Eslamy peninsula, 360 km 2 in area, is located in the eastern coast of Urmieh lake in the northwest of Iran. This peninsula is a complex stratovolcano with a collapsed center, which is elevated due to later intrusions of sub-volcanic masses with trachytic to microsyenitic composition. The composite cone consists of a sequence of leucite tephrite, tephrite, leucite basanite, basanite and related pyroclastic rocks. Magmatic activities in the Eslamy peninsula begin with potassic alkaline to ultrapotassic and basic, silica-undersaturated shoshonitic rocks and they are followed by intrusions of lamprophyric dykes and end with acidic magmatism including trachytic, microsyenitic, syenitic and phonolitic domes. The original magma of the Eslamy peninsula rocks has a potassic alkaline nature (Roman type) rich in LREE and LILE and depleted of HREE. These characteristics suggest that the origin of magma can be from deep mantle with a garnet lherzolite composition, a low partial melting rate which has been contaminated by crustal materials in its way up. Fractional crystallization of olivine, diopsidic clinopyroxene and leucite played an important role in the evolution of magmas. Scrutinizing the geodynamic environment of Eslamy peninsula rocks in discrimination diagrams indicates that these rocks must have been formed in a post-collision magmatic arc setting.
In NW Iran, the bluish grey pencil shale intercalated with thin detritic limestone and siltstone was deposited on the grey limestone of Paleocene. Based on the X-ray diffraction results, the shale forming minerals are composed of calcite, quartz, feldspar, dolomite, muscovite, hematite and clay minerals including chlorite, illite, montmorionite, kaolinite and palygorskite. The comparison of major and trace element content of the shale with the typical samples indicates abundance in CaO, Sr, and Cs and scarcity in SiO 2 , Al 2 O 3 , and Ba. The values of weathering indices imply moderate weathering in the source area and deposition of sediments in an area with relatively high uplift. According to the major and trace elements ratios, provenance of the shale was probably felsic and/or intermediate igneous rock. The elemental ratios and geochemical parameters values such as Ti/Zr = 38, Th/Sc = 0.55, La/Sc = 1.9, La/Th = 3.4, ΣREE = 117.34, Eu/Eu* = 0.76, and (La/Yb) N = 8.3 suggest a immature continental arc setting for the studied shale. The inferred tectonic setting for the studied shale is in agreement with the tectonic evolutionary history of NW Iran during the Upper Cretaceous-Upper Paleocene. The detailed observation of facies distribution in the NW Iran during Cretaceous-Paleocene shows that the studied shale could be supplied from the volcanic-sedimentary succession of Upper-Cretaceous in a basin related to the Neo-Tethys II subduction.
Ali Javad porphyry copper-gold deposit is located in Arasbaran porphyry copper belt at northwestern Iran, some 20 km east of Sungun Mine. Porphyry mineralization at the Ali Javad deposit occurred in post-Oligocene quartz monzonite bodies which intruded in the Eocene volcanic rocks. Mineralization occurred as veins, veinlets and dissemination both as hypogene and supergene type. Several types of veinlets were distinguished during the study of the deposit. Fluid inclusion studies on fluids trapped in quartz which were taken from drill core samples indicated a wide range of homogenization temperature in the veinlets from 138˚C to 565˚C which their salinity demonstrated 33-61 wt% NaCl equivalent. Mineralizing fluids density at the deposit was 0.8-1.2 g/cm 3. Fluid inclusion studies suggested that Ali Javad deposit is an Au-rich porphyry copper deposit; its fluid inclusion features were comparable with other porphyry deposits.
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