The mineralization of Cu (Au-(AG)) NE Narb(AG)hi is located in the middle part of the Urumieh-Dokhtar m(AG)matic arc, adjacent to the Kuh-Pang and Narb(AG)hi Cu DEPOSITs. The main rock units include Eocene volcano-sedimentary rocks and subvolcanic Oligo-miocene that their location is related to strike-slip faults in shallow sedimentary basins. Hydrothermal alteration includes silicification, argillic (intermediate-rarely advanced), propylitic, sericitic, carbonatization and sulfidization. Mineralization is directly related to fractures and relatively long veins (<400 with aver(AG)e width of 1m) with breccia, disseminate and vein-veinlet textures. These veins often include quartz, sericite, siderite and chalcopyrite, bornite, chalcocite, pyrite, covelite and rarely sulfosalts such as tennantite and tetrahedrite. This system starts with different types of alteration in the form of white–quartz veins and continues with hydrothermal breccia and infiltration of siliceous-sulfide fluids. Copper has the highest correlations with zinc, silver, arsenic and gold. Mineralization forms at 240-145° C and salinity of 20 to 30 wt.% NaCl. The coexistence of liquid-rich two-phase fluids and single-phase vapor refers to the boiling process and the reduction of temperature and pressure drop. Accordingly, this system provides evidence of intermediate sulfidation epithelial systems in the m(AG)matic arc. The m(AG)matic fluid in the presence of permeable structures and mixing with peripheral fluids is probable cause copper-gold precipitation together with siderite.

The massive sulfide of Taknar DEPOSITs are part of meta volcanic-sedimentary complex (Taknar Formation, Ordovician) and consist of clastic sediments, carbonate, felsic and mafic volcanic and sub-volcanic rocks. The Taknar polymetal DEPOSIT shows good layering; therefore it is syngenetic in origin. Taknar zone was affected by low grade metamorphism (Green Schist facies) in the late Paleozoic. As a result, pelitic and subarkosic rocks were changed to sericite or sericite-chlorite schist. Taknar DEPOSIT is situated within Taknar zone which is an allochthonous block. This block is situated between two major faults, Drouneh Fault to the south and Rivash (Taknar) Fault to the north. These DEPOSITs which are called Tak-I, II, III, and IV, originally were part of one big DEPOSIT but due to faulting they are being truncated and moved at least 1 km from each other. Three types of mineralization such as layered, massive and stockwork are present. The layered section is composed of alternating layers of pyrite, chalcopyrite, m(AG)netite, sphalerite, galena and chlorite. The Individual sulphide layers range in thickness from millimeters to 2 cm. Chlorite is the dominate silicate mineral within the layered ore. Massive ore horizons, having >50% m(AG)netite, occur at the stratigraphic top of the mineralized zone. Major minerals are: m(AG)netite + pyrite + chalcopyrite + sphalerite ± galena + chlorite ± quartz ± sericite ± calcite. Pyrite and chalcopyrite content are higher in the lower layers and m(AG)netite, sphalerite and galena are higher within the upper layers. In stockwork mineralization, major minerals are: pyrite + chalcopyrite ± m(AG)netite + quartz + chlorite + sericite ± calcite. Chemical variations of some elements in different DEPOSIT are: Tak-I: Cu=0.01-5.86%, Zn=269-15600 (ppm), Pb=27-4400 (ppm), Au=0.86-7 (ppm), (AG)=2-95 (ppm), Bi=34-2200 (ppm), and Mo=85-1300 (ppm). Tak- II: Cu=0.33-2.56%, Zn=0.3-7.7%, Pb=93-5000 (ppm), Au=0.33-11 (ppm), (AG)=19-105 (ppm), Bi=79-214 (ppm), and Mo=54-116 (ppm). Tak-III: Cu=0.05-5.54%, Zn=62-179 (ppm), Pb=17-47 (ppm), Au=0.06-0.33 (ppm), (AG)=2-40 (ppm), and Bi=11-250 (ppm). Based on par(AG)enesis, alteration, style of mineralization, petrography, geochemistry, and structure, Taknar is a new type of m(AG)netite rich polymetal volcanic massive sulfide DEPOSIT. Lack of pyrrhotite and high m(AG)netite associated with sulfide minerals make this DEPOSIT very different from other VMS DEPOSIT. Based on the mineral par(AG)enesis the estimated physiochemical conditions of formation are: Tak-I: T °C ≥ 250, Log f O2=(-29) to (-30), pH=5-7. Tak-II: T °C ≤ 250, Log f S2=(-11) to (-12), Log f O2=(-36) to (-39), 5<pH>9. Tak- III: T °C ≥ 270, Log f O2=(-28) to (-29), pH>5.

The North Narb(AG)hi DEPOSIT is located 26 km northeast of the city of Saveh in the central part of Urumieh-Dokhtar m(AG)matic arc of Iran. In this area, the Oligo-Miocene intrusions 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 Narb(AG)hi, with vein-veinlet and breccia geometries is mainly hosted in andesite, lithic tuff, diorite and monzodiorite. At the North Narb(AG)hi 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 Narb(AG)hi 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 Narb(AG)hi DEPOSIT can be classified as a typical intermediate-sulfidation (IS) epithermal mineralization.

Gomish-Tappeh Zn-Pb-Cu ((AG)) DEPOSIT is located 90 km southwest of Zanjan, in northwestern part of Urumieh-Dokhtar volcano-plutonic zone. Exposed rocks at the area include Oligo-Miocene volcano-sedimentary and sedimentary sequences as well as Pliocene volcano-plutonic sequence (andesite porphyry dykes, dacitic sub volcanic dome and rhyodacitic volcanics). Alteration in the DEPOSIT developed as silicic, silicic-sulfidic, sericitic, carbonate, argillic and propylitic. Main mineralization at the Gomish-Tappeh DEPOSIT is observed as veins occurring in a steeply-deeping normal fault defined by an NE-SW trend in host rocks such as dacitic crystal litic tuff, dacitic sub volcanic dome, specifically the rhyolitic tuff. Para genetic minerals in the ore veins consist of pyrite, arsenopyrite, chalcopyrite, bornite, low-Fe sphalerite, galena, tetrahedrite and specularite. Gangue minerals accompanying the ores include quartz, calcite, chlorite, sericite and clay minerals. Based on geochemical data, aver(AG)e grades for samples from the ore veins at the Gomish-Tappeh DEPOSIT are: 4% Pb, 6% Zn, 2% Cu and 88 ppm (AG). Moreover, REE distribution patterns for altered samples of the dacitic sub volcanic dome and acidic tuff when compared with fresh samples, show enrichment in LREE, while HREE demonstrate various bahaviours. The negative Eu anomaly in chondrite-normalized REE patterns for these rocks is related to the increase in fluid/rock ratio and destruction of those grains of pl(AG)ioclase enriched in Eu. REE distribution patterns for the silty tuff (footwall to the ore) compared with acidic tuff represent enrichment in all REE as well as positive Eu anomalies. However, the ore samples indicate more enrichment in LREE/HREE ratios and higher Eu contents when compared with wallrock of the ore veins (silty tuff). This is due to the influence of chloric m(AG)matic-hydrothermal fluids that caused alteration along the ore zone, releasing LREE and Eu from the host rocks and finally, concentrating and transporting these elements in the ore fluid.

The Qaleh-Zari specularite- rich Cu-Au-(AG) DEPOSIT is located 180 Km south of Birjand. Host rocks are mainly Tertiary andesites and andesitic basalts and some Jurassic shales and sandstones. Andesitic rocks from the western region of Qaleh-Zari were dated to 40.5±2 Ma. Four trends of faults and joints are identified in the mine area.  The oldest is mineralized. Three major sub-parallel quartz veins are present. No. 2 vein is the main vein and can be traced for more than 3.5 km along strike (N40°W) and more than 350 m down dip. Par(AG)enesis: St(AG)e I: specularite, quartz, Fe-chlorite, chalcopyrite and sulfosalts. Specularite DEPOSITed first and forms 10 to 25 percent of the vein. Ore grade is 2 to 9% Cu, (AG) 100 to 650 ppm, and Au 0.5 to 35 ppm. Propylitic alteration is dominant and epidote is very abundant. Argillic alteration is locally present. Silicification is mainly found within the vein zone. Temperature of homogenization of primary fluid inclusions in quartz associated with specularite and Cu, (AG), and Au mineralization was between 240°C and 360°C. The salinity of ore fluid was between 1.0 and 6.0 wt% equiv. NaCl and the CO2 was < 0.1 mole%. Based on the presence of hematite, chalcopyrite, Fe-rich chlorite, and, locally pyrite, and on the absence of m(AG)netite and pyrrhotite, the ore fluid was very oxidizing. Some important differences between Qaleh-Zari and other iron-Oxides Cu-Au DEPOSITs are: (1) The salinity is very low (< 6 wt% NaCl equiv.), (2) absence of m(AG)netite and apatite, (3) low REE and P., and 4) high grade Cu, (AG), and Au. Differences in the amount of Cu, Au, REE, P, U, F and some other elementals in iron-oxides Cu-Au DEPOSITs are related to: Tectonic setting, depth of m(AG)matism, source of m(AG)ma, degree of partial melting, physicochemical condition of melting, rate of ascending, crystal assimilation, degree of fractionation, and depth of emplacement.

The study area is situated 21 km SW of Ardestan city and 80 km NE of Esfahan (Central Iran). and according to the sedimentary structural divisions (Fig. 1; (AG)hanabati, 1998) in the central part of Urumieh-Dokhtar M(AG)matic Belt (UDMB) The UDMB in the Alpine-Himalayan orogenic belt, the most productive metallic belt of Iran, composed of basic to acidic volcanic and plutonic rocks, tuff and (AG)glomerate. The UDMB represents geochemical characteristics of subduction zones with features of calc-alkaline locally toward alkaline (Berberian and Berberian, 1981; Alavi, 1994; Shahabpour, 2007; Omrani et al., 2008; Ghorbani and Bezenjani, 2011; Yeganehfar, 2013; Rajabpour et al., 2017). The UDMB hosts several porphyry Cu±Mo±Au DEPOSITs including Sungun, Sarcheshmeh, Kahang, Darehzar, Nowchun and Meiduk (Atapour and Aftabi, 2007; Zarasvandi et al., 2015; Zamanian et al., 2016; Alirezaei et al., 2017; Jamali, 2017) and associated porphyry copper-gold, gold epithermal and manganese-iron DEPOSITs (Rajabpour et al., 2017; Ostadhosseini et al., 2018; Alaminia et al., 2020; Ostadhosseini et al., 2021). Different st(AG)es of Cenozoic m(AG)matic activity in the middle segment of the UDMB around the study area consist of different successions of volcanic and intrusive rocks (Radfar, 1998). The Eocene to Miocene diorite- monzodiorite bodies were intruded the Eocene volcanic and subvolcanic rocks. In the middle of the area, these intrusive units are juxtaposed with a fault boundary (Marbin fault) adjacent to Eocene volcanic units.    The Eocene volcanic st(AG)e is dominated by basalt, andesitic basalt, andesite, tuffs and ignimbrites rocks. Quaternary sediments are widespread in the northeastern and southern parts of the area. The oldest rock unit of this area is the Shotori dolomite formation trending NW-SW and belonging to Triassic (AG)e and located in the southwest of the study area. Cu mineralization occurs within the Eocene volcano-sedimentary sequence. The purpose of this study is to determine the type of Cu mineralization based on the mineralization characteristics, geometry, texture, structure and alteration studies, as well as the geochemistry and tectonic environment of the host volcanic rock. Materials and Methods For the purposes of this study, 60 thin sections of volcanic rocks and 30 polished thin sections of ore samples were studied by a standard petrographic microscope under reflected and transmitted lights. 10 surface and drill–holes samples from volcanic rocks were crushed and powdered in tungsten carbide swing mill for whole-rock analysis. The chemical analyses were performed for the major elements using X-ray fluorescence (XRF) and trace elements using Inductively Coupled Plasma-Mass Spectrometry (ICP-MS). Electron microprobe analyses were performed, using a JXA-8100 electron microprobe. Operating conditions were 35 kV accelerating volt(AG)e, a beam current of 20 nA, and a beam diameter of 2-10 μm. All the petrographic studies as well as chemical analyses including XRF, ICP-MS and EPMA were carried out at the Seoul National University Laboratories, Seoul, South Korean. Results and Discussion The dominant rocks of the area under study are basalt, basaltic andesite, andesite and a small volume of pyroclastic rocks which are metaluminous composition and calc-alkaline affinity. Geochemically, they are enriched in LREE relative to HREE, enrichment of LILE and negative anomalies of HFSE (i.e., Nb, Ti), pointing to characteristics of subduction-related m(AG)matic possibly generated by partial melting of metasomatized lithospheric mantle source. As the discrimination di(AG)rams of tectonic setting display, the volcanic rocks are also classified as a subduction-related m(AG)matic arc. Alteration zones were developed in the rock types including silicic, propylitic, argillic, sericitic and zeolitic. The propylitic and silicic alterations were extended within the mineralized zones. The propylitic alteration is the dominant alteration consisting mainly epidote, chlorite, and calcite. The silicification zone consists of crystalline quartz-formation, which occurs as veins and veinlets including some copper minerals. The carbonate alteration is observed in basaltic andesite and andesite rocks. Copper mineralization is mainly strata-bound, and occurs partially as veins, veinlets and disseminated in the andesite, basaltic andesites, and basaltic rocks. Based on microscopic studies, three mineralization st(AG)es were recognized in the Rahimabad DEPOSIT including pre-mineralization, mineralization, and post-mineralization st(AG)es. In the pre-mineralization st(AG)e, pyrite is formed in decreasing conditions in the host rock. In the main mineralization st(AG)e, pyrite is replaced by primary Cu and (AG) sulfide minerals such as chalcopyrite, bornite, chalcocite, digenite, jalpaite and acanthite. Finally, in the post mineralization st(AG)e, copper sulfide minerals are replaced by secondary copper sulfide minerals (chalcocite, covellite and digenite) and oxide minerals (malachite, azurite, goethite and hematite). Conclusions The Rahimabad Cu ((AG)) DEPOSIT lies in the SW of the Ardestan city in the Urumieh-Dokhtar M(AG)matic Belts, Central Iran. In this area, Cu and (AG) mineralization is observed in the volcano-sedimentary rocks. The copper ((AG)) mineralization occurs in andesite, basaltic andesite and basaltic lavas. These rocks are meta-aluminous and have a calc-alkaline affinity and indicate a subduction-related m(AG)matic arc. The main alterations zones are silicic, propylitic, argillic, sericitic and zeolitic. The geometry of mineralization is strata-bound and the texture and structure of mineralization is open space filling, disseminated, vein-veinlet and replacement. Based on microscopic as well as EPMA data, the most important Cu and (AG) minerals include chalcopyrite, bornite, chalcocite- covellite group minerals, malachite, azurite, acanthite and jalpaite, which are accompanied by m(AG)netite and hematite. Pyrite is mostly observed as a separate mineral in the host rock. The overall mineralization characteristics and tectonic setting, the type of host rock, geometry, texture and structure, mineralogy and the par(AG)enetic of Cu minerals and finally the alteration zones with different types of copper DEPOSITs document that the Rahimabad copper DEPOSIT share many features with those of Manto type copper DEPOSITs. Acknowledgment The present study was financially supported by the Cu-Au company of Ardestan. The authors are grateful to Mr. Sharif for providing sampling facilities and let us access to drill cores and exploration data.

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 m(AG)matism related to the Urumieh-Dokhtar M(AG)matic Belt crosscutting northeastern rim of the Sanandaj- Sirjan Metamorphic-M(AG)matic Zone. This m(AG)matic 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 (AG)e 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, par(AG)enesis 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.

The Mahour Zn-Cu-(Pb-Bi-(AG)) DEPOSIT located in central Lut Block, formed in an intensely crushed fault zone, dominantly in dacite­ rhyodacite volcanic-subvolcanic unit of Late Eocene- Oligocene (AG)e. Mineralization occurred as veins, veinlets and breccia massive sulfide and/or as quartz, quartz-carbonate or quartz-muscovite (sericite)- carbonate vein-veinlets. Apart from negligible dark sphalerite, only fine-grained pyrite is observed as disseminated phase within the host rocks. Hypogene mineralization is complex and the main minerals, in order of abundance, are pyrite, Fe-bearing sphalerite and chalcopyrite, with subordinate galena, Cu-sulfosalts, Bi-sulfosalts, Fe-poor sphalerite, and afi:w greenokite, arsenopyrite, digenite and probably covellite. The Considerable amounts of (AG) exist in lattice of some sulfosalt and sulfide minerals, as well as locally negligible Au-bearing W minerals. Mineralization is dominantly associated with sericitic, intermediate argillic and propyllitic alterations and rarely with advanced argillic and quartz- adularia that formed at three main st(AG)es including: 1- quartz­ pyrite, 2- Fe- bearing sphalerite, and 3- chalcopyrite st(AG)e with sulfosalts and minor high sulfidation minerals. Mineralization occurred after silicification and disseminated pyritization that comprise tourmaline (sericitic alteration prior to mineralization) and then weathering process affected it According to very low dissolution of Cu in Cu-Zn-S equilibrium system, high density of chalcopyrite inclusions in Fe-bearing dark sphalerites in Mahour reveals replacement origin of chalcopyrite disease texture. This texture and mineralogy (ore and alteration) indicate formation of Mahour polymetal mineralization at temperature range of 200-400°C and from an intermediate sulfidation state and low acidity fluid which was neutralized to alkaline by interaction with wall rock. Although, a minor evidence for evolution to high sulfidation state, more acidic and oxidation conditions is recorded in Cu- rich zone. Mineralogical features of the Mahour DEPOSIT indicate predominantly m(AG)matic origin for mineralizing hydrothermal fluid, and in combination with mineralization structure, association with calc-alkaline to shoshonitic igneous rocks and tectonic setting of host rocks, are very similar to cordilleran style polymetallode DEPOSITs.

The Senj Cu-Mo DEPOSIT is located in the central part of the Alborz M(AG)matic Arc (AMA), northern Alborz province (Karaj). Geology of the Senj area composed of mafic to intermediate Tertiary intrusive rocks and various types of volcaniclastic rocks. The early st(AG)e volcaniclastic rocks of Karaj Formation were intruded by the Oligocene Karaj Dam basement sill (composed of monzogabbro, monzodiorite and diorite) and Cu-Mo (±(AG) and Au) mineralization occurred in contact of this rocks. Ore minerals such as sulfides (chalcopyrite, bornite, molybdenite, and pyrite), oxides (m(AG)netite and hematite), and carbonates (malachite and azurite) are the main mineralogical par(AG)enesis in the area. Stockwork quartz-sulfide mineralization as the richest part of ore body have aver(AG)e grade of 3.0 wt% Cu and 0.2 wt% Mo occur in porphyritic tuff host rock with potassic-phyllic alteration. The disseminated mineralization consist of chalcopyrite and molybdenite disseminated minerals with aver(AG)e grade of 1.8 wt% Cu and 0.1 wt% Mo occur in the porphyritic andesite tuff and intermediate argillic alteration. The supergene enrichment zone with limited exposure is composed of oxide-hydroxide upper ore with low grade Cu mineralization and sulfidation replacement lower ore zone with highest grade of 2.8 wt% Cu. The m(AG)netite-biotite (K-silicate), potassic-phyllic (K-feldsapr-biotite-sericite-quartz±pyrite), intermediate argillic (kaolinite-illite±quartz±calcite) and propylitic (epidote-chlorite-laumontite-calcite±pyrite) are the main alteration assembl(AG)es related to mineral DEPOSIT. Based on geochemistry of alteration assembl(AG)es, the highest concentration of Cu and Mo mineralized elements occurred in the potassic-phyllic alteration and the intermediate argillic alteration and propylitic alteration have lower ore grade.

Rock unites which are exposed in Tak-I mine area are: Taknar formation (Ordovician), Mid-late Paleozoic and younger intrusive rocks. Taknar formation consists of sericite schist, chlorite schist, chlorite-sericite schist and some meta-diabase- gabbro-diorite. Taknar Polymetal (Cu-Zn-Au- (AG)-Pb) Massive sulfide DEPOSIT formed at certain horizon of Taknar formation. Three style of mineralization are: stockwork, layered and massive. Due to strong tectonic activity in the area, dimension and geometry of DEPOSIT are being changed. Para genetic minerals within the massive and layered are: m(AG)netite + pyrite + chalcopyrite ± sphalerite ± galena ± sulphosalt ±gold + chlorite ± carbonate± Seri cite. M(AG)netite is the main mineral in the massive zone. Par (AG)enesis within stock work are: pyrite + chalcopyrite ±m(AG)netite + chlorite + quartz + sericite ±carbonate. Based on mineral par (AG)enesis, the ore bearing solution had the following condition: T≥ 270°C, pH= 5 -7, Logƒ02 = (-29) to (-30). Also, The range of chemical composition of some elements within Tak-I massive sulfide is as follow :Cu = %0.01 - %5.86, Zn = 269 -15600 (ppm), Pb = 27 - 4400 (ppm), Au = 0.86 - 7.53 (ppm), (AG) = 2.4 - 95.1 (ppm), Bi = 34 - 2200 (ppm).Based on the par (AG)enesis, alteration, style of mineralization, petrography, geochemistry, and structure, Tak-I is part of massive sulfide DEPOSIT. Due to high content of Cu, Zn, Au, (AG) and Pb, Taknar massive sulfide DEPOSIT is a polymetal DEPOSIT. Based on high m(AG)netite within sulfides and lack of pyrrhotite, Taknar is a special massive sulfide DEPOSIT.