Abstract

The structural–morphological types and localization conditions of talc occurrences in the Beloretsk district of the Western Urals talc province are discussed. The talc mineralization is represented by low-iron talcites and talc stones in the Riphean clastic–carbonate complexes of the Bashkirian Meganticlinorium. Prospective talc objects in the Beloretsk district are classified as apocarbonate, to be distinguished from the apoultramafic deposits, which are predominant in the Urals. The hydrothermal–metasomatic genesis of the talc ores, their association with the metamorphosed dolomite-bearing members of the Lower and Middle Riphean Kyzyltash and Avzyan formations, the cooccurrence with magnesite deposits, and the absence of relationship with granitoid magmatism are established. The inner resources of the Riphean sedimentary basins, activated by metamorphic processes, are viewed as the sources of ore-forming fluids. The flanks of magnesite bodies in dolomite sequences near contacts with silicate interbeds are considered as the lithological settings favorable for talcite formation. The presence of the stacks of interbedded magnesian–carbonate and aluminosilicate rocks in the Riphean sequences facilitates the silica–magnesium bimetasomatism but leads to the formation of predominantly lean talc–chlorite stone varieties. The morphological types of mineralization are represented by the stratiform bed-like talcite and talc stone bodies; the saddle-like and ribbon-like talcite bodies confined to monoclines and fold hinges and limbs; and the fault controlled steeply dipping linear bodies of rich talc ores.

中文翻译：

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西乌拉尔省贝洛列茨克地区Apocar​​bonate滑石成矿的结构形态类型和定位条件

摘要

讨论了西部乌拉尔滑石省Beloretsk地区滑石的构造形态类型和定位条件。在Bashkirian Meganticlinorium的Riphean碎屑碳酸盐复合体中，低铁滑石和滑石代表了滑石的矿化作用。Beloretsk地区的预期滑石对象被归为高碳酸盐岩，以区别于乌拉尔地区普遍存在的无碳镁铁矿床。确定了滑石矿石的热液代物成因，与下，中里夫安Kyzyltash和Avzyan地层变质的含白云岩成员的联系，与菱镁矿的共生以及与花岗质岩浆作用的关系。Riphean沉积盆地的内部资源，通过变质过程活化的矿物被视为成矿流体的来源。在与硅酸盐夹层接触的附近，白云岩层序中菱镁矿体的侧面被认为是有利于滑石形成的岩性背景。Riphean层序中夹杂着镁碳酸盐岩和铝硅酸盐岩的叠层，这有利于硅镁双金属成岩作用，但会导致形成滑石粉为主的亚滑石一绿泥石。矿化的形态类型以层状床状滑石和滑石体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。在与硅酸盐夹层接触的附近，白云岩层序中菱镁矿体的侧面被认为是有利于滑石形成的岩性背景。Riphean层序中夹杂着镁碳酸盐岩和铝硅酸盐岩的叠层，这有利于硅镁双金属成岩作用，但会导致形成滑石粉为主的亚滑石一绿泥石。矿化的形态类型以层状床状滑石和滑石块体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。在与硅酸盐夹层接触的附近，白云岩层序中菱镁矿体的侧面被认为是有利于滑石形成的岩性背景。Riphean层序中夹杂着镁碳酸盐岩和铝硅酸盐岩的叠层的存在促进了硅镁双相生作用，但导致形成了稀薄的滑石一绿泥石。矿化的形态类型以层状床状滑石和滑石体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。Riphean层序中夹杂着镁碳酸盐岩和铝硅酸盐岩的叠层，这有利于硅镁双金属成岩作用，但会导致形成滑石粉为主的亚滑石一绿泥石。矿化的形态类型以层状床状滑石和滑石体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。Riphean层序中夹杂着镁碳酸盐岩和铝硅酸盐岩的叠层，这有利于硅镁双金属成岩作用，但会导致形成滑石粉为主的亚滑石一绿泥石。矿化的形态类型以层状床状滑石和滑石体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。矿化的形态类型以层状床状滑石和滑石块体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。矿化的形态类型以层状床状滑石和滑石块体为代表。鞍状和带状的滑石体被限制在单斜线上，并折叠铰链和四肢；断层控制了富滑石矿的陡倾线性体。