact a part of magmatism related to the Urumieh-Dokhtar Magmatic Belt crosscutting northeastern rim of the Sanandaj-Sirjan Metamorphic-Magmatic Zone. This magmatic system is composed of pyroclastics and lava flow sequences. The volcanic and subvolcanic rocks of the complex constitute a part of the volcano-sedimentary sequence of the Qom Formation, which formed in an extensional regime of basement uplifting and intra-continental basin. Zircon LA-ICP-MS U-Pb dating shows age between 18.4±1.0 and 18.7±0.55 Ma (Lower Miocene) for the volcanism. The hydrothermal alteration types (propylitic, argillic, phyllic, sericitic, advanced argillic and silicification) and evolving mineralization in relation to brecciation and deposition of copper sulfides and sulfosalts imply that the mineralization at Touzlar is similar to that of high sulfidation deposits in volcanic settings. The gold mineralization textures in the Touzlar deposit appear as disseminated, open space filling, veins and veinlets. The main sulfide minerals are pyrite, chalcopyrite, bornite, as well as small amounts of enargite, chalcocite, covellite, digenite, tetrahedrite, galena and sphalerite. The gold in this mineralization occurs as freed from oxidized pyrite grains, also in quartz in hydrothermal breccias as well as solid solution in other minerals such as sulfides and sulfosalts. The main difference in the formation of Touzlar with high sulfidation deposits is in its setting. The formation setting for this mineralization confirms its genesis at low depth and pressure. The deposit formed at the shallow submarine environment of the Qom basin in relation to extensional tectonic regime, while high sulfidation epithermal deposits usually form in subaerial environments related to tensional settings. Structural, host rock type, alteration, paragenesis and Au-Ag (Cu) ore mineralization characteristics of the deposit suggest that Touzlar is most similar to subvolcanic intrusion-related epithermal (high sulfidation) gold deposits formed in intra-arc extensional settings.
H Kouhestani; M.H Ghaderi; M.H Emami; S Meffre; V Kamenetsky; J McPhie; Kh Zaw
Abstract
The Chah Zard Ag-Au deposit, a typical breccia-hosted low- to intermediate-sulfidation epithermal system, is located within late Miocene andesitic to rhyolitic volcanic complex in the central part of the Urumieh-Dokhtar magmatic belt. The orebodies are emplaced in breccia bodies dominantly hosted by ...
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The Chah Zard Ag-Au deposit, a typical breccia-hosted low- to intermediate-sulfidation epithermal system, is located within late Miocene andesitic to rhyolitic volcanic complex in the central part of the Urumieh-Dokhtar magmatic belt. The orebodies are emplaced in breccia bodies dominantly hosted by rhyolite porphyries. Systematic whole-rock geochemical investigations on the volcanic rocks show that both intermediate and felsic rocks are characterized by significant Large Ion Lithophile Elements (LILE) and Light Rare Earth Elements (LREE) enrichment coupled with High Field Strength Elements (HFSE) depletion. These geochemical data indicate subduction-related magmatic arc affinity for the volcanic rocks, and suggest that hornblende fractionation appears to be an important controlling factor on the evolution of mineralized subvolcanic rocks. Although the rhyolite porphyry has relatively high 87Sr/86Sr ratios, the volcanic rocks have similar Sr and Nd isotopic compositions, displaying 87Sr/86Sr range of 0.704910-0.705967 and εNd(i) values of +2.33 to +2.70. These data suggest that the rhyolitic magmas probably represent the final diffetentiates of parental andesitic magmas with minor crustal contamination. The andesitic magmas generated from partial melting of a mixture of an incompatible element depleted anhydrous asthenospheric mantle source and a hydrous LILE and LREE enriched lithospheric mantle source in response to slab-break-off and upwelling of asthenospheric mantle. The rhyolite porphyry is inferred to have supplied heat that drove the convective hydrothermal system at Chah Zard deposit, but also provided some of the fluid sources responsible for the development of the Chah Zard epithermal system.
Majid Ghaderi; H. Kouhestani; M. H. Emami; K. Zaw
Abstract
The breccia-hosted epithermal Ag-Au deposit of Chah Zard is located within an andesitic to rhyolitic volcanic complex in the central part of the Urumieh-Dokhtar magmatic belt. At this location, magmatic and hydrothermal activity was associated with local extensional tectonics, formed in the Dehshir-Baft ...
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The breccia-hosted epithermal Ag-Au deposit of Chah Zard is located within an andesitic to rhyolitic volcanic complex in the central part of the Urumieh-Dokhtar magmatic belt. At this location, magmatic and hydrothermal activity was associated with local extensional tectonics, formed in the Dehshir-Baft strike-slip fault system. The host rocks of the volcanic complex consist of Eocene sedimentary and volcanic rocks covered by Miocene sedimentary rocks. LA-ICP-MS U–Pb zircon geochronology yields ages between 6.36±0.14 and 6.19±0.24 Ma, and a mean age of 6.23±0.16 Ma for magmatic activity at Chah Zard. Breccias and veins were formed during and after the waning stages of strong explosive eruption of magmatic-hydrothermal and phreatomagmatic brecciation events due to shallow emplacement of the rhyolite porphyry. Detailed systematic mapping leads to the recognition of three distinct breccia bodies: the volcaniclastic breccia with a dominantly clastic matrix, the gray polymict breccia with a greater proportion of hydrothermal cements, and the mono-polymict breccia with argillic groundmass matrix. The polymictic breccias generated bulk-mineable ore, whereas the volcaniclastic breccia is relatively impermeable and largely barren. Variable hydrothermal alteration occurs in outcrops, covering about 9 km2 at Chah Zard. Hydrothermal alteration assemblages are zoned around the breccias and veins, consisting of secondary quartz, illite, pyrite, adularia, chlorite, various carbonate minerals, and minor K-feldspar. Iron oxide-hydroxide, jarosite, gypsum, kaolinite, halloysite and rare alunite are the supergene alteration minerals replacing primary minerals, and filling the fractures and vugs. Precious metals occur with sulfide and sulfosalt minerals as disseminations in the veins and breccia cement. There is a progression from pyrite-dominated (stage 1) to pyrite-base metal sulfide and sulfosalt-dominated (stages 2 and 3) to base metal sulfide-dominated (stage 4) breccias and veins. Deposition of gangue minerals progressed from illite-quartz to quartz-adularia, carbonate and finally gypsum-dominated assemblages. Free gold occurs in stages 2 and 4, principally as intergrown with pyrite, quartz, chalcopyrite, galena, sphalerite, and Ag-rich tennantite-tetrahedrite; and also as inclusions in pyrite. The U-Pb zircon age of 6.19±0.24 Ma for emplacement of the rhyolitic magmas represents the maximum age of mineralization at Chah Zard. It may indicate that there was a previously unrecognized mineralization event in Urumieh-Dokhtar at this time.
M. H. Emami; R. Monsef; N. Rashid Nejad Omran
Abstract
Miocene to Pliocene volcanic rocks in the Raveh region have exposed northern part of the Urumieh - Dokhtar Magmatic Belt. Neogene volcanic rocks are situated on Upper Red Formation. Magmatic activity separated in two phase. The first phase is composed of basic to intermediate volcanic rocks such as basaltic-andesite ...
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Miocene to Pliocene volcanic rocks in the Raveh region have exposed northern part of the Urumieh - Dokhtar Magmatic Belt. Neogene volcanic rocks are situated on Upper Red Formation. Magmatic activity separated in two phase. The first phase is composed of basic to intermediate volcanic rocks such as basaltic-andesite to andesitic lavas and pyroclastics (Ngv1).The second phase has intermediate to acidic rocks as well as andesite, quartz andesite and dacite (Ngv2).According to geochemical data, these samples show magmatic affinities to the calc-alkaline series. REE and trace element patterns show LREE enrichment relative to HREE, depletion in Nb, Ta and Ti, and also high Th/Yb and Th/Nb ratios relative to MORB and OIB. The parent magma of the Raveh volcanic rocks, with calc-alkaline compositions, has been originated probably from the metasomatized mantle with effective of fluids and sediment resulted from the Neothytian subducting slab. After collision between Arabian plate and Central Iran Block in Early Cenozoic, region experienced of crustal thickening and volcanism activity formed in relation to localized extensional basin in Early Miocene to Early Pliocene. The volcanism postdates continental collision, occurring in transtentional tectonic setting.