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Manto-type copper mines occur in the Bardaskan-Doruneh copper belt. On the basis of structural sedimentary division of Iran, this belt is located in the northeastern part of the Central Iran. At the southern border of this belt, the Yazd structural block and in the north of it is the Sabzevar subzone. The important regional structures of the region are Doruneh and Taknar faults. The majority of the units in this belt are Tertiary volcanic rocks that is associated with some sedimentary units, also some intrusive units are sometimes visible in the form of dyke and stock structures. The main host-rock of mineralization is conglomerate, which is different in grain size, clasts and cement. The most common sulphide mineral is chalcocite and the most important copper carbonates are malachite and azurite. The intense alteration is not observed in the region, and the chloritic alteration is partial, and the alteration of Fe-Oxide, zeolite, calcite, and silica is just observed locally. Mineral solution is reduced and poor in iron and silica. Introduction Manto type copper deposits in the Bardaskan-Doruneh copper belt, with a length of approximately 60 km in a northeast-southwest direction, host more than ten active copper mines such as Zangalu, Zarmehr, Dahane-Siah, Mehr-Ajin, Mes-e-Sorh, Cheshme Hadi, Nasim, Sepidsarw, Cheshme Marzieh and a number of mineral areas, which according to the characteristics of these types of deposits (location, genetic pattern, geometry, host rock, minerals, etc.) and their similarities with Manto type copper deposits in Chile, Canada and the northern Michigan area, it is called as Manto-copper deposits in Iran. Materials and Methods This research includes two parts of field and laboratory investigations. Field studies were carried out in a region with about 60 km in length. Field operations include surveying and searching the area, sampling and distinguishing rock units and mineralization indicators, as well as important geological features of the area. The number of 20 thin sections for lithological investigations, as well as 20 polished thin sections and 10 blocks of drill cores (examination and study of 20,000 meters of drill core related to Nasim, Zarmehr, Mes-e- Sorkh, Cheshme Hadi and Kimia mines) and surface outcrops for a map of mineralization in the area was prepared and studied. Field surveys were conducted for mineralization controllers and host rock changes in the mining pits of Nasim, Zarmehr, Mes-e-Sorkh and Cheshme Hadi mines. Also, due to the importance of tectonic structures, a structural map of the mines was prepared. Discussion and Results The rock units from old to young include: Basalt, Andesite-Basalt, Andesite, Conglomerate with more volcanic fragments, Limestone, Siltstone, Marl and evaporite sediments including gypsum Marl. The general extension of this lithological sequence is northeast-southwest. Mineralization has occurred within the conglomerate unit. There are different types of conglomerate based on the size of the clasts, the lithology of the clasts, and the cement. The type of conglomerate has a great effect on mineralization and grade changes. Conglomerate is a suitable host for mineralization due to the porosity of the rock. The dip and strike of the ore body follows the dip and strike of the lithological units of the region and the deposit is of the stratibound type. Mineralization zone has a variable thickness between 2 and 6 meters (in some places, the thickness increases due to the action of faults). The dip of the ore body varies in different parts and is between 15 and 80 degrees towards the south and southeast. The mineralization texture is mostly disseminated and veined and is mainly as chalcocite mineral. In some places, due to effect of tectonic forces and the formation of fault structures, the order and sequence of units has been dislocated and messed up. Fault structures: The first group of fault structures with the northeast-east to southwest-west direction are the most important fault structures. These fault structures form the boundary between the Andesite unit and the sedimentary units and in the surface of mineralization outcrop can be seen along its length and it is one of the old structures in the region because it has been cut and dislocated many times by other fault structures. The second group is the north-south oriented structures and caused displacements in the mineralized host unit. This fault system, which itself consists of several parallel fault structures, has caused the creation of secondary spaces and the intensification of mineralization, and as a result, the grade has increased in some parts of the region by joining these parallel faults together and with deepening of the basin the intensity of mineralization has increased. The third group of fault structures with the northwest-southeast direction are right lateral strike-slip and minor left lateral strike-slip faults. These structures are one of the most important fault structures in the region, which displaced the rock units of the region, especially the host of mineralization.

Sagh mineral occurrence is located southeast of Torbat-e-Heydarieh, Khorasan Razavi province, and in the eastern part of the Khaf-Kashmar-Bardeskan magmatic belt. The rock units of area are divided into two categories: intrusions (monzonite, monzodiorite, diorite, and syenite) in the southern half, and conglomerate in the northern half. One square kilometer of continuous mineralization may be observed as stockwork, while there are other locations where it has a linear trend and is supported by intrusive rocks. Primary minerals include specularite, chalcopyrite, pyrite, galena, and sulfosalt, and secondary minerals include malachite, goethite, hematite, chalcosite, caveolite, and anglesite. The mineralization textures are vein-veinlet, disseminated, replacement, and cloform, mainly with a strong chloritic-silicified alteration. The average amount of copper is 0.8 with a maximum of more than 3%, the average amount of silver is 24.4 with a maximum of more than 113 ppm, and the average amount of gold is 44 with a maximum of 250 ppb. The average amount of lead is 761 ppm with a maximum of 0.4% and the average amount of zinc is 430 ppm with a maximum of 0.1%. The formation temperature of ore-forming fluid is between 159 and 328 °C and the salinity is between 7.2 and 16.7 wt.% equiv. NaCl. The mixing of magmatic fluids with meteoric waters with low temperatures and salinity was the most important mechanism of mineral formation. Based on the evidence of tectonic setting, lithology, type of alteration, shape, and state of mineralization, and the presence of abundant specularity with copper, silver, and gold anomalies, probably the Sagh area is iron oxide Cu-Ag±Au type. Introduction The geological settings, hydrothermal alteration, and mineralizing fluid compositions vary among the deposits of “IOCG-type” (Hitzman et al., 1992; Sillitoe, 2003). However, they belong to a family of Cu ±Au deposits that include substantial hydrothermal alkali (Na/Ca/K) alteration and a lot of low-Ti iron oxide (magnetite and/or hematite). According to Williams et al. (2005), these deposits likewise exhibit strong structural constraints and a temporal but not a tight geographical relationship with igneous rocks. They formed in rift or subduction settings (Hitzman, 2002) from the Late Archean to the Pliocene (Groves et al., 2010). Sagh mineral occurrence is located the southeast of Torbat-e-Heydarieh, Khorasan Razavi province, and in the eastern part of the Khaf-Kashmar-Bardeskan magmatic belt (Fig.1). This belt has a high potential for iron oxide copper-gold type deposits and sometimes skarn and porphyry copper (Karimpour, 2004). The purpose of this research is geological studies and determine the relationship of intrusions with mineralization, examine the total paragenesis sequence, geochemistry, fluid inclusions studies and finally determine the mineralization model, and the formation of mineral occurrences in the Sagh area, for the first time is done. Materials and methods To investigate the lithology, alteration, and mineralization of the Sagh area, 61 samples were taken mainly from the intrusions. 32 samples for the thin section and 10 samples for the polished thin section and polished block were selected, prepared, and studied. Then, the geological and alteration-mineralization map with a scale of 1:5000 was prepared in Arc GIS software. Furthermore, for geochemical studies of mineralization zones and veins, 24 samples were taken and sent to the Zarazma laboratory for analysis. Analysis was done by the ICP-OES method. Furthermore, 11 samples were selected for gold analysis with Fire assay, and sent to Zarazma laboratory. Using a cooling and heating system made by Linkam Company, model THM 600, microthermometric tests and salinity determination were performed on 2 wafers of quartz minerals and 31 fluid inclusions at Ferdowsi University of Mashhad. Result The rock units of the area are divided into two categories: subvolcanic and plutonic intrusions in the southern half and conglomerate units in the northern half. Intrusive rocks are composed of monzonite, monzodiorite, diorite and syenite. Mineralization can be seen in the form of stockwork in a wide and continuous zone with an area of about one square kilometer, but in some places, it has a linear trend (NE-SW and NW-SE trend) which is hosted by intrusive rocks. Primary minerals include specularite, chalcopyrite, pyrite, galena, and sulfosalt, and secondary minerals include malachite, goethite, hematite, chalcosite, covellite, and anglesite. Vein-veinlet, disseminated, replacement, and cloform mineralization textures are seen, with a dominant chloritic-silicified alteration. The average concentration of copper is 0.8%, with a maximum concentration of more than 3%, silver is 24.4 ppm, with a maximum concentration of more than 113 ppm, and gold is 44 ppb, with a maximum concentration of more than 250 ppb, according to geochemical data. The average amount of lead is 761 ppm with a maximum of 0.4% and the average amount of zinc is 430 ppm with a maximum of 0.1%. Based on fluid inclusions studies, the formation temperature of ore-forming fluid is between 159 and 328 °C, and the salinity is between 7.2 and 16.7 wt.% equiv. NaCl. Discussion and Conclusion Comparing the characteristics of Sagh prospect area with other copper-bearing deposits shows that this area is very similar to iron oxide copper-gold deposits. An empiric definition of IOCG deposits is summarized as having the following five characteristics (Williams et al., 2005): (1) copper, with or without gold, as economic metals, (2) hydrothermal ore styles and strong structural controls, (3) abundant magnetite and/or hematite, (4) Fe oxides with Fe/Ti ratios greater than those in most igneous rocks and bulk crust, and (5) no clear spatial associations with igneous intrusions as, for example, displayed by porphyry and skarn ore deposits. Sillitoe (2003) proposed a close genetic relationship between IOCG deposits in northern Chile, and dioritic plutons. Mineralization in the Sagh area has a close relationship with monzonitic, monzodiorite, and diorite, which are similar to Kuh-e-Zar, Bahariyeh, Namaq, Fadiheh, Chenar, and other KKBMB deposits (Table 3). The main alteration related to mineralization in the Sagh is propylitic-silicified, and its propylitic alteration is characterized by chlorite mineral. Extensive chlorite alteration in the Sagh area is similar to Monteverde deposit in Peru (Vila et al., 1998), Mont-del-Aigle in Canada (Simard et al., 2006), Kuh-e-Zar Tarbat Heydarieh (Karimpour et al., 2017), and other IOCG type deposits in the KKBMB belt (Almasi et al., 2015; Taghadosi and Malekzadeh Shafaroudi, 2018; Najmi et al., 2023; Sahebi Khader et al., 2021; Behnamnia et al., 2023) and Qala Zari (Karimpour, 2005) in the Lut block, where the temperature and salinity of ore-fluid are lower than some IOCG type deposits in the world. Based on the available evidence, the mineral occurrence of the Sagh includes 1) the presence of oxidant intrusions formed in the subduction zone in the KKBMB, 2) mineral paragenesis of specularity, chalcopyrite, pyrite, and galena, 3) structural control of mineralization, 4) copper, silver, gold, and lead geochemical anomaly, 5) chloritic-silicified alteration, which is very compatible with iron oxide copper-silver-gold systems. The location of this area in the KKBMB belt, which has great potential for IOCG deposits, and near other IOCG deposits that have many similarities (Almasi et al., 2015; Karimpour et al., 2017; Sahebi Khader et al., 2021; Najmi et al., 2023), is a confirmation of this claim. Although monzonitic, monzodiorite, diorite, and syenitic intrusions are the host rock of mineralization and mineralization is controlled by structures and faults, this magmatism can be represented of source rock at deep. The mineral paragenesis of the Sagh and the abundance of specularity with sulphide minerals of copper, lead, and silver, which are associated with quartz and chlorite, show that mineralization generated from a high fO2, Fe-Si rich ore fluid. The metal originated from an oxidan magmatism from deep, and moved up through faults, joints, and fractures. The mixing of magmatic ore solution with higher temperature and salinity with meteoric water with lower temperature and salinity has finally led to the deposition of sulfides, and the formation of mineralization. Temperature-salinity and alteration evidence show that we are currently in the upper parts of the system, and we need more information. The relevance of this magmatic belt in eastern Iran as a significant metallogenic zone for deposits of copper, gold, and silver is growing as more and more IOCG mineral occurrences are found there.

Balazard prospecting area is located in eastern Iran, about 120 km south-west of Nehbandan in the Central part of Lut Block. This area consists of exposed Eocene volcanic rocks, intruded by several diorite and monzodiorite dykes and stocks. These intrusive rocks display porphyritic textures with mm-sized phenocrysts, most commonly of plagioclase, clinopyroxene and hornblende, embedded in a fine-grained groundmass with variable amounts of plagioclase, quartz, and opaque minerals. The assessment of geochemical properties of the major elements showed that these granitoids are metaluminous and of high-K calc-alkaline variety. The patterns of trace elements are identical, denoting enrichments in the light REE (LREE) to heavy REE (HREE). Moreover, LILE enrichment relative to HFSE and Nb, Ti, and P show negative anomalies. The Eu/Eu* ratios range from 0.96 to 0.76, which means that the plagioclase is a slag remnant in the origin of magma. The (87Sr/86Sr)i values of the assessed intrusive rocks range from 0.706 to 0.707, assuming an Oligocene age, while the εNdi values are between -1.9 to -3.2. These results manifest that the magmas were contaminated by continental crust. The contamination has probably occurred over the ascent of magma to crustal levels, and geochemical data verifies the preposition that the investigated intrusions were intruded in a volcanic belt resting on a subduction zone. Early magmas were created through the melting of mantle wedge peridotite, occasioning magma differentiation through crystal fractionation and crust contamination as they ascended to crustal levels. Introduction Balazard prospecting area is located 120 km of the south-west of Nehbandan in South Khorasan Province, Iran. The area is part of the volcanic-plutonic belt known as Lut Block, which owns an elongated shape stretched north-southwardly. Nehbandan Fault forms the eastern boundary of Lut Block. This is while it has been bordered by the Great Kavir Fault in the north, and by Nayband Fault in the west. The southern part of the block is likely defined by South Jazmourian Fault. Karimpour et al. (2012) argue that ~65% of the rocks cropped out in Lut Block are volcanic and plutonic. The magmatic activity of Lut Block initiated over the Middle Jurassic, particularly between 165-162 million years ago, which was associated with the intrusion of Shah-Kuh batholith (Esmaeily et al., 2005). This activity reached its highest level over the Tertiary period, particularly over the Middle Eocene (Arjmandzadeh & Santos, 2014). Over half of Lut Block is overlain by volcanic and subvolcanic rocks of Tertiary. These rocks show a thickness of up to 2000 m. They have been developed as a result of subduction before the collision between the Arabian and Asian plates (Berberian & King, 1981). There is a perceptible potential for a variety of mineralization in Eastern Iran and particularly in Lut Block, which is due to its past tectonism as a subduction zone that led to extensive magmatic activity. The Middle Eocene to the Early Oligocene (30-39 million years ago) is perceptible, particularly, in respect of magmatism and mineralization (Karimpour et al., 2012). Karimpour et al. (2012) believe that a great deal of the magmatism and mineralization events in eastern Iran have occurred over the Tertiary. However, mineralization associated with Cretaceous magmatism has also been identified, such as Sn-Cu mineralization observed in Cretaceous monzonitic rocks in Kalateh Ahani (Karimpour et al., 2012). Here we present new geochemical data (elemental and isotopic) from shallow intrusive rocks, with the aim of providing a more detailed understanding of the petrogenetic processes and geodynamic evolution of Lut Block. Material and methods A total of six samples from unaltered intrusive rocks at Balazard prospecting area and representing the main lithologies were grabbed to chemically analyze major and trace elements through petrographic assessment. Major and trace elements were determined using fused disks and a Philips PW 1410 spectrometer through wavelength-dispersive X-ray fluorescence (XRF) spectrometry. The chemical analysis was undertaken at Amethyst Laboratory in Mashhad, Iran. Inductively Coupled Plasma-mass Spectrometry (ICP-MS) was applied to analyze four of the samples for trace elements at Acme Laboratories in Vancouver (Canada). The samples were tested by a lithium metaborate/tetraborate fusion and total digestion with nitric acid prior to analysis. Four whole-rock samples of Balazard granitoid rocks were analyzed for their Sr and Nd isotopic compositions at the University of Aveiro's Laboratory of Isotope Geology in Portugal. The ground samples were treated with a HF/HNO3 solution in Teflon Parr acid digestion bombs, which were heated at 200°C for three days. The ultimate solution was evaporated and the samples were then dissolved in HCl (6.2 N) in acid digestion bombs and dried again. The elements were purified before being analyzed by means of a two-stage conventional ion chromatography technique: a) Sr and REE elements were separated in an ion exchange column by AG8 50W Bio-Rad cation exchange resin; b) Nd was purified from other lanthanides by means of columns with Ln Resin (ElChrom Technologies) cation exchange resin. All reagents that were applied to prepare the samples were sub-boiling distilled, and the water was produced using a Milli-Q Element (Millipore) apparatus. Sr was loaded onto a single Ta filament with H3PO4, while Nd was loaded onto a Ta outer side filament with HCl in a triple filament arrangement. The 87Sr/86Sr and 143Nd/144Nd isotopic ratios were determined using a Multi-Collector Thermal Ionization Mass Spectrometer (TIMS) VG Sector 54, with data acquired in dynamic mode and peak measurements at 1-2 V for 88Sr and 0.5-1.0 V for 144Nd. The Sr and Nd isotopic ratios were corrected for mass fractionation relative to 88Sr/86Sr = 0.1194 and 146Nd/144Nd = 0.7219. While the investigation was in progress, the SRM-987 standard yielded an average 87Sr/86Sr value of 0.710266 ± 14 (conf. lim 95%, N = 13) and a 143Nd/144Nd value of 0.5121019 ± 75 (conf. lim 95%, N = 12) in comparison to the JNdi-1 standard. Result and discussion Balazard intrusive rocks consist of diorite, quartz diorite, and quartz monzodiorite, and exhibit characteristics typical of high-K calc-alkaline rocks from a volcanic arc setting. The primitive mantle-normalized trace element spider diagrams display significant enrichment in LILE, including Rb, Sr, Ba, Zr, Cs, and Th, and depletion in some HFSE, such as P, Nb, and Y. Chondrite-normalized plots exhibit LREE enrichment and a significant La/Yb fractionation. Balazard granitoid rocks have (87Sr/86Sr)i values that vary between 0.7064 and 0.7066. In terms of isotopic compositions, Balazard granitoid rocks have εNdi between -1.9 and -3.2. The geochemical data are commensurate with the settlement of the investigated intrusions in a magmatic belt above a subduction zone suggesting contamination through being exposed to the continental crust during magma ascent to crustal levels. Balazard granitoid rocks display a range of (87Sr/86Sr)i values between 0.7064 and 0.7066. Additionally, the isotopic compositions of the rocks show εNdi values ranging from -1.9 to -3.2. These geochemical characteristics suggest that the investigated intrusions were emplaced in a magmatic belt above a subduction zone and were subsequently contaminated during magma ascent to continental crust.

Ruchun-Mazar region is located in southern Sanandaj-Sirjan Zone, southwest of Baft city in Kerman province, Iran. Seh Chah, Chah Sorbi, Chah Nar, Zardbazi Dar, and Chah Sorbi Arjmand Pb-Zn deposits located in this region were investigated. The most outcrops of the geological units in the area include the Paleozoic metamorphic complexes of Gol Ghohar (amphibolite, gneiss and micaschist), Ruchun (schist, marble, calcschist, black chert, slate and phyllite), and Khabar (marble, calcschist). Microdioritic, monzodioritic and diabasic dykes have intruded into the metamorphic units. Dolomitic and calcitic marble of Ruchun complex is the host rock for Pb-Zn mineralization. Primary mineralization in Seh Chah, Chah Sorbi, and Chah Nar deposits includes galena, sphalerite, and pyrite ± chalcopyrite along with quartz, calcite, and dolomite ± barite. Vein-veinlet, open space filling, brecciated ± disseminated ± laminate structures and textures can be seen in these deposits. The most important alterations in these deposits are silicification and carbonitization (calcitic and dolomitic alterations). Primary sulfide ore in Zardbazi Dar and Chah Sorbi Arjmand deposits has been weathered and mining has been carried out on nonsulfide ore (supergene ore). The nonsulfide ore formed at the expense of sulfides, and mainly consists of smithsonite, hydrozincite, hemimorphite, and cerussite. It seems that these deposits belong to the direct replacement and, to a lesser extent, wall rock replacement nonsulfide zinc deposits. Based on the geological, mineralogical and alteration evidence, the primary mineralization in the region can be divided into two groups of SEDEX type (Chah Sorbi deposit) and vein type (Chah Nar and Seh Chah deposits). It was concluded that under supergene conditions in some deposits, nonsulfide ore was also formed. Moreover, the deposits of this region can be categorized into primary sulfide (hydrothermal) and nonsulfide (supergene). Introduction Iran embraces extensive areas having high potential for carbonate-hosted (CH) Zn-Pb deposits due to the suitable geodynamic conditions and the occurrence of large carbonate platforms (Rajabi et al., 2012). A wide variety of Zn-Pb deposits have been reported along Sanandaj-Sirjan Zone (SSZ) in Iran. The development of SSZ is related to the generation of the Neo-Tethys Ocean during the Permian and its subsequent destruction due to the convergent and continental collision between the Arabian and Iran plates during Cretaceous to Tertiary periods (Mohajjel et al., 2003; Ghasemi and Talbot, 2006). Ruchun-Mazar (Rechan) region is located in the southern Sanandaj-Sirjan zone (Fig. 1). This area is located at 75 km southwest of Baft city in Kerman province, Iran. In this region, the lower paleozoic marble rocks of Ruchun complex host numerous Zn-Pb deposits (Fig. 2). Although sulfide mineralization is dominant in this region (e.g., Seh Chah, Chah Sorbi, and Chah Nar deposits), secondary non-sulfide ores are common (e.g., Zardbazi Dar and Chah Sorbi Arjmand deposits). Based on geology, mineralogy, mineralization and alteration, the similarities and differences among the Pb-Zn deposits of this region were investigated. Material and methods At the first step, a 1:50,000 integrated geological map of Ruchun-Mazar region was prepared. Then, a more detailed investigation of the deposits, including field sampling of rock units, ore veins, tunnels and other mining works was done. Field observations were supplemented by petrographic studies and X-ray powder diffraction (XRD) analysis. From the collected samples (224 samples), 95 thin sections, 48 polished thin sections, and 41 polished sections were prepared for petrographic and mineralogical studies. Twenty-eight samples (sulfide and nonsulfide ores and gossan) were analyzed by XRD at the GSI. Nonsulfide ores, which contain Zn, were identified (stained bright red) by Zinc Zap, a solution of 3% potassium ferricyanide K3Fe(CN)6 and 0.5% diethylaniline dissolved in 3% oxalic acid. Results Ruchun-Mazar mining area is located in the southern part of Sanandaj-Sirjan zone (Fig. 1). Based on stratigraphy of the region, chronological sequences from the oldest to youngest include Paleozoic Gol Gohar, Ruchun and Khabar metamorphic complexes, Permian-Triassic metamorphosed carbonates, Jurassic-Cretaceous meta flysch, Cretaceous marbles (Koh-e-Khabar), Eocene-Oligocene flysch, and Quaternary sediments (Fig. 2). Gol Gohar complex (unit Pz2) contains gneiss, micaschist and amphibolite with a probable Cambrian age which has been intruded by mafic intrusive bodies. The Ruchun complex (unit Pz3) is the host complex for lead, zinc and iron mineralizations in the region. Sequence of stratigraphic layers from bottom to the top contains Gol Gohar complex (Camberian), Ruchun complex (Camberian-Ordovician), and Khabar complex (Middle-Upper Devonian), respectively. Metamorphosed carbonate rocks (dolomitic and calcitic marbles) of Ruchun complex (Pz3d and Pz3m) are seen in brown and light to dark gray colors and often alternate associated with metamorphosed sedimentary and volcanic rocks (Pz3sch unit) (Fig. 3A). The Ruchun complex was intruded by microdiorite, monzodiorite, microgabbro, and diabase dikes (Fig. 3B). Quartz and calcite veins have cut most of the Ruchun complex units (Fig. 3C and 3D). Calcitic and dolomitic marbles with probable Permian-Triassic age (Fig. 3E and F) can be seen on Ruchun complex (units PTm and PTd). Mafic (gabbro) to felsic (granite) intrusive bodies (gabbro to granite) were exposed in the west of DehSard village, next to Permian-Triassic dolomite (Fig. 3F). Pb-Zn mineralization in the Mazar-Ruchun region is formed in the calcitic and dolomitic marble (Pz3d and Pz3m) of the Ruchun complex (Fig. 4A, B, C and D). These metamorphosed carbonates are composed of calcite and dolomite, and minor minerals such as muscovite, quartz, and opaque minerals (Fig. 4E and F). Based on the morphology of calcite blade (Burkhard, 1993), and the presence of calcite (type I and II), the temperature of metamorphism of this marble is between 250 and 350 degrees, which corresponds with the green schist facies. Marbles alternate associate with schist (green schist, mica schist and graphite schist) and phyllite (Fig. 3A, E and G). Primary mineralization in Seh Chah, Chah Sorbi and Chah Nar deposits includes galena, sphalerite, pyrite ± chalcopyrite associated with quartz, calcite, and dolomite ± barite. Vein-veinlet, open space filling, brecciated ± disseminated ± laminated structures and textures can be seen in these deposits. The most important alterations in these deposits are silicification and carbonitization (calcitic and dolomitic alterations). Carbonate host rock and structural control can be considered as the most important factors for controlling primary ore mineralization in the Seh Chah and Chah Nar Pb-Zn deposits. Dolomitic and calcitic marble in the Seh Chah deposit are highly altered (Fig. 4B). A number of basic to intermediate intrusive bodies (often as dykes) can be seen in this area. Chah Nar and Seh Chah deposits were formed epigenetically with vein-veinlet, open space filling and brecciated structures and textures (Fig. 5B and C). Graphite schist in Chah Sorbi deposit is sometimes seen alternating with marble in the Ruchun complex sequence. In this deposit, in addition to vein-veinlet, open space filling and brecciated textures (which were also observed in the Seh Chah and Chah Nar deposits), part of the ore has a laminated and disseminated textures. It seems that the type of sulfide mineralization in Chah Sorbi deposit is different from the other two deposits (Fig. 6A to C). In Chah Sorbi deposit, galena, sphalerite, pyrite and chalcopyrite associated with quartz, calcite, organic matter, dolomite and barite were deposited in the hydrothermal mineralization stage (Fig. 6D and Table 1). The effects of metamorphism and deformation in this deposit can be traced by such evidence as microscopic and mesoscopic folds and faults in the ore and host rock (Fig. 6E and F). In contrast, Chah Nar and Seh Chah deposits were formed after the last metamorphic event (probably post Late Cretaceous) and no evidence of metamorphism can be seen in them. Primary sulfide ores in Zardbazi Dar and Chah Sorbi Arjmand deposits have been weathered and mining has been carried out on nonsulfide ore (supergene ore). The nonsulfide ore formed at the expense of sulfides, and mainly consists of smithsonite, hydrozincite, hemimorphite, and cerussite (Fig. 8A and G, and Table 1). Discussion and conclusion Sediment-hosted Pb-Zn deposits represent the world’s largest accumulations of base metals (Goodfellow and Lydon, 2007; Wilkinson, 2014). Table 2 shows a comparison of the general characteristics of these deposits with Pb-Zn deposits in Ruchun-Mazar area. The host rock of the studied deposits (calcitic and dolomitic marble) is different from the SEDEX type deposits (shale as the dominant host rock). Chah Nar and Seh Chah, deposits were formed epigenetically (within fracture and fault and as replacements) and deposited after the last metamorphic event (probably post Late Cretaceous). These deposits are classified as a group of epigenetic deposits and show a significant similarity to MVT deposits, although they also display fundamental differences with this category of ore deposit (especially host rock alteration). The presence of laminated and disseminated textures (before the metamorphism event) in Chah Sorbi deposit classified it as a syngenetic to early diagenetic Pb-Zn deposit (e.g., Irish type or SEDEX). Chah Sorbi deposit shows notable similarity to Howard’s Pass district, Selwyn Basin, of sedimentary exhalative (SEDEX) Zn-Pb deposits (Gadd et al., 2017). Mineralization in Howard’s Pass district (Late Ordovician to Early Silurian) was hosted by carbonaceous, calcareous and, to a lesser extent, siliceous mudstones. Mining works in Zardbazi Dar and Chah Sorbi Arjmand deposits was carried out on nonsulfide ore (supergene ore). The supergene nonsulfide deposits are unmetamorphosed and undeformed. They consist of low-temperature and low-pressure assemblages that precipitated from meteoric fluids, replacing sulfides and carbonate groundmass to form encrustations and fill pore spaces, veins, and fractures. Some of the key controls on the formation of carbonate-hosted nonsulfide Zn-Pb deposits are the nature and availability of near-surface sulfide protore, lithology, sub-aerial exposure, tectonic uplift, climate and favorable hydrology (Hitzman et al., 2003). Hitzman et al. (2003) described two specific forms of nonsulfide ore from various nonsulfide deposits around the world: red ore and white ore. Red ore is gossanous, usually found immediately above the sulfide protore, and typically contains >20% Zn, 7% Fe and Pb, and minor silver (Simandl and Paradis, 2008). Typical red ore nonsulfide minerals include iron-oxyhydroxides, goethite, hematite, hemimorphite, smithsonite, and/or hydrozincite and cerussite (Reichert and Borg, 2008). White ore contains up to 40% Zn but less than 7% Fe and Pb. Smithsonite and hydrozincite are common minerals in white ore with only small amounts of Fe-oxyhydroxides and cerussite (Reichert and Borg, 2008). Zinc and Pb nonsulfides can be used as indirect indicator minerals in exploration for MVT, SEDEX, Irish-type, carbonate replacement, and vein-type Zn-Pb deposits. It seems that Zardbazi Dar and Chah Sorbi Arjmand deposits belong to the direct replacement and lesser extent wall rock replacement nonsulfide zinc deposits. Acknowledgments This study was done supported by a grant of Ferdowsi University of Mashhad. The study is part of the Project number 41179 and also part of the first author’s doctoral thesis. We gratefully thank Dr. Mohammad Salehi Tinoni, Mohsen Jorjandipour, Ali Rashidi, Dr. Ali Amiri and Dr. Ahmad Rashidi Bosharabadi who helped us in different field works. We are grateful to the respected reviewers who played a significant role in the scientific improvement of the article.

The most important Manto-type deposits are located in the Coastal and Central Cordillera, northern Chile. Manto-type copper deposits have been reported in Iran in Saveh-Jiroft zone, the volcanoes of eastern Iran, the volcanic-intrusive complex of Alborz-Azerbaijan, Sabzevar zone, and Sanandaj-Sirjan zone. Nasim copper deposit is located in the northwest of Bardaskan, northeastern Iran. The deposit is part of the Iranian Plateau, Sabzevar Subzone, and Oryan region, located at the end part of the Khaf-Kashmar-Bardaskan magmatic belt. The geological units in the area include the Late Tertiary (Paleocene-Eocene), volcanic rocks, and sedimentary rocks including conglomerate and limestone. In Nasim deposit, mineralization has been done in conglomerate unit as a particular horizon. This unit is composed of volcanic fragments with carbonate and volcanic cements. Chalcocite is the most important and main sulphide mineral in the study area. Alteration can be divided into pre-mineralization and syn-mineralization stages. Pre-mineralization includes Celadonite, Carbonate, Silicified, and Propylitic alteration. Syn-mineralization consists of small amounts of Chlorite, Zeolite, and Calcite. In this system, the chemistry of solution is different from those of other systems such as IOCG, massive sulfide, porphyry etc., due to completely reduced and iron and silica-deficient solution. Introduction Nasim deposit is located in northeastern Iran, 50 kilometers northwest of Bardaskan. The study area is part of the Iranian Plateau, Sabzevar subzone, and Oryan region, which is located in the end part of the Khaf-Kashmar-Bardaskan magmatic belt. The most important Manto-type deposits of Iran are located in Bardaskan region. The study area includes Paleocene-Eocene volcanic rocks, major volcanic and minor intrusive fragments. In this study, the chemistry of solution was investigated based on alteration and paragenesis in Bardaskan region. Material and Methods This study was done in two parts: field studies and laboratory works. Sampling and structural studies were done while doing field studies. Logging drill cores was done for about 1000 meters in 20 boreholes. After field work, a total of 150 thin sections and 50 polished sections were prepared and studied to investigate petrography and mineralogy and to prepare geological map. Discussion and Results Geology of the area includes sequence of volcanic rocks of basalt, basaltic-andesite and andesite, respectively, formed in a non-marine environment. Conglomerate and limestone units formed after volcanic activity. Mineralization occurred only within the conglomerate unit due to useful porosity. Mineralization formed clearly post-dates conglomerate and limestone in the region. Chalcocite is the most important primary copper mineral in Manto Chalcocite systems, which has a high amount of copper and lacks iron. Mainly in the conglomerate unit, due to the good porosity of the conglomerate, the solution has risen up through the faults and penetrated into the conglomerate. Limited mineralization is observed in the carbonate rock. The mineralizations have no time and origin relationship with the volcanic cycle and the time of conglomerate formation. The porosity in the conglomerate and the fault structure in the region have played an important role in the mineralization. Manto copper solution is a solution poor in iron and poor in silica, and it is completely reducing. This solution cannot react with lime under any conditions; so the mineralization rate is very low in lime, and this shows that the solution has a special chemistry. Some exploration consultants have used the word agglomerate instead of conglomerate in Bardaskan. This is not acceptable because agglomerate is created during volcanic activity and its fragments consist of only one type of composition and have a rounded state (volcanic bomb). But conglomerate is formed during the erosion cycle and all the pieces are rounded when transported by river water or on the seashore. The use of the term agglomerate becomes a fundamental problem regarding the time and manner of formation of copper mineralization. Not knowing the exact time of Qata mineralization challenges the exploration. Alteration assemblage do not consist of epidote and quartz due to the lack of iron and silica in the solution. Moreover, the reducing solution is due to the presence of organic substances. Some researchers (e.g., Wilson and Zentilli, 2006; Tosdal and Munizaga, 2003) suggest a volcanic origin for Manto-type deposits. The volcanic rocks contain at least 5% primary magnetite. If the rocks are the origin, the solution will be rich in iron, but there is no evidence of iron-bearing minerals such as chalcopyrite and pyrite in the area. Other researchers (e.g., Palacios, 1986; Oliveros et al., 2008) see intrusive rocks as the origin of these deposits. If the rocks are the origin, solution will be definitely rich in silica, iron, and aluminum, but there is no evidence of quartz-chalcocite mineral assemblage. Therefore, the determination of the origin of the deposits requires further studies and consideration of other factors. Acknowledgments We would like to thank Ferdowsi University of Mashhad and Kome Madan Pars Company for cooperating and supporting this research. We thanks the reviewers and editor(s) for their thoughtful contributions.

Bahariyeh deposit is located in the central segment of the Khaf-Kashmar-Bardaskan magmatic belt (KKBMB), NE Iran. This belt is dominated by plutons of Kashmar batholith and associated volcanic rocks along the northern side of the Dorouneh Fault and is one of the most important metallogenic provinces in Iran. Based on geochemical data carried out for the purpose of the present study, the expansion of Cu and other metals mineralization is determined, and on the basis of investigation of trace and rare earth elements behavior, the genetic-lithological relationship of the intrusive rocks is determined in the North of Bahariyeh region.Method of study About 80 thin sections of intrusive rocks were prepared and 10 least altered 10 samples were selected and analyzed by X-ray fluorescence (XRF; PHILIPS PW 1480) at the Analytical Laboratory of the Kansaran Binaloud Institute of Mashhad, Iran. Also, 10 samples were selected for geochemical analysis by (ICP-OES) at the Zarazma Mineral Studies Co., Mashhad, Iran.Regional GeologyBased on field observations a 1:10,000 geological map prepared from the study area, the existing rock outcrops mainly include an alternative of pyroclastic units, Eocene-Oligocene lavas, as well as subvolcanic and intrusive rocks.Field observations show the North of Bahariyeh area is composed of dacite-rhyodacite and andesite volcanic units, and has been intruded by granodiorite, quartz monzonite, monzodiorite-diorite porphyry. These acidic-intermediate intrusive masses have a granular texture and are mainly porphyroid, which have been affected by propylitic, siliceous, argillic, and sericitic alterations. Copper mineralization is observed in the form of veins in different parts of the region, the thickness of these veins varies from about 5 mm to more than 10 cm. Two types of vein-veinlets can be distinguished in the mineralization zone of North of Bahariyeh: 1) vein-veinlets containing quartz + chalcopyrite + specularite + pyrite; 2) specularite-rich veins.PetrographyGranodiorite: Granodiorite shows a coarse-grained granular texture with graphic and myrmekitic intergrowths. The main minerals consist of plagioclase, K-feldspar (orthoclase), quartz, hornblende, and opaque minerals. The euhedral-subhedral plagioclase and K-feldspar phenocrysts have been altered to sericite, clay minerals, epidote, and chlorite.Monzodiorite porphyry: This unit has porphyritic and glomeroporphyritic textures with medium-grained groundmass. The monzodiorite porphyry contains up to 45-50 vol.% phenocrysts, consisting of plagioclase (15–20 vol.%), K-feldspar (10–15 vol.%), hornblende (5–7 vol.%), clinopyroxene (5–8 vol.%), and biotite (2–5 vol.%). The same minerals are also present in groundmass. Hornblende and biotite are replaced by chlorite in some places. Also, some plagioclase and feldspar phenocrysts have been altered to sericite, chlorite, and epidote.Quartz monzonite porphyry: The quartz monzonite porphyry has a porphyritic texture (0.1–0.2 mm) with a fine-grained groundmass and normally contains 40–45 vol.% phenocrysts that are 0.1–4 mm in diameter. It is mainly composed of plagioclase (30-35 vol.%), K-feldspar (25-30 vol.%), quartz (15–20 vol.%), and hornblende (5-10 vol.%). The same minerals are also present in groundmass.Diorite porphyry: This unit has porphyritic and glomeroporphyritic textures, with medium-grained groundmass with phenocrysts 0.1–5 mm across, and 40-50 vol.% phenocrysts including 25-30 vol.% plagioclase and 15-20 vol.% clinopyroxene and hornblende with minor biotite and alkali feldspar. The same minerals are also present in groundmass. Its accessory minerals are quartz, zircon, and magnetite (2–3 vol.% and 0.5 mm).DiscussionNorth of Bahariyeh provides important insights for reconstructing the Middle Eocene tectono-magmatic evolution of the NE of Iran. Significant outcomes of this work are:The intrusive sequence in the North of Bahariyeh is inferred as monzodiorite porphyry, diorite porphyry, quartz monzonite, and granodiorite of middle Eocene. and all intrusive rocks belong to I-type metaluminous-peraluminous granites. Major and trace element geochemistry indicate the acidic-intermediate intrusive rocks in the North of Bahariyeh were likely generated by partial melting from the subcontinental lithospheric mantle affected by both slab-derived fluids and lower continental crustal components.The enrichment of LILE (Ba, K, and Cs), depletion of HFSE (Nb, Ti), and the enrichment of LREE relative to HREE indicate crustal contamination and formation of the source magmas in a subduction environment zone by low degrees of partial melting. Trace element geochemistry confirms the evolution of dioritic rocks by a partial melting process (1-5%). Geochemical results, combined with regional geological data, demonstrate a shallow mantle with a clear subduction imprint (metasomatized mantle wedge melts). The post-collisional transtensional tectonic regime favored magma genesis with decompression melting and magma rise through the well-developed fault system and the subvolcanic and intrusive units in the North of Bahariyeh area form the active continental margin-related subduction zone.Overall, the data of the rare earth elements of acidic-intermediate units in the area of study shows that the rocks under investigation were originated by partial melting of enriched mantle under the influence of the fluids released from the subduction blade and then under the contamination of the crust.AcknowledgmentsThis study was supported by a grant from the Research Foundation of Ferdowsi University of Mashhad (Iran) (Project No. 46590.3, Date: 15 May 2018). We thank anonymous reviewers and editors for their thoughtful reviews.

Granites are the most important components of the continental crusts. As an important part of the Alpine-Himalayan global belt and the result of the Tethys evolutionary cycle, the Urmia-Dokhtar Magmatic Arc (UDMA) has formed during different magmatic periods. The most important magmatic episode of UDMA igneous rocks, which is the result of lithospheric extenssion and extensive magmatism, occurred during 55 to 37 Ma (Moghadam et al., 2015). In order to enhance our understanding of tectonomagmic evolution of the continental crust during this period, in this research, the intrusive masses of Aftabru and Qlichkandi will be investigated using geochemical data and the isotopic composition of neodymium and strontium. The mentioned intrusive masses are located in the southwest region of Buin Zahra in Central Iran zone.Geology BackgroundUrmia-Dokhtar magmatic arc with Cenozoic intrusive and Eocene-Quaternary extrusive rocks shows different levels and rock outcrops in terms of time of origin and erosion rate, same what is seen in the subduction arc of the Andean continental margin. The lithospheric stresses caused by the interaction of the African-Eurasian-Indian lithosphere led to the emergence of Paleogene extensive magmatic activity and a magmatic flare-up lasting 30 Myrs during Eocene and Oligocene. As a result, more than 4 km of Paleogene igneous rocks formed in Saveh, Zarandiyeh, and Tafresh regions. In the south of Bouin Zahra region, pyroclastic outcrops and Eocene lava with a width of about 5km2 and 10 km2 are found in Aftabru and Qlichkandi areas, respectively.MethodsAfter field observations and detailed textural and petrographic studies, 12 suitable samples with minimal weathering and alteration were selected from intrusive rocks and analyzed by XRF and ICP-MS methods for major, trace and rare earth elements. 6 whole rock samples were analyzed for Sr-Nd isotopes.PetrographyIn Aftabru and Qlichkandi areas, quartz monzonites intruded the lower-middle Eocene volcanic and pyroclastic rocks.AftabruPetrological observations show that the Aftabru intrusion contains 7-16 Vol% quartz, 25-30 Vol% K-feldspar, 39-54 Vol% plagioclase, 5-10 Vol% pyroxene, 8-15 Vol% amphibole, as well as 1 Vol% accessory minerals.QlichkandiThe medium-grained Qlichkandi intrusive rocks with granular texture, composed of quartz 9-15 Vol% quartz, 25-28 Vol% K-feldspar, 35-45 Vol% plagioclase, 1-5 Vol% pyroxene, 5-10 Vol% of the common mafic mineral of amphibole, 5 Vol% biotite, and less than 1 Vol% accessory minerals.DiscussionBased on new geochemical and isotopic data, we will investigate the tectonic location, genesis and magmatic processes affecting the parental magma and the possible source rock of the intrusive masses in the south of Bouin Zahra region.Tectonic-magmatic zone:As the pattern of rare earth elements and the spider diagrams of enrichment in LILE and LREE elements and depletion of HFSE and HREE elements display, the most important characteristic of intrusive rocks in the studied area is their similarity to continental margin arc rocks. Generation and magmatic processes:Some incompatible trace elements ratios, such as Y/Nb, Nb/Ta and Nb/La that are less affected by diffrentiation are good indicators for investigation of the magma origin and the crustal contamination effect on the magma. The higher amounts of Y belong to crustal melts or impregnation with crustal materials, and the higher amounts of Nb belong to melts derived from the mantle. In the studied intrusive rocks, Y/Nb ratio is 1.6 on average with a range of 0.6-3.6, which probably indicates mantle with crustal mixing in the magama origin. The Nb/La value is 0.1 in primary mantle and 0.46 in the crustal rocks (Morata et al., 2005), it is about 0.86 on average and equals to the range of 0.1-0.52 in the intrusive rocks of the southern region of Buin Zahra (Qlichkandi, Aftabru). This value indicates a mantle origin for the studied rocks. The Nb/Ta value in mantle rocks is 17.5 and in crustal rocks it is equal to 11-12 (Green, 1995). This ratio is 15 on average (ranging from 8 to 8. 26), supporting the mantle origin as well.Neodymium model age (460-550 Ma) and positive ԑNd(t) indicate the Cadomian origin of lithospheric rocks of the Aftbaru region, while the model age of the samples from Qlichkandi region is 0.9. It shows ԑNd(t) less than zero. This difference is probably due to the high magma mixing with crustal materials in Qlichkandi region, which is confirmed by the diagram of ԑNd versus Sr isotope. 143Nd/144Nd ratio for the Aftabru samples is 0.51270-0.51280. But in the Qlichkandi samples, it is 0.51252-0.51242, which is a sign of contamination with the lower continental crust materials and a tendency towards lower crust. 87Sr/86Sr ratio is 0.70472-0.70510 in Aftabru and 0.70631-0.70607 in Qlichkandi samples. Therefore, according to the intrusive rock petrologic diagrams, it shows signs of contamination with the underlying crustal materials.AcknowledgementsThe authors would like to express their utmost gratitude for the research grant number 41200/3 from Ferdowsi University of Mashhad, and we are also grateful to all dear referees who did not spare their kindness in increasing the scientific richness and literature of this article.

Introduction About 75% of world copper, 50% of molybdenum, and 20% of gold are produced from porphyry copper deposits (Sillitoe, 2010) with an average ore grade of 0.45–1.5% Cu, 0.007–0.04% Mo and up to 1.5 ppm Au. Porphyry copper deposits are commonly associated with intermediate composition arc-related igneous rocks with high Sr/Y and La/Yb ratios (Richards, 2011). Igneous rocks having ratios of Sr/ Y > 25 and Y < 10 ppm are considered adakitic type. The aim of this work is to modify the name of Urumieh-Dokhtar magmatic belt (UDMB), petrological studies of granitoids from Saveh to Jiroft, determination of the genetic relationship between porphyry copper deposits and adakitic and non-adakitic granitoids, and comparison of Miocene-Pliocene adakitic volcanic rock in different parts of Iran with barren adakitic granitoids. The role of a thermal gradient, depth of dehydration, water content, source rock, partial melting percentage, and oxygen fugacity in the formation or non-formation of mineralization, grade, and reserve of porphyry copper deposits are also investigated. Materials and methods The information used can be divided into three parts: 1) data related to I-type magnetite series granitoids related to porphyry copper deposits of Miocene age in Saveh-Nain-Jiroft magmatic belt (SNJMB) which in Table 2 are presented, 2) data related to barren I-type magnetite series granitoids of Miocene age of SNJBM are reported in Table 3. In addition, radiogenic isotope information of barren and fertile SNJMB granitoids and volcanic rocks is presented in Table 4. 3) Information related to Miocene-Pliocene adakitic volcanic rocks, which is shown in Table 5. Result Granitoids show the characteristics of subduction zone magmas. So that the enrichment of LILE elements and the depletion of HFSE elements can be seen. Also, enrichment of LILE elements and depletion of HFSE elements of fertile granitoids is more than barren units. Dalli deposit samples show a moderate pattern between barren and fertile granitoids (Fig. 3). All the evidence presented shows that all granitoids are I-type and magnetite series. In the fertile granitoids, the ratio of (La/Yb)n is between 15 and 38. However, this is between 2 and 14 (mostly below 10) in barren granitoids (Tables 2 and 3, Figs. 5A and 5B). Negative anomalous values ​​of Eu are seen in Miocene barren granitoids (Eu /Eu* value between 0.43 and 1 with an average of 0.65) (Table 3). While fertile granitoids have positive to slightly negative Eu anomalies (Eu / Eu* value between 0.82 and 1.3 with an average of 1.2). The initial values of 87Sr/86Sr of Miocene fertile granitoids vary between 0.704253 and 0.704702; while in barren granitoids, it is between 0.705 and 0.7085. Fertile Miocene granitoids have positive εNd (i) (0.29 to 3.39 mean 2.15) and in barren units is between 3- and 2.6 (Table 4). The value of the ratio (La/Yb)n of all volcanic units is between 13 and 78 and mostly above 20. They have positive to slightly negative Eu anomalies (Eu/Eu * values between 0.89 and 1.72) (Table 5). Figure 9 shows the fertile granitoids of the SNJMB similar to adakite volcanic rocks are located in the adakite field. In addition, Figure 11 show that all samples are high silica adakitic type. However, barren granitoids, which are mainly located between Saveh and Nain, are non-adakitic and are plotted within the normal arc range (Fig. 9). Discussion and Conclusion In this paper, the name of UDMB was changed to Saveh-Nain-Jiroft magmatic belt (SNJMB) based on the evidence of lack of magmatism between Saveh to the extent of Takab and absence of air magnet anomaly. Magmatism of Urumieh to Takab is a continuation of the western Alborz magmatic belt. Based on the characteristics of magmatism and mineralization, SNJMB can be divided into two distinct belts: 1) Saveh-Nain Magmatic Belt (SNMB), which mainly consists of non-adakitic barren I-type magnetic granitoids. Based on the ratio (La/Yb)n, these granitoids originate from a depth of 60 to 80 km, and a mantle wedge and based on the amount of Eu/Eu*, conditions were oxidant. The initial 87Sr / 86Sr ratio indicates that they had a lot of contamination with the continental crust. The crustal thickness in SNMB is less than 48 km, 2) Nain-Jiroft Magmatic Belt (NJMB) which hosts porphyry copper deposits. The Miocene granitoids of this belt are magnetite series and I-type adakite. Based on the ratio (La/Yb)n, these granitoids originate from the depth of garnet stability (more than 90 km) and partial melting of slabs and are based on Eu/Eu* Oxidizing conditions have been established at the place of origin. The initial 87Sr / 86Sr ratio indicates slight contamination with the continental crust. The crustal thickness in NJMB is 48 to more than 52 km. Geochemically, adakitic volcanic rocks are similar to the fertile adakitic granitoids of NJMB, but these units do not contain any mineralization. The characteristics of the oceanic slabs of Neo-Tethys varied considerably during the SNJMB, leading to various magmatism and mineralization. The thermal gradient, depth of dehydration, amount of water, source rock, and the percentage of partial melting along the belt control the type of magmatism and the formation of mineralization. Note Figure 15. References Richards, J.P., 2011. High Sr/Y arc magmas and porphyry Cu ± Mo ± Au deposits: Just add water. Economic Geology, 106(7): 1075–1081. https://doi.org/10.2113/econgeo.106.7.1075 Sillitoe, R.H., 2010. Porphyry copper systems. Economic Geology, 105(1): 3–41. https://doi.org/10.2113/gsecongeo.105.1.3

The Zangalou mine area, a part of NW Bardaskan magmatic assemblage, located south of Sabzevar and northwest of Bardaskan cities in Khorasan Razavi province. The rock units of the area are dominated by sedimentary and volcanic racks (andesite, trachyandesite, latite and andesitic tuff). The dominant minerals are plagioclase, hornblende, pyroxene and alkali feldspar locally affected by argillic and propylitic alterations and the main textures are porphyritic, glomeroporphyritic, amygdaloidal and fine grain. The rocks under study formed in continental volcanic arc related to subduction zone, are calcalkaline in nature, metaluminous in composition and classified as shoshoite series. LREE and LILE enrichment compared to HREE and HFSE of the investigated rocks indicate their magma generation in subduction setting. Both Zr/Ba and Sm/Yb ratios point to lithospheric mantle origin and the rare or the absence of garnet in the origin respectively. The parent magma formed from partial melting of an enriched phlogopite spinel lherzolite. The geochemical properties of Zangalou share many signatures with those of the volacic rocks distributed in other parts of NW Bardaskan volcanic assemblage indicate high similarity in geochemical signatures of volcanic rocks. Studying geochemistry of volcanic rocks in these areas indicates formation of these rocks in a subduction setting.

Iranian porphyry copper deposits (PCDs), resulted from the evolution of Neo–Tethys Ocean during the Mesozoic and Cenozoic, dominantly distributed in the five main tectono-magmatic belts that meanwhile the Kerman Porphyry Copper Belt (KPCB) is the most famous and important belt in the south of Iran while the Lut Block is the oldest and modern known porphyry belt in eastern Iran. PCDs of the KPCB (+Najmabad; group 1) hosting moderate to giant world-class deposits belong to the Oligocene–Miocene. On the other hand, PCDs of the Lut Block (except Najmabad; group 2) formed during the Eocene–Oligocene, are mostly subeconomic to barren. Despite the similarities in tectonic setting, host rock composition, hydrothermal alteration zones, and mineralization type, there are significant differences in geochemical characteristics (depression in MREE/HREE pattern (group 1) vs. horizontal trend (group 2), Sm/Yb greater than 2.4 (group 1) vs.

ntroduction The granitic rocks are divided into magnetite and ilmenite series (Ishihara 1977), coinciding spatially with the I-type (εNdi0; (87Sr/86Sr)i~0.704-0.706) and S-type granites (εNdi0.707, N-MORB normalized patterns with enrichment in Low- and High Field Strength Elements (LFSE and HFSE) and depletion in P and Ti contents, chondrite-normalized patterns with flat heavy rare earth elements (HREE) patterns, magnetic susceptibility 4 km, regional metamorphism at ​​green schist facies (and amphibolite) following Cimmerian orogeny, low (Eu/Eu)N (reducing conditions), magnetic susceptibility 0.707) show that, unlike previous studies, these granitoids are S-type granitoids formed by melting the continental crust in a collisional zone. Therefore, tin mineralization might probably occurred in connection with them. However, there is ample evidence of the absence of tin mineralization by the magma that forms these S-type granitoids, that are including the lack of hydrothermal fluids and consequently mineralization potential (due to the absence of alteration minerals in ASTER satellite images), low content of tin, copper, lead and zinc elements in these granitoids Sanandaj-Sirjan Zone and associated river sediments, (Eu/Eu)N value > 0.2, Rb/Sr 200 ppm, as well as the geological, geophysical and geochemical similarities to barren S-type (ilmenite series) granitoids in Lut block (in Najmabad, Sorkh kuh to Shah kuh areas) which have formed in a continental collision system during the Cimmerian orogeny. References Ahadnejad, V., Valizadeh, M., Deevsalar, R. and Rezaei-kahkhaei, M., 2011. Age and geotectonic position of the Malayer granitoids: Implication for plutonism in the Sanandaj-Sirjan Zone, W Iran. Neues Jahrbuch für Geologie und Paläontologie - Abhandlungen, 261(1): 61–75. https://doi.org/10.1127/0077-7749/2011/0149 Bayati, M., Esmaeily, D., Maghdour-mashhour, R., Li, X. and Stern, R.J., 2017. Geochemistry and petrogenesis of Kolah-Ghazi granitoids of Iran: Insights into the Jurassic Sanandaj-Sirjan magmatic arc. Chemie der Erde- Geochemistry, 77(2): 281–302. https://doi.org/10.1016/j.chemer.2017.02.003 Esna-Ashari, A., Tiepolo, M., Valizadeh, M., Hassanzadeh, J. and Sepahi, A., 2012. Geochemistry and zircon U–Pb geochronology of Aligoodarz granitoid complex, Sanandaj-Sirjan Zone, Iran. Journal of Asian Earth Sciences, 43(1): 11–22. https://doi.org/10.1016/j.jseaes.2011.09.001 Ishihara, S., 1977. The Magnetite-series and Ilmenite-series Granitic Rocks. Mining Geology, 27(145): 293–305. https://doi.org/10.11456/shigenchishitsu1951.27.293 Khalaji, A.A., Esmaeily, D. and Valizadeh, M. V., 2007. Petrology and geochemistry of the granitoid complex of Boroujerd, Sanandaj-Sirjan Zone, Western Iran. Journal of Asian Earth Sciences, 29(5-6): 859–877. https://doi.org/10.1016/j.jseaes.2006.06.005 Neiva, A.M.R., 2002. Portuguese granites associated with Sn-W and Au mineralizations. Bulletin of the Geological Society of Finland, 74: 79–101. https://doi.org/10.17741/bgsf/74.1-2.003 Shahbazi, H., Siebel, W., Pourmoafee, M., Ghorbani, M., Sepahi, A.A., Shang, C.K. and Abedini, M.V., 2010. Geochemistry and U – Pb zircon geochronology of the Alvand plutonic complex in Sanandaj – Sirjan Zone (Iran): New evidence for Jurassic magmatism. Journal of Asian Earth Sciences, 39(6): 668–683. https://doi.org/10.1016/j.jseaes.2010.04.014 Takahashi, M., Aramaki, S. and Ishihara, S., 1980. Magnetite-Series/Ilmenite Series vs. I-type/S-type granitoids, Granitic Magmatism and related mineralization. Mining Geology, Special Issue, 8: 13–28. Tahmasbi, Z., Castro, A., Khalili, M., Khalaji, A.A. and De, J., 2010. Petrologic and geochemical constraints on the origin of Astaneh pluton, Zagros. Journal of Asian Earth Sciences, 39(3): 81–96. https://doi.org/10.1016/j.jseaes.2010.03.001 Zheng, W., Mao, J., Zhao, C., Zhang, Z., Xiao, W., Ji, W., Majidifard, M.R., Rezaeian, M., Talebian, M., Xiang, D., Chen, L., Wan, B., Ao, S. and Esmaeili, R., 2018. Geochemistry, zircon U-Pb and Hf isotope for granitoids, NW Sanandaj-Sirjan zone, Iran: Implications for Mesozoic-Cenozoic episodic magmatism during Neo-Tethyan lithospheric subduction. Gondwana Research, 62: 227–245. https://doi.org/10.1016/j.gr.2018.04.002

Introduction The Robaie copper area is located 95 kilometers South of Damghan in the Semnan province. The study area has coordinates between 54˚30΄37˝to 54˚30΄42.71˝ latitude and 35˚22΄29.41˝ to 35˚23΄47.54˝ longitude. Geotectonically, the study area is located in the central Iran and in the northern part of the Torud-Chahshirin volcanic-plutonic belt (Houshmandzadeh et al., 1978). The Torud-Chahshirin volcanic-plutonic belt is a Tertiary magmatism in central Iran which is composed of volcanic rocks with dominant andesite composition and granodiorite intrusive with dominant diorite composition (Fard et al., 2001). Torud-Chahshirin volcanic-plutonic belt has created a favorable geological situation for base metals such as copper, lead, zinc, gold, silver and other precious and base metals, such as the Robaie copper area, Chah Messi (Cu±Pb-Zn; Imamjome et al., 2009), Kuh-Zar (Cu-Au; Rohbakhsh et al., 2018) and other instances. The main objective of this study is geology, petrography, U-Pb zircon dating and Sr-Nd isotope and also alteration, mineralization, geochemistry and fluid inclusion in the study area. Materials and methods 60 samples were collected from the study area. Petrographic studies were done on 40 thin sections. Mineralization and paragnesis of the system were studied based on 10 polished-thin sections and 6 polished sections. The measurements were conducted on a Linkam THMSG 600 at the Ferdowsi University of Mashhad. REE (ICP-MS method-ACME Laboratory in Vancouver, Canada) elements were analyzed for 3 samples of diorite dykes. Eight sampels for geochemistry and four samples for fire assay were analyzed at the Zar Azma Company. U-Pb dating in zircon of diorite dyke was conducted by the ICP-MS method in the Arizona LaserChron Center. Sr and Nd isotopic compositions were determined at the Laboratório de Geologia Isotópica da Universidade de Aveiro, Portugal. Results The geology of the area is dominated by volcanic rocks (andesite and trachyandesite), which were intruded by diorite dykes. Alteration zones are propylitic, argillic, sericitic and carbonate. The Copper deposit in the study area occurs as ore veins situated along fault zone with NS-SW trending. Vein thickness varies from 1-5m. Vein thickness varies from 1-5m. The primary minerals are chalcopyrite, pyrite and chalcocite, covellite, bornite, malachite, azurite, hematite, goethite and limonite are secondary minerals. The amount of Cu is between 0.01 to 5.6 % and amount of Ag, Sb, Pb, Zn, As elements is low. The homogenization temperature (Th) values ranged from 165 to 300 oC. Salinities of ore-forming fluids ranged from 7 to 16 wt. % NaCl equivalents. Diorite dykes in the Robaie area have characteristics of enrichment in LREE versus HREE, enrichment of LILE and depletion in HFSE. The initial 87Sr/86Sr and 143Nd/144Nd ratios of biotite-hornblende diorite are 0.705664 and 0.512486, respectively. The εNdI value is -1.7. In the εNdI versus initial 87Sr/86Sr diagram diorite dykes of the Robaie area plot to the right part of the mantle array. The mean age of diorite dyke is 50.49±0.49 Ma. Therefore, the U-Th-Pb zircon dating indicates that diorite dyke formed in the early Eocene (Ypresian) era. Discussion Diorite dykes originated from mantle-derived magmas. The parental melt would have originated in a non-depleted mantle source. Isotopic data from diorite dykes show that subduction source with contamination to continental crust. In tectonic setting diagrams (Pearce et al., 1984) diorite dykes plot on the fields of the volcanic arc granites (VAG). In the Dy/Yb vs. Dy system (Shaw, 1970) diorite dykes of Robaie area were formed by 15-20% partial melting of spinel-phlogopite lherzolite. According to Yh/Yb vs. Ta/Yb (Pearce et al., 1984) and Ba/La vs. Th/Nd diagrams (Shaw, 1970) diorite dykes were formed from slab-drive fluid in the active continental margins. Fluid inclusions data of the Robaie area manifest that the ore-forming fluids were medium to low temperature and medium to low salinity. The pressure determined for the Robaie area was approximately < 10 MPa, which is equivalent to a depth of approximately < 1 km assuming lithostatic pressure. Fluid inclusion studies indicate that there is a positive correlation between homogenization temperature and fluid salinity, similar to the process of fluid mixing. The decrease in salinity has been the most important factor in the precipitation of copper in the area. All of evidence shows that mineralization in the Robaie area is of epithermal type deposit. Acknowledgment The financial support provided by grant no. 42842.3, date: 3 Jan 2017 is greatly appreciated. We would like to thank Mr. Ehsan Azizian of the Zamin Pouyan Fraz Assia Company for the generous support and the access to mine data.

Introduction The investigated area in northeastern Iran that is known as the Tarik Darreh arsenopyrite-Au-W prospecting target is situated in the Kopeh Dagh zone (Fig. 1). Most of the study area is covered with black slate rocks which most authors have referred to as Upper Triassic with Norian age (e.g., Behroozi et al., 1993). Plutonic rocks with gabbro, diorite, and quartz diorite and monzodiorite composition were introduced in the slate rocks. The previous studies in the Tarik Darreh are the preliminary report of arsenopyrite with Au-W quartz lode mineralization carried out by Taghizadeh (1965). Since then, the Geological Survey of Iran (e.g., Alavi Naini and Mossavi-Khorzughi, 2006) a few geologic companies and the universities (Shafi Niya, 2002) and Ghavi et al. (2013) have been studying in the area. In the present study, we provide more information, complete with new information about the geology of the Tarik Darreh area. Materials and methods Expansive field geology surveying to draw a geology map in 1:8000 scale and sampling from plutonic rocks was performed and two main fault system were distinguished in Tarik Darreh (Figs. 2 and 3). Thin section microscopic studies were carried out following field investigations. Magnetic susceptibility was measured with a portable Model KT-10 and GMS-2 Fugro instrument (precision of 0.0001 SI units). Sixteen samples of intrusive bodies and dykes were analyzed for major and trace elements using 4E-Reserch package (INAA, FUS ICP-OMS, ICP-MS) at the Acme Lab (Canada). Gabbroic units were selected for U-Pb geochronological study. In the heavy liquid process, zircon crystals were separated, hand-picked under microscope. Zircon grains for Th-U-Pb dating were examined by an Agilent 7700 quadrupole ICPMS at the University of Tasmania (Australia). Discussion and Results Plutonic rocks in the Tarik Darreh area are in the form of bodies and dykes. The plutonic bodies are mostly gabbro, gabbro diorite, diorite (hornblende pyroxene diorite, biotite hornblende diorite and hornblende biotite diorite), biotite hornblende monzodiorite, quartz diorite, and quartz monzonite in composition. However, it is diorite with granular textures as a common rock (Figs. 4 and 6). Other rocks as dyke have more hornblende diorite composition with porphyritic textures. Common mafic minerals in the plutonic rocks in the Tarik Darreh include pyroxene, hornblende and biotite. The alteration assemblages of uralite, chlorite, calcite and sericite are very common gabbroic-diorite rocks (Fig. 5). The plutonic rocks have SiO2 with values in the range of 46 to 56% (Table 1). Therefore, these rocks are intermediate in composition. Most of these rocks also have high K-calc-alkaline composition with metaluminous characteristic (Fig. 7). Enrichment in LREE relative to HREE, low La/By ratio, enrichment in LILE and negative anomaly of Eu, Ti, Zr, Y and Ba are shared in all of the studied plutonic rocks and dykes (Figs. 8 and 9). All the plutonic rocks have low values of magnetic susceptibility (less than 3×10-3 SI). Two main systems of fault have affected the area (Fig. 10). Plutonic rocks from the Tarik Darreh area are placed within the volcanic arc to within plate’s environment in tectonic setting discrimination diagrams (Fig. 11). Zircon U-Pb dating results on the gabbroic rocks are shown in Table 2. Zircon grains through cathodoluminescence imaging show euhedral, clear crystals with no visible heritage cores. However, some of them have inclusions. Zircon U-Pb dating indicates that the gabbroic rocks formed at 215.5±0.9 Ma (late Triassic) (Fig. 12). Thus, it is obvious that the country rock (called Miankuhi Formation), must be older than the late Triassic plutonic rocks rather than Norian age as previously thought. The variation of major elements with SiO2 in the plutonic rocks from Tarik Darreh (Fig. 13) indicates that the primary magma of these plutonic rocks underwent fractional crystallization from gabbro to quartz monzodiorite. Geochemical characteristics such as low ratios of (La/Yb)N (

Introduction This research study is based on knowledge-driven approach to synthesize the different parameters which rule on the formation of carbonate hosted zinc and lead deposits. The analysis of available data sets of the north Irankuh district demonstrates the complexity of decision making due to the different anomalous prospects introduced by geophysical, geochemical and surface evidences. Five known deposit/active mines, namely Gushfil, Zone 1 Gushfil, Blind, Tapeh Sorkh and Zone 5 Romarmar with total geological resources quoted as 13.4 million tons at 5.53% combined lead and zinc (Fig. 10) were selected to be examined in order to asset a knowledge-driven approach to the exploration of carbonate hosted zinc and lead deposits. The diversity of geometry, mineralogy and host rock of the deposits is tightly confined by the parameters surrounding the genesis of MVT deposits such as genetics of solutions, temperature of deposit formation, tectonic channel ways, different episodes of deposition of sphalerite and galena, hydrologic system of area, solution direction, wall rock reactions (Leach et al., 2010), depth of solution penetration, solution response to the Magnesian regime and metal bearing. Materials, Methods, and Procedures The present study consists of detailed underground and surface mapping, reinterpretation of district geology, detailed logging of about 100000 meters’ diamond drilling, ore geology, tectonic settings, deposits geometry, geochemical and geophysical survey within 7 square kilometers of north Irankuh district between the Gushfil and Tapeh Sorkh deposits. Discussion and Results Five known deposits in the north Irankuh district occur in the area of an intense detachment faulting (Fig. 1 and Fig. 5). The Gushfil, Zone 1 Gushfil and Blind deposits occur in north Irankuh reverse fault and Tapeh Sorkh and Zone 5 Romarmar in the trust fault. The deposits are confined to a certain stratigraphic unit locally called K3D (Figs. 2 and 3). Widespread regional selective dolomitization shows an extensive lateral movement from NW to SE and the depth of dolomitization in certain units drastically decreases. Two main regimes of solutions initially started with sphalerite and they were subsequently followed by galena the later of which is found in the secondary porosity. Mineralogy of the deposits is simple but the pyrite amount of the deposits varies from 2% to 20% which reflects the higher temperature of the solutions responsible for sulphide precipitation (Marie et al., 2001), geometry of the deposits and their distance to the current topography effect on chargeability values (Fig. 20). Sparry dolomite is found in three types as barren, with pyrite and light color sphalerite that occur in country rocks of all deposits except for the blind deposits. They can be used as a guide, addressing potential deposits. EPMA analysis revealed a considerable amount of Cadmium, Silver, Antimony, Arsenic and Copper within Sphalerite and Galena minerals (Fig. 12). Because of the semiarid climate in the area the decomposition of sphalerite, galena (Hitzman et al., 2003) and carbonate host rock has caused widespread distribution of Zn, Pb, Ag, Cd, Sb, As, Cu, Mn, Mg, Fe and Ca in the secondary halo of the area. The soil samples have been studied based on the static and machine learning methods (Figs. 13–A and B) by different researchers (Zekri et al., 2019). The anomalous areas based on geochemical studies have been tested by core drilling and the results are considered to be negative even in the area called Zone 3 which coincides with both geochemical and geophysical anomallies. In a different approach to understand the structure of geochemical elements the distribution of Zn, Pb, Ag, Cd, Sb, As, Cu, Mn, Ba together with elements such as Mg, Fe and Ca has been compared (Figs. 14, 15 and 16). The soils are heavily polluted due to widespread mineralization and no background value (Reimann and De Caritat, 2012) can be recognized. The comparative analysis of element concentrations in 5 selected populations in the studied area (Fig. 15) did not show any signs that could help recognize important anomalies from the false anomaly. However, it seems that the sudden decrease of Mg content (Fig. 17–C) in the area of Zone 3 (Zekri et al., 2019) is meaningful. Two geochemical profiles of soil samples crossing along this population and the next one crossing an active mine (Zone 5 Romarmar) (Fig. 18) provide us with a better understanding of the important anomalies versus the false anomaly since in the false anomaly the increase of Zn, Pb, Ag, Cd, Sb, As, Cu coincides with a sudden drop of concentration of Mg, Fe and Ca (Figs. 18–A and B). Recognition of ore containing strata (Sangster, 1995) is very important (Figs. 2 and 3) in locating successful drill holes in the exploration of carbonate hosted zinc and lead deposits. Eventually the use of data driven methods even opting advanced machine learning methods is not properly sufficient to recognize productive areas and we recommended the knowledge -driven approach.

The rocks of the Robaie area located in the Torud-Chahshirin belt and south of Damghan, includes the Eocene andesite and trachyandesite rocks in which subvolcanic igneous rocks as stoke and dyke with diorite, monzonite and monzodiorite porphyry composition are intruded. The main textures of volcanic rocks are porphyritic characterized by plagioclase, hornblende and biotite phenocrysts as well as apatite and zircon as minor minerals. The rocks studied are mainly of shoshonitic nature and only one sample is considered as high-K calc-alkaline. Several line of evidence including LILE and LREE enrichment, HREE and HFSE depletion, high Th/Yb with negative anomalies of Ti, Nb and the position of the samples on the tectonic discrimination diagrams indicate that the volcanic rocks in discussion were emplaced into the subduction zone related to an active continental margin setting. The initial 87Sr/86Sr, 143Nd/144Nd ratios and (εNd)i value of andesite are 0.704445, 0.512691 and 2.29, respectively. All of these evidences confirm that the studied volcanic rocks were generated from partial melting of the mantle wedge above the subduction zone. Petrographic observations along with geochemistry of rare earth and trace elements suggest that the calc-alkaline affinity of the rocks studied and their parent magma from a subducted-related environment as well as crustal assimilation and fractional crystallization

Introduction The Cheshmeh Khuri area is located in the north of the Lut Block volcanic–plutonic belt, in eastern Iran, about 111 Km northwest of the city of Birjand. Extensive Tertiary magmatic activity in the Lut Block, is spatially and temporally associated with several types of mineralization events (Karimpour et. al., 2012). The episode of Middle Eocene to lower Oligocene (42–33 Ma) was very important in terms of magmatism and mineralization (Karimpour et. al., 2012). The North Khur area includes numerous cases of Cu±Pb±Zn vein-type mineralization, such as the Shikasteh Sabz, Mir-e-Khash, Rashidi, Shurk, Ghar-e-Kaftar, Howz-e-Dagh, as well as kaolin deposit (Cheshmeh Khuri area). We present and discuss alteration, ore petrography, geochemistry, fluid inclusion micro thermometry, and sulfur isotope geochemistry, which help clarify the ore genesis of the Cheshmeh Khuri area. Materials and methods The present study involves detailed field work and study of thin and polished sections from the intrusive rocks and ore samples under the optical microscope. Metal concentrations were analyzed at the IMPRC laboratory of Iran using the ICP-OES techniques on fifteen samples. Five samples were analyzed for Fire Assay analysis and four samples for XRD analysis at IMPRC laboratory of Iran. Twelve spot analyses (microanalyses) were performed on an X-ray Analytical Microscope at IMPRC laboratory. Doubly polished wafers (150 μm thick) were prepared from five samples taken from surface and trenches. Micro thermometric measurements were carried out using a Linkam THM 600 heating–freezing stage mounted on an Olympus TH4–200 microscope stage at the Ferdowsi University of Mashhad, Iran. Two pyrite samples from quartz-sulfide veinlet were analyzed for the sulfur isotope compositions after careful hand picking and purification at Iso–Analytical limited, United Kingdom. Discussion and results The main alterations consists of propylitic, argillic, quartz-sericite-pyrite and silicified. The mineralization is mainly observed as vein and is disseminated in quartz-sericite-pyrite, argillic- silicified and propylitic alteration zones and is disseminated in the argillic alteration zone. Pyrite is the only primary sulfide mineral in the area. Due to the great influence of weathering processes on the primary ore, secondary sulphide and oxide mineralization (malachite, azurite, chalcocite, covellite, goethite, and hematite) are widely spread and have finally created lithocap (Sillitoe, 1993; Sillitoe et. al., 1998). The maximum anomalies of copper (654 ppm) and lead (1622 ppm) are associated with quartz-sericite-pyrite alteration. Primary fluid inclusions of quartz in paragenesis with mineralization in quartz-sericite-pyrite zone, argillic-silicified zone and calcite in paragnesis with mineralization in propylitic zone have an average of homogenization temperatures of 321°C, 305 °C and 263 °C, respectively. Based on freezing studies, the average calculated temperature of last melting point of these is equal to 12, 11.6 and 7.9 wt.% NaCl, respectively. Homogenization temperature and salinity of the fluids shows a shifting trend from relatively high in quartz-sericite-pyrite zone to relatively low homogenization temperatures in the propylitic zone, which can be due to physicochemical changes in the fluid such as cooling and mixing with meteoric water (Naden et al. 2005). According to the textural evidence, boiling has also been effective during the evolution of the fluid. The amount of δ34S for pyrite has a range between 2.35 to 2.46 and the amount of δ34 equilibrium with pyrite has a range of 1.25 to 1.36 that show a magmatic origin for sulfur (Ohmoto and Rye, 1979; Lesage, 2011). The expansion of propylitic and argillic alteration zones on the surface, the limited quartz-sericite -pyrite zone, the absence of potassic alteration, the existence of lithocap, geochemical anomalies, the range of temperature and salinity of the fluid inclusion can be indicative of the upper part of a porphyry copper system. References Karimpour, M.H., Malekzadeh Shafaroudi, A., Stern, C.R. and Farmer, L., 2012. Petrogenesis of Granitoids, U–Pb zircon geochronology, Sr–Nd isotopic characteristic and important occurrence of Tertiary mineralization within the Lut Block, Eastern Iran. Journal of Economic Geology, 4(1): 1–27. (in Persian with English abstract) Lesage, G., 2011. Geochronology, Petrography, Geochemical constrain, and fluid characterization of the Buritica gold deposit. Ph.D. thesis, University of Alberta, Alberta, United State America, 152 pp. Naden, J., Killias, S.P. and Darbyshire, D.P.F., 2005. Active geothermal system with entrained seawater as modern analogs for transitional volcanic-hosted massive sulfide and continental magmato-hydrothermal mineralization: the example of Milos Island, Greece. Geology, 33(7): 541–544. Ohmoto, H. and Rye, R.O., 1979. Isotopes of sulfur and carbon: In: H.L. Barnes (Editor), Geochemistry of Hydrothermal Ore Deposits, Wiley Interscience, New York, pp. 509–567. Sillitoe, R.H., 1993. Epithermal models: Genetic types, geometrical controls and shallow features. Geological Association of Canada, Special Paper, 40(1): 403–417.

The Firouzeh mine is located in the Northwest of Neyshabour in the Khorasan Razavi province, Northeast of Iran, and eastern side of the Quchan-Sabzevar Cenozoic magmatic arc. Widespread magmatic activity in the Quchan-Sabzevar arc, is spatially and temporally associated with several types of mineralizations such as IOCG, Cu-Au porphyry and Kiruna types (Ghiasvand et al., 2016; Karimpour et al., 2011; Fatehi, 2014; Zarei et al., 2016). The aim of this investigation is to provide an understanding of the geology, alteration, mineralization, geochemistry, fluids evolution and genesis of the Firouzeh mine. Materials and methods Two hundred and fifty thin and polished sections were prepared for microscopic study. Twenty-nine samples were analyzed by X-ray fluorescence (XRF) method at the laboratory of Zar Azma company, Tehran, Iran. Twenty-one samples were analyzed by the X-ray Diffraction (XRD) method at the laboratory of Kansaran Binalood company, Tehran, Iran. Sixty samples were selected for 55-elemental analysis by composition of ICP-AES (Inductively coupled plasma atomic emission spectroscopy) and ICP-MS (Inductively coupled plasma Mass Spectrometry). Moreover, Sixty samples were selected for Au analysis by Aqua Regia Digestion at the SGS Laboratories, Canada. Six doubly polished sections of quartz mineralization were prepared for microthermometric analysis. Homogenization and last ice-melting temperatures were measured using a Linkam THMSG 600 combined heating and freezing stage at the Ferdowsi University of Mashhad. Result The Firouzeh mine contains various Middle-Eocene subvolcanic rocks as dykes which have intruded into Paleocene-Eocene volcanic rocks. Important altrations consist of silicified, argillic and carbonate among which silicified is the most extensive. Primary minerals are magnetite, specularite, pyrite, chalcopyrite and bornite and secondary minerals are hematite, alunite, covellite, turquoise and limonite. Mineralization has occurred in the cracks and fractures at the surface and in tunnels, mainly as disseminated, stockwork, vein-veinlet and hydrothermal breccia. Geochemical explorations showed anomalies of copper (up to ppm 1074), gold (up to ppb 699), iron (up to over percent 30), cerium (up to ppm 464), lanthanum (up to ppm 227), uranium (up to ppm 243) and cobalt (up to over ppm 10000) that has many similarities with IOCG type deposits (Corriveau, 2007; Zamora and Castillo, 2001; Marschik et al., 2000(. Fluid inclusions are relatively simple liduid+vapor types, with homogenization temperature from 147 to 278ºC and average temperature of 203ºC and Salinity containing 5.56 to 17.08 wt. percent NaCl equiv. which has resulted from fluids with KCl, CaCl2, MgCl2 and NaCl compositions. Mixing process between hot and saline fluid with cold and low saline fluid and also, boiling process can caused deposition of elements. Discussion Firouzeh mineral deposit has magmatic-hydrothermal source and is related to tertiary magmatic activities of subduction of Neothetys Sabzevar oceanic crust beneath the Turan crust. Fluid mixing has played an important role for precipitation during mineralization and includes the source of hot and saline magmatic fluids with high contents of metallogenic elements and the mixing with cold and low saline meteoric waters resulting in the formation of deposit (Bastrakov et al., 2007; Simard et al., 2006; Wilkinson, 2001; Beane, 1983). Based on geological characteristics, alteration, mineralization, geochemistry, geophysics and fluid inclusion studies, Firouzeh mine is a great mineralization of iron oxide copper-gold-U-LREE which has similarities to the hematite-dominant section of Olympic Dam IOCG deposit. Acknowledgments The Research Foundation of the Ferdowsi University of Mashhad, Iran, supported this study (Project No. 3/18303). We would like to thank the Iranian mineral processing research center and laboratories of Zar Azma, Kansaran Binalood, ACME and SGS. We also thank rural cooperation of Firouzeh mine for its liaison in field survey. References Bastrakov, E.N., Skirrow, R.G. and Davidson, G.J., 2007. Fluid evolution and origins of Iron Oxide Cu-Au prospects in the Olympic Dam district, Gawler craton, South Australia. Economic Geology, 102(8): 1415–1440. Beane, R.E., 1983. The Magmatic-Meteoric Transition. Geothermal Resources Council, California, Report 13, 253 pp. Corriveau, L., 2007. Iron oxide copper gold deposits: A Canadian perspective. In: W. Goodfellow (Editor), Mineral deposit of Canada: A synthesis of major deposit- types, district metallogeny, the evolution of geological provinces, and exploration methods. Geological Association of Canada Mineral deposits Division, Vancouver, pp. 307–328. Fatehi, H., 2014. Geology, mineralization and geochemistry of Jalambadan deposit, NW Sabzevar. M.Sc. Thesis, Ferdowsi University of Mashhad, Mashhad, Iran, 240 pp. (in Persian) Ghiasvand, A., Karimpour, M.H., Heidarian Shahri, M.R. and Malekzadeh Shafaroudi, A., 2016. Mineralization and ground magnetic survey for mineralization prospecting and identify of intrusive bodies in the Neyshabour Firouzeh mine, Khorasan Razavi province. Journal of Advanced Applied Geology, 20(6): 86–103. (in Persian) Karimpour, M.H., Malekzadeh Shafaroudi, A., Sfandiarpour, A. and Mohammadnejad, H., 2011. Neyshabour turquoise mine: The first IOCG-U-REE. Journal of Economic Geology, 2(3): 193–216. (in Persian) Marschik, R., Leveille, R.A. and Martin, W., 2000. La Candelaria and the Punta del Cobre district, Chile, Early Cretaceous iron oxide Cu-Au (-Zn-Ag) mineralization. In: T.M. Porter (Editor), Hydrothermal iron oxide copper-gold and related deposits, A global perspective. Australian Mineral Foundation, Adelaide, pp. 163–175. Simard, M., Beaudoin, G., Bernard, J. and Hupe, A., 2006. Metallogeny of the Mont-de-l’Aigle IOCG deposit, Gaspé Peninsula, Québec, Canada. Mineralium Deposita, 41(6): 607–636. Wilkinson, J.J., 2001. Fluid inclusions in hydrothermal ore deposits. Lithos, 55(1–4): 229–272. Zamora, R. and Castillo, B., 2001. Mineralizacio´ n de Fe-Cu-Au en el distritoMantoverde, Cordillera de la Costa, III Regio´n de Atacama, Chile. Proc 2ndCongrInt de Prospectores y Exploradores, Inst de Ingenieros de Minas del Peru´, Lima, Peru. Zarei, A., Malekzadeh Shafaroudi, A. and Karimpour, M.H., 2016. Geochemistry and genesis of iron-apatite ore in Khanlogh deposit, eastern Cenozoic Quchan-Sabzevar magmatic arc, NE Iran. Acta Geologica Sinica, 90(1): 121–137.

Introduction The study area is located in the northeast of Iran (the Khorasan Razavi province) and 28 km northwest of Bardaskan city and in position of 57˚ 46΄ to 57˚ 52΄ latitude and 35˚ 21΄ to 35˚ 24΄ longitude. The study area is a part of Taknar zone. The Taknar geological-structural zone is situated in the north Central Iranian microcontinental and it is a part of Lut block (Fig.1). Taknar plutonic complex that is situated in the Taknar structural zone is located in the northern part of Iranian microcontinent. Materials and methods Chemical analysis of REE and minor elements of samples of the Bornaward diorites and gabbro’s took place in the ACME Lab. in Vancouver, Canada, by the ICP-MS method (Table. 1). For the Bornaward diorite dating by the U-Pb method, zircon grains of material remaining in the sieve, Bromoform were isolated from light minerals by cleaning and were isolated with a minimum size of 25 microns, and then studies took place in the Crohn's Laser Lab Arizona (Gehrels et al., 2008). Measurement of Rb, Sr, Sm and Nd isotopes and (143Nd/144Nd)i , (87Sr/86Sr)i ratios and ƐNd (T=552), ƐNd (T=0), ƐSr (T=552) and ƐSr (T=0) took place in radioisotope Laboratory, University of Aveiro in Portugal. Discussion Geology of study area The study area forms the central part of the Bornaward plutonic complex. This complex is a granitoid assemblage including granite, granodiorite, tonalite and granophyre.tscentral part has been formed by intermediate and basic intrusive rocks such as diorite, quartz diorite and gabbro units (Fig. 2). From the genetic point of view, the intermediate and mafic rocks of the Taknar plutonic complex does not have any relationship with granitoid rocks of this assemblage, and they are related to a similar magmatic phase but are separated from this granitoid assemblage. However, these mafic and intermediate units are older than granitic units at the rim of the complex that are called Bornaward granite. Petrography The main minerals in the diorite and quartz diorite rocks are plagioclase and hornblende and we can see biotite in the quartz dioritic rocks. Quartz exist as tiny grains and anhedral and in the matrix rock. The amount of Quartz in the quartz diorites is 5 to 20%. Plagioclases usually have normal zoning and are highly altered to sericite. Most of the plagioclases were saussuritized. Altered minerals resulted from plagioclase and hornblende are sericite, epidote, chlorite, zoisite and clinozoisite. The main minerals in the gabbro are pyroxene, hornblende, and fine grains plagioclase. Minor minerals in the rocks are apatite, magnetite and other opaque. The main texture of intermediate and mafic rocks in this assemblage is medium granular to coarse grain and especially in the intermediate rocks and gabbro rocks, we can see scattered poikilitic, intersertal, sub-ophitic and porphyroid texture. Geochemistry The area diorite and gabbro is located locate in Tholeiitic and Calc-alkaline series (Fig. 9). Shand index (Al2O3/(CaO+Na2O+K2O)) is obtained under 1.1, in Metaluminous field (Fig. 7) and I-type granite field (Chappell and White, 2001). Based on the TAS diagram (Middlemost, 1985), all the diorite and gabbro samples are located in diorite, gabbro-diorite and gabbro-norite groups (Fig. 6). The diorite and gabbro’s show enrichment LREE and low ascending pattern ((La/Yb)N =1.40-6.12 and LaN =12.26-75.81). U-Pb zircon geochronology Measurement of U-Th-Pb isotopes of the Bornaward diorite zircons of BKCh-03 sample (Table 2) show that its age is related to 551.96±4.32 Ma ago (Upper Precambrian (Neoproterozoic) (Ediacaran) (Fig. 14). Sr-Nd isotopes The (87Sr/86Sr)i and (143Nd/144Nd)i content of Bornaward diorite and gabbro rocks is located in the range of 0.7038 to 0.7135 and 0.51203 to 0.51214, respectively (Tables 3 and 4). It shows that the diorite and gabbro rocks can be affected by hydrothermal alteration because their (87Sr/86Sr)i is above (Fig. 16). The numeral amounts of ƐNd(T=552) of Bornaward diorite and gabbro are 2.0 to 4.0. Petrogenesis The Bornaward diorite and gabbro rocks show a widespread enriched pattern of Rb, U, K, Pb, La and Th elements than chondrite, while Ba, Ti, Ta, Sr and Nb elements show reduction as a result of fractional crystallization (Fig. 11). The rocks of this complex are formed at the continental margin and VAG environment (Fig. 18) which is related to the subduction of the oceanic crust that exists between the Iranian microcontinent and the Afghan Block. Results This assemblage with age of Late Neoproterozoic is the result of extensive magmatism in the northern part of the Iranian microcontinent due to Katangahi orogeny event. The similar magmatism in the northern part of the Iranian microcontinent is existing as Khaf-Kashmar-Bardeskan volcano-plutonic belt. Based on the geochemical investigations, the magmatism of these rocks has been tholeiitic and calk-alkaline and have formed the coexistent rocks with I-type granites. Alumina saturation index for intermediate and mafic rocks of Bornaward complex is metalumina. These are medium-K rocks and enriched in the LILE such as Rb, Pb, U and Th while depleted of the Nb, Ti, Ta, Sr and Ba. Therefore, it shows that these rocks have resulted from the mixing by the lower crust. The low (87Sr/86Sr)i Bornaward diorite and gabbro rocks and the numeral amounts of Ɛ0Nd(present) of these rocks from -0.2 to 4.0 show that production of such intrusive masses can be attributed to the source of upper mantle or contaminated lower continental crust. Environment of formation of the intermediate and basic rocks of the Bornaward plutonic complex is active continental margin and volcanic arc environment. References Chappell, B.W. and White, A.J.R., 2001. Two contrasting granite types: 25 years later. Australian Journal of Earth Sciences, 48(4): 489–499. Gehrels, G.E., Valencia, V.A. and Ruiz, J., 2008. Enhanced precision, accuracy, efficiency, and spatial resolution of U–Pb ages by laser ablation– multicollector– inductively coupled plasma-mass spectrometry. Geochemistry, Geophysics, Geosystems, 9(3): 1–13. Middlemost, E.A.K., 1985. Magmas and Magmatic Rocks. An Introduction to Igneous Petrology. Longman, London, New York, 266 pp.

Introduction The Simorgh prospect area is located in 113 km southwest of the Nehbandan in South Khorasan province. This area is part of the Tertiary volcanic-plutonic rocks in the center of the Lut block. The Lut Block, which is located at the eastern part of the Central Iranian Microcontinent (CIM), is famous by its complex tectonic evolution and extensive magmatic activities with a range of interesting geochemistry. Extensive magmatic activities in Lut Block have produced several types of mineralization events (Karimpour et al., 2012). Around the Simorgh prospect area, various mineral deposits, including Cu-Mo porphyry Dehsalm in 90 km southwest of Nehbandan have been reported (Arjmandzadeh and Santos 2013) and Mahoor copper (Miri Beydokhti et al., 2015). Until now there has not been a detailed studies on the Simorgh prospect area especially on granitoids. In this study, we present field investigations, geology, alteration, mineralization, geochemical exploration, Petrogenesis, zircon U-Pb geochronology and Hf isotopes of sub-volcanic rocks in the Simorgh prospect area. Materials and methods 1- Preparation of 336 thin sections for the study of petrography, alteration and mapping of geological and alteration maps. 2- Preparation and study of twenty-five polished thin sections and thirty-two polished blocks for mineralization studies. 3- Analysis of forty-five chip composite samples in the Zar Azma laboratory by using the fire assay method for Au element and ICP-OES for thirty-four elements. The solubilization method of 4- Acid (1EX) was used. 4- Analysis of one hundred and sixty core samples in the Zar Azma laboratory by using the fire assay method for Au element and ICP-OES for 34 elements (method 1EX). 5- Chemical analysis of seventeen samples of syn-mineralization sub-volvanic intrusive rocks with at least alteration, by ICP-MS for thirty-one trace and rare earth elements with LF100 method (alkali fusion) at the AcmeLabs Laboratory. 6- Separation of three samples from syn-mineralization sub-volcanic intrusive rocks for U-Pb zircon geochronolg by Quadruple Laser-Ablation ICP-MS at the CODES, the Tasmania University of Australia. 7- Analysis of three samples of syn-mineralization sub-volvanic intrusive rocks for Lu-Hf isotopes with multi-collector ICP-MS at the CCFS of Macquarie University of Sydney, Australia. Discussion and results Petrographic studies indicated that the composition of sub-volcanic rocks in the Simorgh area are diorite porphyry and pyroxene diorite porphyry stocks with granite porphyry and granodiorite porphyry dikes. Several alteration zones such as: propylitic, argillic, silicified quartz-sericite-pyrite (QSP) and carbonate-quartz-sericite-pyrite (CQSP) based on field and laboratory studies are identified Major oxides analysis shows that intrusive units are metaluminous to peraluminus, calc-alkaline to high-K calc-alkaline. More of these rocks belong to the I-type granitoid (Chappell and White, 2001), and they have been formed in a volcanic arc granitoids (VAG) tectonic setting (Pearce et al., 1984). Mantle-normalized, trace-element spider diagrams display enrichment in large ion lithophile elements, such as Rb, Sr, K, and Cs, and depletion in high field strength elements, e.g., Nb, Ti, P. Enrichment of LREE versus HREE and enrichment of LILE and depletion in HFSE indicate magma formation in the subduction zone. In the subduction zones, high oxygen fugacity leads to the depletion of Ti. All of the intrusive rocks have a negative Eu anomaly. The amount of Eu/Eu* in sub-volcanic units of the Simorgh area varies from 0.49 to 0.91. Therefore, negative Eu anomaly can be evidence of the partial presence of plagioclase in the origin (Tepper et al., 1993). Three types of mineralization occur in this area such as: veinlet, disseminated and hydrothermal breccia among which hydrothermal breccia is the most important. Pyrite is the most sulfide mineralization in the sub-volcanic and hydrothermal breccias. Compositional variations of elements within the Simorgh prospect are as follows: Cu = 2-240 ppm, Mo = 0.5-49 ppm, Zn = 9-935 ppm, Pb = 7-582 ppm, ppm, As = 2-207 ppm and Au = 1-93 ppb. In the Simorgh area, zircon U-Pb geochronology was carried out on syn-mineralization sub-volcanic intrusive rocks. The age of two granite porphyry dikes are 25.37±0.56 Ma and 25.94±0.76 Ma and the age of pyroxene porphyry diorite is 24.85±0.51 Ma (Chattian). Diorite porphyry is pre-mineralization because it is cut by granite porphyry dikes and pyroxene diorite porphyry, so diorite porphyry is the oldest sub-volcanic intrusive rock in this area. The low positive values of εHf(i) indicate that the origin of these sub-volcanic intrusive rocks is mantle, which has low contamination with the crust. According to the above evidence, the sub-volcanic units of this area are related to porphyry systems, and the hydrothermal breccias are the main host rock mineralization in this system. This system does not have any valuable mineralization expect pyrite, from the surface to 180 m depth. References Arjmandzadeh, R. and Santos, J.F., 2013. Sr-Nd isotope geochemistry and tectonomagmatic setting of the Dehsalm Cu-Mo porphyry mineralizing intrusives from Lut Block, eastern Iran. International Journal of Earth Sciences, 103(1): 123–140. Chappell, B. and White, A., 2001. Two contrasting granite types: 25 years later. Australian Journal Earth Sciences, 48(4): 489–499. Karimpour, M.H., Malekzadeh shafaroudi, A., Farmer, G.L. and Stern, C.R., 2012. Petrogenesis of Granitoids, U-Pb zircon geochronology, Sr-Nd Petrogenesis of granitoids, U-Pb zircon geochronology, Sr-Nd isotopic characteristics, and important occurrence of Tertiary mineralization within the Lut block, eastern Iran. Journal of Economic Geology, 4(1): 1–28. (in Persian with English abstract) Miri Beydokhti, R., Karimpour, M.H., Mazaheri, S.A., Santos, J.F. and Klötzlid, U., 2015. U-Pb zircon geochronology, Sr-Nd geochemistry, petrogenesis and tectonic setting of Mahoor granitoid rocks (Lut Block, Eastern Iran). Journal of Asian Earth Sciences, 111(1): 192–205. Pearce, J.A., Harris, N.B.W. and Tindle, A.G., 1984. Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. Journal of Petrology, 25(4): 956–983. Tepper, J.H., Nelson, B.K., Bergantz, G.W. and Irving, A.J., 1993. Petrology of the Chilliwack batholith, North Cascades, Washington: generation of calc-alkaline granitoids by melting of mafic lower crust with variable water fugacity. Contributions to Mineralogy and Petrology, 113(3): 333–351.

Introduction Mississippi Valley-Type (MVT) deposits are epigenetic zinc and lead deposits with minor copper hosted by dolostone, limestone, and locally sandstone in platform carbonate sequences inboard of major orogenic belts (Leach and Sangster, 1993; Leach et al., 2010). The Irankuh-Ahangaran Belt, which is the most important Pb-Zn mineralized zone of Iran, is situated within the Sanandaj-Sirjan tectonic zone. This belt is 400 km in length and 100 km in width. Three deposits including Irankuh mininig district, Ahangaran and Hosseinabad deposits were studied in this article (Fig. 1). The aim of this research is study of thermal gradient of subducted slab and age of formation of Pb-Zn deposits at Irankuh-Ahangaran belt, which is contrary information has been published so far on the type and their formation. Also, chemistry of ore-fluid in MVT deposits and impact of dolomitic and shale host rock on paragenesis, alteration, style, reserves and grade of deposits were discussed.These parameters will certainly be useful for exploration of the hidden MVT type deposits in the Irankou-Ahangan belt. Result and Discussion The Irankuh mineralization is hosted by Cretaceous dolostone and minor Jurassic shale rocks as epigenetic. The constructive thrust fault, which has been cut the Jurassic and Cretaceous host rocks, has played a major role in the rising of fluid and formation of mineralization. Mineralization is occurred as replacement and open space filling (fault breccia, veinlets and cavity of rock) in dolostone and breccia, veinlet and open space filling in shale host rock. The mineral assembelages are Fe-rich sphalerite, Fe- and Mn-rich dolomite, ankrite, galena, minor pyrite, bituminous, calcite ± quartz ± barite within carbonate host rocks, whereas quartz, pyrite, Fe-rich sphalerite, galena, minor chalcopyrite, low Fe-dolomite, bituminous, ± barite ± calcite are important primary minerals at clastic hos rocks (Karimpour et al., 2018). The Ahangaran deposit is very similar to Irankuh in host rock, alteration, paragenesis, and form of mineralization. Thrust fault has a constructive role for occurrence of mineralization and later destructive strike slip and normal faults have caused the displacement and destruction of mineralization. The Hosseinabad deposit is hosted by Jurassic shale, siltstone, and sandstone rocks as vein-veinlets, breccia and open space filling with structural control. Alteratin consists of silicification, chlorite, bituminous, and minor siderite, dolomite and ankerite similar to mineralization hosted by shale in Irankuh district. The mineral assemblages are galena, Fe-rich sphalerite, pyrite, chalcopyrite and minor phyrotite. Due to the lack of a proper dolostone unit in the Husseinabad deposit, mineralization is concentrated in particular areas with low-grade and low-reserves. Based on lithology, alteration, mineralization style, structural control by thrust faults, mineral paragenesis, and comparison with differnet types of Pb-Zn deposits, all deposits of Irankuh-Ahangaran belt are MVT-type. Deep-seated thrust faults formed during the early stages of subduction (~ 70 to 75 Ma), and played an important role in the upward migration of hydrothermal fluids from the basement to shallow depths. The geochronology of pyrite in Irankuh district based on Re-Os method indicate age of Irankuh Pb-Zn mineralization is 66.5 ± 1.6 Ma (Liu et al., 2019). Since the thrust faults have been cut the Jurassic to Upper Cretaceous rocks, and according to the absoulte age determined in Irankuh, the mineralization of this belt have been formed in the age range of 66 to 56 million years ago, mainly in the Paleocene (Fig. 15). Karimpour and Sadeghi (2018) suggested the hydrothermal fluid originated from the dehydration of a hot and young oceanic subducted slab, which liberated Pb, Zn, and other metals, and may have removed metals from rocks and organic material of the continental crust. More than 90% of all the water within the oceanic slab was released in the depth zone of the forearc region (depth of 30 to 50 km) (Karimpour and Sadeghi, 2018). In the depth zone, Mg-rich silicate minerals (such as antigorite, hornblende, chlorite, talc) have broken and the produced fluid is rich in Mg and Fe (Fig. 17). The ore-fluid of MVT deposits is Si-poor and Fe- and Mg- rich. Such fluid is mineralized on the hosts of the dolstone (Irankuh and Ahangaran) or Shale-Siltstone (Hossein Abad, and part of Irankuh and Ahangaran). There are significant differences in the type of paragenesis, alteration, shape, dimensions, reserves and grade in the deposits of this belt, which is controlled by the host rock type. Based on all lithological evidence, alteration, shape of mineralization, existence of thrust faults, mineral paragenesis and specific geological and geographic location, it can be used to exploration of the hidden MVT deposits in this belt. References Karimpour, M.H., Malekzadeh Shafaroudi, A., Esmaeili Sevieri, A., Shabani, S., Allaz, J.M. and Stern, C.R., 2018b. Geology, mineralization, mineral chemistry, and ore-fluid conditions of Irankuh Pb-Zn mining district, south of Isfahan. Journal of Economic Geology, 9(2): 267–294. (in Persian with English abstract) Karimpour, M.H. and Sadeghi, M., 2018. Dehydration of hot oceanic slab at depth 30–50 km: KEY to formation of Irankuh-Emarat Pb-Zn MVT belt, Central Iran. Journal of Geochemical Exploration, 194: 88–103. Leach, D.L. and Sangster, D., 1993. Mississippi Valley-type lead-zinc deposits. Geological Association of Canadian. Specific Paper, 40: 289–314. Leach, D.L, Taylor, R.D., Fey, D.L., Diehl, S.F. and Saltus, R.W., 2010. A Deposit Model for Mississippi Valley-Type Lead-Zinc Ores, Chapter A of Mineral Deposit Models for Resource Assessment. U.S. Geological Survey, Reston, Virginia, Scientific Investigations Report 2010–5070–A., 64 pp. Liu, Y., Song, Y., Fard, M., Zhou, L., Hou, Z. and Kendricke, M.A., 2019. Pyrite Re-Os age constraints on the Irankuh Zn-Pb deposit, Iran, and regional implications. Ore Geology Reviews, 104: 148–159.

The Tannurjeh porphyry Au-Cu prospect area is located in the northeastern Kashmar, the Khorasan Razavi province, and central of the Khaf-Kashmar-Bardaskan magmatic belt. Geologically, the area is dominated by the Tertiary rhyolitic-rhyodacitic volcanic rocks, which are intruded by monzonitic to dioritic subvolcanic intrusive rocks. The texture in the most of the study igneous rocks is porphyry with fine groundmass and the main minerals are plagioclase, alkali feldspar, quartz, biotite, hornblende and magnetite. The monzonitic intrusions are the source of widespred mineralization and alteration, whereas the diorite is the later phase, which is devoid of mineralization. Using zircon U-Pb method, the age of monzonitic intrusive was determined at 39.8 Ma (Middle Eocene), geochemically as well as mineralogically, the igneous rocks of the area are calc-alkaline granitoids belonging to magnetite series (I-type) which were developed in subduction tectonic setting. The LREE enrichment relative to HREE and enrichment in K, Rb, Cs, Th, and U in comparison to Ti and Nb elements are observed in all of the samples studied. Eu negative anomalies and low Sr/Y ratios can be attributed to the presence of residual plagioclase in the source. (87Sr/86Sr)i (0.705673 and 0.705158), (143Nd/144Nd)i (0.512524 and 0.512570), and εNdi (-1.22 and -0.32) values indicate magma is derived from mantle wedge above subducted slab, which is assimilated with upper crust. Finally, the Eocene is an important metallogenic episode, particuarly for Au and Cu, in NE of Iran.

The Golgohar iron mine is located at 55 km southwest of Sirjan in the Sanandaj-Sirjan structural zone. The host rocks of the ore deposit include metamorphosed rocks in green schist and amphibolite facies. The mineralization is massive or disseminated in adjacent rocks. The metabasic rocks are classified into amphibolite, epidote amphibolite, epidote-biotite amphibolite and biotite amphibolite types. Base on major, trace, and rare earth elements, the protolithsof these rocks are basic igneous rocks varying from basalt, basaltic andesite, trachy basalt, basaltic trachy andesite compositions. The trace elements pattern shows enrichment in large-ion lithophileelements and depletion in high field strength elements, suggesting their island arc signatures. LREEs enrichment and relatively flat HREEs patterns further support this interpretation. According to geochemical data these rocks were derived from depleted mantle that was contaminated by the melts of subducted sediments. The relative age of these rocks does not match with the tectonic setting. It seems that the Neo-Tethyan subduction along the northern subduction zone caused the emplacement of the study rocks in the Upper Triassic time. In this case, geochronological data may be helpful.

Introduction Kuh Zar Au-Cu deposit is located in the central part of the Torud-Chah Shirin Volcanic-Plutonic Belt, 100 km southeast of the city of Damghan. Mineralization including quartz-base metal veins are common throughout this Cenozoic volcano-plutonic belt (Liaghat et al., 2008; Mehrabi and Ghasemi Siani, 2010). The major part of the study area is covered with Cenozoic pyroclastic and volcanic rocks that are intruded by subvolcanic rocks. This paper aims to study the geological, geochemical and petrogenesis of the area using exploration keys for new mineral deposits in the Torud-Chah Shirin zone. Materials and methods To better understand the geological units and identify the alteration zones of the area, 200 rock samples were collected from the field and 132 thin sections with 15 polished thin sections were prepared for petrography and mineralization studies. Ten samples of intrusions with the least alteration were analyzed using the XRF at the East Amethyst Laboratory in Mashhad, Iran. These samples were also analyzed for trace and rare earth elements using ICP-MS, following a lithium metaborate/tetraborate fusion in the Acme Analytical Laboratories Ltd, Vancouver, Canada. 137 geochemistry samples were prepared by the chip composite method of alteration and mineralization zones and were analyzed in the Acme laboratory by Aqua Regia AQ250. Results The geology of the area consists of pyroclastic (crystal tuff) and volcanic rocks with andesite and latite composition, which were intruded by subvolcanic intrusive rocks with porphyritic texture and monzonitic composition. Monzonite rocks were intruded by younger subvolcanic units with dioritic composition. The intrusion of monzonitic pluton and stocks led to the formation of QSP, propylitic, carbonate and silicification-tourmaline broad alteration zones in the area. Monzonite rocks accompanied with disseminated mineralization of about 1 to 10% of pyrite and these sulfides have been converted to secondary iron oxides such as goethite, hematite and limonite. Lithogeochemical exploration revealed Au (up to 598 ppb), Ag (up to 3747 ppb), Cu (up to 679 ppm), Pb (up to 1427 ppm) and Zn (up to 1013 ppm) anomalies. Based on geochemical studies, intrusive rocks have characteristics of high-K Calc-alkaline to slightly shoshonitic and they are within metaluminous to the slightly peraluminous range. Enrichment of LREE versus HREE, enrichment of LILE and depletion in HFSE indicate that the magma was formed in the subduction zones. The negative Eu anomaly is due to the presence of plagioclase as a residual mineral in the magma source. The parent magma is probably formed by the partial melting of amphibolites. The presence of monzonite porphyry source rock, QSP and propylitic alterations, pyrite disseminated mineralization and geochemical anomalies of Au and Cu in the Kuh Zar deposit represents Au-Cu porphyry mineralization in the area. Discussion Tectonic setting discrimination diagrams (Pearce et al., 1984) show that subvolcanic rocks plot almost on the fields of the volcanic arc granites (VAG). In the Rb/Zr vs. Nb diagram from (Brown et al., 1984), the samples are plotted in the field of primitive island arc/continental margin arc. The Torud-Chah Shirin Belt is a part of the Alborz magmatic assemblage (AMA). The AMA has been interpreted to represent the subduction of the Neo Tethyan oceanic lithosphere beneath the Central Iranian continental microplate and the subsequent continental collision of the Arabian and Iranian microplates in the late Cretaceous-early Cenozoic (Berberian and Berberian, 1981; Berberian et al., 1982; Alavi, 1994; Golonka, 2004). Acknowledgement This study has been supported by the Research Foundation of the Ferdowsi University of Mashhad, Iran (Project No. 27126.3). The authors would like to acknowledge the East Amethyst Laboratory for XRF analysis. We also thank the Gold Company of Iran for providing conditions for camping and accommodation. References Alavi, M., 1994 .Tectonics of the Zagros orogenic belt of Iran: new data and Interpretations. Tectonophysics, 22(1): 211–238. Berberian, F. and Berberian, M., 1981. Tectono-plutonic episodes in Iran. In: F.M. Delany and H.K. Gupta (Editors), Zagros Hindukosh. Himalaya Geodynamic Evolution. American Geophysical Union, Washington DC, pp. 5–32. Berberian, F., Muir, I.D., Pankhurst, R.J. and Berberian, M., 1982 .Late Cretaceous and early Miocene Andean type plutonic activity in northern Makran and central Iran. Journal of the Geological Society, 139(5): 605–614. Brown, G.C., Thorpe, R.S. and Webb, P.C., 1984. The geochemical characteristics of granitoids in contrasting arcs and comments on magma sources. Journal of Geological Society, 141(3): 413–426. Golonka, J., 2004. Plate tectonic evolution of the southern margin of Eurasia in the Mesozoic and Cenozoic. Tectonophysics, 381(1-4): 235–273. Liaghat, S., sheykhi, V. and Najjaran, M., 2008. Petrology, gheochemistry and genesis of Baghu turquoise, Damghan. Journal of Science, University of Tehran, 34(2): 133–142. (in Persian with English abstract) Mehrabi, B. and Ghasemi Siani, M., 2010. Mineralogy and economic geology of Cheshmeh Hafez polymetallic deposit, Semnan province, Iran. Journal of Economic Geology, 2(1): 1–20. (in Persian with English abstract) Pearce, J.A., Haris, N.B.W. and Tindle, A.G., 1984. Trace element discrimination diagrams for the tectonic interpretation of granitic rocks, Journal of Petrology, 25(4): 956–983.

Introduction The Hamech prospect area is located in the eastern Iran, 85 kilometers southwest of Birjand. The study area coordinates between 58¬¬˚¬53΄¬00 ˝ to 59˚¬00΄¬00˝ latitude and 32˚¬22΄¬30 ˝ to 32˚¬26΄¬00˝ longitude. Due to the high volume of magmatism and the presence of geo-structure special condition in the Lut Block at a different time, a variety of metal (copper, lead, zinc, gold, etc.) and non-metallic mineralization has been formed (Karimpour et al., 2012). The studied area (Hamech) includes Paleocene-Eocene igneous outcrops which contain a wide range of subvolcanic bodies (diorite to monzonite porphyry) associated with mafic intrusives, volcanic units (andesite), volcaniclastic and sedimentary rocks. Material and Methods This study was done in two parts including field and laboratory works. Sampling and structural studies were done during field work. Geological and alteration maps for the study area were also prepared. 200 thin and 60 polished sections for petrographic purpose were studied. The number of 200 thin sections and 60 polished sections were prepared and studied in order to investigate petrography and mineralogy. Major oxides (XRF method- East Amethyst Laboratory in Mashhad), rare earth elements and trace (ICP-MS method-ACME Laboratory in Vancouver, Canada) elements were analyzed for 13 samples that included subvolcanic units and intrusive bodies. Data processing and geological and alteration mapping is done by the GCD.kit and Arcgis software. Discussion and Results Based on lab work and XRF analysis, the rocks in the area are composed of intrusive-subvolcanic bodies and volcanic rocks (andesite, trachyandesite and dacite) together with volcano-classic and sedimentary rocks. Also, alteration zones consist of a variety of argillic, silicified, quartz-sericite-pyrite (QSP), propylitic and carbonate. Igneous rock textures are mainly porphyritic for sub-volcanic and granular for intrusive bodies. Phenocrysts mainly consist of plagioclase and hornblende dominated with minor of biotite and pyroxene. XRF studies and output charts show that rocks include monzonite, diorite, gabbro and gabbroic diorite. Intermediate subvolcanic units (monzonite, diorite) and mafic intrusives (gabbro and gabbroic-diorite) are related to high-potassium calc-alkaline (K2O between 2.42 to 4%) and tholeiitic (K2O between 0.15 to 0.27%) series, respectively. Subvolcanic units belong to the I-type granitoid (Chappell and White, 2001). Mantle normalized , trace-element spider diagrams display enrichment in LREE, such as Rb, Sr, K, and Cs, and depletion in HREE, e.g., Nb, Ti, Zr that indicate magma formed in the subduction zone. Nb depletion (less than 6 ppm, between 0.5 to 5.2 ppm) in subvolcanic bodies represents a volcanic arc granitoids (VAG) tectonic setting that is related to the subduction zone (Pearce et al., 1984). Also, this reduction shows that these rocks are derived of oceanic crust (Wilson, 1989). Enrichment in LREE and depletion of HREE with a low (La/Yb)N ratio in the Hamech subvolcanic rocks (6/85 to 8/13) could represent a low degree of mantle partial melting (Wass and Rogers, 1980). Zr/Nb ratio of more than 10 for Hamech rocks (between 21 and 35 for intermediate subvolcanic and 67 to 72 for mafic bodies) indicates that parental magma has minimal crustal contamination (Karimpour et al., 2012). Sr enrichment (between 646 to 1124) and low negative Eu anomaly (Eu/Eu* ratio between 0.81 to 1/02) show that plagioclase is rare (or is not present) as residue mineral in the source and melt conditions have been in oxidation state (Tepper et al., 1993). Based on Sm/Yb vs. La/Sm (Shaw, 1970) and Ce/Yb vs. Sm/Yb (Wang et al., 2002) diagrams, parent magma is composed of 1 to 5% spinel-garnet lherzolite partial melting (with small amounts of garnet) at a depth between 65 to 67 km (upper mantle) for subvolcanic units and 5 to 20% spinel lherzolite partial melting (depletion mantle-NMORB) with a depth of less than 55 km for mafic bodies. Suitable tectonic setting, existence of subvolcanic units with intermediate composition, magnetic activity with the nature of calc-alkaline and oxidants, data from major and REE studies, mineralization as disseminated and veinlets with high secondary iron oxides in surface show suitable conditions of porphyry and epithermal mineralization in the Hamech prospect area. References Chappell, B.W. and White, A.J.R., 2001. Two contrasting granite types, 25years later. Australian Journal of Earth Sdiences, 48(4): 489–500. Karimpour, M.H., Malekzadeh Shafaroudi, A., Farmer, L. and Stern, C.R., 2012. Petrogenesis of Granitoids, U-Pb zircon geochronology, Sr-Nd Petrogenesis of granitoids, U-Pb zircon geochronology, Sr-Nd isotopic characteristics, and important occurrence of Tertiary mineralization within the Lut block, eastern Iran. Journal of Economic Geology, 4(1): 1–27. (in Persian with English abstract) Pearce, J.A., Harris, N.W. and Tindle, A.G., 1984. Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. Journal of Petrology, 25(4): 956–983. Shaw, D.M., 1970. Trace element fractionation during anataxis. Geochimica et Cosmochimica Acta, 34(2): 237–243. Tepper, J.H., Nelson, B.K., Bergantz, G.W. and Irving, A.J., 1993. Petrology of the Chilliwack batholith, North Cascades, Washington: generation of calc-alkalinegranitoids by melting of mafic lower crust with variable water fugacity. Contributions to Mineralogy and Petrology, 113(3): 333–351. Wang, K., Plank, T., Walker, J.D. and Smith, E.I., 2002. A mantle melting profile across the Basin and Range, SW USA. Journal of Geophysical Research: Solid Earth, 107(B1): 5–21. Wass, S.Y. and Rogers, N.W., 1980. Mantle metasomatism- precursor to alkaline continental volcanism. Geochimica et Cosmochimica Acta, 44(11): 1811–1823. Wilson, M., 1989. Igneous Petrogenesis. Chapman and Hall, London, 466 pp.

The Zeber Kuh prospect area is located southwest of Bardaskan, South Khorasan province, in the northeastern Iran. Lithologically, the area includes Rizu and Soltanieh Formations metamorphosed carbonate rocks, which were intruded by syenogranitic and syenodioritic intrusions. Field observations and laboratory studies such as structural controls of orebody, metasomatic replacement and formation of low temperature H2O-bearing minerals, and the occurrence of magnetite and pyrite associated with chlorite, epidote, calcite, and quartz indicate that the iron mineralization is low temperature skarn-type. The source of Fe mineralization is probably a younger intrusive rock at depth. Hydrothermal ore fluid was ascended within fault zone and/or contact between the intrusive rock and the carbonate unit and generated orebody. Iron grade ranges from 54 to 65 wt.% and sulfur value is > 3 wt.%. Magnetite chemistry and Ti, V, Al, Mn, Ni, and Cr contents are similar to skarn deposit. Biotite syenodiorite host rock has hypidiomorphic granular texture and it consists of plagioclase, K-feldspar, biotite, and apatite minerals. Chemically, this intrusive rock is K-series alkaline type, which was generated in within plate zone. This magma is characterized by strong enrichment in LREE, LILE (Rb, Cs, Ba, and K), HFSE (Nb, Zr, and Ti), and P elements. The primary magma is produced by low degree partial melting of garnet lherzolite from asthenospheric to boundary of asthenospheric-lithospheric mantle.

Introduction The Irankuh mining district area located at the southern part of the Malayer-Isfahan metallogenic belt, south of Isfahan, consists of several Zn-Pb deposits and occurrences such as Tappehsorkh, Rowmarmar 5, Kolahdarvazeh, Blind ore, and Gushfil deposits as well as Rowmarmar 1-4 and Gushfil 1 prospects. Based on geology, alteration, form and texture of mineralization, and paragenesis assemblages, Pb-Zn mineralization is Mississippi-type deposit (Rastad, 1981; Ghazban et al., 1994; Ghasemi, 1995; Reichert, 2007; Timoori-Asl (2010); Ayati et al., 2013; Hosseini-Dinani et al., 2015). Geology of the area consists of Jurassic siltstone and shale and different types of Cretaceous dolostone and limestone. The aim of this research is new geological studies such as revision of old geologic map, study of different types of textures and mineral assemblages within carbonate and clastic host rocks, and chemistry of galena, sphalerite, and dolomite. Finally, we combined these results with isotopic and fluid inclusion data and discussed on ore-fluid conditions. Materials and Methods In order to achieve the aims of this work, at first field surveying and sampling were done. Then, 200 thin and 70 polished thin sections were prepared. Some of the samples were selected for microprobe analysis and galena and sphalerite minerals were analyzed by using JEOL- JAX-8230 analyzer at Colorado University, USA. The chemistry of dolomite and fluid inclusion data are used after Boveiri Konari and Rastad (2016) and stable isotope is used after Ghazban et al. (1994). Discussion The Irankuh mineralization is hosted by carbonate rocks (dolostone and limestone) and minor clastic rocks as epigenetic. Mineralization has occurred as breccia, veinlet, open space filling, spoted, dessiminated, and replacement (carbonate hosted rock). The mineral assemblages are Fe-rich sphalerite, galena, minor pyrite, Fe- and Mn-rich dolomite, bituminous, ankrite, calcite ± quartz ± barite within carbonate host rocks, whereas Fe-rich sphalerite, galena, pyrite, minor chalcopyrite, low Fe-dolomite, quartz, bituminous, ± barite ± calcite are important primary minerals at clastic host rocks. There is positive correlation between Ag and Sb values within galena mineral. Sb/Bi ratio in galena is up to 20, which is an indicator of low temperature deposits (Malakhov, 1968). The Irankuh homogenization temperature (170 to 260 ºC) is higher than that of US Mississippi-type deposits (80 to 120 ºC). Based on comparison of Th and Fe and Cd contents in sphalerite from Irankuh and US deposits (Viets et al., 1992), homogenization temperature of deposit has a positive relation with Fe values and a negative relation with Cd contents in sphalerite. Fe content in Irankuh sphalerite has reached up to 5% and Cd value is lower than 2000 ppm. In addition, carbonate hosted rock hydrothermal dolomites that are Fe-rich and ankrite have formed at some places. The evidence shows that Irankuh ore-fluid is Fe-rich. However, clastic hosted rock hydrothermal dolomites are low-Fe due to reaction of Fe and S resulting in pyrite formation. Based on O isotope (16–19 ‰) value from hydrothermal dolomites (Ghazban et al., 1994), ore-fluid has been derived from continental crust. Results Fe-rich sphalerite and dolomite and ankrite are the most important characteristics of Irankuh mining district. Temperature and Fe-rich nature of ore-fluid and mineralogy signatures of Irankuh area can be used for exploration of this type of mineralization in Iran and the world. The Irankuh mining district is MVT type mineralization. Acknowledgements The Research Division of the Ferdowsi University of Mashhad, Iran, supported this study (Project No. 40221.3). Thanks to Bama Co. (especially Mr. Eslami) for the collaborations. References Ayati, F., Dehghani, H., Mokhtari, A.R. and Mojtahedzadeh, H., 2013. Geochemistry and mineralogy studies of Gushfil Pb-Zn deposit, Irankuh, Isfahan. Analytical and Numerical Methods in Mining Engineering, 6: 83-91 (in Persian). Boveiri Konari, M. and Rastad, E., 2016. Nature and origin of dolomitization associated with sulphide mineralization: new insights from the Tappehsorkh Zn-Pb (-Ag-Ba) deposit, Irankuh Mining District, Iran. Geological Journal, DOI: 10.1002/gj.2875 Ghasemi, A., 1995. Facies analysis and geochemistry of Kolah-Darvazaeh, Goud-Zendan, and Khaneh-Gorgi Pb-Zn deposits from south of Irankuh. M.Sc. thesis, Tarbiat Modares University, Tehran, Iran, 158 pp. (in Persian) Ghazban, F., McNutt, R.H. and Schwarcz, H. P., 1994. Genesis of sediment-hosted Zn-Pb-Ba deposits in the Irankuh district, Esfahan area, west-central Iran. Economic Geology, 89: 1262-1278. Hosseini-Dinani, H., Aftabi, A., Esmaeili, A. and Rabbani, M., 2015. Composite soil-geochemical halos delineating carbonate-hosted zinc–lead–barium mineralization in the Irankuh district, Isfahan, west-central Iran. Journal of Geochemical Exploration, 156: 114-130. Malakhov, A.A., 1968. Bismuth and antimony in galena, indicators of conditions of ore deposition. Geokhimiya, 11: 1283-1296. Rastad, E., 1981. Geological, mineralogical and ore facies investigations on the Lower Cretaceous stratabound Zn – Pb – Ba – Cu deposits of the Irankuh mountain range, Isfahan, west central Iran. Ph.D. thesis, Heidelberg University, Heidelberg, Germany, 334 pp. Reichert, J., 2007. A metallogenetic model for carbonate-hosted non-sulphide zinc deposits based on observations of Mehdi Abad and Irankuh, Central and Southwestern Iran. Ph.D. thesis, Martin Luther University Halle Wittenberg, Halle, Germany, 152 pp. Timoori-Asl, F., 2010. Sedimentology and petrology of Jurassic deposits and Basinal brines studies in formation of Irankuh deposit. M.Sc. thesis, Isfahan University, Isfahan, Iran, 120 pp. (in Persian) Viets, J.G., Hopkins, R.T. and Miller, B.M., 1992. Variation in minor and trace metals in sphalerite from Mississippi Valley-type deposits of the Ozark Region: genetic implications. Economic Geology, 87:1897–1905.

Introduction The Iju porphyry copper deposit is located in the southern part of the Urumieh-Dokhtar magmatic arc (Dehaj-Sarduieh belt) within the Kerman copper belt (Dimitrijevic, 1973). The Porphyry Copper mineralization in the Iranian plate occurs dominantly along the Urumieh-Dokhtar arc, which has resulted from the subduction of the Arabian plate beneath the central Iran and the closure of the Neo-Tethys Ocean during the Alpine orogeny (Hassanzadeh, 1993). The Iju porphyry copper deposit with 25 million tons of ore reserves is one of the main copper deposits within the Kerman copper belt. The mining area is composed of upper Miocene volcanic and subvolcanic rocks (mineralized and barren subvolcanic rocks) and quaternary deposits. Two hydrothermal alteration zones of quartz-sericite-pyrite and propylitic zones can be identified in the Iju area. The copper mineralization in the Iju deposit occurs as disseminated, stockwork and hydrothermal breccia. In the hypogene zone, the mineral paragenesis include chalcopyrite, pyrite, with minor occurrences of bornite and magnetite. This paper reports geological, mineralogical, fluid inclusion and S isotope data from the Iju deposit in order to investigate ore-bearing fluids’ characteristics and the mechanisms of ore deposition. Materials and methods Fifteen samples of syngenetic quartz+pyrite bearing veinlets within the quartz-sericite-pyrite zone were selected from different depths across the seven boreholes. Quartz was used for double-polished thin sections and pyrite was used for sulfur isotope analysis. Fluid inclusion studies were performed using the Linkam cooling and heating stage, the THMSG 600 model. The syngenetic pyrite with thermometry quartz sample was used for the sulfur isotope experiments. Stable isotope analysis was performed at the Hatch Stable Isotope Laboratory in the University of Ottawa, Canada. Results The fluid inclusions of the Iju deposit represent a wide range in the homogenization temperatures between 140 to 480°C and salinity between 0.18 to >52.99 wt.% NaCl equiv., which are most similar to the results of the other Iranian porphyry copper deposits. Being located in the quartz-sericite-pyrite alteration zone, the results of thermometry indicates that ore deposition in the Iju deposit has occurred via mixing of magmatic and surface fluids. Variations in salinity and paragenesis of the saline multiphase fluid inclusions and two-phase gas-rich fluid inclusions indicate the occurrence of boiling phenomenon in some samples of the Iju deposit. The amount of δ34S for pyrite has a limited range close to zero (average, 0.229‰) that shows a magmatic origin for sulfur. Considering the presence of subvolcanic rocks, the type and extension of alteration zones, the structure and texture of ore bodies, thermometry results of fluid inclusions and sulfur isotope values, the Iju deposit is similar to porphyry copper deposits. Discussion In the quartz-sericite-pyrite zone, three main groups of veinlets have been identified. The quartz+pyrite veinlets are more abundant than the other types and they were selected for fluid inclusions and stable isotope studies. Petrographic studies of fluid inclusions identifies two groups of fluids including: 1- fluid inclusions without the halite phase, including the types L+V, L+V+S1 and (L+V+S1+S2, that is secondary), 2- fluid inclusions with halite phase, including the types L+V+H, L+V+H+S1, L+V+H+S1+S2 and L+V+H+S1+An. Homogenization temperature and salinity for the fluid inclusions without halite phase are as follows: 140 to 380°C and 0.18 to 24 wt.% NaCl (Fig. 8A and C) and for the fluid inclusions with halite phase they range from 230 to 480°C and 30 to 52 wt.% NaCl (Fig. 9A, B and D), In addition, the pressure and depth for the fluid inclusions containing halite phase are 750 bar and 3500 m on the average. Fluid inclusions available at the quartz veinlets of porphyry copper deposits can be formed in a wide range of chemical composition and under different temperature and pressure conditions (Rusk and Reed, 2008). The wide range in fluid inclusions data of the Iju deposit can be justified by physicochemical changes in the fluid as it is boiling and mixing with the surface fluids. Cooling, fluids mixing, boiling and fluid-rock reaction play important roles in the settling of chalcopyrite from the hydrothermal fluid and the dilution of saline ore-bearing fluids can cause the formation of copper ores from the ore-bearing fluid (Ulrich et al., 2002). Pyrite δ34S value ranges from -0.86 to +1.27‰ (average, +0.22‰) and the δ34SH2S value of the syngenetic fluid with pyrite ranges from -0.23 to -2.36‰ (average, -1.17‰). The limited and near zero range that is observed about δ34S value of the sulfur minerals indicates the controlling role of magmatic processes in the mineralization events (Chen et al., 2009). Acknowledgments This article is related to Project No. 27124.3 dated 2015, 2, 7 at the Ferdowsi University of Mashhad. We are thankful to and appreciate the Research and Development center of National Iranian Cu Industries (Shahr-e-Babak, Meiduk), especially S.M. Mousavi, for the financial support of this project and the necessary proceedings. References Chen, Y.J., Piranjno, F., Li, N., Guo, D.Sh. and Lai, Y., 2009. Isotope systematica and fluid inclusion studies of the Qiyugou breccia pipe- hosted gold deposit, Qinling Orogen, Henan province, China: Implication for ore genesis. Ore Geology Reviews, 35(2): 245-261. Dimitrijevic, M.D., 1973. Geology of Kerman region. Geological Survey of Iran, Tehran, Report No. Yu/52, 334 pp. Hassanzadeh, J., 1993. Metallogenic and tectonomagmatic events in the SE sector of the Cenozoic active continental margin of central Iran (Shahr e Babak area, Keman Province). Ph.D. thesis, University of California, Los Angeles, America, 204 pp. Rusk, B.G. and Reed, M.H., 2008. Fluid inclusion evidence for magmatic-hydrothermal fluid evolution in the porphyry copper- molybdenum deposit at Butte, Montana. Economic Geology, 103(2): 307-334. Ulrich, T., Gunther, D. and Heinrich, C.A., 2002. The evolution of a porphyry Cu-Au deposit, based on LA-ICP-MS analysis of fluid inclusions: Bajo de la Alumbrera, Argentina. Economic Geology, 97(8): 1889-1920.

Introduction The Shah Soltan Ali area is located 85 km southwest of Birjand in the South Khorasan province. This area is part of the Tertiary volcanic-plutonic rocks in the east of the Lut block. The Lut block is bounded to the east by the Nehbandan and associated faults, to the north by the Doruneh and related faults (Sabzevar zone), to the south by the Makran arc and Bazman volcanic complex and to the west by the Nayband Fault. The Lut block is the main metallogenic province in the east of Iran (Karimpour et al., 2012), that comprises of numerous porphyry Cu and Cu–Au deposits, low and high sulfidation epithermal Au deposits, iron oxide deposits, base-metal deposits and Cu–Pb–Zn vein-type deposits. The geology of Shah Soltan Ali area is dominated by volcanic rocks, comprised of andesite and basalt, which are intruded by subvolanic units such as monzonite porphyry, monzodiorite porphyry and diorite porphyry. Materials and methods 1. 170 thin sections of the rock samples as well as 25 polished and thin polished sections were prepared for petrography, alteration and mineralization. 2. Twenty five samples were analyzed for Cu, Pb, Zn, Sb, Mo and As elements by the Aqua regia method in the Zarazama laboratory in Tehran, Iran. 3. Nine samples were analyzed for trace elements [including rare earth elements (REEs)]. As a result of these analyses, trace elements and REE were determined by inductively coupled plasma mass spectrometry (ICP-MS) in the ACME Analytical Laboratories (Vancouver) Ltd., Canada. 4. Ten samples were analyzed for major elements by wavelength dispersive X-ray fluorescence spectrometry in the East Amethyst laboratory in Mashhad, Iran. 5. Five samples were analyzed for Firre Assay analysis in the Zarazma Laboratory in Tehran, Iran. 6. The results of XRD analysis were used for 4 samples. Discussion and results Petrographic studies indicate that subvolcanic rocks consist of diorite porphyry, monzonite porphyry and monzodiorite porphyry. Based on field and lab work several alteration zones such as: quartz–sericite–pyrite (QSP), propylitic, argillic, silicified, sericitic and carbonate were identified. Geochemical studies show that intrusive units are metaluminous, high calcalkalic to shoshonitic. These rocks belong to the I-type granitoid (Chappell and White, 2001), and they have formed in a volcanic arc granitoids (VAG) tectonic setting (Pearce et al., 1984). Mantle-normalized, trace-element spider diagrams display enrichment in large ion lithophile elements, such as Rb, Sr, K, and Cs, and depletion in high field strength elements, e.g., Nb, Ti, Zr. Enrichment of LREE versus HREE and enrichment of LILE and depletion in HFSE indicate magma formed in the subduction zone. Negative Nb and Ti anomalies are recognized as a fingerprint of a subduction process (Nagudi et al., 2003). All of the intrusive rocks have a weak negative Eu anomaly (Eu/Eu*=0.82–0.94) (Tepper et al., 1993), and a low ratio of (La/Yb)N. The magmatic source of intrusive rocks had been generated from 1% to 5% of partial melting of garnet-spinel lherzolite (Aldanmaz et al., 2000). In the south area, four types of mineralization such as: veinlet to vein, disseminated, hydrothermal breccia and stockwork occur from which stockwork is the most important type of mineralization. The veinlets that were found within the stockwork zone are:1) pyrite + chalcopyrite, 2) quartz + pyrite ± chalcopyrite, 3) quartz ± pyrite. Compositional variations of elements within the Shah Soltan Ali area are as follows: Cu = 30-454 (ppm), Zn = 27-279 (ppm), Pb = 11- 70 (ppm), Sb = 0.9-152 (ppm), Au= 5-128 (ppb), As = 7-203 (ppm). There is a high concentration of Cu – Zn – Au and Sb that is associated with the high density of veinlets in the quartz-sericite-pyrite zone in the southeast of Shah Soltan Ali area. Based on the obtained data, the Shah Soltan Ali area is a part of the porphyry Cu-Au deposit. References Aldanmaz, E., Pearce, J.A., Thirlwall, M.F. and Mitchell, J.G., 2000. Petrogenetic evolution of late Cenozoic, post-collision volcanism in western Anatolia, Turkey. Journal of Volcanology and Geothermal Research, 102(1): 67–95. Chappell, B.W. and White, A.J.R., 2001. Two contrasting granite types, 25years later. Australian Journal of Earth Sdiences, 48(4): 489-500. Karimpour, M.H., Malekzadeh shafaroudi, A., Farmer, G.L. and Stern, C.R., 2012. Petrogenesis of Granitoids, U-Pb zircon geochronology, Sr-Nd Petrogenesis of granitoids, U-Pb zircon geochronology, Sr-Nd isotopic characteristics, and important occurrence of Tertiary mineralization within the Lut block, eastern Iran. Journal of Economic Geology, 4(1): 1-28. (in Persian with English abstract) Nagudi, N., Koberl, Ch. and Kurat, G., 2003. Petrography and Geochemistry of the sigo granite, Uganda and implications for origin, Journal of African earth Sciences, 36(1): 1-14. Pearce, J.A., Harris, N.B.W. and Tindle, A.G., 1984. Trace element discrimination diagrams for thetectonic interpretation of granitic rocks. Journal of Petrology, 25(4): 956-983. Tepper, J.H., Nelson, B.K., Bergantz, G.W. and Irving, A.J., 1993. Petrology of the Chilliwack batholith, North Cascades, Washington: generation of calc-alkalinegranitoids by melting of mafic lower crust with variable water fugacity. Contributions to Mineralogy and Petrology, 113(3): 333-351.

Introduction The study area is located in the central part of the Khaf- Kashmar- Bardaskan volcano-plotunic belt (briefly KKBB). Several IOCG deposits such as Tanourjeh Au-bearing magnetite deposit and Kuh-e-Zar Specularite-rich Au deposit have been explored in KKBB. Geology, alteration, mineralization, geochemistry and fluid inclusion results in Kashmar suggest the IOCG type Au-bearing magnetite mineralization. These IOCG deposits at KKBB form at an active continental arc related to SSZ-type Sabzevar oceanic subduction. Materials and methods Use of Landsat 7+, IRS and Aster satellites. Petrography and alteration Studies in 150 thin sections of volcanic and intrusive rocks. Sampling of ore-bearing quartz vein and mineralography. Preparation of 28 geochemistry samples by the chip composite method of ore-bearing quartz vein and analyzing them in the ACME laboratory by Aqua Regia 1DX1. Fluid inclusions studies of 14 samples of quartz and barite related to the ore minerals of ore-bearing quartz vein by THM600 stage of Linkam company. Results Magmatic events in Kashmar occur at Paleocene-Eocene and include: (1) old mafic - intermediate volcano-plutonic series; (2) felsic volcanic and granitoids; and (3) parallel swarm dykes which are youngest (Almasi et al., 2016). Geochemically, Kashmar rocks are metaluminous to highly peraluminous and Tholeitic to calc-alkaline and shoshonitic in composition (Almasi et al., 2016). The field characteristics, together with isotope and geochemical analyses show that all rock types are essentially co-magmatic and post-collisional I-type (Almasi et al., 2016). Alteration of Kashmar is described in two ways: (1) intense ellipsoidal-linear Argillic-Sillicification and low sericitic with Silica caps and with medium widespread and propylitic alterations in triple regions, next to Dorouneh fault; and (2) Medium Hematite-Carbonate-Chlorite-Silicification alterations in Kamarmard heights. In parts of near the Doruneh fault, sometimes fractures of rocks are filled with tourmaline (Dumortierite type) and iron oxides. Kashmar surface mineralization is described in the ore-bearing quartz veins. Principal mineralization textures are layered, comb and Brecciation. The most important types of veins are those containing Chalcopyrite - Quartz veins, Specularite-rich veins – Quartz-Galena veins accompany with hydrothermal Breccias. Barren barite veins also exist in the region. The Chalcopyrite - Quartz veins occur on the main fracture zone and next to the Argillic alterations and silica cap in three regions (Bahariyeh, Uch Palang and Sarsefidal). Hydrothermal Breccias, Spicularite- rich veins, Quartz - Galena and barite veins occurred within Hematite- Carbonate-Chlorite-Silicification alterations in the Kamarmard area. Geochemistry of veins indicates anomalies of gold, copper, lead and zinc in them. Most enrichments of gold are accompanied with copper, lead and zinc and they occurs in hydrothermal Breccias and then specularite- rich veins. Gold values up to about 15 ppm and Cu, Pb and Zn each to > 1%. Temperature – salinity studies of fluid inclusions of ore-bearing Quartz veins in Kashmar show the fluid temperature and salinity values in all veins are close together. Temperatures are moderate to relatively high and between 245° C and 530 ° C and salinities are relatively low to moderate and between 14 to 18 (wt% NaCl). Maximum and minimum of temperatures and salinities are related to fluid inclusions of hydrothermal Breccias and Quartz-Galena vein. Co-existence between two-phase liquid-vapor rich fluids and single-phase gas fluids in the veins indicate that conditions were close to boiling, and maybe a little boiling occurred, which strengthened with brecciaing of rock and view rare CO2-bearing fluid inclusion in veins on the Kamarmard peak. Non-existence of vuggy Quartz in silica caps in the region shows this issue. The frequency of oxide minerals (Specularite, Barite), H2O-NaCl-CaCl2 system, and the low amounts of sulfide minerals in Kashmar, all represent the oxidized conditions of hydrothermal fluid and the impact of CO2-bearing chloride complex in transport, non-interference of meteoric waters and precipitation of metallic elements with reducing of temperature. Discussion Most important IOCG deposits of south America (Candelaria, Mantoverde and Raul Condstable) have Au-bearing massive magnetite bodies accompanied with Potassium (actinolite, biotite and K-feldspar) alterations with high temperatures (500-700 O C) and salinities (>40%wt NaCl) at deepest parts (Sillitoe, 2003). At the upper levels, there are magnetite changes to hematite (Specular) and the possibility of coarse calcite (± silver mineralisation). Hematite zone may display hydrothermal/tectonic brecciation. The hematite-rich veins tend to contain sericite and/or chlorite, with or without K-feldspar or albite, and to possess alteration haloes characterized by these same minerals. Both the magnetite- and specular hematite-rich IOCG veins contain chalcopyrite and generally subordinate Pyrite (Fuller et al., 1965). References Almasi, A., Karimpour, M.H., Ebrahimi Nasrabadi, Kh., Rahimi, B. and KlÖtzli, U, 2016. Geology and geochemistry of sub-volcanic and plutonic bodies of Kashmar (North of Lut Block). Iranian Journal of Crystallography and Mineralogy, 24 (3): 539-556. (in Persian) Fuller, R.C., Corvala´n, J., Klohn, C., Klohn, E. and Levi, B., 1965. Geologı´a y yacimientos metalı´feros de Chile. Instituto de Investigaciones Geolo´ gicas, Santiago, 305 pp. Sillitoe, R.H., 2003. Iron oxide-copper-gold deposits: An Andean view. Mineralium Deposita, 38(7): 787–812.

Introduction The investigated area is situated in the south west of the Khorasan Razavi Province along the North West of the Lut Block. Different types of metal ore bodies along with non-metal deposits have already been documented in the Lut Block (Karimpour et al., 2008). Most of the study area is covered with granitoid rocks. Metamorphic rocks with unknown age are present in the north of the area. Skarns are observed in contact with fault zones and intrusive bodies. Eocene volcanic rocks with andesite and andesibasalt composition are located in the east and north east of the area (Ahmadirouhani et al., 2015). The study area that is a part of the Lut Block has a high potentials for Cu, Fe, Au, and Barite mineralization along the observed alteration zones. In the present study, the petrography, petrogenesis, Sr–Nd isotopes, and U–Pb zircon age of acidic granitoids in the east of Bajestan were investigated. Materials and methods In the current study, 400 rock samples were collected from the field and 170 thin sections were prepared for petrography studies. Thirty samples of volcanic rocks, intrusions, and dykes were analyzed using XRF at the Geological Survey of Iran. Twenty-five samples were selected for the elemental analysis using ICP-MS by the Acme Lab Company (Canada), 16 samples of them were related to acidic intrusive bodies and dykes. In addition, zircon crystals from four samples of the granitoids bodies were collected for U–Pb dating. Approximately 50 zircon grains (i.e. euhedral, clear, uncracked crystals with no visible heritage cores and no inclusions) were hand-picked from each sample. Through cathodoluminescence imaging, the internal structure and the origin of zircon grains were examined at the Geological Survey of Vienna, Austria. Moreover, zircons were dated using the (LA)-ICP-MS method at the Laboratory of Geochronology, the University of Vienna, Austria using the methodology outlined in Klötzli et al., (2009). Sr and Nd isotopic compositions were also determined for the same samples (i.e. U-Pb samples) using the whole-rock method. The samples were analyzed in the Laboratório de Geologia Isotópica da Universidade de Aveiro, Portugal. Results Granitoids in the study area have mostly monzogranite (biotite monzogranite, hornblende biotite monzogranite and pyroxene hornblende biotite monzogranite), granite, and syenogranite composition. Granular, micro-granular, and porphyritic textures are common textures in these rocks. Common mafic minerals in these rocks include biotite, hornblende and pyroxene. Based on mineralogy, low values of magnetic susceptibility, high aluminum saturation index, and high initial 87Sr/86Sr ratios (> 0.710) of the study of granitoid rocks belong to the ilmenite-series of the reduced S-type granitoids. These magmas originated from the upper continental crust at a syncollosion zone. Furthermore, the rocks normalizing spider diagrams showed characteristics of a crustal environment. The age of the granitoids based on zircon U–Pb age dating was determined, including granite porphyry (79±1 Ma), syenogranite (76±1 Ma), biotite monzogranite (76±1 Ma), all of which belong to the Upper Cretaceous (Campanian), except pyroxene hornblende biotite monzogranite with 30.7±1 Ma, Oligocene age (Rupelian) has a different age. The ranges of their initial 87Sr/86Sr and 143Nd/144Nd ratios for Upper Cretaceous granitoids are 0.710897–0.717908 and 0.511995–0.512186, respectively while they are 0.713292 and 0.512186 for Oligocene intrusion. The initial єNd isotope values for the syenogranite, biotite monzogranite, and granite porphyry are -10.65, -7.38 and -9.51, respectively. The initial єNd isotope value for pyroxene hornblende biotite monzogranite is -8.06. The values of the igneous rocks could be considered as representative of continental crust derived from magma, and melt derived from psammite rocks is considered to have been the source of the granitoids. Discussion Based on the U-Pb dating results, there are two magmatism phases (Upper Cretaceous and Oligocene) in the area which have not reported in the north of Lut Block yet. During the Upper Cretaceous, three localities of granitoids are reported, excluding Bajestan: Bazman (initial 87Sr/86Sr =0.7056) is located in the southern part of the Lut Block, Gazu (initial 87Sr/86Sr =0.7045) is located near the Nayband fault in the Tabas Block and Kaje is located in Ferdows (initial 87Sr/86Sr =0.7061-0.7080). All of these granitoids were formed due to the subduction zone and their magma (I type) originated from mantle. However, granitoids in Bajestan with the initial 87Sr/86Sr =0.711-0.718 were formed during the continental collision while their magma was originated from the continental crust. In addition, the Middle Jurassic granitoids in the Lut Block (Shah Kuh, KlatehAhani and SurkhKuh) with the origin of continental crustal magma have an initial 87Sr/86Sr = 0.7068-0.7081. That is, the continental crust from which Bajestan granitoid magma is originated, is different from the other parts of the Lut Block due to very high (87Sr/86Sr). This indicates that Bajestan perhaps joined the Lut Block after the Upper Cretaceous collision. In addition to Bajestan, the Oligocene granitoids in the Lut block are reported in the Chah-Shaljami, Dehsalm, Mahoor and Khunik areas. Except Bajestan, all of these granitoids were formed in the subduction zone and their magma is I type. Mineralization in Chah-shaljami, Dehsalm, and Mahoor is related to the porphyric system, whereas no mineralization in Khunik and Bajestan Granitoids has been reported yet. References Ahmadirouhani, R., Karimpour, M.H., Rahimi, B. and Malekzadeh Shafaroudi, A., 2015. Enhance of alteration zones and lineation in the east of Bajestan using SPOT, ASTER, ETM+ and Geophysics data. Scientific Quaternary Journal Geosciences, 24: 253-262. Karimpour, M.H., Malekzadeh-Shafaroudi. A., Stern. C.R. and Hidarian, M.R., 2008. Using ETM+ and airborne geophysics data to locating porphyry copper and epithermal gold deposits in Eastern Iran. Journal of Applied Science, 8: 4004–4016. Klötzli, U., Klötzli, E., Günes, Z. and Kosler, J., 2009. Accuracy of laser ablation U–Pb zircon dating: results from test using five different reference zircons. Geostandards and Geoanalytical Research, 33: 5–15.

The Khunik area is located in the south of Birjand, Khorasan province, in the eastern margin of Lut block. Tertiary volcanic rocks have andesite to trachy-andesite composition. Dating analyzing by Rb-Sr method on plagioclase and hornblende as well as whole-rock isochron method was performed on pyroxene-hornblende andesite rock unit. On this basis the emplacement age is Upper Paleocene (58±11 Ma). These rocks have initial 87Sr/86Sr and εNd 0.7046-0.7049 and 2.16-3.12, respectively. According to isotopic data, volcanic rocks originated from depleted mantle and have the least crust contamination while it was fractionated. Geochemically, Khunik volcanic rocks have features typical of calk-alkaline to shoshonite and are metaluminous. Enrichment in LILEs and typical negative anomalies of Nb and Ti are evidences that the volcanic rocks formed in a subduction zone and active continental margin. Modeling suggests that these rocks were derived dominantly from 1–5% partial melting of a mainly spinel garnet lherzolite mantle source that is metasomatized by slab-derived fluid.

Khur area is located in east of Iran and northwest of Birjand. The area comprises outcrops of Eocene to Oligocene volcanics with basaltic andesite to rhyolite composition, which were intruded by subvolcanic and intrusive bodies of granodiorite to gabbro. In the present work, petrogenesis of volcanic units in Cheshmeh Khuri and Shekasteh Sabz areas was studied, which are located in Khur area and these volcanics have most widespread in them. Rhyolite, dacite, andesite, trachyandesite and basaltic andesite units in Cheshmeh Khuri and trachyandesite unit in Shekasteh Sabz were identified. The main textures of these units are porphyritic, hialoporphyritic and microlitic and plagioclase, pyroxene, K-feldspar, hornblende, biotite and quartz are the main minerals. Volcanic units of Cheshmeh Khuri have characteristic of high-K Calc-alkaline. Enrichment of LREE relative to HREE and LILE to HFSE are important evidences that magma was formed in a magmatic belt of a subduction zone. Based on the initial 87Sr/86Sr of andesite and dacite, their magma has originated from partial melting of an enriched mantle and contaminated with the crust through its differentiation. Trachyandesites of Shekaste Sabz have characteristic of shoshonitic nature. These units are characterized by high FeOt/FeOt+MgO, K2O/Na2O and Zr>360 ppm, Y>39 ppm, and Ce> 100 ppm. Also, they are enrichment in REE particularly in LREE, depletion of Eu, strong enrichment in HFSE, and depletion in Ba and Sr. Therefore, trachyandesites of Shekaste Sabz belong to post collision volcanics.

Introduction The Bornaward area is located in the Northeastern Iran (in the Khorasan Razavi province) 28 km northwest of the city of Bardaskan at 57˚ 46΄ to 57˚ 52΄ N latitude and 35˚ 21΄ to 35˚ 24΄E longitude. The Taknar structural zone, situated in the North central Iranian micro continent, is part of the Lut block (Forster, 1978). The Taknar zone is an allochthonous block bounded by the Darouneh and Taknar major faults. Much of this zone consists of metarhyolite-rhyodacite volcanic rocks, and rhyolitic tuff with interlayers of sandstone and dolomite (Taknar Formation). Analytical Results ICP-MS analysis of REE and minor elements of samples of the Bornaward metarhyolites was carried out at the ACME Laboratory in Vancouver, Canada. U-Pb dating of the metarhyolites was performed on isolated zircons in Crohn's Laser Lab, in Arizona (Gehrels et al., 2008). Measurement of Rb, Sr, Sm and Nd isotopes and (143Nd/144Nd)i and (87Sr/86Sr)i ratios took place in the radioisotope laboratory of the University of Aveiro in Portugal. Petrography The volcanic rocks are porphyritic, commonly containing phenocrysts of orthoclase and rarely sanidine, quartz and intermediate plagioclase in a groundmass of fine-grained quartz and feldspar. An alteration has produced oriented needles of sericite and clay minerals, clusters of fine-grained green biotite and clots of epidote and chlorite. Geochemistry The compositions of the volcanic rocks are calc alkaline and high K- calc alkaline. The obtained Shand index (Al2O3/( CaO+Na2O+K2O) is above 1.1, in the peraluminous S-type granite field (Chappell and White, 2001). Plotted on the TAS diagram (Middlemost, 1994), all the metarhyolite-rhyodacite samples are located in the sub-alkaline field and the majority fall into the rhyolite group. The metarhyolite-rhyodacites show enrichment of LREE with a moderately ascending pattern ((La/Yb)N=2.51-10.11 and La=46.45-145.48). Europium shows a negative anomaly (Eu/Eu*=0.23-0.71). U-Pb zircon geochronology Measurement of U-Pb isotopes of the Bornaward metarhyolite zircons of sample BKCh-103, indicates an age of 552.23+4.73,-6.62 Ma (Upper Precambrian). Sr-Nd isotopes The Sr ratios of the metarhyolites (87Sr/86Sr) were found to fall in the range of 0.688949 to 0.723435 and the Nd ratios (143Nd/144Nd)i were in the range of 0.511701 to 0.511855. These values indicate that the metarhyolites of samples BKCh-12, BKCh-103 and BKCh-177 were affected by hydrothermal alteration since their (87Sr/86Sr)I ratios are high. The Sr ratios suggest that the more negative Nd anomaly and the more negative ɛNd(552) of the samples BKCh-12, BKCh-103 and BKCh-177 indicate that these lavas originated in an enriched upper mantle source and/or lower continental crust. In contrast, two recent examples (Xua et al., 2005) can be related to sialic continental crust with significant contamination. Petrogenesis The Bornaward metarhyolite- rhyodacites show an enriched pattern for Rb, Th, U, K, Pb, Nd and Y relative to the primitive mantle, while Ba, P, Ti, Sr, Zr and Nb show a reduction as a result of fractional crystallization. Based on isotopic correlations of207Pb/204Pb vs 206Pb/204Pb, the primitive source of the Bornaward metarhyolite- rhyodacites is the lower continental crust. This part of the continental crust is only slightly depleted in Pb. Consequently, it has a low 87Sr/86Sr ratio (Samples BKCh-138 and BKCh-198). In contrast, the samples of BKCh-12, BKCh-103 and BKCh-177 have high 87Sr/86Sr ratios that could be the result of significant contamination to parts of the continental crust with very high 87Sr/86Sr (Karimpour et al., 2011). Results and Conclusions The calc-alkaline compositions of samples BKCh-12, BKCh-103 and BKCh-177, the high K- calc alkaline of samples BKCh-138 and BKCh-198 of the Bornaward metarhyolites and the higher temperature overgrowth of plagioclase on lower temperature microcline phenocrysts can be a reason for entrance lavas with different generations. The distinct isotopic characteristics of the two groups of rhyolitic samples are the reasons for two different sources for the production of these lavas: 1) partial melting of an enriched mantle reservoir or lower continental crust, and 2) sialic continental crust with high contamination. With respect to the Bornaward metarhyolite- rhyodacites with (143Nd/144Nd)i ratios from 0.511701 to 0.511855, geochemical characteristics and the high volume of volcanic rocks in the area, their formation can be attributed to a continental rift environment. This rift system can be formed by initiation of a plume in the upper mantle beneath East Iran during Neoproterozoic time. References Chappell, B.W. and White, A.J.R., 2001. Two contrasting granite types. Australian Journal of Earth Sciences, 48(4): 489-499. Forster, H., 1978. Mesozoic – cenozoic metallogenesis in Iran. Journal of the Geological Society, 135(4): 443-455. Gehrels, G.E., Valencia, V.A. and Ruiz, J., 2008. Enhanced precision, accuracy, efficiency, and spatial resolution of U–Pb ages by laser ablation–multicollector–inductively coupled plasma-mass spectrometry. Geochemistry, Geophysics, Geosystems, 9(3): 1-13. Karimpour, M.H., Farmer, G.L., Stern, C.R. and Salati, E., 2011. U-Pb zircon geochronology and Sr-Nd isotopic characteristic of Late Neoproterozoic Bornaward granitoids (Taknar zone exotic block), Iran. Iranian Society of Crystallography and Mineralogy, 19(1): 1-18. Middlemost, E.A.K., 1994.Naming materials in the magma igneous rock system. Earth Science Reviews, 37(3- 4): 215-224. Xua, B., Jianb, P., Zhenga, H., Zouc, H., Zhanga, L. and Liub, D., 2005. U–Pb zircon geochronology and geochemistry of Neoproterozoic volcanic rocks in the Tarim Block of northwest China: implications for the breakup of Rodinia supercontinent and Neoproterozoic glaciations. Precambrian Research, 136(2): 107–123.

Introduction The study area is located in NW Gonabad, Razavi Khorasan Province, northern Lut block and eastern Iran north of the Lut Block. Magmatism in NW Gonabad produced plutonic and volcanic rock associations with varying geochemical compositions. These rocks are related to the Cenozoic magmatic rocks in Iran and belong to the Lut Block volcanic–plutonic belt. In this study, petrogenesis of volcanic units in northwest Gonabad was investigated. The volcanic rocks are andesites/trachyandesites, rhyolites, dacites/ rhyodacites and pyroclastics.These rocks show porphyritic, trachytic and embayed textures in phenocrysts with plagioclase, sanidine and quartz (most notably in dacite and rhyolite), hornblende and rare biotite. The most important alteration zones are propylitic, silicification and argillic.Four kaolinite- bearing clay deposits have been located in areas affectedby hydrothermal alteration of Eocene rhyolite, dacite and rhyodacite. Analytical techniques Five samples were analyzed for major elements by wavelength dispersive X-ray fluorescence (XRF) and six samples were analyzed for trace elements using inductively coupled plasma-mass spectrometry (ICP-MS) in the Acme Laboratories, Vancouver (Canada).Sr and Nd isotopic compositions were determined for four whole-rock samples at the Laboratório de GeologiaIsotópica da Universidade de Aveiro, Portugal. Results Petrography. The rocks in this area are consist of trachyte, andesite/ trachyandesite, dacite/ rhyodacite, principally as ignimbrites and soft tuff. The textures of phenocrysts are mainly porphyritic, glomerophyric, trachytic and embayed textures in plagioclase, hornblende and biotite. The groundmasses consist of plagioclase and fine-grainedcrystals of hornblende. Plagioclase phenocrysts and microlitesare by far the most abundant textures in andesite - trachyandesites (>25% and in size from 0.01 to 0.1mm). Euhedral to subhedral hornblende phenocrysts areabundant (3-5%)and 0.1 to 0.6mmin size. Trachyte is characterized by trachytic texture. Ninety percent of the rock consists of sanidine. In trachytes, 3 to 5% hornblende ( 0.3 mm) is replaced by carbonates. Rhyolites contain quartz, plagioclase, sanidine, and biotite phenocrysts in a microcrystalline to glassy groundmass. Rhyodacitehas phenocrysts, some glomerophyric, consisting of quartz, 2 to 3% (0.1-0.5 mm), plagioclase 7 to 10% (0.2- 0.8 mm), hornblende 5% and biotite 1%. Up to 15% of sanidineis altered to clay minerals. Crystal tuff and lithic-crystal tuff are distributed overa large area. Using the Zr/TiO2 and Nb/Y diagram of Winchester and Fold (1977), samples are designated as rhyolite, dacite and sub-alkaline basalt. In the Co vs. Th diagram of Hastie et al. (2007), samples plot in the shoshonitic and high calc-alkaline, rhyolite, dacite and andesite-basalt fields. The REE patterns and trace element contents of the volcanic samples show: (1) LREE/HREE enrichment ((La/Yb) N = 0.3 to 15.27), (2) Low negative Eu anomaly (ave.Eu*/Eu=0.2-0.85), (3) depletion in Ba, Sr, K2O, Zr and Ti (Lower continental crust-normalized spider diagram from Taylor and McLennan, 1985 and Chondrite-normalized diagram from Nakamura, 1974. Rhyolites show the most extreme negative Eu anomaly (Eu/Eu* = 0.2-0.3) compared with 0.65–0.85 for volcanic elsewhere and also show considerably differences in the contents of Rb,Sr,K,Ti,Zr,Hf,Ce. These differences are related to greater magmatic differentiation or derivation from the other sources. The Sr and Nd isotopic ratios of these volcanic rocks are: 87Sr/86Sr = 0.70699 to 0.71014 and 143Nd/144Nd =0.512144 to 0.512539. Assuming an age of 60 Ma, the initial 87Sr/86Sr ratios vary from 0.70671 to 0.71066 and initial 143Nd/144Nd values vary from 0.512098 0.51249 (εNdi = -9.1) to 0.51249 (εNdi = -1.4).In the εNdi versus (87Sr/86Sr)i diagram, the samples plot in the field typical of magmas that are of crustal origin or, at least, that underwent important processes of crustal assimilation/contamination. Andesitic rocks displays lightly lower rangesof87Sr/86Sr (0.7067-0.7068) and εNdi values from -1.44 to -2.34, than rhyolite. Distinct Sr and Nd isotopic compositions are seen between rhyolitic rocks and andesitic rocks. The geochemical data suggest that the rhyolitic magmas probably represent the final differentiates of parental magmas, resulting from partial melting of mafic lower crust. Generally, the magmas from this area have low Sr (less than 400 ppm), high K2O/Na2O and negative Eu anomalies. References Hastie, A.R., Kerr, A.C., Pearce, J.A. and Mitchell, S.F., 2007. Classification of altered volcanic island arc rocks using immobile trace elements: development of the Th-Co discrimination diagram. Journal of Petrology, 48(12): 2341- 2357. Nakamura, N., 1974. Determination of REE, Ba, Fe, Mg, Na, and K in carbonaceous and ordinary chondrites. Geochim, Cosmochim, Acta, 38(5): 757–775. Taylor, S.R. and McLennan, S.M., 1985. The continental crust, its composition and evolution, an examination of the geochemical record preserved in sedimentary rocks. Blackwell, Oxford, 312 pp. Winchester, J.A. and Floyd, P.A., 1977. Geochemical discrimination of different magma series and their differentiation products using immobile elements. Chemical Geology, 20(4): 325-343.

Introduction Pyrite is the most abundant sulfide mineral in low sulfidation ore deposits. Experimental studies have shown that low-temperature ( 200°C) from hydrothermal or metamorphic fluids (Butler and Rickard, 2000). Framboidal pyrite mostly occurs in sedimentary environments, though it could also form during metamorphism and hydrothermal alteration (Scott et al., 2009). The pyrite formed tends to be enriched in various trace elements such as Au and As. For this study we have combined the geology, alteration, mineralization with recent studies of the description of the deposit from core logging and underground mapping and geochemistry in the CheshmehZard gold district and also investigated the compositional variation and textural differences between pyrite types. This study is based on the results of our alteration and mineralization mapping and detailed logging of 1937.8 m of drill core. Materials and Methods Geology, hydrothermal alteration and mineralization were examined in drill holes along several cross sections. Host-rock alteration minerals and veins were determined for 11 samples using standard X-ray diffraction (XRD) and X-ray fluorescence spectrometry (XRF) techniques. Polished sections were studied by reflected light microscopy and backscattered electron images (BSE). In this study, the trace-element composition of pyrite samples from the Au-III vein system was obtained using electron microprobe analyzer (EMPA) data. All analyseswere carried out at the department of Materials Engineering and Physics of the University of Salzburg in Austria. The EMPA measurements and BSE imaging were made using a JXA-8600 electron microprobe. Spot analyses of 30 pyrite grains from CheshmehZard are given in Table 1. Results The study area is located in the north of Khorasan Razavi Province 45 km to the south of Neyshabour. The area near CheshmehZard could become important as a site of economically significant gold mineralization. Six gold-bearing vein systems were recognized east of Arghash. The estimated resources are about 2 million metric tons of potential ore with an average of 1.9 g/t Au (Samadi, 2001;Ashrafpour et al., 2012). Multiple intrusive events are recognized in the region including Precambrian to post-Oligocene-Miocene igneous rocks (Alaminia et al., 2013a). This includes the Arghash diorite pluton, upper Cretaceous granitoids (minor diorite, mainly quartz monzodiorite and granodiorite), early Eocene granite and several lamprophyre and small intrusions of quartz monzodiorite porphyries. Volcanicsinclude andesite, dacite, pillow basalt and tuffs. Sedimentary rocks are conglomerate and minor limestone. Gold veins are hosted by intermediate to silicic volcanic rocks, tuffs, granite, granodiorite, and conglomerate. Veins consist of calcite and quartz. The main alteration zones mapped at the surface and underground are sericite-quartz-pyrite-calcite, withsilicified, propylitic, argillic, and carbonate zones. The mineralization associated with sericiticalteration and silicificationoccurs asveinlets and disseminated in the propylitic zone. Gangue minerals are quartz, chalcedony, calcite, adularia, illite, and kaolinite. Mineralization occurs as veinlets, breccia filling and disseminated. The veinlets are comprised of pyrite, arsenopyrite, minor chalcopyrite, sphalerite, galena, magnetite and hematite. Pyrite is the main sulfide mineral in the hypogene ore. Samples were collected with the objective of studying the pyrite in the Au (III) vein systems. All samples were therefore pyrite rich. The paragenesiswas determined to show four stages of mineralization based on the following microscopic observations: 1. an initial pyrite veinlet stage with associated quartz, chlorite, epidote. Pyrite is fine to medium grained, anhedral and gold-poor. 2. a second pyritic stage (polymetallic sulfide stage) contains pyrite, chalcopyrite, galena, sphalerite, quartz and chalcedony, minor adularia and arsenopyrite. 3. An As-bearing pyrite stage with sericite, chalcedony and quartz. The pyrite isframboidal.. 4. Finally, a carbonate-dominated stage. The pyrite is euhedral to anhedral and coarse grained. The Au concentration in Stages 2 and 3 pyrite is higher than that in Stage 4 pyrite. Conclusions The gangue mineral assemblages of carbonate, chlorite, quartz, and minor sericite and potassium feldspar in the ore-forming process of the CheshmehZard gold district suggest that the pH value of the hydrothermal fluids was near neutral to slightly acid (approximately 4.5 to 5.3 under 250 to 300 °C and 1 kbar conditions) and that gold would be transported mainly as Au(HS)2- (Stefansson and Seward, 2004). Three types of pyrite based on the chemical composition have been investigated: As- bearing pyrite, Ti-V - bearing pyrite and pure or barren pyrite. EMPA analyses of the pyrite in gold veins show maximum concentrations of As (3.62 wt.%), Ti (3.91 wt.%) and V (0.53 wt.%) respectively. The occurrence of the gold is usually associated with arsenian pyrite and Ti-V - bearing pyrite. Veinlets of the Py1 coexisting with arseno-pyrite and gold Py2 implies the substitution of sulfur by arsenic. Gold precipitated under relatively reducing conditions in framboidal pyrite. Py3 formed prior to barren pyrite (IV). References Alaminia, Z., Karimpour, M.H., Homam, S.M. and Finger, F., 2013a. The magmatic record in the Arghash region, NE Iran, and tectonic implications. International Journal of Earth Sciences, 102(6):1603-1625. Ashrafpour, E., Ansdell, K.M. and Alirezaei, S., 2012. Hydrothermal fluid evolution and ore genesis in the Arghash epithermal gold prospect, northeastern Iran. Journal of Asian Earth Sciences, 51(1):30–44. Butler, I.B. and Rickard, D., 2000. Framboidal pyrite formation via the oxidation of iron (II) monosulfide by hydrogen sulphide. Geochimica et Cosmochimica Acta, 64(15): 2665–2672. Samadi, M., 2001. Exploration in Arghash Gold Prospect. Geological Survey of Iran, unpublished report, Tehran, 73 pp. (in Persian) Scott, R.J., Meffre, S., Woodhead, J., Gilbert, S.E., Berry, R.F. and Emsbo, P., 2009. Development of framboidal pyrite during diagenesis, low-grade regional metamorphism, and hydrothermal alteration. Economic Geology, 104(8):1143–1168. Stefansson, A. and Seward, T.M., 2004. Gold (I) complexing in aqueous sulphide solutions to 500 °C at 500 bar. Geochimica et Cosmochimica Acta, 68(20):4121–4143.

Introduction The Baqoroq Cu-Zn-As deposit is located northeast of the town ofAnarak in Isfahan province, in theeast central areaof Iran. Copper mineralization occursin upper cretaceous carbonate rocks.Studyof thegeologyof the Nakhlak area, the location ofa carbonate-hosted base metaldeposit, indicatesthe importance of stratigraphic, lithological and structural controls in the placement of this ore deposit. (Jazi et al., 2015).Some of the most world’s most important epigenetic, stratabound and discordant copperdeposits are the carbonate hosted Tsumeb and Kipushi type deposits,located in Africa. The Baqoroq deposit is believed to be of this type. Materials and methods In the current study, fifty rock samples were collected from old tunnels and surface mineralization. Twenty-two thin sections, ten polished sections and four thin-polished sections were prepared for microscopic study. Ten samples were selected for elemental analysis by ICP-OES (Inductively coupled plasma optical emission spectrometry) by the Zar Azma Company (Tehran) and AAS (Atomic absorption spectrometry) at the Ferdowsi University of Mashhad. Seven doubly polished sections of barite mineralization were prepared for microthermometric analysis. Homogenization and last ice-melting temperatures were measured using a Linkam THMSG 600 combined heating and freezing stage at Ferdowsi University of Mashhad. Sulfur isotopes of five barite samples were determined by the Iso-Analytical Ltd. Company of the UK. The isotopic ratios are presented in per mil (‰)notation relative to the Canyon Diablo Troilite. Results The upper Cretaceoushost rocks of the Baqoroq deposit include limestone, sandstone, and conglomerate units. Mineralization is controlled by two main factors: lithostratigraphy and structure. Epigenetic Cu-Zn mineralizationoccurs in ore zones as stratabound barite and barite-calcite veins and minor disseminated mineralization. Open space filling occurred as breccia matrix, crustification banding,andbotryoidaltexture. The host rock has undergone dolomitization alteration Hypogene minerals include chalcopyrite, pyrite, sphalerite, galena, enargite, barite, and calcite. Supergene minerals include malachite, azurite, covellite, chrysocolla, chalcocite, cerussite, smithsonite, native copper and iron oxide minerals. Sulfantimonides and sulfardenides are abundant in low- and moderate temperature stages of the deposit, while bismuth sulfides generally occur in higher temperature ores, according to Malakhov, 1968. Analysis of rich ore samples indicates copper is the most abundant heavy metal in the ore (average 20.28 wt%), followed by zinc (average ~ 1 wt%) and arsenic (average ~ 1 wt%), respectively. Thepresence of many trace elements in the ore, such as Sb, Pb, Ag and V, are very important. Element pairs such as Ag-Cu, Zn-Cd, Zn-Sb, Fe-V and Pb-Mo are correlated with each other. The Baqoroq ore minerals are rich in As, Sb and poor in Bi. Highamountsof antimony usually occur in a low temperature stage (Marshall and Joensuu, 1961). Malakhov (1968) suggested thata high Sb/Biratio in the ore indicates a low temperature of formation for the Baqoroq deposit. Sulfide mineralization fluids were found to have homogenization temperatures between 259 and 354°C and salinities between 8.37 and 13.18 wt% NaCl eq. Surface water apparently diluted theore-bearing fluids in the final stages and deposited sulfide-freecalcite veins at relatively low temperatures (78 to 112 °C) and low salinities (3.59 to 6.07 wt% NaCl eq.). The δ34S values of barite of the Baqoroq deposit range from +13.1 to +14.37‰from whichδ34S values of ore fluids were calculated to vary between -8.57‰ and -7.23‰. Sulfur within natural environments is derived ultimately from either igneous or seawater sources (Ohmoto and Rye, 1979). Barite δ34S values of Baqoroq deposit lie within the range of Cretaceous-age oceanic sulfate values. The reduction of sulfate to sulfide couldhave been caused either by bacterial sulfate reduction or by nonbacterial sulfate reduction through a reaction with organic materialin the sedimentary rocks (thermochemical sulfate reduction). However, the narrow range of δ34S and positive values indicates that they were not produced by bacterial sulfate reduction.Partial thermochemical reduction of sulfates has apparently produced light sulfurvalues (~ 21‰ lighter) and it has been effective inthe deposition of ore minerals. Organic matter occurs as graphite in the Baqoroq formation in proximity of Baqoroq deposit (Cherepovsky et al., 1982). Discussion Epigenetic, stratabound and discordant Cu-Zn-As mineralization in the Baqoroq deposit occurs as open space filling of upper Cretaceous rocks. Host rock is partially dolomitized by ascending warm, saline fluids. Seawater sulfates were the source of the sulfidesulfur and the sulfate in the barite. The reduced sulfur was generated by partial thermochemical reduction and it was effective inthe deposition ofthe ore minerals. Based onthe evidence of carbonate host rocks, the absence of igneous activity, the open space filling texture, mineralogy, dolomite alteration, ore geochemistry (As and Sb high content and absence of Bi), microthermometric data of ore bearing fluid and sulfur isotope values, the Baqoroq deposit is very similar to the carbonate hosted copper deposits in Africa and in particular the Tsumeb deposit in Namibia. The Baqoroqdepositmay have been produced bymetamorphicfluids during orogenyrelated to theclosureof the Neo-Tethys ocean. References Cherepovsky, N., Plyaskin, V., Zhitinev, N., Kokorin, Y., Susov, M., Melnikov, B. and Aistov, L., 1982. Report on detailed geological prospecting in Anarak area (Central Iran) Nakhlak locality. Geological Survey of Iran and Technoexport Company, Tehran. Report 14, 196 pp. Jazi, M.A., Karimpour, M.H., Malekzadeh, A. and Rahimi, B., 2015. Stratigraphic, lithological and structural controls in placement of Nakhlak deposit (northeast of Esfahan). Advanced Applied Geology, 15(1): 59-75. (in Persian with English abstract) Malakhov, A.A., 1968. Bismuth and antimony in galena as indicators of some conditions of ore formation. Geochemistry International, 7(11): 1055-1068. Marshall, R.R. and Joensuu, O., 1961. Crystal habit and trace element content of some galena. Economic Geology, 56(4): 758-771. Ohmoto, H. and Rye, R.O., 1979. Isotopes of sulphur and carbon. In: H.L. Barnes (Editor), Geochemistry of Hydrothermal Ore Deposits. Wiley-Interscience, New York, pp. 509-567.

Alireza Almasi1, Mohammad Hassan Karimpour1*, Khosrow Ebrahimi Nasrabadi1, Behnam Rahimi1, Urs KlÖtzli2 and Jose Francisco Santos3 Introduction The study area is located in central part of the Khaf- Kashmar-Bardeskan belt which is volcano-plutonic belt at the north of the Dorouneh fault in the north of Lut block. The north of the Lut block is affected by tectonic rotation and subduction processes which occur in the east of Iran (Tirrul et al., 1983). The magmatism of Lut block begins in Jurassic and continues in Tertiary (Aghanabati, 1995). Karimpour (Karimpour, 2006) pointed out the Khaf-Kashmar-Bardeskan belt has significant potential for IOCG type mineralization such as Kuh-e-Zar, Tannurjeh, and Sangan (Karimpour, 2006; Mazloumi, 2009). The data gathered on the I-type intrusive rocks include their field geology, petrography, U–Pb zircon dating and Sr–Nd isotope and also alteration and mineralization in the study area. Materials and methods - Preparation of 150 thin sections of rock samples for study of petrography and alteration of the intrusive rocks. - Magnetic susceptibility measuring of intrusive rocks. - U-Pb dating in zircon of I-type intrusive rocks by Laser-Ablation Multi Collector ICP-MS method. - Sr-Nd analysis on 5 samples of I-type intrusive rocks by Multi-Collector Thermal Ionization Mass Spectrometer (TIMS) VG Sector 54 instrument. - Mineralography and paragenetic studies of ore-bearing quartz veins and geochemical analysis for 28 samples. - Production of the geology, alteration and mineralization maps by scale: 1:20000 in GIS. Results Oblique subduction in southern America initiated an arc-parallel fault and shear zones in the back of continental magmatic arc (Sillitoe, 2003). Because of this event, pull-apart basins were formed and high-K to shoshonitic calc-alkalineI- and A-type magmatism occur (Sillitoe, 2003). Most important deposits accompany with this magmatism are Au-Cu deposits types and Fe-Skarns (Sillitoe, 2003). We have similar scenario to Neotethys subduction. Khaf-Kashmar-Bardeskan volcano-plutonic belt is located between Neotethys suture and Alborz- Sabzevar Back- arc (Asiabanha and Foden, 2012). We suggest Khaf-Kashmar-Bardeskan volcano-plutonic belt forms at the arc-parallel fault and shear zones in the back of continental magmatic arc. In the basis of all evidences (Shear zone system, high-K to shoshonitic calc-alkaline I- and A-type magmatism, typical alterations related to upper zones of IOCG deposits and IOCG mineralization), we suggest IOCG (Au-Cu) mineralization in Kashmar. Discussion On the basis of former regional (Muller and Walter, 1983) and local structural studies (this research), regional compression causes sinistral strike-slip movements of Dorouneh and Taknar faults, shear zone, pull-apart and Riedel fractures (P, R and R' types) in the study area. These events cause magma intrusion and circulation of hydrothermal fluids. On the basis of geology, geochemistry and magnetic susceptibility measuring of intrusive rocks, several high K to shoshonitic calc-alkaline to alkaline I-type and one A-type intrusive rocks are intruded in Kashmar area. Swarm dykes are the youngest and the agent for alteration and mineralization. U-Pb dating related to quartz monzonite body (preventative sample for I-type intrusive rocks which are older than A-type series) show 40 Ma (Middle Eocene) for this rock group in Kashmar. The mean of initial 87Sr/86Sr and 143Nd/144Nd are 0.705-0.707 and 0.5135-0.5126 for I-type series, respectively. εNd(i) amounts for I-type series are in negative to positive limit ranges (-1.65 to 1.33). These amounts show subduction source with contamination to continental crust. Two type alteration and mineralization occur in Kashmar: 1) primary alterations (advanced argillic+ sericite+ silicification) which are synchronous with sulfide base-metal veins (chalcopyrite+ pyrite± galena± quartz± chloride) and 2) Lateral alterations (carbonatization+ Fe-oxides+ silicification+ epidotization+ chloride+ sericite+ barite) which are synchronous with IOCG veins (specularite+ chalcopyrite+ pyrite± galena± sphalerite± barite± siderite ± etc.). Primary centralized and sulfide base-metal veins in crosscutting points between Dorouneh fault and minor faults. Bahariyeh, Uchpalang and Sarsefidal areas are located in these crosscutting points. Tourmaline (demorterite) ±chloride fill the fractures in the intrusive rocks of southern part of area next to the Dorouneh fault occasionally. Lateral alteration synchronous with IOCG veins occur in Kamarmard area. Geochemical data of all veins show Cu, Pb, Zn anomalies (>1%) in two type veins, Au anomalies (to about 15 ppm) only in IOCG veins, Mn anomalies in two type veins and Ba anomalies in IOCG veins. Alteration and mineralization in the world-class IOCG deposits identified by sodic-calcic and potassic (hydrothermal actinolite and biotite) and magnetite± gold in deep parts (Sillitoe, 2003) and advanced argillic+ pyrite+ sericite+ toulrmaline (demorterite) in shallow parts (Ray and Dick, 2002). Generally, alteration in the study area is similar to shallow parts of world-class IOCG deposits. Tanourjeh is a IOCG deposit next to the northwest of the study area. In Tanourjeh, the gold-bearing magnetite is synchronous to potassic alteration (hydrothermal biotite) and other alterations are advanced argillic, silicification and sericite. These characteristics are similar to deep parts of world-class IOCG deposits. Bahariyeh, Uchpalang and Sarsefidal have similarities to alterations in Tanourjeh. Considering Tanourjeh lie in the lower level rather to Bahariyeh, Uchpalang and Sarsefidal, we believe they erosion surface in Tanourjeh is lower. Kamarmard lies in the highest erosion surface in the study area. Alterations and Mineralization as similar to Kuh e Zar IOCG deposit (specularite+chalcopyrite+gold) which is next to the Kamarmard area in Northeast of study area. In Bahariyeh-Uchpalang areas we can see only one IOCG vein but in Sarsefidal area exist several IOCG vein. Because of current surface in Bahariyeh-Uchpalang areas is lower than Sarsefidal current surface in Sarsefidal is lower than Kamarmard, we believe that IOCG vein in Bahariyeh-Uchpalang area have been eroded. We Believe to two circulation of oxidized Fe-bearing hydrothermal fluid in Kashmar. During the first circulation, Potassic alteration and gold-bearing magnetite bodies in depth and primary alterations with sulfide base-metal veins was formed. At the second circulation, lateral alterations and IOCG veins was formed at the near of paleo-surface. References Aghanabati, A., 1995. Geology of Iran. Geological Survey of Iran, Iran, 606 pp. Asiabanha, A. and Foden, J., 2012. Post-collisional transition from an extensional volcano-sedimentary basin to a continental arc in the Alborz Ranges, N-Iran. Lithos, 148: 98-111. Karimpour, M.H., 2006. Cu-Au mineralizaion accompany with magnetite-specularite (IOCG) and examples in Iran. 9th Geological Society of Iran Conference, Tarbiat Moallem University, Tehran, Iran. Mazloomi Bajestani, A., 2009. Mineralization, Geochemistry and Au-W mineralization in Koh e Zar of Torbat e Heydarieh area. Ph.D. Thesis, University of Shahid Beheshti, Tehran, Iran, 291 pp. Muller, R. and Walter, R., 1983. Geology of the Precambrian-Paleozoic Taknar inlier, northwest of Kashmar, Khorasan province, northeast Iran. Geological Survey of Iran, Tehran, Report 50, 252 pp. Ray, G.E. and Dick, L.A., 2002. The Productora prospect in north-central Chile: An example of an intrusion-related Candelaria type Fe-Cu-Au hydrothermal system. Porter GeoConsultancy Publishing, Adelaide, 2:131–151. Sillitoe, R.M., 2003. Iron oxide-copper-gold deposits: An Andean view. Mineralium Deposita, 38(7): 787–812. Tirrul, R., Bell, I.R., Griffis, R.J. and Camp, V.E., 1983. The Sistan suture zone of eastern Iran. Geological Society of America Bulletin, 94(1): 134-150.

Introduction The study area is located 196 km south of Birjand in eastern border of the Lut block )Berberian and King, 1981) in eastern Iran between 59°05′35" and 59°09′12" E longitude and 31°42′29" and 31°44′13" N latitude. The magmatic activity in the Lut block began in the middle Jurassic such as Kalateh Ahani, Shah Kuh and Surkh Kuh granitoids that are among the oldest rocks exposed within the Lut block (Esmaeily et al., 2005; Tarkian et al., 1983; Moradi Noghondar et al., 2011-2012). Eastern Iran, and particularly the Lut block, has great potential for different types of mineralization as skarnification in Bisheh area which has been studied in this paper. The goal of this study is to highlight the geochronology, geochemistry of major and trace elements, Rb-Sr, Sm-Nd isotopes for skarnified pyroxene-bearing diorites. Materials and methods Major element compositions of thirteen samples were determined by wavelength-dispersive X-ray fluorescence (XRF) spectrometry, using fused discs and the Phillips PW 1410 XRF spectrometer at Ferdowsi University, Mashhad, Iran. These samples were analysed for trace elements using inductively coupled plasma-mass spectrometry (ICP-MS) in the Acme Analytical Laboratories, Vancouver, British Columbia, Canada. Zircon grains were separated from pyroxene diorite porphyrys using heavy liquid and magnetic techniques at the Institute of Earth Sciences, Academia Sinica, Taipei, Taiwan. Zircon U-Pb dating was performed by laser ablation-inductively-coupled plasma-mass spectrometry (LA-ICP-MS), using an Agilent 7500 s machine and a New Wave UP213 laser ablation system, equipped at the Dr Shen-Su Sun memorial laboratory in the Department of Geosciences, National Taiwan University, Taiwan. Strontium and Nd isotopic analyses were performed on a six-collector Finnigan MAT 261 thermal-ionization mass spectrometer at the University of Colorado, Boulder, Colorado, United States. 87Sr/86Sr ratios were determined using four-collector static mode measurements. Several measurements of SRM-987 during the study period yielded a mean of 87Sr/86Sr = 0.71032 ± 2 (error is the 2σ mean). Measured 87Sr/86Sr ratios were corrected to SRM-987 = 0.71028. Measured 143Nd/144Nd was normalized to 146Nd/144Nd = 0.7219. Analyses were conducted as dynamic mode, three-collector measurements. Several measurements of the La Jolla Nd standard during the study period yielded a mean of 143Nd/144Nd = 0.511838 ± 8 (error is the 2σ mean). Results In the Bisheh area that is located east of Lut block, pyroxene-bearing dioritic rocks are high-K calk-alkaline and meta-aluminous. Primitive mantle-normalized trace element spider diagrams display strong enrichment in LILE, such as Rb, Ba, and Cs, and depletion in some HFSE, e.g., Nb, P, Ti, Y and Yb. Chondrite-normalized REE diagrams show (La/Yb)N ratios ranging from 7.75 to 8.63 and small negative Eu anomalies. These features along with high Th/Yb and Ta/Yb ratios show that magmatism is related to continental margin subduction. Obvious depletion of Nb and Ti, relatively high values of Mg#, initial 87Sr/86Sr (0.70606) and 143Nd/144Nd (0.512424) ratios as well as εNd (-3.05) suggest that the magma originated from an enriched mantle with crustal contamination. High values of Rb, Th and K and low amount of P and Ti support the magma contamination in upper crust during magma evolution. Zircon U-Pb age dating for a porphyritic pyroxene diorite sample yield an age of 44.07±0.69 Ma indicating middle Eocene (Lutetian). Discussion The isotopic value for the Bisheh dioritic porphyry can be considered as indicative of lithospheric mantle melting. The trace element characteristics of these rocks can be used to characterize their mantle source. The MORB normalized trace element pattern (Pearce, 1983) of all samples shows a negative anomaly for Nb, Ti and Ta. The negative anomaly of these elements can be explained by the presence of a residual TNT phase (Ti-Nb-Ta, e.g., rutile, ilmenite and perovskite) during the melting of the source (Reagan and Gill, 1989). This pattern followed that of calc-alkaline magmas derived from a sub-arc mantle, with scarce or no garnet in the source. Furthermore, Bisheh subvolcanic bodies were enriched in Rb, Ba and Th, indicating that they had experienced interaction with the continental crust (Kuşcu et al., 2002). The chondrite-normalized rare earth element pattern of the studied rocks shows a high ratio of light rare earth elements (LREE) to heavy rare earth elements (HREE). All the samples have been plotted in the VAG field. The dioritic rocks from the Bisheh have relatively high Mg# (0.4-0.56), which is consistent with derivation from mantle melts contaminated by continental crust (Rapp and Watson, 1995). The initial 87Sr/86Sr of Bisheh pyroxene diorite porphyry was 0.70606 and the (143Nd/144Nd)i isotope compositions and εNd value of these rocks was 0.512424 and -3.05, respectively. These values show that the magma originated from an enriched mantle with crustal contamination. Acknowledgements The authors are grateful to Professor Sun-Lin Chung from the Department of Geosciences, National Taiwan University, for supporting the researchers in the use of U-Th-Pb zircon age dating. References Berberian, M. and King, G.C., 1981. Towards a palaeogeography and tectonics evolution of Iran. Canadian Journal of Earth Science, 18(2): 210–265. Esmaeily, D., Nedelec, A., Valizadeh, M.V., Moore, F. and Cotton, J., 2005. Petrology of the Jurassic Shah-Kuh granite (eastern Iran), with reference to tin mineralization. Journal of Asian Earth Sciences, 25(6): 961-980. Tarkian, M., Lotfi, M. and Baumann, A., 1983. Tectonic, magmatism and the formation of mineral deposits in the central Lut, east Iran. Geological Survey of Iran, geodynamic project (geotraverse) in Iran, Tehran, Report 51, 519 pp. Moradi Noghondar, M., Karimpour, M.H., Farmer, G.L. and Stern, C.R., 2011-2012. Sr-Nd isotopic characteristic, U-Pb zircon geochronology, and petrogenesis of Najmabad Granodiorite batholith, Eastern Iran. Journal of Economic Geology, 3(2): 127-145. (in Persian) Pearce, J.A., 1983. Role of the sub-continental lithosphere in magma genesis at active continental margins. In: C.J. Hawkesworth and M. J. Norry (Editors), Continental basalts and mantle xenoliths. Shiva Publications, Nantwich, UK, pp. 230-249. Reagan, M. K. and Gill, J. B., 1989. Coexisting calcalkaline and high niobium basalts from Turrialba volcano, Costa Rica: implication for residual titanates in arc magma source. Journal of Geophysical Research, 94(B4): 4619-4633. Kuşcu, I., Kuşcu, G.G., Meinert, L.D. and Floyd, P.A., 2002. Tectonic setting and petrogenesis of the Çelebi granitoid, (Kirikkale-Turkey) and comparison with world skarn granitoids. Journal of Geochemical Exploration, 76(3): 175–194. Rapp, R.P. and Watson, E.B., 1995. Dehydration melting of metabasalt at 8–32 kbar: Implications for continental growth and crust–mantle recycling. Journal of Petrology, 36(4): 891–931.

Introduction Arefi quartz-bearing conglomerate (Middle Jurassic) is situated within Binalud structural zone. The unit is trending NW-SE located 25 km south of Mashhad. More than 97% of the pebbles are quartz as mono-crystalline, poly-crystalline, and minor fragments of chert, quartzite, and mica schist. Less that 3% of the remaining minerals are feldspar, mica, chlorite, hornblende, tourmaline, zircon, sphene, and opaque minerals. The cement is mainly silica. Hashemi (Hashemi, 2004) suggested this unit is orthoquartzitic polymictic conglomerate. In this study, we carried out detailed mineralogical studies, geochemical analyses for SiO2 and troublesome elements, determination of quartz pebbles source using geological observations and fluid inclusion microthermometry, and industrial application studies with new insight for porcelain and ceramic factories as the nearest silica-rich reserve to Mashhad. Material and methods 1. Preparing geologic map in 1:10000 scale in the Arefi area. 2. Petrographic study of 65 samples from the quartz-bearing conglomerate unit. 3. Major elements such as SiO2, TFeO, TiO2, and CaO were analyzed at the Maghsoud Porcelain Factories Group, using a Philips PW1480 X-ray spectrometer. 4. Ore dressing analyses in Danesh Faravaran Engineering Company. 5. Fluid-inclusion studies in 4 samples doubly-polished wafers of quartz crystals were studied using standard techniques (Roedder, 1984) and Linkam THM 600 heating-freezing stage (from –190 to 600ºC) mounted on a Olympus TH4–200 microscope stage at Ferdowsi University of Mashhad, Iran. Salinities and density of fluid inclusions were calculated using the Microsoft Excel spreadsheet HOKIEFLINCS-H2O-NACL (Steele-MacInnis et al., 2012; Lecumberri-Sanchez et al., 2012) Results and Discussion Fluid Inclusion studies of both mono- and poly- crystalline quartz revealed that the inclusions consist of three phases (LVS) with NaCl crystals. Homogenization temperature is between 484 and more than 600ºC with average 559ºC and the salinity is between 49.6 and 72.1 wt% NaCl with average 61.2 wt% NaCl. These data indicate a magmatic origin according to Kesler (Kesler, 2005) diagram. Homogenization temperature of two phases (LV) inclusions in the metamorphosed quartz is between 287 and 365ºC with average 318ºC. The main source of quartz pebbles is quartz veins formed within the top of pegmatite-granite (upper Triassic) of Khajeh-Morad area and quartz veins formed due to regional metamorphism. Based on chemical analysis of 93 samples which were taken from the surface (channel method) and power drilling, the SiO2 content is more than 98%, TFeO is less than 0.42% and TiO2 is less than 0.16%. The proved ore reserve is more than 50 million tonnes. Using dry magnetic method, the TFeO became less that 0.03% and TiO2 less than 0.02%. Arefi silica deposit is a first-class reserve and can be used in different types of ceramic. Acknowledgments The Research Foundation of Ferdowsi University of Mashhad, Iran, supported this study (Project No. 29057.2). We also thank Danesh Faravaran Engineering Company for the ore dressing analyses. Reference Hasemi, S.F., 2004. Petrology and depositional environment of Jurrasic conglomerate in south of Mashhad. Unpublished M.Sc. thesis, Ferdowsi University of Mashhad, Mashhad, Iran, 200 pp. (in Persian) Kesler, E.S., 2005. Fluids in Planetary Systems: ore-Forming Fluids. Elements, 1(1): 13–18. Lecumberri-Sanchez, P., Steel-MacInnis, M. and Bodnar, R.J., 2012. A numerical model to estimate trapping conditions of fluid inclusions that homogenize by halite disappearance. Geochim Cosmochim Acta, 92: 14-22. Roedder, E., 1984. Fluid inclusions. Reviews in Mineralogy 12, 644 pp. Steele-MacInnis, M., Lecumberri-Sanchez, P. and Bodnar, R.J., 2012. HOKIEFLINCS-H2O-NACL: A Microsoft Excel spreadsheet for interpreting microthermometric data from fluid inclusions based on the PVTX properties of H2O–NaCl. Computers Geosciences, 49: 334–337.

The Halak Abad prospect occurs in the northeastern part of Central Iran zone (Sabzevar structural zone). In this investigation, geochemical evolution, age and source of part of northeastern Iran magmatic arc (intrusive bodies) in Halak Abad area in the Khorasan Razavi province has been studied. The exposed rocks consist of volcanic rocks with andesite and dacite nature, limestone, plutonic rocks mostly diorite, quartz diorite, monzodiorite, quartz monzonite, granodiorite and granite and sedimentary rocks such as limestone, sandstone and conglomerate. Magnetic susceptibility of intrusive rocks is >100 × 10-5 SI, so they belong to the magnetite-series (oxidized). This magmatism is mainly low-K (tholeiite series) and meta-aluminous. The amounts of Zr, Th, Nb and Ti show depletion compared to N-MORB. Trace elements behavior shows a nearly flat pattern. Age of granodiorite body based on U-Pb zircon dating is 99.7±1.8 Ma (Mid-Cretaceous) and 87Sr/86Sr initial ratio is 0.7047. The geochemical signature and 87Sr/86Sr initial ratio in the area suggest volcanic arc magmatism in subduction zone. This magmatism has characteristic such as high Na2O (3-7 %), low K2O (0.12-1 %), high CaO (4-5.7%), low Rb (1-20 ppm), low total REE (

Kalateh Ahani is located 27 km southeast of Gonabad within the Khorasan Razavi province. The area is part of Lut Block. Sub-volcanic monzonitic rocks intruded regional metamorphosed Shemshak Formation (Jurassic age). Magnetic susceptibility of less altered monzonitic rocks is < 25 ×10-5 SI, therefore they belong to reduced type ilmenite granitoid series. Both intrusive and metamorphic rocks are altered to argillic, propylitic, silicification and some iron oxides. Argillic alteration is dominant within the intrusive rocks. Two major quartz sulfide (sulfides are oxidized) veins trending NW-SE are recognized within the study area. Based on core logging, both disseminated and veinlet mineralization types are recognized within the intrusive and metamorphic rocks. Eight types of veinlet and vein are identified within the intrusive rocks. Maximum density of the veinlets is about 35 per meter within the biotite monzonite porphyry. Hypogene minerals include pyrite, chalcopyrite, sphalerite, galena and quartz. Secondary minerals comprise malachite, hematite, chrysocolla, goethite and gangue minerals are quartz and siderite. Rock geochemistry shows high anomalies of Cu, Pb, Zn, Sn, As, and Au both in the surface and within the mineralized core. Cu > 0.6%., As, Pb and Zn > 1%, Au up to 150 ppb and Sn = 133 ppm. The Sn content of vein in the northern part of Kalateh Ahani (Rud Gaz) is > 1%. Based on mineralization, alteration and geochemistry, it seems that Sn mineralization is associated with the Cretaceous monzonitic rocks. Zircon U–Pb dating indicates that the age of the monzonitic rocks associated with mineralization is 109 Ma (Lower Cretaceous). Based on (87Sr/86Sr)i = 0.71089-0.710647 and (143Nd/144Nd)i = 0.512113-0.51227 of the monzonitic rocks, the magma for these rocks were originated from the continental crust. This research has opened new window with respect to Sn-Cu mineralization and exploration within the Lut Block which is associated with Cretaceous granitoid rocks (reduced type, ilmenite series) originated from the continental crust.

Sangan magnetite skarn mine is located 300 km southeast of Mashhad, along the eastern part of Khaf-Drouneh volcanic-plutonic belt. Granitoids from three areas within the Sangan mine A, C-North and Dardvay were studied. Within the study area, three intrusive rocks including biotite-hornblende monzonite porphyry, biotite syenite and syenogranite were recognized. Based on field cross cutting, absence of garnet-magnetite skarn around the contact, and alteration by younger hydrothermal fluids, these granitoids are older than the magnetite skarn. U-Pb zircon age of the granitoid is 42 Ma (Middle Eocene). Magnetic susceptibility of the granitoids are 310-900 × 10-5 (SI units) and therefore, they are classified as belonging to the magnetite-series (oxidant type) I-type. Chemically, these granitoids are metaluminous, alkali-calcic to alkali and shoshonite to ultrapotassic. Enrichment of LREE, relative to HREE and enrichment of LILE (Sr, Cs, Rb, K and Ba) relative to HFSE (Nb, Ta, Ti, Hf and Zr) indicate that the magma formed in island arc setting. This magma originated from low partial melting (

Granitoid rocks of Kaje area, northwest Ferdows, with the composition of diorite, monzodiorite, monzonite, monzogranite, syenogranite and granite, with calk-alkaline and high potassium affinities, have trace and rare earth element geochemical characteristics similar to those from subduction zones, belonging to I-type granitoid rocks. Most of these rocks are oxidized (magnetite series), while one suite is reduced (ilmenite series) showing S-type characteristics. Three samples of granitoid rocks were dated using zircon U-Pb method. Granitoid rocks belong to upper Cretaceous epoch. A granite porphyry with the age of 84.2±1.3 Ma (Santonian stage) is the oldest body followed by a biotite hornblende monzogranite of 70.8±1.4 Ma (Campanian stage) and the youngest body is a hornblende quartz diorite with the age of 67.9±1 Ma (Maastrichtian stage). Initial 87Sr/86Sr and 143Nd/144Nd ratios as well as єNdi for the granite porphyry are 0.708080, 0.512129 and -7.81, respectively. Those ratios for the biotite hornblende monzogranite are 0.706125, 0.512416 and -2.55, respectively; and for the hornblende quartz diorite are 0.707491, 0.512221 and -6.43, respectively. Based on geochemical and isotopic data, three types of granitoid can be distinguished having three different sources and characteristics. The first and oldest one is the granite porphyry of continental crust source, the second one is the monzonite and monzodiorite and the third group is the diorite of mantle source which originated and emplaced in different depths with various rates of contamination. These rocks have higher (87Sr/86Sr)i values compared with the other upper Cretaceous rocks in Bazman and Gazu areas, and lower (87Sr/86Sr)i values in comparison with the Bejestan rocks. Petrochemistry of the granite group is similar to the Bejestan rocks, but these are 10 m.y. younger and the other two groups have similar geochemistry and source to Bazman and Gazu with more contamination by the crust.

Roudgaz prospect area is a Cu, Sn, Pb, Zn, and Au polymetal vein system located to the southeast of Gonabad and in the northeast of Lut block. Oxidan subvolcanic Tertiary rocks with monzonite to monzodiorite porphyry composition intruded the metamorphic rocks of middle Jurassic. The majority of intrusive bodies are affected by carbonation, argillic, sericitic, and silicification-tourmaline alteration. Mineralization in the area is controlled by fault and is present as vein with domination of NW-SE direction and 85-90º dip. Primary minerals are quartz, tourmaline, chalcopyrite, pyrite, and secondary minerals are malachite, azurite, and goethite. Geochemical sampling using chip composite method indicated high anomalies of Cu, Sn, Pb, and As (up to 10000 ppm), Zn (up to 5527 ppm), and Au (up to 325 ppb). Broad gossan zone is present in the area and is related to the oxidation of sulfide minerals. IP/RS survey was performed over the geochemical anomalies for identification of the location and extension of sulfide mineralization at depth. Generally, chargeability increases in gossan zones, veins, old workings and geochemical anomalies. Resistivity over the quartzite unit and also in locations where mineralized vein is associated with quartz has a high anomaly of up to 425 ohm-m. Due to high geochemical anomaly of Sn and its relation with reduced subvolcanic intrusives, ground magnetic survey was performed to identify the location of magnetite (oxidant) and ilmenite (reduced) series at depth. Variation of Total Magnetic Intensity (TMI) is 335.1 Gamma in the TMI map. The highest magnetic anomalies in the RTP map are located to the north of the survey area which is related to magnetite series (hornblende biotite monzodiorite porphyry) and extend to the south at depth. The lowest magnetic anomaly is located to the center of the survey area and particularly to the east of the Roudgaz village correlating the highest chargeability and geochemical anomaly. Based on coincidence of geochemical and chargeability anomalies, two holes were drilled in the area and 24 samples were collected from the core drills for geochemical analyses. The highest anomalies are accompanied by silicification and chlorite alteration and locations of extension of secondary Fe oxides.

One of the most intensive occurrences of magmatism in Iran was in the middle Jurassic period. Among the granitoid intrusions in this period as discrete bodies or complexes can be pointed to Aligoodarz, Alvand, Astaneh, Boroujerd, Malayer, and Chah-Dozdan in the Sanandaj-Sirjan zone; Shir-kuh and Ayrakan in the Central Iran zone; Shah-kuh, Sorkh-kuh and Kalateh-Ahani in the Lut Block. These granitoids are mostly peraluminous and belong to high-K calc-alkaline series. CaO/Na2O ratios (0.12 to 8.37) mostly suggest a clay-free source for formation of the intrusive rocks magma. Chondrite-normalized Rare Earth Elements (REEs) diagram do not display high enrichment of Light Rare Earth Elements (LREEs) than Heavy Rare Earth Elements (HREEs) and general pattern is relatively flat. In addition, diagram shows Eu negative anomaly, which can be attributed to indicate reducing conditions in formation of magma and/or magma derived from plagioclase depth as source. The lower continental crust-normalized spider diagram indicates enrichment in LILE (Rb, Cs, and K) and LREE (La and Ce) and depletion in Ba, Nb, Ta, Sr, and Ti. Initial 87Sr/86Sr ratios are 0.70609 to 0.71938 and initial εNd values are negative (from -6.51 to -1.1) indicating that magma derived from continental crust. Geochemical and isotopic evidence of the intrusive rocks shows continental crust origin (S-type granitoid) and due to continental collision. Geological findings such as stop in sedimentation, regional metamorphism, ophiolite displacement, and continental collision-related mineralization confirm continental collision between Iranian and Arabian plates in the Middle Jurassic period.

Keybarkuh area is located 70 km southwest of Khaf, Khorasan Razavi province. The study area is situated in northeastern Lut block. The rock units in the area are Paleozoic metamorphic rocks and Cretaceous to Tertiary subvolcanic intrusions intruded as dike, stock and batholith; their composition varies from granite to diorite. Based on magnetic susceptibility, the intrusive rocks are divided into oxidant and reduced series. In this study, the oxidant intrusions are discussed. These intrusions are mostly high-K to shoshonitic and also meta-aluminous type. Their magma formed in subduction magmatic arc and they belong to I-type granitoid series. Enrichment of Large Ion Lithophile Elements (LILE) such as Rb, Cs, K, Ba, and Th relative to High Field Stength Elements (HFSE) such as Nb, Zr, and Ti supported the idea. Enrichment of Light Rare Earth Elements (LREE) and depletion of Heavy Rare Earth Elements (HREE) are also typical of subduction magmatism. Negative anomalies of Eu/Eu* can be attributed to the presence of residual plagioclase in a mantle source and contamination of magma by reduced continental crust. The amount of Nb > 11 ppm, lower ratio of Zr/Nb < 2, the initial 87Sr/86Sr isotope ratio (> 0.706), initial 143Nd/144Nd (> 0.512) and εNd (< -3.5) indicate that magma contaminated by reduced continental crust. Hornblende biotite granodiorite porphyry dated using U-Pb zircon geochronology at 43.44 Ma (Middle Eocene). Based on calculated TDM, magma derived from ancient slab with 820 Ma age in the Keybarkuh area, was affected by the highest continental crust contamination during its ascent.

Tertiary intrusive granitoids within the Lut block in the Khorasan Razavi and South Khorasan provinces are mainly sub-volcanic with porphyry texture and their composition varies from granite to diorite but monzonite is dominant. With the exception of Hired, these are classified as belonging to the magnetite-series of I-type granitoids. Chemically, these rocks are meta-aluminous. Those with mineralization are K-rich and those without mineralization such as Najmabad are Na-rich. All intrusive rocks plot in the field of calc-alkaline to adakite except Najmabad that plot in the adakite field. Based on low content of Nb (30), low initial 87Sr/86Sr (17 ppm), low ratio of Zr/Nb (0.707) and low initial εNd value (-3), magmas in the Kaybar-Kuh were more contaminated in the continental crust. Based on depletion in HREE and high ratio of (La/Yb)N (17-23), magma in Najmabad originated in the deep region in which garnet was present. Based on REE pattern and ration of Eu/Eu* (0.8-1), intrusive rocks within Maherabad, Khoopik, Chah-Shaljami, Kuh Shah and Dehsalm are calc-alkaline and their magma formed in an oxidant condition whereas Kaybar Kuh magma with low ratio of Eu/Eu* (

The Kuh Shah prospecting area is located in Tertiary volcano-plutonic belt of the Lut Block. More than seventeen subvolcanic intermediate to acidic intrusive rocks, diorite to syenite in composition, were identified in the study area. The intrusions are related to hydrothermal alteration zones and contain argillic, propylitic, advanced argillic, silicified, quartz-sericite-pyrite, gossan and hydrothermal breccia which overprinted to each other and are accompanied by weathering which made it complicated to distinguish zoning. Mineralization is observed as sulfide (pyrite and rare chalcopyrite), disseminated Fe-oxides and quartz-Fe-oxide stockwork veinlets. Intrusive rocks are metaluminous, calc-alkaline with shoshonitic affinity with high values of magnetic susceptibility. The Kuh Shah intrusive rocks are classified as magnetite-series of oxidant I-type granitoids. Based on zircon U–Pb age dating, the age of these granitoid rocks is 39.7± 0.7 Ma (Middle Eocene). The radioisotope data (initial 87Sr/86Sr and 143Nd/144Nd ratios as well as εNd) and geochemical data suggest that the Kuh Shah granitoid rocks formed from depleted mantle in a subduction-related magmatic arc setting. Geochemical anomalies of elements such as Cu, Au, Fe, Pb, Zn, As, Sb, Mo, Bi, Hg and also Mn, Ba, Te and Se, correlated with quartz-sericite-pyrite, gossan-stockwork-hydrothermal breccias, irregular silicified bodies and advanced argillic hydrothermal alteration zones. Geophysical anomalies correlated with hydrothermal alteration and mineralization zones. The interpretation of the results represents complex patterns of sub-circular to ellipsoid shape with north-east to south-west direction. These evidences are similar to the other for known Cu-Au porphyry and Au-epithermal systems in Iran and worldwide.

The study area is located south of Ghonabad in Eastern Iran. This area is situated between two major faults, Darouneh to the north and Dashtbyaz to the south. The movements of these faults cased major dislocation of this block. Najmabad granodiorite to granite batholith is elongated trending east-west 2×8 Km2. Mineralization is associated with granite and monzonite. Alteration zones are: propylitic, sericitic, argillic and silicification. Chemically, granite-granodiorite is met-aluminous,, spider diagram normalized to lower continental crust show enrichment of LILE such as Rb, Cs, K and LREE (La, Ce) , depletion of Ti, Sr, Ta, Nb, Ba, Cs. Based on low values of magnetic susceptibility [(5 to 11) × 10-5 SI], therefore it is classified as belonging to the ilmenite-series (reduced type). The result of U-Pb zircon age dating of granodiorite is 161.85 Ma (Middle Jurassic, Callovian time). Based on Initial εNd isotope values for granodiorite is -6.51, initial 87Sr/86Sr and 143Nd/144Nd ratios for granodiorite is (0.70913 and 0.512095), the magma for granite and granodiorite originated from the continental crust. During Middle Jurassic (Callovian) due to continental collision, Upper Triassic to Lower Jurassic rocks is regionally metamorphosed. During the continental collision, Middle Jurassic (164-162Ma) reduced type granitoid magma (Ilmenite series, continental crust melting) formed and intruded these regional metamorphosed rock in Najmabad, Shah Kuh and Sorkh Kuh area.

Neyshabour turquoise mine is located in northwest of Neyshabour, southern Quchan volcanic belt. Eocene andesite and dacite forming as lava and pyroclastic rocks cover most of the area. Subvolcanic diorite to syenite porphyry (granitoids of magnetite series) intruded the volcanic rocks. Both volcanic and subvolcanic rocks are highly altered. Four types of alteration are recognized including: silicification, argillic, calcification and propylitic. Silicification is dominant followed by argillic alteration. Mineralization is present as stockwork, disseminated and hydrothermal breccia. Hypogene minerals are pyrite, magnetite, specularite, chalcopyrite, and bornite. Secondary minerals are turquoise, chalcocite, covellite, and iron oxides. A broad zone of gossan has developed in the area. Oxidized zone has a thickness of about 80 m. Mineralized samples show high anomalies of Cu, Au, Zn, As, Mo, Co, U, LREE, Nb, and Th. Both aeromagnetic and radiometric (U and Th) maps show very strong anomalies (10 × 5km) within the mineralized area. Based on geology, alteration, mineralization, geochemistry, and geophysics, Neyshabour turquoise mine is a large Iron oxide Cu-Au-U-LREE (IOCG) mineralized system. In comparison with other IOCG deposits, it has some similarities with Olympic Dam (Australia) and Candelaria (Chile). In comparison with Qaleh Zari and Kuh Zar mines, Neyshabour turquoise mine is the first Iron oxide Cu-Au-U-LREE (IOCG) mineralized system discovered in Iran.