Geochemical studies of the PINAVAND FLUORITE MINES indicates that FLUORITE has been deposited from a high salinity, typically low temperature and Mg-rich fluid in two stages: Based on geothermometrical data, at the first stage FLUORITEs were formed at relatively high temperature (85-235Co) and accompanied by host rock replacement (in the form of epigenetic dolomitization). The second stage of FLUORITE mineralization has occurred at low temperature (65-115oC) and has formed lodes and vein-likes along the breccia and fault zones. However, the salinity was relatively invariable (15-23 wt% NaCl), suggesting salinity of FLUORITE-forming fluid was the same at all occurrences. By studying of REE patterns and regarding to some ratios of HREE to LREE, it could be observed that the first stage of FLUORITEs was enriched in LREE revealing mineralization has occurred in early stage of crystallization .In contrast, the second stage of FLUORITEs containing high proportion of HREE were deposited in the last stages of crystallization event. Based on the calculated (Yb/La), (Yb/Ca), (Tb/La) and (Tb/Ca) ratios, two mechanisms could be proposed: assimilation (replacement) for the first type FLUORITEs and remobilization (rejuvinilization) for FLUORITEs of the second stage.

FLUORITE deposits in Iran are widely located in dolomites and dolomitic limestones (Triassic-Cretaceous age) (Darvishzadeh, 1991) in Alborz and the Central Iran zone (Rajabi et al., 2013). Qishlaqi (2002) investigated the geochemistry and genesis of the PINAVAND FLUORITE MINES. Shafahizadeh (2011) investigated the mineralogy and fluids involved in FLUORITE and barite mineralization in the PINAVAND region. Heidari et al. (2021) investigated the paragenetic relationships of minerals in the alteration zone of the PINAVAND deposit. In the present paper, the semi-precious gem fluorine in the limestones of the PINAVAND deposit is investigated from the point of view of geochemistry and gemology. Also, the connection of the host rock with the minerals of this area and the reaction of the ore-forming fluid with them will be determined.Materials and MethodsFollowing field studies, several thin sections (about 25) and polished sections were prepared for petrographic studies. The fluorine mineral of the studied deposit was subjected to SEM analysis (at the Isfahan University of Technology) and gemological investigations (at Isfahan University). Also, the results of geochemical analyses of FLUORITEs (ICP-MS) (Shafahizadeh, 2011) were applied.Results and Discussion Mineralization of FLUORITE and barite occurred in scattered, massive, veined, breccia and lens-shaped in the Lower Cretaceous limestone and dolomitic host rocks. Major alterations observed in the region including silicification and to a lesser extent dolomitization. The main minerals are quartz, calcite, dolomite, FLUORITE, and barite scattered in the limestone. The FLUORITE decomposed into carbonate along fractures, which indicates the continuous influx of hydrothermal solutions. A final silicification process has occurred following fluorine formation. It seems that the Mississippi Valley deposit type is one of the proposed models for the formation of PINAVAND mineral region. Dolomitization and silicification processes are the characteristics of the Mississippi Valley-type deposits (Pirajno, 2009). However, in the Mississippi Valley-type deposits, unlike epithermal mineralization, dolomitization process occurs with a weak silicification. The mineralogy in PINAVAND deposit includes pyrite, chalcopyrite, chalcocite, galena, goethite, FLUORITE, barite, quartz, calcite and dolomite. No proximity with evaporite rocks is observed. A low extent of dolomitization with a larger scale of silicification can be an indication of epithermal type alterations. As optical and gemological characteristics display the fluorine crystals with glassy and transparent feature and specific weight of 3.18 vary from colorless to green to pale blue in color. They are without any birefringence and their refractive index is 1.43. The presence of rare elements such as Sc, Sr and Zr can affect the color of this mineral. Yellow and transparent FLUORITEs have a higher Yb/La ratio than blue and purple FLUORITEs (Palmer and Williams-Jones, 1996). It seems that various of color in FLUORITE crystals are related to the amount of Y and ∑REE (e.g., Dill et al., 2011). The concentration of REE in the PINAVAND FLUORITEs is generally low, and LREEs are more enriched than heavy earth elements (HREE). The low REE in FLUORITEs can be attributed to the high fluid-to-rock ratio (Sánchez et al., 2010). The low level of rare earth elements can be attributed to the high pH of the fluids and the reaction of the fluids with the carbonate host rock as well as the high ratio of fluid/rock. On the other hand, the low values of rare earth elements can indicate the mixing of magmatic fluids and atmospheric waters (Valenza et al., 2000). According to Moller et al. (1986) the FLUORITEs formed in the early or middle stages of crystallization are enriched with LREE, the amount of La element is high and the amount of Tb is low, but the FLUORITEs related to the final stage of crystallization are enriched with HREE. So, the PINAVAND FLUORITEs created in the early stages of crystallization. The examined FLUORITEs have a small positive anomaly in europium, indicating the substitution of Eu2+ for Ca2+ and the deposit formation temperature is less than 250°C (Schwin and Markl, 2005). The negative anomaly of cerium points to its removal from the environment as a consequence of fluid reaction with calcareous wall rock giving rise to increment to oxygen fugacity. FLUORITEs are divided into three sedimentary, hydrothermal and pegmatitic environments (Constantopoulos, 1988). The studied FLUORITEs are classified as sedimentary type with some features of primary crystallization and fluid's reaction with calcareous host rocks.ConclusionsPINAVAND deposit is a FLUORITE-barite deposit consisting both of the non-metallic and metallic minerals. The latter minerals were formed under the influence of hydrothermal alteration. The negative anomaly of cerium in the FLUORITEs suggests that it has been removed from the environment as a result of the fluid's reaction with the limestone wall rock, which in turn increased the oxygen fugacity. This process highlights the significant role of fluid-rock interactions in the removal and redistribution of certain elements within the depositional environment. Mineralization of the FLUORITE and barite formed as veins, veinlets, lenticular and breccia shapes have occurred mainly in the Lower Cretaceous limestone units. The main minerals of this deposit include quartz, calcite, saddle dolomite, FLUORITE and barite, scattered in the limestone background. The major changes in the region include silicification and, to a lesser extent, dolomitization processes. FLUORITE can observe as coarse-grained or fine-grained in size, and its gemological characteristics are as follows: transparent to semi-transparent crystals, pale blue colors, green and violet, hardness 4, specific gravity 3.18, vitreous luster, without birefringence and having a refractive index of 1.43. Based on the geochemical studies, the concentration of LREE in the PINAVAND deposit indicates the formation of FLUORITEs in the early to middle stages of crystallization. The Mineralogy in the PINAVAND deposit is simple like in the Mississippi Valley deposit. Based on the type of minerals as well as alteration type, the PINAVAND mineralization shows some characteristics of MVT deposits, and due to the huge of silicification process, it also shows similarity to the alteration of epithermal deposits.

Sulfur source tracing based on of sulfide (galena and pyrite) and sulfate (barite) mineralization in FLUORITE deposits of Elika Formation (East of Mazandaran Province) is studied. In present research.  d34S values vary between -1.82 – +12.49 ‰, +13.22 – +25.83 ‰ and +22.69 – +32.91 ‰ for galena, pyrite and barite, respectively. Regionally, although wide range of δ34S in sulfides is interpreted as isotopic heterogeneity of source and/or processes of reduced sulfur supply for sulfide mineralization in the studied area, but each deposit has narrow range of d34S. Compared to sulfides, barites show isotopic homogeneity in heavier d34S which are corresponding to evaporates from coexisted sea water (Middle-Upper Triassic; Paland Formation). Based on stratigraphic and mineralogical data of host rocks, co-existing evaporates of Triassic sea water and also diagenetic primary sulfates in matrix of host rocks (anhydrite, gypsum, barite) are introduced as the most probable sources of sulfur for sulfide mineralization in Shesh Rodbar and Era deposits. In contrast, contribution of organic matter and/or diagenetic primary pyrites had main role in generation of light d34S values in Pachi Miana and Kamarposht deposits. Thermo-chemical reduction of digenetic primary sulfates and thermal decomposition of diagenetic primary sulfides as well as sulfur bonds in organic matter-bearing laminaes in the host rock are introduced as main processes for reduced sulfur supply in sulfide mineralization.

Mineralogical and liberation studies are the most important parameters used in the selection of separation. An investigation was carried out to identify the various types of minerals present in FLUORITE ore and to determine the suitability of the methods for its preconcentration and final concentration. The sample has been evaluated and characterized by ore microscopy, x-ray diffraction, chemical analysis and also approximate mineralogy based on chemical analysis and Microscopic studies and also the texture characteristics such as grain size, Situation of infor locked particle and their arrangement in the ore body were also investigated. According to surveys conducted this ore contains of FLUORITE (40.52%), calcite (24%), quartz (20%), smitsonite (8%), galena (2%), clay minerals (3%), barite (1%) and goethite (0.6%). Carbonate phases is two parts sparry calcite, micrite to microsparate piece has been observed. Quartz, in the form of microcrystalline with limonite and goethite oxide of stained has been observed. The liberation degrees of crushed ore in different size fractions was estimated by the Counting method of showed that for FLUORITE (1000m), Calcite (100m) and quartz (90m) of FLUORITE in size 100 mesh (150m) with quartz (36%) and calcite (23%) were determined. The size fraction of -600, +425, can be assessed for gravity concentration as a preconcentration process and for the size fraction -150,+75 mm for flotation.

The Emaft FLUORITE mine is located in 20 km on south east of Pole Sefid city in Mazandaran province. Structurally the studied area is in the form of a perche syncline and its axial surface trends NE-SW. The Emaft syncline is very important for having FLUORITE ore because the Kerman and Emaft MINES that are located in Lar and Tizkouh Formations are located in the core of this syncline. On the other hand, on the southern limb of syncline and around Elika Formation, FLUORITE may be found and explored. The structural studies in the area began by measuring the bedding layers, fractures and folds of the area. Then, the data extracted were analyzed by computer (Tectonics Fp1.62 software) and finally the tectonic interplay of the ore-deposit was established. The coordinates of syncline axis in Emaft is 14-N024 that indicates a low plunge of the axis of syncline. The trend of syncline axial surface is N028 and dip is 73NW. The consideration of Emaf FLUORITE mine shows that the said veins have a trend approaching the axial surface (ranging from 30° to 50° of northeastern). The dips of veins are nearly between 70° to 80° towards northwest the axial surface. According to the data obtained, we find that folding in this region caused linear fractures and the fractures were filled with FLUORITE solution.

This article is aimed at explaining details of huge sources of the MINES which have been neglected so far.Khums of MINES, due to their diversity and abundance, can be potentially a great support for propagation of religion and Shiite Islam. In this article, we have demonstrated that even state-owned MINES are liable tokhums which has to be paid and spent underwali faqih’s supervision. Discussions about the nesab of mine [quorum] and thatkhums for MINES is calculated before deducting extraction costs have been covered. In addition, we have mentioned that the fact that MINES areanfal [national assets] does not conflict with the obligation ofkhums for MINES and that khums of MINES, whether extracted in national lands or private lands, has to be paid. The differencekhums of MINES andkhums of profits accrued from businesses has also been explained and it has been proven that ifkhums of MINES is paid, there is no need to paykhums of profits accrued annually.

Damghan FLUORITE deposit (south of Aresk) is located in the north-west of Damghan. This deposit is limited to the Arsk Mountains and from south it limited to the Atary fault. The mineralized zone is located in member 1 of the mila formation which is mostly dolomite along with interbeds of marl and yellow shal (yellow shal has the same age as middle Cambrian). FLUORITE mineralization is mostly white color and a lesser amount with violate color and it is occurred as vein or open space filling. Along with FLUORITE mineralization, other minerals could be seen as sulfide minerals (like galena, pyrite, chalcopyrite, coveline) and also cerussite minerals, iron hydroxides, calcite and barite. According to the micro thermometry data carried out on fluid inclusions of white and violate FLUORITE, the temperature domain of homogenization is changing between 100 to 360 ° C and the salinity domain of mineralizing fluid is changing between 0. 2 to 20. 2 wt% NaCl equ. . Evidence shows that FLUORITE mineralization probably occurred from mixing of hydrothermal fluid with meteoric and basinal fluids in reducing conditions.

FLUORITE mineralization in Kamar Posht mine, east of Central Alborz, is mostly occurred in dolomitic limestone rocks of the Elika Formation. The aim of this current research was to recognize the types of breccia and dolomite based on microscopic studies (transmitted and cathodoluMINEScence light) and ore fabric and texture applying to the genesis of this deposit. Using the above methods combined with time-space relationship between dolomites and FLUORITE led to recognition of 2 main groups of dolomites including (1) pre-mineralization dolomicrites without luMINESce in the matrix of host dolomitic limestone and (2) dolomicrosparite-dolosparites associated and coeval with mineralization that show red to orange-yellow luMINEScence color. Pre-mineralization dolomicrites introduced as shallow buried diagenetic-type, whereas syn-mineralization dolomicrosparite-dolosparites interpreted to form due to re-crystallization of primary dolomicrites of host rock and/or precipitation of hydrothermal solution (basinal brine) causing dolomitic alteration. Dissolution-collapse and faults breccias dominated over diagenetic breccia and were main features of mineralization in Kamarposht mine. They were interpreted as evidence of epigenetic origin of FLUORITE mineralization in high-grade zones of the KamarPosht mine. They were probably formed as a result of post-diagenetic processes (tectonic and basinal brines) on dolomitic limestone host rocks overlaying clastic rocks of Shemshak group.

Introduction: Development of natural resources and mining activities are prerequisite for economic and industrial growth in many countries. In many cases, such mining areas lie within residential or agricultural lands or natural habitats intensifying the contradiction between land use and environmental protection.Different components of mining activities including exploration, extraction and processing impose extensive physical, chemical and biological changes on the environment due to nature and characteristics of the activities.