فهرست مطالب حسن زمانیان

The Sarkuh porphyry Cu deposit located in the Urumieh – Dokhtar Magmatic Belt (UDMB), is associated with the emplacement of Miocene intrusions mainly containing granite – granodiorite within Eocene units including tuff, andesite, basaltic andesite, and pyroclastic breccia. Potassic alteration of the deposit (dominated by magnetite, secondary and re-equilibrated biotites as well as anhydrite) is well extended. In this study EDX spectra of accessory minerals within potassic alteration was assessed to trace the occurrence of rare minerals. Additionally, EMPA results of magnetite paragenesis were linked to physicochemical attributes of rare minerals occurrences. Results indicate that unusual occurrence of Ce-La rich epidotes with REE-enriched monazites and Ce-bearing titanites are accompanied with apatite, anhydrite, hydrothermal biotite, quartz, and magnetite assemblages in the potassic alteration. Magnetite composition implies that early-stages high temperature magmatic – hydrothermal fluids (>500 °C) with low rates of fluid – rock interaction were contributed in the magnetite crystallization. Commonly, these magnetites are accompanied by hematite and anhydrite providing insights into the very high oxygen fugacity conditions (near magnetite - hematite buffers ~ ΔFMQ+4). Considering the chemistry of magnetite paragenesis, it seems that the occurrence of rare minerals are mainly associated pre-ore stages in the potassic alteration

Paleoclimate is a new branch of science that investigates the climate changes of the past by using different sciences. Carbonates are a type of rocks that have been studied a lot in the geochemistry of stable isotopes and are found in all time intervals. A common type of carbonate rock is speleothem, which is capable of providing reliable records of climate change over many years. The studies conducted in the last decade show that the past climate can be understood by δ18O and δ13C. One of the common forms of speleothem is stalagmites, whose layers are known as a potential source of high-quality climatic information. By using speleothem, it is possible to reconstruct the climatic conditions up to about 600 thousand years ago. Comprehensive and complete information is not available about the climatic and environmental conditions of Iran during the Holocene period. Meanwhile, Iran's location as a transition zone between Europe, Asia and Africa is of great importance for study the past climate; However, compared to other regions, it has been less studied, which has provided a special position for this research. In the present research, it is intended to be analyzed with the help of the information received from a cave in the Zagros region of the past climate of Iran.

For paleoclimate analysis in central Zagros, Maghar cave in Khorramabad (located in Lorestan province and in Karkheh watershed) was selected. The condition of this cave is such that it has little connection with the environment outside the cave and is not affected by the wind and other meteorological parameters outside the cave. After evaluating inside the cave, a stalagmite with a length of about 18 cm and a diameter of 8 cm was selected. After cutting it, it was transferred to the soil mechanics laboratory of Lorestan University, where its surface was polished in order to observe the layers. Since the primary core of the stalagmite is not located right in the center, it can be concluded that the primary bed of stalagmite formation is located on a sloping surface, which caused the drop of water to move on the sloping surface after hitting the surface of the cave. As the limit has increased in length, it has grown in width. For dating, three points were considered, including the stalagmite primary core (D1), middle (D2) and on top of it (D3). Age measurement was done by Multi-Collector Inductively Coupled Plasma-Mass Spectrometer (MC-ICP-M) located in the laboratory of the University of Queensland, Australia. For stable isotope analysis, 34 samples were sent to Arak laboratory for δ13C and δ18O analysis, and the analysis was done by Isotope Ratio Mass Spectrometer (IRMS) (30 samples in the direction of stalagmite growth length and 4 other samples for Hendy test). According to the standard of this device, 50 mg of powder was prepared for each sample. This was done with the help of a dental drill and movement on the stalagmite layers. To determine the percentage of calcite and aragonite, 4 samples (50 grams each) were sent to the laboratory of Lorestan University for XRD testing.

According to the XRD results, the percentage of aragonite was considered zero for all four samples. According to the Hendy test, stalagmites are formed in isotopic equilibrium conditions. The age of three samples was estimated to be 550, 368 and 8.6 thousand years respectively. The analysis of δ18O isotopic results over time showed that the isotopic data is increasing with a relatively large slope, which indicates that the conditions of the studied area during the last 550 thousand years are becoming

Climatic periods are always changing and dry and wet periods have occurred on a larger scale in the form of glacial and interglacial periods. In the past, these changes happened very slowly, but in the last 5 thousand years, the changes are fast. These changes intensify over time. So that there have been sudden changes in the last hundred years. Today, climate change is not hidden from anyone, but unfortunately, it has not been found in a suitable solution. Many countries use different methods to prevent the damages of climate change in the future. It is clear that disturbing the order of nature disturbs the balance. Further research similar to the present research can tell the past climate in more detail.

Magmatic fluids released at the end of magmatic crystallization interact with carbonate country rocks through metasomatism and form the skarns (Meinert et al., 2005). In general, the magmatic rocks are associated with skarnization range from diorite-gabbro to granite in composition (Kuşcu et al., 2019). The ore deposits types (e.g., Cu, Au, Fe, Zn) are controlled by the nature of the magmatic source region (Wu et al., 2017). In this study, we first synthesized the spatial distribution, and geological and geochemical data of Late Mesozoic (Middle Jurassic–Early Cretaceous) granitoids and associated mineral deposits of Songhor plutonic in the northwest of Sanandaj-Sirjan zone and compared with worldwide skarn associated granitoids. Finally we try to reach a better understanding evolution of granitoid and correlations between skarns and the related mineralization of the Songhor plutonic assembleg during Late Mesozoic. 

Redgional geology:

The Galali Fe deposit is typical of skarn deposits in the Sanandaj-Sirjan metallogenic zone (SSZ), in the northeast Songhor. Mineralization in the Galali deposit is related to Songhor intrusive rocks assembleg (Eocene-Oligocene) and orebodies are predominantly hosted by Songhor Formation (Triassic-Jurassic). Petrography and geochemistry of Songhor granitoid complex (SGC) intrusive rocks have been investigated by some workers (i.e. Aliani, 2014).

Major oxides were determined using an X-ray fluorescence spectrometer, whereas the trace and rare-earth elements were analyzed by Inductively Coupled Plasma Atomic Emission Spectrometry (ICP-AES) at Zarazma laboratory company, Tehran Iran.Petrography, mineral chemistry, whole rock chemistry Based on mineralogy and geochemistry, three main facies have been recognized in the Songhor plutonic assemblage: (1) the granite (leucocratic), (2) monzonite to diorite (mesocratics) and (3) gabbro. In the Galali district both calcic exoskarn and endoskarn occur along the contacts between granitoid and host carbonated rocks. The field observations and the whole rock geochemical data obtained from the intrusive rocks in the northeast of Sonqor indicate the relationship between the region's deposits (Iron Skarn) and their tectonic and petrogenic nature.In general, Songhor granitoid complex mineralogically contain Ca-plagioclase and magnesio-hornblende, and it has a metaluminous (ASI < 1) composition, with LREE, LILE enrichment and HREE depletion. The SGC samples can be divided into two groups, based on their SiO2 contents, Na2O/K2O ratios, and incompatible elements compositions. The samples have a relatively wide range of SiO2 content and Mg# values, indicating that these units formed from magmas with variable amounts of fractional crystallization. In the Harker diagrams, there is a negative correlation between SiO2 and FeO, MgO, and CaO. Thus, these rocks record the hornblende and biotite fractionation. Similar to studies of Wu et al. (2017), the strong depletion in Ba, Sr, Eu, and Ti points to an extensive fractional crystallization during the emplacement.

Fractional crystallization would significantly increase the concentrations of W or the other incompatible elements in the magmas, which is necessary for the occurrence of related mineralization (Romer and Kroner, 2016). The results of this research indicate that the Songhor A-type alkali granite formed from the depleted mantle-derived magmas which have undergone assimilation and fractional crystallization processes. The progression from I-type to A-type magmatism appears to mark a significant change from a collisional to an extensional setting in this region, in the Late Jurassic. Geochemical characteristics in Rb versus Sc and Rb/Sr versus Zr diagrams show that mesocratic phase 1 unit, highly-oxidized and less-evolved granitoids generated by a mixture of mantle-derived and mature crust-derived components, related to subduction of Neo-Tethyan oceanic crust beneath the Sanandaj-Sirjan zone. These intrusions are syn-collisional and have a high potential for skarn Fe- Cu-Au deposits.The A-type leucocratic granite shows an alkaline nature, high potassium, high ratio Ga/Al, enrichment of HFSE (i.e. Ta, Nb, Ga, Zr, and Pb), Eu, and compatible elements (i.e. Cr) depletion in the pattern. It has formed in a magmatic arc or post-collisional setting from a hybrid source, with crustal and mantle components, contaminated by interaction with the upper crust. It is a highly-evolved granitoid that can be highly prospective for Mo, Sn, and W mineralization.

The study area is located at east of Bam city and southeast of Kerman province. This area is located at 45 km from the Bam-Zahedan Road. From the main asphalt road of Bam - Zahedan it has 15 km of dirt and car accessible road. It is part of the NW-SE trending volcanic belt east of Bam.

This study aims to geochemically investigate the behavioral pattern of hydrothermal mineralization elements in the region in order to determine local and regional uranium enrichment at 1: 5000 scale. For this purpose 616 lithogeochemical samples were collected and analyzed. The study area is located southwest of Allahabad 1: 250000 Map. The Eocene outcrops are divided into two classes of pyroclastic and lava based on 1: 5000 scale studies. These deposits are cut by numerous dykes with an approximate northwest-southeast trend. These basaltic-diabase dykes can actually be attributed to the Eocene. The most important statistical parameters used in interpretation of area data are mean, median, mode, variance, standard deviation, coefficient of variation, skewness and kurtosis which were calculated for all data.

After normalizing and eliminating outlier values data, the data were analyzed using Pearson correlation matrix method to identify the correlation coefficients of the elements that accordingly, the highest correlation of uranium was observed with Be, Cd, Co, Cu, Mn, Mo, Na, Ni, Sc, Se, Tl, V, Y, Zn, Zr, Ga, Ge, and Hf. It indicates the paragenetic relationship of these elements with each other.Based on data clustering, four groups of chemical elements can be of particular interest due to their strong association with uranium, which include:Rare earth elements: Y, La, Ce Polymetallic elements: As,Sb, Ba, Cu, Pb, Zn, Mn, Fe, Se, Sr Related to acidic volcanism: Be, Mo, W, Zr Related to basic magmatic activities: Co, Cr, Ni, V The pattern of uranium paragenesis element groups in this diagram is roughly consistent with previous studies in the field of uranium volcanogenic deposits. Based on factor analysis, an 8-factor model with 78.6% variance was obtained for 43 elements. The second factor with a variance coverage of about 12.5% contains As, Mo, Sb elements with high factor loadings and Ag, Be, Ce, La, Pb, Tl, U, W, Y elements with average factor loadings. This factor is related to uranium mineralization in the region. Based on the results of the statistical analysis and interpretation of the geochemical map of the uranium element, the enrichment limit for this element is considered to be 5.67 ppm and background and threshold values were 2.39 ppm and 4.3 ppm, respectively.

The impact of hydrothermal solutions is strongly observed on the volcanics of the area, resulting in geochemical imbalances. Mo in the region forms large lithogeochemical haloes that are highly consistent with U elemental haloes and are generally concentrated at high U concentrations. Due to the Mo mineralization in the deeper regions, probability of U mineralization also exists in the deeper parts of the region and it is anticipated that subsurface studies will show significant results in terms of the occurrence of U compounds. Much of the southern half of the region, except for abnormal areas, is consistent with fault trends and concentrated along fault lines. There is widespread argillic alteration in the Eocene units of the region, with enrichment of the REEs, especially associated with lanthanum. Increasing the intensity of alteration and increasing joints and fractures allow the fluid to move, thereby increasing the fluid / rock ratio and facilitating migration of anomalies. The trend of uranium anomalies is often consistent with the cerium, yttrium, and lanthanum anomalies, and is usually in the margins of the basic dykes which indicates the convection of these elements from a mineralized fluid. This indicates the mobility of rare earth elements during alteration processes and their concentration by geochemical dams, including basic dykes. By comparing the obtained paragenesis for the uranium element in the region and the geochemical pattern observed with different types of known uranium deposits in the world, the most likely option for the type of mineralization in the region, is volcanogene uranium type.

Computer games are a kind of growing and attractive new communication technology. This has prompted researchers to study the effects of these games on users. This study aims to determine was performed the prevalence of computer game addiction and related factors in adolescent boys of Gonabad in 2018.

In this cross-sectional descriptive-analytical study, 507 male students of the first-grade in Gonabad were examined by multi-stage sampling method. Data collection tools were included in two sections: Demographic Information and the Lumens Computer Games addiction questionnaire. The data were analyzed by using SPSS software (Version 19) with the help of the Chi-Esquire and Fisher's exact test.

The average age of the students in this study was 13.5 ±1 years. The most popular feature of computer games is a lot of excitement (42%), competitive games (29%) and the most common types of computer games were football (48.9%) and violent games (21.7%). 28.4% of students went to Game Center to play computer games. The prevalence of dependence on computer games was moderate to high (73.2%) It showed a significant relationship with the level of education of the mother (P = 0.03), playing computer games by the parents (P <0.001) and the educational level of the students (P = 0.04).

The results showed that the highest level of dependence of students was at the intermediate level, which indicates the importance of the problem and the need for the authorities to intervene in this field.

The Kalchuye Cu-Au deposit is located in the central part of the Urumieh – Dokhtar magmatic arc. This mineralization is mainly hosted by diorite, quartz diorite and andesite rocks. The mineralization is characterized by chalcopyrite, pyrite, galena and magnetite in the hypogen stage followed by chalcocite, covellite, malachite and goethite in supergen stage. According to the geochemical studies, the Lan/Ybn ratio is between 2.2 to 6.3 and Eu/Eu* varies from 0.7 to 1.1; so that intrusions which are the host of mineralization in the Kalchuye region represent characteristics of magmas in the subduction zone (enrichment of LILE, depletion of HFSE in association with negative Ti anomaly). Fluid inclusion data show the temperature of 150-310 ˚C, salinity of 0.1- 4 (wt%NaCl eq.) and depth of 400m, approximately, for the Klchuyeh deposit. Fluid evolution in the Kalchuye exhibits cooling, surface dilution and boiling. Evidences such as bounded and comb textures in quartz, bladed calcite, hydrothermal breccia, propelitic alteration and fluid inclusion information such as temperature and salinity prove the low-sulfidation epithermal nature for the Kalchuye deposition.

The study area is located 45Km NE Zanjan in the Azerbaijan-Western Alborz zone. Quartz-monzonite and dacitic brecciated tuffs are the main host rocks to the Lubin-Zardeh deposit. These rocks are predominantly of K-high calc-alkaline shoshonitic I-type, metaluminous magnesian affinities of Cordilleran type. The intrusive rocks are enriched in LILE, LREE and depleted from HFSE, MREE and HREE and Y. A listric-shaped REE pattern and average La/Yb ratios of host rock indicates higher water content and fO2 in the magma and hornblende fractionation. Their relatively low to moderate ISr values (0.7047–0.7051), positive εNd (t = 36 Ma) values (0.39–2.1) and TDM ages of 0.69 to 1.06 Ga, with Pb isotopic ratios of (206Pb/204Pb) i = 18.49–18.68, (207Pb/204Pb) i = 15.58–15.61 and (208Pb/204Pb) i = 38.33–38.77. Based on textural evidence (coarse amphibole crystals), geochemical data (major, trace and Rare earth elements) and isotopic contents of Pb, Sr-Nd, it is suggested that these rocks correspond to geochemical and isotopic compositions of the host rocks of porphyry and epithermal deposits in the Urmia Dokhtar zone of West Alborz-Azerbaijan (Arasbaran) and Eastern Pontides epithermal deposits, Turkey.

The Milajerd prospecting area is located within 100 km of western Ardestan and belongs to Naein-Natanz prospecting region. This area is one of the favorable target areas that have been defined by multidiscipline GIS-based metallogenic modellings for metallic resources. This area consists of two main zones with different geologic and geophysical (magnetic) characteristics. The first zone (on the west and south) presents sialic continental crust with Gondwana-type Paleozoic-Middle Triassic epi-platform sediments that is covered by Eurasian-type Upper Triassic to Lower Jurassic coal-bearing silici-clastic series of Nayband Formation. The Nayband Formation is overlaid by Cretaceous conglomerate -sandstone beds that are followed by limestone and marls upward.  The conglomerate and sandstone beds present angular unconformity with Nayband and older formations. The second zone on the east and north belongs to Molla-Ahmad-Karkas arc-type volcano-plutonic belt, which is composed of intermediate to acidic Eocene volcanic series that have been intruded by Late Eocene to Miocene granitodes.

The Milajerd Pb-Zn±Au polymetallic prospecting zone in Naein-Qom Magmatic Zone is one of the favorable targets defined by multidisciplinary metallogenic modellings for gold and base metal resources. Ground controlling of the aforesaid target area has been carried out by coarse 1000*1000 m2 grid litho-geochemical surveying. A total of 176 rock-chips samples each weighting 1500gr were collected. Each of them was  assayed by ICP AES method  in Kanpazhuh Laboratory for  Au,As,Ag,Ba,Pb,Zn, Cu,Mo, Ni,Co,V,Ti,P,Bi,Cr,Fe,In,La,K,Na,Mg,Mn,S,Sb,Sc,Sr,Th,U,W,Zr.

The main approach for evaluating the favorability and mineral resources, was data processing and information analysis based on defining “Polarized Geochemical Systems (PGS) and related depleted, background and enriched zones. These zones are spatially forming unified systems referred to as” PGS” and present localities of ore deposit formation. According to the defined PGS, there are four systems with three expected types of ore mineralization; 1) porphyry Cu-Mo-(Au), 2) contact- halo Polymetal, and 3) epithermal gold ore formation. There is good correlation between lost copper in depleted zones and its concentrated amount in enrichments zones.

It is estimated that the depleted value would be almost equal to 1,969,800 t that is probably accumulated in enrichment zones. The tonnage of enriched copper is estimated to be 2,063,500 t (probably originated from Eocene-Miocene volcano-plutonic rocks and the Crust), almost equal to depleted value. These values could be considered as the key criteria to assess the favorability of the prospecting area for aforesaid-types’ ore mineralization.

The Rangraz area is located about 20 km north of Saveh, which is situated in the central part of Uromieh–Dokhtar magmatic arc. The exposed rocks in the study area consist of a volcanic and volcanoclastic subvolcanic dikes and quartz monzodiorite intrusions. Mineralization in this area is mostly related to the silicic, argillic and chloritization alteration assemblages. The Rangraz area consists of 6 mineralized zones and mineralization appears in veins-veinlets and dissemination. The main ore minerals are chalcopyrite, specularite, pyrite, magnetite, bornite, chalcocite, covellite, and the gangue minerals are quartz, barite, and calcite. Supergene processes in the upper part of the mineralized zones have led to the formation of malachite, azurite, hydrated Fe and Mn oxides, covellite, chalcocite, and digenite. Gold in the study area does not occur as a free mineral, but the SEM observations revealed that chalcopyrite and specularite have a high content of gold. According to geochemical data, igneous host rocks in this area are calc-alkaline in nature and are formed at a magmatic- volcanic arc zone. In comparison with primitive mantle, they are enriched in LILE elements (Ba-k) and depleted in HFSE elements (Nb-Ti) and such pattern is similar to subduction environments. In addition, enrichment of LREE relative to HREE in chondrite normalized diagram show that the igneous rocks are formed in a subduction zone

Bagoushi deposit is located in 37 km northwestern Masiri in Fars province. Structurally the deposit is situated in the Zagros Simply Folded Mountain belt and developed in Upper Cretaceous carbonates. From the top to bottom, the deposit is consisting of red, pisolitic, brown, brecciate, and kaolinitic bauxite horizons. Boehmite, kaolinite, hematite, pyrophyllite, anatase, calcite and diaspore are the major mineral phases. The main ore textures of the deposit include pisolitic, pisolitic-oolitic and clastic with pelitomorphic and microgranular matrixes. According to the formation conditions of the major minerals, the Bagoushi deposit formed in an environment ranging from acidic-oxidizing surface water to basic and reducing groundwater. Some textural features such as pelitomorphic matrix, pisolitic and oolitic textures, radial fractures in pisoids, growth of simple cortex around earlier pisoids, pisoids with cortexes lacking radial and circular fractures, are indicative of allochthonous origin; and broken pisoids, allogeneic pisoids and clastic grains reveal the transportation of bauxitic materials; therefore the bauxite materials is authigenic, but in some parts were transported and re-deposited, at least locally. The mass change calculations relative to the immobile element Ti show that elements such as Si, Fe, Mg, K and Na are leached out; Al, Zr, V, Th, Nb, Ba and REEs particularly LREE are concentrated; and Hf, Ta, Co, Rb, Cs, Be and U are relatively immobile during the bauxitisation process. The bauxite ores are characterized by progressive enrichment of the REE compared to parent rock, intense LREE/HREE fractionation, relatively stable negative Eu anomalies, and weak negative Ce anomalies.

The Rangraz copper deposit is located in 18 km of northern Saveh which is in the central part of the Uromieh–Dokhtar magmatic arc. The host rocks are mainly volcanics and volcaniclastics of Eocene which altered and mineralized by intruding the quartz monzodiorite intrusion and andesitic-basaltic dikes in them. Hydrothermal alterations are propylitic, sericitization, silicification, and the chlorite-clay minerals-quartz assemblage. The principal hypogene ore minerals include pyrite, chalcopyrite, bornite, specular hematite, and magnetite. The Rangraz quartz monzodiorite composes of plagioclase, K-feldspar, quartz, fine grain biotite and amphibole shows granular to porphyritic textures. These rocks are commonly metaluminous and calc-alkaline. The high CaO (2.61 to 5.81) and Na2O (6.90 to 7.78) and low K2O(0.04 to 0.38), Fe2O3 (2.60 to 4.58), and MgO(1.22 to 2.81) contents can be caused by the extensive propylitic alteration in intrusion rocks of the study area. According to the tectonic setting discrimination diagrams, and trace and rare earth elements distribution patterns, depletion of Ti, P and LREE enrichment are the subduction at active continental margin tectonic characteristics. Significant negative Eu anomalies and relative depletion in Sr indicate the presence of plagioclase as a stable phase at magmatic source. The result of petrogenetic studies represent that crystal fractionation, and magma mixing were the most dominant processes controlling magmatic evolution.

The Urumieh-Dokhtar Magmatic Assemblage (UDMA) forms a distinct NW-SE linear intrusive– extrusive complex Magmatism of the UDMA that occurred from Eocene to Quaternary, although the maximum activity was in the middle Eocene (Berberian and King, 1981; Ghasemi and Talbot, 2006). Collision of Arabian and Iranian plates led to termination of Neo-Tethys crust subduction and magmatism activity was abated in the UDMA, although there is no common agreement on collision timing. The Takht magmatic complex is located in the north of the Hamedan province (west Iran), and it belongs to the UDMA. The assemblage of volcano-plutonic rocks is present in the study area. The volcanic rocks include dacite, rhyodacite and trachyandesite with some tuff and agglomerated and the plutonic rocks are mostly occupied by granodiorite and diorite (containing mafic micro-granular enclaves) with some gabbro. These bodies are mostly intruded in Jurassic schists and are in contact with Cretaceous limestone leading to the formation of a skarn iron-ore deposit. The detailed geochemical and isotopic data is lacking and the age of the Takht granodiorite has not been determined. In the present study, the authors mainly have focused on the geochemistry and Sr-Nd isotopic ratios of the Takht magmatic complex to clarify questions regarding pterogenesis and its geodynamic evolution. We also reported U–Pb zircon ages for Takht granodiorite to study the relationship between its genesis and geological evolution history of the UDMA. A total of about 80 samples from the Takht plutonic-volcanic rocks were collected. 16 plutonic-volcanic samples were selected for wholerock chemical analysis. Major element oxides were analyzed by the X-ray fluorescence spectrometry (XRF) method using an Optima 7300DV XRF instrument in the Lab West laboratory, Australia. Trace elements were also analyzed in this laboratory with the inductively-coupled plasma mass spectrometry (ICP-MS) method using a NeXION 300 ICPMS instrument. Three chip samples with equal weight (4.5 kg) were collected from the Takht granodiorite. Then upon mixing, average samples were obtained for U–Pb dating of zircon. Hand-picked zircon crystals were supplied to the ALC (Arizona Laser Chron Center) in Arizona University. The 14 selected samples for Nd-Sm and Rb-Sr isotope analysis were crushed to less than 60μm. All isotope analyses were performed on a Nu Instruments Nu Plasma HR in the MC-ICP-MS facility, in the University of Cape Town, Rondebosch, South Africa. The plutonic rocks have metaluminous nature and are of calc-alkaline affinity. The Sr/Nd, Nb/La and Th/U ratios of the granodiorite show that its magma was formed mainly by melting of continental crust, and that its enclaves were formed from a mantle derived mafic magma. The samples have negative anomalies in Nb, Sr, Ti, P and Eu and positive anomalies in Th, K, Zr, Yb and Rb thus indicating contribution of mantle and crustal materials in their generation. The Takht granodiorite has geochemical features of I and A-type granites and also shows properties of both volcanic arc and within plate magmatism association granitoids (high levels of LILEs and HFSEs). In order to obtain better results, all the data were plotted on a common 206Pb/238U versus 207Pb/235U diagram. The results show an age of 16.8 ± 0.24 Ma (Middle Miocene) for the Takht granodiorite. Based on the results, the Takht granodiorite was generated in Miocene. In the Takht magmatic complex initial 87Sr/86Sr range from 0.70678 to 0.70778 and εNd also changes from -0.79398 to -5.83370. Nd-Sm isotopic contents and trace element ratios indicate that the Takht magmatic complex has originated from oceanic slab break-off with continental crust mingling in the post-collision stage. The εNd (16.8 Ma) vs. initial 87Sr/86Sr ratios diagram reveals, the role of continental crust materials in the generation of the granodiorite samples, while where the enclaves lie are plotted in the mantle evolution array field. The Takht magmatic complex has geochemical properties of arc related igneous rocks such as Ba, Nb, Sr, P, Ti and Y negative anomalies and for Rb, Th, U, K, Nd and Zr positive anomalies. Most of the Takht area samples are plotted in the triple junction of volcanic arc granites (VAG), within plate granites (WPG) and syn-collision (syn- COLG) on Y versus Nb and the Y+Nb versus Rb diagrams (Pearce et al., 1984). These data suggest post-collisional tectonic setting for the Takht magmatic complex. Field, microscopic and geochemical evidences indicate that simple fractional crystallization of a mafic magma was not the only processes involved in the generation of the studied rocks. On this basis, continental crust material had extensive contribution in the generation of the granodiorites whereas the enclaves are from mantle derived magmas. Relatively high fractionated REE patterns of the granodiorite samples with high LREE/HREE indicate an amphibole-bearing, garnet-free source for the samples while small to moderate negative Eu anomalies require residual plagioclase in the source. The granodiorite samples basically have geochemical properties of I-type granites and it is confirmed by their Nd and Sr isotopic ratios. However, relatively high HFSE contents make them similar to A-type granites. Melting of a former continental arc crust and contamination with mantle derived magmas led to both volcanic arc and within plate geochemical properties of the granodiorites that make them similar to I-type and A-type granitoids. The age of 16.8 ± 0.24 Ma (Middle Miocene) of the Takht granodiorite is consistent with the other post-collisional igneous rocks of the area and regarding its post-collisional geochemical properties the age of collision and related orogeny must be considered at least before Miocene.

The studied area is located in the central Iran micro-continent, in the southern part of Lut block, 45 kilometers east of Bam Township. The main units of the area are mostly intercalation of pyroclastic rocks and lava layers in the age of Eocane, with the general trend of southwest- northeast and include high potassium calc- alkaline magma that their formation are related to the tectonic environments of magmatic arc and subduction zone. Argillic, silica, hematite, zeolite and chlorite alteration are observed in the area in relationship with uranium mineralization. The geochemical complexes related to uranium presence were identified in the study area. They are: complexes in relation with acidic and moderate rocks, including U-W-As-Mo-S-Cu-Ag, and complexes related to the basic igneous rocks, including U-Ni-V-Ag-Co-W-Mo-Cr-Cu-S. The main observed structures and textures in this area involve stock work, vein veinlet, corrosion, radial, release and peripheral membrane. The main mineralization in the area includes uranium secondary minerals contains Boltwoodite, Phosphuranylite and carnotite, manganese oxides, iron oxides and hydroxides, a few sulfide, zeolite mineral group and other minerals groups which mostly are formed under the influence of hydrothermal and late supergene processes. Based on a comparison pattern of mineralization in the area and its adjustment with the geological, alteration and geochemical conditions in uranium deposits, the most possible choice for mineralization type in the area has been introduced as volcanogenic uranium mineralization.

The Takht iron deposit is located 120 km northeast of the Hamedan City in the Urumieh-Dokhtar magmatic belt. The Miocene Takht granodiorite intruded into the Cretaceous carbonates and resulted in Fe-skarn formation. Epigenetic mineralization in the Takht Deposit occurred predominantly as vein and lenticular ore bodies accompanied with argillic, carbonation, chloritization, epidotization and silicfication alterations and minerals including garnet, pyroxene, epidote, tremolite- actinolite, phlogopite, hornblende, quartz, calcite, magnetite, pyrite, specularite, chalcopyrite, hematite, limonite, goethite and malachite. Chemical composition indicates the presence of Si, Al, Ca, Mg, Ti and chalcophile elements such as Cu, Zn, As and Pb that originate from the coexistence of silicate and sulfide minerals with magnetite. The microthermometric results revealed homogenization temperatures (Th) from 153.2°C to 338.3°C and salinity from 0.827 wt.% NaCl eq. to 25.36 wt.% NaCl eq.. The δ18O (SMOW) values of magnetite were measured in the range of −0.46‰ to .31‰ and δ18O water is .1‰ to .9‰, respectively. These isotope values are similar to magmatic fluids that were also equilibrated with 18O enriched sources. The δ34S (V-CDT) values of pyrite show ranges of .3‰ to .5‰ and the original fluid δ34S H2S values were estimated ranging from .7‰ to .9‰. These positive δ34S values confirm that sulfur is provided by evaporate sulfates. During the retrograde stage of the Takht Skarn, re-mobilized metals accompanied with metal-bearing fluids (provided by intrusion) were mixed with sulfur-bearing descending meteoric waters and eventually, the mixing of the two fluids led to calcic Fe-skarn mineralization in Cretaceous carbonates.

The intrusive bodies of Almogholagh Batholith, in western Iran are emplaced into the Sanandaj–Sirjan magmatic-metamorphic zone and comprise three main groups: (1) gabbro-diorite, (2) quartz syenite, and (3) quartz monzonite, which crop out in most of the area. The quartz syenite and quartz monzonite rocks, having characteristics such as metaluminous, generally ferroan, alkalic to alkali-calcic types, high content of Na2O⭣, Zr, Ce, Ga, Y, Nb, Ta, REE, and depletion in Eu, Sr and Ti, show the features of borderline between A1 and A2-type granitoids with more A1-type affinity. On the basis of the results of the various diagrams, the gabbroic-dioritic rocks show between A1 and I-type granitoids nature with more I-type affinity. Distinctive peak patterns in spider diagrams accompanied by (La/Yb)CN values of 2.4 to 6.1 and Ba/La ratio >3 indicate magmatic activity in a volcanic arc environment, and the characteristics (Ba/Rb)CN 0.512638, εtNd >0, εtSr >0, high content of Nb, Ta and very high content of Zr (589 ppm) indicate that there was a subsidiary subduction after the initial collision for a long time and the magmas of Amogholagh batholiths were originated from mantle wedge, overlying the subduction zone or from mantle components around fragments resulting from delamination between continental crust and mantle lithosphere, demonstrating the involvement of subduction zone fluids, high flux of mantle-derived halogen-rich volatiles, and contamination within the crust during the petrogenesis of intrusions.

The Mazraeh Shadi is located about 130 km northeast of Tabriz (NW Iran) in the Arasbaran metallogenic belt. The deposit occurs as a series of veins within the Eocene andesites. Mineralization shows epithermal system that controlled by fault distribution. Epithermal textures within the veins include comb, vaggy quartz, cockade, boxworke, plate calcite and breccia. Pyrite is the main ore mineral associated with chalcopyrite, chalcocite, covellite, sphalerite, galena and gold. The result of geochemistry on the small rock samples from silica veins shows values of gold (max17100 ppb), Pb(max 21100 ppm), Ag(max 9.43ppm), Cu(max 611ppm) and Zn (max 333 ppm). Microthermometric studies were conducted on quartz samples from silicified and mineralized zones and provides substantial micro-thermometric data for a new interpretation. Fluid inclusions generally occur in range from 5 to 90 μm in size. Three types of fluid inclusions are typically observed at Mazraeh Shadi:(1) liquid-rich two-phase, (2) vapour-rich two-phase (3) vapour-rich mono-phase. The homogenization temperatures of all inclusions from 160 to 324 °C and the average of homogenization temperature is 228°C .The salinities are 0.17–5.1 wt.% NaCl equiv. The last ice-melting temperature is between –2.2 and -3.2°C. All fluid inclusions are plotted into the epithermal box and into the region between the primary magmatic water box and the meteoric water. Mineralization of Au is the result of pyrite precipitation, dilution- mixing of an oxidized meteoric water decreasing of pH, boiling and fluid mixing and there are two fluids participated in the formation of Mazraeh Shadi deposit. Fluid inclusion data shows the depth of mineralization at Mazraeh Shadi deposit probably ranged from 230 m to 380 m below the paleosurface and three-dimensional graphs confirm the deposition of lead and zinc in with high temperature-low salinity fluid and deposition of gold with low temperature-high salinity fluid. The zoning pattern shows clearly base metals such as Cu, Pb, Zn and Mo occur at the deepest levels, whereas precious metals occur at higher elevations with respect to base metals due to boiling of hydrothermal fluids in epithermal system.

The Samen granitoid is located along the northwestern part of the Sanandaj- Sirjan Zone in the Southwestern of Malayer. Based on mineralogical and geochemical characteristics, five main facies have been recognized in the Samen granitoid which included granodiorite, monzogranite, syenogranite, alkali-feldspar granite and quartz-monzonite. Granodiorite is the main facies of the pluton and is more wide spread than other facies. Geochemistry of major elements indicates that the Samen granitoid is metalomious (ACNK=0.75) to peralomious (ACNK=1.21) and is classified as volcanic arc granites (VAG) related to active continental margins and petrochemically belongs to calc alkaline with high K rock series. Depletion in Nb, Zr, Hf, Y, Ti and HREE and enrichment in K, Rb, Cs, Th and LREE is consistent with an arc setting related to the subduction of Neo-Tethyan oceanic crust beneath the Sanandaj-Sirjan zone. The pluton has been contaminated by interaction with upper crust. In the Samen district both calcic exoskarn (grossular-andradite/augite-diopside) and endoskarn (tremolite-actinolite/epidote) occur along the contacts between granitoid and marble. The present study indicates that geochemical characteristics of the granodiorite and quartz-monzonite Samen rocks are similar to the averages for Au-Cu- and Fe- skarns granitoids, whereas the geochemical characteristics of the monzogranite, syenogranite and alkali-feldspar granite are similar to averages for Sn- and Mo-skarn granitoids. Based on oxidizing conditions and magma evolution, the Samen granitoid is characterized by relatively unevolved to moderately evolved and oxidized suites, as in most Au-Cu core metal associations globally.

Considering the high resistance of quartz against stress and alteration, this mineral was chosen for Geothermobarometry in Almogholagh intrusive masses. To determine the temperature and pressure of crystallization of quartz, the amount of Ti contained in the quartz was measured by Electron Microprobe –Analyzer method and then, the pressure and temperature of crystallization of analyzed points were calculated. The growth and crystallization temperature range of quartz was determined using the P-T diagrams were drawn and contoured. The results show that the negative effects of stress and active fluids on the calculated crystallization temperature can be reduced by contouring. Moreover, in this study, it was found that quartz crystals of intermediate-to-basic rocks and the acidic rocks have been crystallized in a temperature range of 683 to 757 °C and 667 to 741 °C respectively. The examination of fluid inclusions in quartz veins by heating and freezing stage microscope showed that silicic veins in intrusive masses and in the immediate adjacent rock have been formed at temperatures between 134 to 255 °C.

The Mombi bauxite deposit is located about 160Km northwest of Dehdasht in the Zagros Simply Folded Belt. The bauxite deposit exhibits an ooilitic and pisolitic texture. It contains higher amount of boehmite than those of diaspore, hematite, kaolinite, and anatase. This study uses the geochemistry of immobile elements in order to calculate the mass changes that took placed during weathering and bauxitization. The results reveal that elements such as Si, Fe, Mg, P, K, Ba, Sr and Zn are depleted, while Al, Zr, V, Cr, Ni, Ga, Y and LREEs indicate positive mass changes during the weathering and bauxitization processes. In addition, Nb, Hf, Ta, Rb, Cs, U and HRRE exhibit little changes, suggesting relatively immobile features. Interelemental relationship analyses of the ores, by using R-mode factor analysis, revealed a number of key findings: (i) some low solubility elements were concentrated in detrital zircon (Zr), in anatase (Ti), and possibly in boehmite, hematite and detrital minerals (Ga) during the later stages of bauxitisation; (ii) Fe was concentrated during humid climatic conditions, whereas Al accumulated during dry conditions; (iii) similar and meaningful weightings for U and Th suggest that heavy minerals frequency would be locally important in controling the uranium behavior; (iv) distributions of LREEs and HREEs are controlled by the stability of the carrier complexes of REEs and the existence of REE-bearing mineral phases; and (v) (La/Yb)n ratio values suggest that little LREE/HREE fractionation occurred during bauxite formation and (La/Yb)n ratio fluctuations may also be indicative of fluctuations of pH in soil solution.

The Senj deposit has significant potential for different types of mineralization, particularly porphyry-like Cu deposits, associated with subduction-related Eocene–Oligocene calc-alkaline porphyritic volcano-plutonic rocks. The study of fluid inclusions in hydrothermal ore deposits aims to identify and characterize the pressure, temperature, volume and fluid composition, (PTX) conditions of fluids under which they were trapped (Heinrich et al., 1999; Ulrich and Heinrich, 2001; Redmond et al., 2004). Different characteristics of the deposit such as porphyrtic nature, alteration assemblage and the quartz-sulfide veins of the stockwork were poorly known. In this approach on the basis of alterations, vein cutting relationship and field distribution of fluid inclusions, the physical and chemical evolution of the hydrothermal system forming the porphyry Cu-Mo (±Au-Ag) deposit in Senj is reconstructed.
Over 1000 m of drill core was logged at a scale of 1:1000 by Pichab Kavosh Co. and samples containing various vein and alteration types from different depths were collected for laboratory analyses. A total of 14 samples collected from the altered and least altered igneous rocks in the Senj deposit were analyzed for their major oxide concentrations by X-ray fluorescence in the SGS Mineral Services (Toronto, Canada). The detection limit for major oxide analysis is 0.01%. Trace and rare earth elements (REE) were analyzed using inductively coupled plasma-mass spectrometery (ICP-MS), in the commercial laboratory of SGS Mineral Services. The analytical error for most elements is less than 2%. The detection limit for trace elements and REEs analysis is 0.01 to 0.1 ppm. Fluid inclusion microthermometry was conducted using a Linkam THMS600 heating–freezing stage (-190 °C to  °C) mounted on a ZEISS Axioplan2 microscope in the fluid inclusion laboratory of the Iranian Mineral Processing Research Center (Karaj, Iran).
The Cu-Mo Senj deposit covering an area about 5 km2 is located in the central part of the Alborz Magmatic Arc (AMA). The Nb/Y versus Zr/TiO2 diagram (after Winchester and Floyd, 1977) illustrates a typical trend for the magmas in the Senj magmatic area–starting from basaltic and evolving to dacite/rhyodacitic compositions, with few data plotting in the alkali basalt field. Most of the igneous rocks plot within the medium- and high-K fields in the K2O versus SiO2 diagram. The igneous rocks from the Senj area define a typical high-K calc-alkaline on SiO2 versus K2O diagram (Le Maitre et al., 1989). All studied rocks show similar incompatible trace element patterns with an enrichment of large ion lithophile elements (LILE: K, Rb, Ba, Th) and depletion of high field strength elements (HFSE: Nb and Ti), which are typical features of magmas from convergent margin tectonic settings (Pearce and Can, 1973). At least three veining stages namely QBC, QM, and QP which are related to alteration and mineralization are distinguished at the Senj mineralized area. Three distinct alteration assemblages including K-feldspar-biotite-sericite-quartz, quartz-sericite-K-feldspar-pyrite, and K-feldspar-biotite-sericite-quartz, are distinguishable with these veins. About 80 % of the copper at Senj is associated with the early QBC-stage veins, with another 5 to 15 % in the QM-and QP-stage veins. About 70 % of the molybdenite occur in QM veins.
Fluid inclusion distribution, fluid chemistry, and homogenization behavior document that S2-type fluids are samples of magma-derived aqueous-saline fluids characterized by high salinity and temperature, and high Cu content. Such parental fluids scavenged Cu and Mo from the melt below and transported them to the hydrothermal system above. The increased abundance of S- and LV-types inclusion coinciding with the highest grade Cu mineralization (early QBC-stage veins) at the Senj deposit suggests that brine-vapor unmixing and phase separation plays an important role in Cu-ore precipitation and alteration zonation. In addition to unmixing, cooling and water-rock interaction also played important roles in chalcopyrite precipitation at the Senj deposit.
Compositions, deposit-scale distribution, and trapping conditions of fluid inclusions can be explained by the continued influx of a parental high salinity magmatic hydrothermal fluid, with no significant change in the bulk composition of the input fluid over the integrated lifetime of ore metal precipitation and vein formation. Fluid inclusion evidence and vein-cutting relationships indicate that molybdenum mineralization (QM vein) occurred at moderate temperatures coinciding with phyllic alteration, rather than from later, lower temperature fluids. Furthermore, early fluids decompressed rapidly relative to cooling, forming quartz-stockwork veins with K-silicate alteration at depth and QP veins at shallower levels in the Senj deposit. Later, as the hydrothermal system waned, the rate of decompression relative to fluid cooling slowed, causing the fluid to remain above its solvus, forming barren quartz-dominated veins with quartz-kaolinite±illite alteration which overprint much of the deposit.

The Sarvian magnetitic skarn deposit has been formed due to the granodiorite injection into the oligomiocene limestones. It is a calcic skarn deposit with dominated exoskarn section. Garnet and pyroxene are two coupled indicator minerals that have been formed by Mg-Si-Fe-bearing fluid remained from magma crystallization. These minerals are observed extensively in the metasomatic haloes in the country rocks and could be used to determine the conditions of temperature and pressure that have been governed on skarnization. It is revealed from microprobe analysis that the garnets in the Sarvian deposit are of the grossular-andradite type that are enriched in Fe & Ca, and depleted in Mg & Mn. These garnets show a sharp zoning structure. The distributions of MnO, CaO, Al2O3 and FeO in the zoned garnets indicate that from the core to rim, their composition changes gradually from grossular to andradite. The composition of the garnets and pyroxenes in the Sarvian ore deposit is compatible with the Fe-skarn deposits. Pyroxenes in the Sarvian ore deposit are of Ca-riched diopsid-hedenbergite type. During the prograde stage in which the anhydrous minerals such as garnets and pyroxenes were formed, the temperatures are comparable with albite-epidote and hornblende-hornfelse facieses. According to the temperatures of the garnet-clinopyroxene minerals formation, the temperatures of prograde stage have been determined between 370-500 °C. On the other hand, the results of fluid inclusion studies on quartz grains obtained from mineralized veins suggest that the temperatures during the iron mineralization in the retrograde stage of skarnization have been 400-380 ° C.

Lohneh gold and copper deposits lay in the north west of Iran, 100 kilometers north of Zanjan province. Lohneh mining area is a part of the Tarommetallogenic zone in the Alborz-Azerbaijan region. The presence of numerous minerals, slag melting of mining activities (such as cows and exploratory pits, tunnels) in the Armenian fortress (by Armenian miners) shows that the mineral reserve Lohneh have been considered by old miners. There are 9 gold bearing quartz veins .Two main quartz vein with a length of 500 meters and a width of one meter (visible on the Earth). Rock outcrops in the area consist of the Eocene-Oligocene volcanic rocks (tuffs, tuff breccia, trachyandesite) and intrusive rocks (granodiorite, quartz monzonite, monzonite). On the basis of geochemistry study, intrusive rocks is resemble the I-Type granitoids and a magmatic stand point, the rocks of the area are calc–alkaline, and tectonically they belong to the continental margin and subduction zones. Tuff breccia rocks cut by quartz monzonite and has been altered. The major alteration of the areas consists of silicious, sericitic, and argillic alteration. The main gold minerals have occurred in tuff breccia rocks and a small amount of gold mineral in quartz monzonite. Gold mineralization in the Lohneh area is in the form of open space, vein-veinlet and hydrothermal breccia. According to chemical analysis of gold mineralized samples gold grade is in the range of at least 0.002 to 10ppm. The average gold grade is 4.35ppm. Mineralogy of Lohneh deposit has a metallic minerals (oxide, sulfide) and non-metallic (silicate and carbonate) which is composed of two phases hypogene and supergene. Metallic minerals are including gold particles (free in siliceous gangue and visible under a microscope and SEM study), silver (in the free form in siliceous and involved in galena and tetrahedrite network), pyrite, chalcopyrite, bornite, galena, sphalerite, and tetrahedrite. Non-metallic minerals or gangue consist of quartz, hydrothermal alkali feldspar (adularia), sericite, clay minerals, calcite, and small amount of barite. According to geochemical studies (table correlation of elements, graph clustering and component plot in rotated space) gold with Ag(0.78), cu(0.81), As(0.7), Pb(0.64), Zn(0.6), S(0.4), Bi(0.45), U(0.3), Mo(0.25) is a significant correlation. This correlation geochemistry is corresponded with mineralography evidence (mineral paragenesis sequence) and SEM studies. Fluid inclusion study was performed on primary, large size and rich liquid fluid inclusions on quartz mineral (concurrent with the formation of gold and sulfide minerals).Fluid inclusion data shows in the temperature range 125 to 290 °C and salinity between 1 and 6.5 wt% NaCl and depths less than 1000 m. Fluid inclusion evidence shows cooling effect, boiling and formation of solutions with high salinity and density of the ore forming fluids in Lohneh deposits. Adularia mineral, calcite, bladed and comb quartz and hydrothermal breccia are evidence of boiling effect in the Lohneh deposits.Evidence of the presence of epithermal textures (banded, comb, blade, and hydrothermal breccia), sericitic alteration, and sulfide minerals such as galena, sphalerite, chalcopyrite, tetrahedrite, and fluid inclusions evidence (temperature, salinity, density, vapor-rich inclusions) indicates intermediate sulphidation epithermal gold deposits in Lohneh area.

A wide variety of world-class porphyry Cu deposits occur in the Urumieh-Dohktar magmatic arc (UDMA) of Iran.The arc is composed of calc-alkaline granitoid rocks, and the ore-hosting porphyry intrusions are dominantly granodiorite to quartz-monzonite (Zarasvandi et al., 2015). It is believed that faults played an important role in the emplacement of intrusions and subsequentporphyry-copper type mineralization (Shahabpour, 1999). Three main centers host the porphyry copper mineralization in the UDMA: (1) Ardestan-SarCheshmeh-Kharestan zone, (2) Saveh-Ardestan district; in the central parts of the UDMA, hosting the Dalli porphyry Cu-Au deposit, and (3) Takab-Mianeh-Qharahdagh-Sabalan zone. Mineralized porphyry coppersystems in the UDMA are restricted to Oligocene to Mioceneintrusions and show potassic, sericitic, argillic, propylitic and locally skarn alteration (Zarasvandi et al., 2005; Zarasvandi et al., 2015). In the Dalli porphyry deposit, four hydrothermal alteration zones, includingpotassic, sericitic, propylitic, and argillic types have been described in the two discrete mineralized areas, namely, northern and southern stocks. Hypogenemineralization includes chalcopyrite, pyrite, and magnetite, with minor occurrences of bornite.Supergene activity has produced gossan, oxidized minerals and enrichment zones. The supergene enrichment zone contains chalcocite and covellite with a 10-20 m thickness. Mineralization in the northern stock is mainly composed of pyrite and chalcopyrite. The aim of this study is the investigation and classification of hydrothermal veins and the constraining of physicochemical compositions of ore-forming fluids using systematic investigation of fluid inclusions. Twenty samples were collected from drill holes. Thin and polished sections were prepared from hydrothermal veins of thepotassic, sericitic and propylitic alteration zones. Samples used for fluid inclusion measurements were collected from drill cores DH01, DH02, DH06, and DH07, and outcrop samples. Microthermometric data were obtained by freezing and heating of fluid inclusions on a Linkam THMSG600 mounted on an Olympus microscope at Lorestan University. 1) Five main veintypes were identified, belonging to three stages of mineralization:type (I): barren quartz, type (II): quartz + pyrite + chalcopyrite ± bornite ± chalcocite ± covelite, type (III): quartz + magnetite ± chalcopyrite, type (IV): K-feldspar± quartz ± chalcopyrite, type (V): chlorite + biotite. 2) Seven groups of fluid inclusionswere observed: (IA) liquid-rich mono-phase, (IB) vapor-rich mono-phase, (IIA) liquid-rich two-phase (liquid + vapor), (IIB) vapor-rich two-phase (vapor + liquid), (IIIA) high salinity simple fluids (liquid + vapor + halite), (IIIB) high salinity opaque mineral-bearing fluids (liquid + vapor + halite + pyrite + chalcopyrite + hematite), (IIIAB) multi-phase fluids (liquid + vapor + halite + sylvite + hematite + magnetite + pyrite + chalcopyrite ± erythrosiderite) 3) Multiphase fluid inclusions with predominant homogenization temperatures 420 to 620˚C and predominant salinities 70 to 75 wt.%NaCl, are thought to be the early fluids involved in mineralization. 4) The coexistence of high saline liquid and vapor rich fluid inclusions (IIIAB, IIIB, IIIA and IIA types) resulted either from fluid entrapment during the boiling process or the co-presence of two immiscible fluids generated from the magma. 5) Dalliporphyry Cu-Au deposit was formed in a magmatic-meteoric system. Two conventional thermometric procedures, freezing and heating, were employed for the measurement of temperature of homogenization and approximate salinity. Freezing was conducted mainly for halite-under saturated inclusions (types IIA and IIB), to measure the initial melting temperature (Te) and the last melting point (Tmice), whereas heating was carried out on the halite-bearing inclusions (types IIIA, IIIB and IIIAB). Based on the microthermometric results, the Dalli fluid inclusions can be divided into two distinct groups: (1) medium-high temperature, hypersaline (Types IIIA, IIIB and IIIAB) and (2) low-medium temperature, low salinity group (Types IIA and IIB). Type IIB inclusions, which homogenize to the vapor phase and have a relatively low cooling rate, provide a fairly good estimate of entrapment pressure (Roedder and Bodnar, 1980). Based on the pressure estimated for the Dalli deposit, mineralization likely occurred at depth of 0.6-1.1 km. The calculated depth is coincident with the estimated mineralization depths of the porphyry deposits in the world (Pirajno, 2009). Fluid inclusions with a wide range of vapor and liquid ratios are abundant in all of the Dalli samples. This represents heterogeneous trapping of liquid and vapor. The coexistence of inclusions with different volumes of vapor contents, which homogenize either to liquid (Th(L-V)) or vapor (Th(V-L)), are interpreted as an evidence for the prevailing wide range of physico-chemical conditions during the cooling history of ore-forming fluid at the Dalliporphyry Cu-Au deposit. The boiling process is documented by the abundance of heterogeneously trapped fluid inclusions with extremely variable liquid to vapor ratios (Ahmad and Rose, 1980). Acknowledgements: We thank of ShahidChamran University of Ahvaz for their support and moreover, Lorestan University for microthermometric studies.

The Baba Ali deposit is located about 39 km to the north west of Hamadan city. The syenitic pluton intruded and metamorphosed the diorite host rock producing the skarn deposit. Geochemical considerations indicate that the concentration values of rare earth elements in the syenite and diorite range from 35.4 to 560 ppm. Rare earth elements variation in syenitic, skarn and diorite rock are similar indicating the similar source of the REE. Eu and Ce anomalies show varying values within the range 0.29 -1.24 and 0.8-1.09, respectively. Positive Ce anomalies occurred in the ores of low REE content and negative Ce anomalies occurred in the ores of high REE content. The concordance of the values of CaO with those of Eu revealed that the degree of plagioclase alteration. The Eu anomaly decreases with decreasing intensity of alteration. The La/Y values (suitable parameter for determination of pH in the environment of ore formation) range from 0.37 to 2.89. REE mobility depends on changes in pH. As a whole, epidote has been enriched in REE contents and actinolites, magnitite, are depleted in REE. These REE signatures indicate that hydrothermal fluids responsible for epidote were mostly magmatic origin and for actinolite and phlogopite were magmatic origin with low REE concentration or meteoric water involved in formation of these minerals.