Abpooneh iron mine is located 85 km west of Isfahan province in the middle part of Sanandaj-Sirjan structural zone. The host rock of Abpooneh ore are meta sandstone, schist and phyllite. Silicate minerals that were created during the metamorphosis of the host rock in the ore include muscovite, chlorite and indicate the green schist facies. Iron ore mainly show a banded and lumpy textures. In terms of texture, mineralogy and chemical composition, the iron ore is comparable to the metamorphosed iron ores. The textural and structural features is indicate the sedimentary-diagenetic origin of the ore in Abpooneh. Metamorphism occurred after the formation of the ore and caused the recrystallization of the ore and the host rock. The constituent components of the ore result of the erosion of continental destructive rocks and may have been provided by hydrothermal fluids related to submarine volcanic activities. The pattern of distribution of main and minor elements of ore and host rock is similar in various charts and this indicates their formation in a similar sedimentary environment.

Neyzar iron deposit is located about 50 km southwest Mashhad, northeast Iran. It was developed as layered and discontinuous lenses in a fault zone within quartz-arenite and sub-litharenite sandstones of Lalun Formation (Lower Cambrian).  Mineralographical studies show that hematite is the principal iron ore mineral accompanied by goethite and lesser amounts of pyrite. Microscopic examinations confirm the presence of skeletal, relic replacement, marginal replacement, and pseudomorphic textures within the ores. Based on petrographical data, two series of alteration minerals, hypogene (sericite, pyrite, pyrophyllite, barite, chalcedony, and calcite) and supergene (goethite, jarosite, gypsum, limonite, and hematite) were developed in this deposit. Based on the results obtained from field works, mineralographical and geochemical studies, it appears that the evolution of the studied ores is genetically related to the host rocks.  Both hydrothermal processes and fault systems (existing in the host rocks) played important roles in leaching of elements and depositing of the ores. Results of chemical analyses show that the REE values vary in the iron ores from 6.97 to 18.26 ppm. Eu and Ce anomalies in the ores are within the ranges of 0.01-1.36 and 0.28-1.89, respectively. Geochemical considerations reveal that distribution of rare earth elements within Neyzar iron ores was controlled by pH, abundance of complex-forming ions (CO32-, F־, Cl־, PO43-, and SO42-), scavenging processes, and fixation in neomorph mineral phases.

The Zendan salt dome is located at 80 Km north of Bandar-Lengeh and 110 Km west of Bandar-Khamir cities in the Hormozgan province. Based on the structural geology of Iran, the Zendan salt dome is placed in the southeastern part of the Zagros zone (Stocklin, 1968). Important units in this area are Hormuz, Mishan, Aghajari and Bakhtiari formations with the Precambrian age (Alian and Bazamad, 2014). The Hormuz formation with the four members of H1, H2, H3, and H4 is the oldest formation (Ahmadzadeh Heravi et al., 1991). Basalt and diabase rocks are mostly rocks that are exposed in the Zendan salt dome. Magnetite and hematite iron mineralization happened in all the building rocks of salt dome, and is not a uniform mineralization. Iron mineralization contains hematite, spicularite, magnetite, goethite, and iron hydroxides. Magnetite-hematite-oligist layers (red soil) are the most iron mineralization in the Zendan salt dome, which are usually broken and scattered with gypsum layers (mostly anhydrite), respectively. Another form of iron mineralization is a mixture of hematite and magnetite (about 10 to 15%) in diabase rocks. Copper mineralization consists of pyrite and chalcopyrite minerals that are mostly in tuff and shale units. The presence of low immobile trace elements in the Zendan salt dome and type of alteration shows that maybe the origin of this iron is deposited from brine fluid. Therefore, this deposit can be classified into VMS deposits.

We have taken 60 samples rocks from the Zendan salt dome, and then prepared 20 thin and polished sections. Petrographic studies were done and 9 samples were selected for analysis. These samples were sent to the Zarzma laboratory and the amount of FeO was determined by the wet chemical method and other amounts of oxides were determined by XRF. Six samples were analyzed for determining the major elements with the XRF method in the Binalood laboratory. Nine samples from vines mineralization were sent to the Zarzma laboratory and were analyzed with Inductively Coupled Plasma (ICP-OES). Two samples of igneous rocks were analyzed for determining major, minor and trace elements with ICP in Zarzma laboratory.

Magmatic and evaporate fluids are sources of hydrothermal iron mineralization (Barton and Johnson, 2004). Sodic-calcic, semi sub deep pottasic, low silicific and sericitic alterations are related to magmatic fluids (Barton and Johnson, 2004). In the Zendan salt dome it seems that plutonic rocks prepared the source of temperature and made brine liquids evaporate and then moved the metals. Sodic alteration is one of the frequency alterations in the hydrothermal iron deposits related to high brain liquids (Arencibia and Clark, 1996). Immobile elements such as Ni, P and V show a high amount of magmatic iron deposit (Nystrom and Henriquiz, 1994). There is a significant relationship between the amount of Fe and the frequency elements. With an increase in the Fe content, the amount of TiO2, K2O, SiO2 and Al2O3 oxides decrease and the amounts of Ni and Cr2O3 increase. Low immobile elements’ contents and alteration type in the Zendan salt dome show the iron mineralization effect of brines fluids. On the other hand, this deposit can be classified into VMS deposits.

Iron mineralization in Zendan salt dome is often magnetite, hematite, pyrite and chalcopyrite. Iron mineralization in the Zendan salt dome consists mostly of hematite, limonite and oligist (red soil) layers. They are usually found as scattered discontinuous layers and are alternated with gypsum layers. Hematite is the most abundant and dominant. There is a significant relationship between the amount of Fe and frequency elements. With increasing the Fe content, the amounts of TiO2, K2O, SiO2 and Al2O3 oxides decrease and the amounts of Ni and Cr2O3 increase . Low immobile element's contents and alteration type in the Zendan salt dome shows the iron mineralization effect on brines fluids. On the other hand, this deposit can be classified into the VMS deposits.
Acknowledgements: The authors would like to thank the Ashrafpour, Hagheghe and all miners.

The Kuh-Baba iron ore deposit is located about 70 km south of Hashtroud, East-Azarbaidjan Province, NW Iran. The deposit is genetically affiliated with intrusive bodies of gabbroic to dioritic composition. The principal host rocks for the Fe mineralization include units of gabbro-norite and pyroxene hornblende gabbro-norite. The widespread alteration zones which are accompanied with Fe-mineralization are actinolitization, chloritization and epidotization. The principal ore mineral is magnetite with subordinate apatite showing massive, vein/veinlet, replacement, brecciated, and disseminated textures. The results of electron probe micro-analysis (EPMA) on 28 points of magnetite crystals show relatively high amounts of elements such as Al, Mn, Ti, and V. The values of components such as TiO2, V2O3, NiO and MgO in massive magnetites are higher than those present in disseminated and veinlet-type magnetites. Studies of primary fluid inclusions in quartz crystals coexisting with magnetite mineralization show that they are mainly liquid-rich 2-phase (L+V) and occasionally monophase-vapor (V). The homogenization temperatures of liquid-rich 2-phase inclusions range from 436ºC to 544ºC (average of 505ºC). Based on temperatures of the last melting point of ice (TM), the obtained average salinity is 15.82 wt% NaCl equ. Considering the measured parameters such as homogenization temperature, salinity, density, and pressure of the fluid inclusion, the depths of magnetite mineralization were estimated to be within the range of 1.3-2.7 (average of 2.3) km (based on the lithostatic pressure). According to the EPMA and fluid inclusion data, the Kuh-Baba iron ores deposit can be classified as a ‘Kiruna-type’ and subtype Iron-Oxide apatite-poor deposits and the origin of magnetite can be conceived as both magmatic and high-temperature hydrothermal.