This paper presents the properties of fluid inclusions found in sphalerite from Latala epithermal base and precious metal deposit (Central Iran), which is hosted in Cenozoic volcanic-sedimentary host-rocks. The Latala Deposit represents an example of vein type, base metal deposits in the Miduk porphyry copper deposits (PCDs) in southern Urumieh-Dokhtar magmatic belt (UDMB). Mineralization in Latala epithermal base and precious metal vein type formed in 3 stages and sphalerite-quartz veins occur in stages 2 and 3. Stage 2 quartz-sphalerite veins are associated with chalcopyrite and zoned sphalerite, along with quartz+hematite, and Stage 3 quartz-sphalerite veins contain galena+sphalerite+ chalcopyrite and quartz with overgrowth of calcite. Mineralization in Stage 3 occurs as replacement bodies and contains Fe-poor sphalerite without zoning in the outer parts of the deposit. This paper focuses on fluid inclusions in veins bearing sphalerite and quartz. The fluid inclusion homogenization temperatures and salinity in sphalerite (some with typical zoning) range from 144 to 285 °C and from 0.2 wt.% to 7.6 wt.% NaCl eq. Sphalerite and fluid inclusions of the Latala base and precious metal deposit formed from relatively low-T and low-salinity solutions. Raman spectroscopy analyses indicate a high percentage of CO₂ in the gas phase of fluid inclusions in Fe-poor sphalerites, as expected with melting temperature for CO₂ of −56.6 °C, and significant amounts of H₂. Lack of reduced carbon species (methane and lighter hydrocarbons) was confirmed in the petrographic study using UV light and Raman spectroscopy. High amounts of H₂ in fluid inclusions of Fe-poor sphalerite can be the result of different intensities of alteration and diffusion processes. The common occurrences of CO₂ in fluid inclusions have originated from magma degassing and dissolution of carbonates. The δ³⁴S values for sulfide minerals in galena of sphalerite bearing veins vary between −9.8‰ and −1.0‰, and the δ³⁴S values calculated for H₂S are between −7.1‰ and +0.6‰. These values correspond to magmatic sulfur whit possible interaction with wall rocks. Magmatic fluids were successively diluted during cooling and continuous ascent. Secondary boiling would lead to variable amounts of potassic or prophylactic alteration and the hydrogen diffusion into the inclusions hosted in sphalerite of Latala.

中文翻译：

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高$$ {f _ {{{\ rm {H}} _ 2}-}} {f _ {{{rm {S}} _ 2}}} $$ f H 2 − f S 2与Latala地热中闪锌矿有关的条件伊朗中部贱金属和贵金属矿床：闪锌矿的成分和成因条件的含义

本文介绍了拉塔拉超热碱闪锌矿和贵金属矿床（伊朗中部）中闪锌矿中发现的流体包裹体的性质，该火山岩含在新生代火山沉积沉积主岩中。拉塔拉矿床是南部Urumieh-Dokhtar岩浆带（UDMB）的Miduk斑岩铜矿床（PCD）中的脉型基本金属矿床的一个例子。拉塔拉超热基底的矿化和贵金属脉型分3个阶段形成，闪锌矿-石英脉发生在第2和第3阶段。第2阶段石英闪锌矿脉与黄铜矿和分区闪锌矿以及石英+赤铁矿和第3阶段石英相关-闪锌矿脉含有方铅矿+闪锌矿+黄铜矿和石英，方解石过度生长。第三阶段的矿化作用是作为置换体发生的，并且含有贫铁的闪锌矿，在矿床的外部没有分区。本文主要研究闪锌矿和石英脉脉中的流体包裹体。闪锌矿中的流体夹杂物均质温度和盐度（有些具有典型的分区）在144至285°C和0.2 wt。％至7.6 wt。％NaCl当量的范围内。拉塔拉基底的闪锌矿和流体包裹体以及由相对较低的矿物组成的贵金属矿床T和低盐度解决方案。拉曼光谱分析表明，贫Fe闪锌矿中流体包裹体的气相中的CO ₂百分含量很高，这是由于对CO ₂的熔化温度为-56.6°C和大量的H ₂所期望的。使用紫外光和拉曼光谱的岩石学研究证实缺乏还原碳物种（甲烷和轻烃）。贫铁闪锌矿流体包裹体中大量的H ₂可能是不同强度的蚀变和扩散过程的结果。流体包裹体中常见的CO ₂发生源于岩浆脱气和碳酸盐的溶解。的δ ³⁴在闪锌矿轴承静脉方铅矿硫化物矿物的价值观之间变化-9.8‰和-1.0‰，δ ³⁴，计算值值ħ ₂ S分别+ 0.6‰之间-7.1‰和。这些值对应于岩浆硫与围岩的可能相互作用。在冷却和连续上升过程中，岩浆液被连续稀释。二次沸腾会导致钾或预防性变化量的变化以及氢扩散到Latala闪锌矿中所含的夹杂物中。