Abstract:Xihuashan is located in. a Caledonian fold region of South China where lots of granitoid intrusions occur ranging in size from large batholiths to small intrusive bodies in association with the regional structures, especially subsequent faults of such different trends as NE, NW, NNE and EW. The Xihuashan granite body is found to be one of the projecting cupolas from a common concealed long batholith ridge trending NE under the roof of slightly metamorphosed flyschoid beds, The isotopic ages dating the batholith range from 140 m. y. to 180 m. y. The exposed surface of the Xihuashan granite body is about 20 km2 in area and ellipsoidalin shape with longer axis running NW-SE. The aureole of hornfels around the igneous body makes up a remarkable feature, suggesting the effect of contact metamorphism. The Xihuashan mining area is situated predominantly at the southern spuror tongue detached from the Xihuashan main grartite body. Within the spur are two phases of granite rather closely related to tungsten metallization. The earlier phase γ (a) is porphyritic medium-to fine-grained biotite granite, heavily fractured but relatively slightly altered, and characterized by RE-bearing accessory mineral association of fairly abundant yttrite, a minor amount of hussakite, monazite and a little yttroparisite. The later phaseγ(a) is represented by medium-grained graniteγ(b-l) with subordinate amounts of porphyritic fine-grained, garnet-bearing graniteγ(b-2). Bothγ(b-l) andγ(b-2)are characterized by such common features as being rather full of miarolitic microcavities, subjected to extensively alkalic feldspathization and containing specific RE-bearing accessory mineral association of comparatively large amounts of yttrite, hussakite and yttroparisite and a little monazite. The contact betweenγ(a) andγ(b) is usually marked with a seam of pegmatitoid where the surface is rather flat, but becomes obscure where the surface is steep. Petrochemically, bothγ(a) andγ(b) are attributed to a common primary magma of peraluminous group in oversaturated category. In addition to containing a minor or trace amount of Sn, Bi, Mo, Be, Zn, Pb, Cu, etc., both granites have abnormally large quantities of W, which reaches as much as ten to hundred-fold of the W abundance of acidic igneous rocks. Compared withγ(a), γ(b) contains less TiO2, Al2O3, Fe2O3+FeO and MgO, more F and MnO, and is fairly rich in such cations with high charges as Ga, Nb, Zr, and all REE but Eu. The presence of quite a few remanent roofs and pendants of γ(a) and country rocks implies that the present outcrop surface is likely near the top of the intrusive body ofγ(b). Almost all the productive lodes are confined to the intrusive body, particularly y(b). On the whole, there are two major sets of nearly parallel lode groups, i.e., (1) NWW or nearly EW trending set with fairly steep northward dip, which is congested at the northern part of the mining area, and (2) NEE trending set with northward dip not so steep as the former at the southern part. Through extensive mining works, it has been realized that economic tungsten lodes are, so far, restricted to an outer altered rock shell right below the roof of the intrusive. 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Unlike the subsequent fissure-filling vein usually characterized by evident selvage on both parallel and symmetrical wallsides, the lodes here, particularly the NWW trending ones, not only show the feature of asymmetrical and often irregular wallsides, but, in cases, also extend gradationally outward through altered wall rock to the country rock in such successions as exampled by zones of silicified margin, K-feldspathization (610℃), greissenization (570-620℃) and alkalic feldspathized (650℃) granite. Still, at lower levels, crumple vein or different kinds of ore nodes have been found under favorable trap. The studies on chemical composition of all the minerals in the igneous body and on fluid inclusions reveal that the residual fluid of late magmatic stage should have contained CO2, F, H2O, P, S, K, Si, W, Be, Nb, Ta, Sn, Th, U, Pb, Cs, Li, Rb, Sr, and REE, and that partial W had migrated upward and relatively concentrated at the upper part of the magmatic ring crystallization. Stable isotope studies suggest that were mainly derived from magmatic water. chamber before or duing crystallization. Stable isotope studies suggest that the ore-bearing fluids were mainly derived from magmatic water. All the ab
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郭文魁.1983.西华山钨矿床的金属矿化作用：一个与岩浆后期渗浸相联系的热液脉矿的实例[J].矿床地质,2(2):1~14.1983.Metallization fo Xihuashan tungsten deposit: An example linking magmatic deuteric infiltration with hydrothermal lodes[J].Mineral Deposits2(2):1~14
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