Abstract:Based on the sorting out and comprehensive study of the data available about the chemical composition of various natural water, the authords hold that some of the important modern ore-bearing solutions occurring in Red Sea, Salton Sea, the middle portion of Mississipi State and Cheleken etc. can be called highly pure chloride brine in that their values of SO42-/C1- and HCO8-/C1- are <0.01, and their composition is appreciably distinct from that of magmatic water. The chemical analytical data of some volcanic hot springs in volcanic cones or craters show that there exists no highly pure chloride brine there at all. Some analytical data of volcanic emanating gas known to us also indicate that highly pure chloric emanation does not develop continuously either. And the same phenomena can be observed in the data of gas-liquid inclusions in minerals of igneous rocks collected by Roedder. This made us believe that there is Little possibility of the highly pure chloride brine relating to magma. In view of the intense solubility of the heavy metals in the highly pure chloride brine, it is conceivable that this brine would possibly extract these metals from wall rocks and accumulate them during its permeation, forming a sort of ore-bearing solution which has nothing to do with the magmatic evolution. Ore deposition in this solution beneath the surface or at the bottom of the surface water is called mineralization of hot vadose brine. In fact, it is very difficult to make a satisfactory explanation about the two rather prevalent theories "volcanic sedimentary deposits with distant sources which are deficient in volcanic material and " telethemal ore deposits" which are independent of the alteration and mineralization halo related to intrusive mass, The authors consider that most of these deposits are likely to be hot vadose brine deposits of various types. Abundant data reveal that there is not any noticeable concentration of barite both in the major deposits of iron or nonferrous metals genetically related to intrusive bodies and in the sedimentary deposits of iron and aluminium. Except for volcanic deposits with close sources and some rare or rare-earth deposits, the accumulation of barite is the result of the action of hot vadose brine and may be regarded as one of the genetic indicators of the deposits of the hot vadose brine type. The relation between the development of silicolites and metallic ore deposits in China shows that some silicolites which are of nonbiological genesis and are not closely related to volcanism might be the products of hot vadose brine so that they also serve as indicators for deposits of hot vadose brine type. From more than 3000 sulfrmc isotopic data of 130 localities of endogenic iron and nonferrous mineralization in China and the data of over 100 foreign copper and copper-nickel deposits, the authors are under the impression that the sulfuric isotopic composition of sulfide might act as another discriminating mark for the mineralization of hot vadose brine. Under certain a conditions, this indicator is of some help in ruling out the possibility of the existence of magmatic origin sulfur or the possibility of the normal sedimentary mineralization, thus facilitating the identification of ore genesis. The deposits of hot vadose brine type bear the characteristics of mineralization between typical endogenic deposits and typical exogenic deposits. This may be taken as an additional indicator for deposits of this sort. According to above described indicators, the deposits formed by hot vadose brine are estimated to make up the great majority of the reserves of the mercury, antimony and manganese ore in China, the majority of the reserves of the lead and. zinc ore, a considerable portion of the reserves of the iron ore and a minor portion of the reserves of the copper, molybdenum and tungsten ore.
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姜齐节, 冯建良, 余大良, 黄超, 刘东升, 陈民扬, 曾骥良.1983.渗流热卤水成矿作用的意义与矿床成因标志[J].矿床地质,2(3):57~59.1983.The role of hot vadose brine in mineralization and the genetic indicators of the ore deposits[J].Mineral Deposits2(3):57~59
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