میثم قلی پور

The role of martyr Qasem Soleimani in the victories of the resistance front against global arrogance, international Zionism, and regional regression was influential and unparalleled. The efforts of Soleimani and his comrades led to the elimination of the self-proclaimed caliphate of ISIS in Iraq and Syria and weakened the influence of the United States and other Western countries in the region. The cowardly assassination of Soleimani has had global implications, particularly on the issues and developments in West Asia. This research aims to answer the question: "What changes and developments have occurred in regional relations since Soleimani's martyrdom, and what are the perspectives of domestic and foreign analysts and experts on this matter?" The research utilizes citation-based methodology, internet searches, and other relevant sources.

The Lakehsiah mining district is hosted in Early Cambrian volcano-sedimentary units (CVSU) of the Kashmar–Kerman zone, Central Iran. The Kashmar-Kerman belt is located between the Yazd block in the west and the Tabas block in the east and it is parallel to the Poshed badam, Tabas and Kalmard faults in the north and Koh Banan and Zarand faults in the south of the area (Ramezani and Tucker, 2003). Compositions of the volcanogenic rocks in this area vary from felsic to mafic and include rhyolitic, rhyodacitic tuff and spilitic lava and diabase. The sedimentary rocks include dolomites, dolomitic limestones and evaporites. Lakehsiah 1 deposit is one of three IOA outcrops in the Lakehsiah district which have been studied in this research.

The mineralogical study of alteration zones was carried out by light microscope with transmission light and X-ray diffraction (XRD) analysis, at the Mineralogical Laboratory of Bu-Ali Sina University and Iran Minerals Processing Research Center, respectively. Fluid inclusion and Raman spectroscopy studies were also performed to determine temperature, composition and evolution of the ore-forming fluid at the Institute of Earth Sciences SAS, Slovakia. Stable isotope geochemistry of quartz (O-H) was performed at the Cornell University, USA.

Iron deposits hosted in the Tashk Group show hydrothermal alteration. The major minerals of the Sodic-Calcic alteration are the crystals of calcic amphiboles (tremolite-actinolite), pyroxene, calcite, magnetite and apatite. Propylitic alteration (chloritization and epidotization) is very widespread and affects volcanic and intrusive rocks. It consists of chlorite, epidote, calcite, and magnetite with minor amounts of sericite. Silicification alteration, occurs as distal alteration in both hanging wall and footwall host rocks, forming fine-grained to coarse grained quartz aggregates, veins and veinlets. Sericitic-argillic alteration occurs mainly in intrusions. Feldspar (plagioclase and K-feldspar) was altered to sericite and clay minerals. Minor quartz occurs as veinlets in this alteration zone. Na- Ca alteration in volcanic and intrusion rocks is exposed in the center of the area. Amphiboles mainly occur as replacements of plagioclase. Plagioclases were altered to chlorite, epidote, and calcite. Additionally, veinlets of quartz-epidote-chlorite, chlorite-epidote, epidote-quartz, quartz-calcite, calcite, chlorite-calcite, and epidote-calcite are observed. Quartz and carbonates (calcite) are widespread and veins of these minerals crosscut all the rocks described above. Lakehsiah 1 deposit, hosted within high-silica rhyolitic tuffs and domes, forms a steeply dipping tabular lens and it includes massive magnetite ± apatite ± quartz ± specular hematite ± Fe-Mg silicates.

Fluid inclusion Petrography:

Four major types of fluid inclusions are observed based on proportions of vapor, liquid, and solid phases present at room temperature in quartz mineral. They are described as follows:1-liquid-rich inclusions (L) 2-vapor-rich inclusions (V) 3-Two-phase liquid rich fluid inclusions (L+V) 4-three phase inclusions with halite solid phase as daughter mineral (L+V+H). Study of inclusions petrography shows that most of the inclusions present within this mineral are primary in origin, although secondary or pseudosecondary types have been identified. They have different sizes (typically 5–15 μm). Fluid inclusion shapes are rounded, elliptical, irregular, negative crystal shapes and square.

Microthermometry and Raman spectroscopy Freezing and heating experiments were performed on Types 3 and 4 fluid inclusions. Stretching of inclusions was noted during heating of large fluid inclusions in quartz from mineralized quartz veins. In such samples, homogenization temperatures range from 217–428 °C for type 3 and 384-467°C   for type 4. Micro-thermometric data were obtained from both Types 3 and 4 inclusions. The data obtained revealed variation in salinity of the trapped fluids. The final ice melting temperature in Types 3 and 4 inclusions varies from −4° to -18 and -9 to -19 °C with a mode at around -12 °C. Final ice-melting temperatures are lowest in the mineralized quartz veins. The first melting temperatures in multiphase Types 3–4 inclusions are also in a similar range which varies from -21 to -34°C. Based on their final ice melting temperatures, it varies between 10 to 27 and 40 to 44 wt. % NaCl equivalent for type 3 and 4 inclusions. T°C vs. salinity plots of inclusions show mixing of magmatic hot fluids with cold meteoric waters. Raman spectroscopy revealed presence of 69 mol % N2 and 31 mol % CO2 and 33 mol % N2 and 67 mol % CO2 in types 3 and 4 inclusions. These gases can be derived from mantle degassing (Wang et al., 2018) and chemical reactions during ascent of fluids.

H-O isotopes:

Isotopic studies are among the most common methods for identifying the primary composition of ore-forming fluids in deposits (Barati and Gholipoor, 2014). In the study area, five quartz samples in quartz grains and veins were used for H-O isotope analyses, with the aim of determining the source(s) of ore-forming fluids. The δDH2O and δ18OH2O values of the ore-forming fluids in quartz samples vary from -60‰ to -80‰, and -4.71‰ to -1.42‰, respectively. The above observations reveal that the early ore-forming fluids are magmatic in origin and is characterized by high temperature and moderate to high salinity, and gradually evolve to low temperature, low salinity meteoric water. The Lakehsiah 1 Fe deposit is associated with the magmatism induced by the protracted subduction. The decrease in temperature, salinity and f(O2), as well as fluid-rock interactions, are the main factors controlling Fe deposition.

The Lakeh-Siah iron± apatite deposit is located in the Bafq-Saghand Metallogenic Province (Central Iran) and situated within rhyolitic rocks. Magnetite with minor apatite are the main ore minerals in this deposit. Monazite and xenotime minerals in microscopic scale formed as inclusion in the apatite and magnetite crystals and micro-fractures. Based on microscopic and EPMA evidences, apatite is primary mineral and has been scavenging from mafic to ultramafic magma affinities. Apatite crystals are shows irregular zoning from dark and bright phases, then the dark portions mostly enriched in secondary monazite and xenotime inclusions. These results are consistent with the dissolution-reprecipitation process. During this process, apatite crystals reacted with secondary hydrothermal fluids along the crystalline boundaries and have depleted from REE and also due to this process, REEs have been undergone preferential differentiation, LREE and HREE enriched in monazite and xenotime, respectively.

The Lakeh-Siah region is situated in the Central Iran Zone (CIZ), 40 km northeast of Bafq city in the Yazd province. The rocks of the study area belonging to the lower Cambrian; including rhyolite, andesite and pyroclastic surge with porphyry to glomeroporphyric textures. The intrusive igneous rocks occur as stock and dyke and have monzonitic and dioritic composition with intergranular and granular textures. Based on geochemical studies, the rocks under study are calc-alkaline, metaluminous to peraluminous nature. The study apatite shows LREE- enrichment relative to HREE, this is a remarkable feature of the Kiruna- type iron deposits. Also, the enrichment of LILE (such as Rb, Ba, La, U, K and Th) and depletion of HFSE (such as Nb, Ta, Zr and Y) in the host rock, is known as a characteristic of the magmatism in the subduction zones. Based on the concentration of rare and trace elements, the volcanic and to the magmatic arc setting. The overall evidences demonstrate that the primary intrusive rocks belong magma of the rocks have been generated from partial melting of oceanic crust, during the closure of the Proto-Tethys Ocean. Iron oxide- phosphorus magma derived from magmatic differentiation of primary mafic magmas and ascended to higher levels through faults and fractures. Oxygen and hydrogen isotopic study of quartz along with magnetite ore in this deposit and calculation the fluid equilibrium with it shows that the ore- bearing fluid has a magmatic origin.

Baba Ali Index 2, iron deposit is located in the northwest of Hamedan province and the southwestern of Baba Ali village in the Sanandaj-Sirjan structural zone. According to the field and microscopic studies, host rocks are including acid to intermediate igneous rocks, schists and skarns. Magnetite-limonite layers are the main ore minerals in this deposit. Limonite layers are unusual in the iron deposits. Limonite in polished sections is found in layer shape and magnetite replacement. Geochemical measurements was performed on magnetite and limonite samples by ICP-MS methods. Correlation and classification diagrams and REE parameters were calculated for geochemistry coditions. According to drown diagrams this index is c IOCG-type and skarn sub-type deposit. Mineralized fluids has injected into host rocks, mixed with layered limestone xenoliths and magnetite has been percipitated and replaced at the high temperature in oxidized condition. Magnetite altered to limonite by Re-injecte hydrothermal fluids. Limonite has been deposited as an initial phase by hydrothermal fluids in large volumes and with the replacement of primary layerd carbonate xenoliths and unusual sequence of magnetite- limonite layers has created in this deposit.

The Tekieh Bala iron index is located in the south east of Kordestan province in Sanandaj- Sirjan geotectonic zone. Exposed rocks at the study area are including granite, gabbro, diorite, quartzmonzonite, quartzmonzodiorite and actinolite schist to chlorite schist.Orebody is located in the fault-beratited zone. Magnetite, hematite, goethite, limonite and pyrite included iron minerals in this index. Epidotization, chloritization, sericitization, actinolitization and silicification are the main alteration around the orebody. Geochemical studies of major and trace elements from the magnetite ore and use of diagrams provided by the various researchers shows that this index placed in group of iron oxide deposits, IOA sub-type and IOCG-type. REE Studies have shown, patterns of these elements, and calculated differential parameters emphasize the similarity of this deposit and IOA-type. Ore forming fluids were formed in differentiation and crystalization of intermediate intrusions rocks as a iron-rich hydrothermal fluids, mixing with the meteoric waters has been led to change in the environmental conditions and deposition of orebody.

The Shahrestanak Mn deposit is located in southern Qom province، 12 km southwest of the city of Kahak. Based on geological-structural divisions of Iran، the deposit belongs to central volcanic belt or Urumieh-Dokhtar zone. The Venarch deposit is one the most important known manganese deposits in Iran. The Sharestanak and Venarch deposits are spatially and temporally related to each other، and have similar geology، mineral texture and structure، host rocks، relationships with faults، and depositional environment. So، their magmatism and deposition conditions can be related to each other. Since no systematic study on the Shahrestanak deposit had been performed before discussing its geological and geochemical characteristics، here it is being attempted to study the geology، petrography، geochemistry of major، minor and trace elements، and Rare Earth Elements (REE) of ore، to distinguish the depositional environments and genesis of this deposit and to compare REE of ore in this deposit with other deposits. Sampling and method of study: Fourteen samples of manganese ore were selected for geochemical study and analyzing of major، minor، trace elements and REE by ICP-AES and ICP-MS and were sent to SGS Co.، Toronto. Detection limits for major elements and trace elements are 0. 01% and 0. 05ppm، respectively.

The deposit is characterized by various lithology and stratigraphy units، consist of: 1) Middle to -Upper Eocene volcano-sedimentary rocks، 2) Oligocene lower red conglomerate and sandstone، 3) Oligo-Miocene limestone and marl (Qom Formation)، and 4) Eocene and Lower Miocene basic to intermediate dykes. The most abundant minerals of the deposit are braunite، hausmannite، pyrolusite، and manganite. Evidences such as high Mn/Fe (11. 33) and Si/Al (4. 86) ratios، low contents of trace elements specially Co (11. 40 ppm)، Ni (24 ppm)، Cu (81. 85 ppm)، and Ce، with high amounts of SiO2، Mn، Fe، Ba، Zn، As and Sr، all represent hydrothermal processes. It seems that hydrogenous processes have not had significant role on the genesis of the Shahrestanak Mn deposit. During deposition of Fe and Mn from hydrothermal solution، they separated from each other and produced different Fe/Mn ratios in sedimentary exhalative deposit (SEDEX). The Fe/Mn ratios are 5. 7 to 40. 35 (ave.، 11. 33). Very high and very low ratios of Fe/Mn can be interpreted as fractionation and separation of these two elements from transportation during hydrothermal activities and mineralization. So، high Fe/Mn ratios here can be considered as in submarine hydrothermal deposits. Cann et al. (Cann et al.، 1977) suggested that Fe/Mn ratios in volcano-sedimentary and hydrothermal deposits are so variable and characteristic. Hydrothermal deposits are in close relationships with ferruginous silica gel which itself formed from submarine hydrothermal outpouring and discharging of metals in marine sediments. So، Si wt. % versus Al wt. % is high in exhalative activities. The average Si/Al ratio is 4. 86 in the Shahrestanak deposit which is in the range of hydrothermal deposits (SEDEX). Nicholson (Nicholson، 1992) suggested Na versus Mg content diagram for distinction between fresh water، shallow and deep marine environments. Bonatti et al. (Bonatti et al.، 1992) introduced Fe-Mn- (Co+Cu+Ni) *10 ternary diagram for distinction between marine sedimentary and hydrothermal Fe-Mn deposit. According to this diagram، hydrothermal oxides depleted in Ni، Cu، Co and zinc relative to sedimentary-marine deposits. Nicholson (Nicholson، 1992) suggested that hydrothermal Mn deposit distinguished with Zn، V، Mo، Cd، Li، Sr، Sb، Pb، Cu، Ba، and As and sedimentary deposit with enrichment in Ni، Cu، Co، Sr، Mg، Ca، Na and K. Hydrogenetic ferromanganese deposit has higher enrichment of Ni، Cu and Co relative to hydrothermal (exhalative) deposit. Low contents of Cu، Co and Ni indicate low input of these elements from hydrothermal activities and derivation of Zn from hydrothermal source. As (Co/Zn) - (Co+Cu+Ni) diagram، the samples from Shahrestanak deposit show close similarities with hydrothermal deposits which in turn show common genesis. Using Pb versus Zn diagram، dubhite (deposits derived from previous mineralized sequence) can be distinguished from other Mn oxide (hydrothermal or supergene) deposits. The dubhite deposits have high Pb/Zn ratios and more than 1 percent Pb and Zn contents. Meanwhile، other types of deposits like shallow marine deposit، hot springs، SEDEX، weathered deposits have lower contents of Pb and Zn. The Shahrestanak deposit has more similarities with SEDEX and shallow marine deposits.

Geological and geochemical evidences show that deposition of ore occurred by submarine hydrothermal activities in Neotethys oceanic basin during Middle to Upper Eocene in calcareous tuff with intercalation of micrite and calcareous limestone. For the genesis of the deposit، it can be stated that the pillow basalt and andesite lavas were leached by hydrothermal activities and Mn، Fe، Si، Ba، Sr and As entered in sedimentary basin by exhalative – volcanic activities through faults، then by regression of the sea and forming oxidizing condition، primary oxide-hydroxide Mn-minerals are deposited.

Zafarabad iron deposit is located northwest of Divandareh، in the northern margin of Sanandaj-Sirjan plutonic-metamorphic zone. The deposit is in lentoid to tubular shape، within a shear zone and occrrued in host rocks of calc-schist and limestone. Magnetite with massive، cataclastic and replacement textures are the main phases، while pyrite and other sulfide minerals are found. Major and trace elements are measured by ICP-MS and ICP-AES methods. Based on some ratios of trace elements in the ore samples and (Ti+V vs. Cal+Al+Mn and Ti+V vs. Ni/(Cr+Mn)) diagrams which are used for classification of iron deposit types، Zafarabad iron deposit fall in the range of skarn deposits. Spider diagrams show a steady decline from LREE to HREE elements with Eu (mean value of 0. 06 ppm) and Ce (mean value of 0. 94 ppm) negative anomalies. Comparing the distribution patterns of REE for the Zafarabad magnetites with those of various types of iron deposits shows that the REE pattern for Zafarabad is similar to these deposits. Analysis of calculated parameters for REE shows that the hydrothermal fluids responsible for mineralization are mainly of magmatic origin through fractionation and crystallization processes of a deep iron rich fluid phase and its emplacement within the carbonate rocks، forming iron skarn.