Tuzgi area is located 60 kilometers southeast of Zahedan, in Eastern Iran Flysch Zone (Nehbandan-khash Zone). Geologically, the study area is covered by flysch deposits and intrusives rocks of different size and mainly of granodiorite composition. The study area consists of high-angle faults of different sizes with general trends of north-east and south-west, along which stibnite mineralization occurs. Based on thin section studies, the most important minerals of these rocks are quartz, biotite, plagioclase and k-feldespar. Stibnite is the most important ore mineral. Fluid inclusions are of primary type and spherical in shape. The melting temperature ranges between -3 to -20 degrees Celsius and the salinity is variable from 0.18 to 7.86 wt% NaCl equivalent to halite weight percentage. Based on above data it is concluded the genetic type of ore-mineralization coincides to low sulphidation of epithermal type.

Kushk sulfide Zn-Pb ore deposit is located in the Posht-e-Badam block, in the central Iranian tectono-magmatic zone. The host rocks of the ore deposit include shale, sandstone and dolomite. In order to investigate the physicochemical condition controlling the formation of the sulfide ore, a number of Fluid inclusions were gathered from silicic thin layers. The silicic contents of the samples have contemporaneously been deposited with shale and sulfide minerals mainly in the footwall and the main mineralized horizon. In this research, the general properties of Fluid inclusions in the ore-forming system are taken into account and the interpretation of these data in terms of Fluid evolution processes is discussed. Considering the syngenetic formation of the silicic thin layers and the mineralized shale, a similar formation condition can be considered for both of these units. Based on the results, two types of Fluids were involved in the formation of the silicic thin layers, including Fluid 1 that is characterized by higher salinity (av. 38. 8% NaCl. eq) and is thought to transport the metals chloride complexes and Fluid 2 with lower salinity (av. 4. 46% NaCl. eq) and is thought to carry sulfide species. Part of sulfide in this type of Fluid could be originated from bacterial activity. Isothermal mixing of the two Fluids sequencially resulted in destabilization of chloride complexes of chalcophile elements, the reaction between the elements and sulfur originated from the low salinity Fluid and formation of the sulfide ore.

Qamsar cobalt deposit is located 26 km south of Kashan, in the middle part of Urumieh-Dokhtar magmatic arc. Exposed rock units in the area include Eocene volcanics, Qom Formation marine sediments and plutonic bodies. The intrusive bodies have quartz-diorite to granodiorite composition as well as porphyry microdiorite. Intruding bodies into the Eocene volcanics and Qom Formation units caused recrystallization and metamorphism and formed assemblages of skarn minerals such as garnet, pyroxene, epidote, tremolite and actinolite. Mineralization occurred as endo-skarn and exo-skarn in massive, vein, brecciated, open space filling and diffusion forms. Magnetite is the main ore mineral and is accompanied by cobaltite, chalcopyrite and pyrite. Fluid inclusion microthermometry studies were performed on prograde stage garnet and pyroxene and retrograde stage quartz. Microthermometry studies show homogenization temperatures from 400 to more than 600°C and from 180 to 200°C as well as salinities between 12 and 20% and between 5.8 and 11.9% wt NaCl equiv. for prograde and retrograde phases, respectively. Isotopic thermometry on pyrite-chalcopyrite pair minerals gives 241 to 528oC and that for quartz-magnetite pair minerals gives 441 to 549oC. Sulfur and oxygen isotopic ratios offer magmatic origin which mixed with basinal Fluid for this mineralization.

Emaft Fluorite mine is located in 20 km southeast of the pole-sefid area in the Mazandaran Province, its part of fluorite belt in this province, this mine is difference among other mine in this area, because having particular properties. The host of ore is Tizkooh Limestone with lower cretaceous age .The structural condition, comprised a syncline with curving axis that it’s have estimating NE-SW trend .There is a lot of fault in this area that almost mineralized in these faults. Host lithology included Mudstone, Micrite that almost altered to dolomite by effect of Hydrothermal activities near to the mineralization. Field and laboratory investigation indicated that mine have simple Paragenesis and mineralogy .It’s included Fluorite, Calcite, Quartz and a few Barite and Sulfur (0/1%).For achievement to ore Fluid characterizes, Fluid inclusion studied for 2 two side- polish section on fluorite mineral of Emaft mine .This studies showed rather low Homogenization temperature (with average 158ºc)and average of salinity 13.7%wt equal NaCl. Simple cooling with willing to Boiling and Boiling (low salinity CO2- bearing ) is mechanism of fluorite deposition .The range of density of ore Fluid vary 0.9 to 1.1 gr/cm3. Base on evidence of lack of filling degree ,existence of a few sample of vapor-rich phase shows boiling of ore Fluid in fault and fracture zones.Base on relation Homogenization temperature- salinity, this ore deposit is one of Mississippi valley type deposits.

The ​​Karat iron deposit is located in the vicinity of Sangan mining district, in the Northeast of Iran. The basement rocks of the Karat area include hornfels, metamorphosed limestone, marble, sandstone, siltstone and red shale with interlayers of marl, shale and marl, thick-layered red conglomerate and alluvial deposits. The intrusion of a granite batholith in the sedimentary units of the Karat iron deposit has led to the formation of iron deposits in the margin of this batholith. The most important ore minerals include magnetite, hematite, goethite, limonite and a small amount of sulfide minerals such as pyrite and chalcopyrite. Geochemical data indicate a strong correlation between the Ni, Mg, and V to Fe in mineralization zone, which indicates the magmatic origin of the Karat iron deposit. In order to investigate the characteristics of the ore-forming Fluid of the skarn Karat iron deposit Fluid inclusions of quartz veins were analyzed. The results show that Fluids are mainly (L+V) type, low to medium salinity (4.48 to 16.42% NaCl) and the homogenization temperature of 200 to 390 degrees Celsius. Mineralogical, geochemical, and Fluid-inclusion data show that the magmatics, meteoric and metamorphic Fluids are responsible for Fe-mineralization in the skarn and Isothermal mixing and surface Fluid dilution are main evolution factors in mineralization Fluids. It seems that the main phase of mineralization has been occurred during the retrograde stage skarn.

based on Qayen 1:100000 geological map, the copper mineralization of Vorezg in volcanic rocks is attributed to Paleocene-Lower Eocene. Submarine volcanic rocks of the study area are found in two forms of lava and pyroclastics. Based on field and laboratory investigations, the outcropped rocks in Vorezg deposit are andesite, andesite – basalt, basalt and several small exposures of pyroclastic rocks such as tuff. Alkaline volcanic rocks of the area show within plate characteristics. Texture of mineralization is vein-veinlet, disseminated and open space filling amygdales. According to the mineralography studies, main minerals of copper are chalcocite, b-chalcocite, bornite, covellite, digenite and rare native copper. Chalcocite is the most abundant mineral. Intergrowth among copper ores is observed in most cases. Silver was detected as accessory phase (copper element paragenesis) in this ore deposit. Whereas silver has not founded an independent crystalline phase, therefore in the crystal of chalcocite, copper was replaced by Ag. Fluid inclusion studies on trapped Fluids in quartz show homogenization temperature average is 230-250 0oC and salinity degree of Fluids is 5-6%wt NaCl. On the basis of recognized characteristics, Vorezg ore deposit is comparable with Manto and Volcanic redbed type copper deposits. Recently, these two types of deposits are considered as synonyms.

Fluid inclusions are closed capsules wich have retained Fluid information completely since their entrapment time. These important Fluid information parameters are temperature and Fluid composition. Geochemical study of Fluid inclusions from Mansuri oil field using microthermometry analysis investigates application of Fluid inclusion properties. Analytical results indicated that Bangestan Formation is a potential hydrocarbon reservoir. Hydrocarbon-bearing Fluid inclusion was noticed only in one well (MI_44E) from Mansuri oil field، and therefore detailed investigation is proposed. Detailed sample analyses resulted in identification of 3 types of Fluid inclusion generation with distinct characteristics. All Fluid inclusions are described as primary in origin، but they show subtle differences in terms of cement type، temperature of homogenization and salinity. Oil inclusions were noticed only in type 3 generation which is described by varied API Gravity with yellow to blue colors suggesting mature oil (93. 1◦ C)، salinity in the range of 11. 46 to 18. 47 % at depth 3425. 9 meter. Finally، it is concluded that only Ilam reservoir from Bangestan group would possibly be favorable to exploration and field development.

Andarian area is located north of Tabriz city, north west Iran, and tectonically is a part of Ahar-Arasbaran magmatic belt. Geology of the area includes Miocene shallow pluton, Cretaceous flysch-type sediments, metamorphic rocks )hornfels and skarn( and volcanic rocks. Mineralization occurred in two stages: primary and secondary. The primary ore minerals include Au, pyrite and stibnite. Malachite, azurite and iron-hydroxides are the main minerals of the secondary phase. Two phases of liquid-rich and gas-rich inclusions are the most common type of inclusions. The average formation temperature of quartz-gold vein deposit is 237° C with low salinity (with an average of 8. 7 wt% NaCl equivalent). The pressure of entrapment for Fluid inclusions is between 26 to 51 bars, which is equal to the depth of 270-550 m. Based on Fluid inclusions studies, the gold bearing quartz veins formed in epithermal condition.

The Dorojin granitoid at the northeastern Isfahan is located in the central Urumieh-Dokhtar zone and within the volcano-sedimentary complex. The Dorojin iron deposit is the one of the several ore deposits that Dorojin granitoid body is caused in its surrounding rocks. According to microscopic evidences, mineral assemblage of wollastonite, garnet, pyroxene (diopside), amphibole, epidote, feldspar, calcite and quartz, Dorojin deposit attributed to the class of calcic skarns that occur during two stages progressive and regressive. Based on electron microprobe analysis, some garnets are andradite (An92-97Gr1-5) in core and andradite-grossular (An53-66Gr30-41Sp2-4) in rim. In the beginning, andradite Fluid inclusions with temperature range from 369˚ to 444˚ C and salinity range from 11. 22 to 12. 96 wt. % NaCl eqv., originate from magmatic Fluids, while with change in the acidity condition of environment and the opening of system, grandite, epidote and calcite Fluids with a temperature between 221˚ and 305˚ C and salinity between 0. 4 and 10. 11 wt. % NaCl eqv., are dominated by mixing and dilution of early magmatic Fluids with meteorite waters. Sr isotopic ratio of garnet vary between 0. 70760 and 0. 70805, suggesting that prominent role of the magmatic Fluids for the formation of andraditic garnet.

IntroductionDehnow-Abid area is a part of the geological map of Eshghabad with scale 1: 100000 (Aghanabati, 1994) that is located about 20 kilometers northeast of Eshghabad and in the coordinates of 57o 6’ 0” to 57o 10’ 0” eastern longitude and 34o 28’ 0” to 34 21’ 0” northern latitude. The Dehnow-Abid area is located in Tabas block and east of central Iran structural zone. The small continent east central Iran (Takin, 1972) includes blocks: Loot, Tabas and Yazd that constitute Iran's eastern part (Davoudzadeh and Schmidt, 1982). In geology, we can acquire more information about temperature forming minerals and rocks, pressure, density of the Fluid and the chemical composition of the ore bearing Fluids by Fluid inclusions studies. Properties as well as their role in our understanding of the sources and evolution of ore bearing hydrothermal Fluids and genesis of mineral deposits are very important (Rodder, 1979). In this study, we tried to use both field and laboratory studies, including petrography and thermometry studies of Fluid inclusions, environment formation of quartz in the specified Dehno-Abid.