黔西南卡林型金矿的成矿机制及成矿预测
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摘要
中国西南地区广布的峨眉山玄武岩是目前国际地学界公认的我国唯一的火成岩省。它的形成与特殊的地幔动力作用过程——峨眉地幔热柱活动有关。峨眉地幔热柱活动及成矿是一个前沿性的研究课题，也是近年来地学工作者研究的热点问题之一。
作为滇黔桂金三角主体的黔西南卡林型金矿是当前中国较有代表性的卡林型金矿。许多部门及学者运用多种研究手段和技术对它进行较为深入地研究，取得较大的研究成果；但目前还没有人真正地将峨眉地幔热柱活动与黔西南卡林型金矿的成因有机地结合起来，对峨眉地幔热柱活动是如何影响卡林型金矿的区域成矿背景、如何诱发热水、如何产生成矿物质、热水沉积作用如何导致金矿床的形成具体过程等等深层次问题，目前国内外研究较少。同时，热水沉积成矿作用在地球上是否具普遍性、整个热水沉积成矿作用的驱动力是什么、成矿流体的来源和如何运移等这些问题至今矿床学界还没有得到令人信服的解释。本论文以黔西南卡林型金矿床为例，研究在峨眉地幔热柱作用下，黔西南卡林型金矿床集中区(简称矿集区)金矿的形成过程，通过峨眉地幔热柱活动形成卡林型金矿床的机制研究，将对上述问题给予一定的解释和回答。
峨眉地幔热柱是中国典型的地幔热柱之一。据地震层析成像编制的地幔热柱三维速度结构图，揭示了峨眉地幔热柱在50～450km深度上为一复合低速柱，由若干个呈“梅花状”分布的次级亚热柱组成。其初始地幔热柱蘑菇状头部直径约1000～1500km，尾部区位于攀枝花一带，直径约250km。这一复合低速柱反映了峨眉山地幔热柱的纵向与横向不均匀性和多级演化特征。活动期为晚古生代至新生代早期。岩浆活动总体演化由基性到酸性，由喷发到侵入，由海相到陆相，物质从幔源到壳幔混合来源。裂谷作用由泥盆纪至三叠纪，从南东向北西依次开裂迁移演化。
伴随峨眉地幔热柱构造作用出现的基性-酸性岩浆活动，始于晚古生代泥盆纪，大规模发育于晚古生代二叠纪至整个中生代，可延续到新生代早期。其中，早期阶段(晚古生代)以基性岩浆大规模喷发活动为主，晚期阶段(中生代-新生代早期)以酸性及碱性岩浆大规模侵入为主，伴随少量的基性-超基性岩浆侵入活动。这种由基性到酸性和碱性的岩浆演化，共包括大约7个活动时期。根据峨眉地幔热柱活动特殊性，结合峨眉地幔热柱活动时期，以及峨眉地幔热柱区域成矿的具体特点，通过系统研究和对比，将峨眉地幔热柱活动区域成矿按区域矿床成矿系列和部分成矿亚系列进行划分，共分成4个区域矿床成矿系列、6个成矿亚系列。黔西南卡林型金矿床就是其中的重要一员。
黔西南地区的沉积地层发育良好，分布广泛。但最主要的赋金地层在扬子地层区是上二叠统和下三叠统，在右江地层区则是中三叠统，分别称之为龙头山层序和赖子山层序。黔西南地区微细浸染型金矿床(卡林型金矿床)可细分为三个亚类：陆源硅质碎屑岩微细浸染型金矿床，不纯碳酸盐岩微细浸染型金矿床，以及火山碎屑岩(凝灰岩)微细浸染型金矿床。
在漫长的卡林型金矿形成过程中，热水沉积作用起到十分重要的作用。在峨眉地幔热柱的整个活动时期，岩浆活动强烈而频繁这为黔西南酿造出一个很好的热水形成环境，热水在该区广泛存在，并且通过长期对流循环模式形成含大量成矿物质的热水，黔西南金矿中的金在热水中主要是以AuH_3SiO4_~°形式迁移，其次是[AuCl_2]~-和[Au(HS)_2]~-的迁移形式。在成矿构造-热液循环体系中，含矿热水在构造驱动下沿控矿断裂构造带迁移上升，到达浅部或近地表的次级容矿或赋矿断裂构造破碎带，含矿热水体系由相对封闭体系到半开放-开放体系，特别是伴随有热水隐爆作用发生时，压力的突然释放、气体挥发份的大量散失、成矿热液发生沸腾，伴随含矿热水的多种物理化学条件或参数的改变，导致热水体系快速远离平衡态，使热水组分的浓度增大，络合物失稳，SiO_2的浓度达到过饱和状态，主要呈AuH_3SiO_4~0、次为[AuCl_2]~-和[Au(HS)_2]~-络合物形式运移的金伴随着大量隐晶-微晶二氧化硅-似碧玉岩和热液期黄铁矿及含砷、锑、汞等硫化物的沉淀而成矿。
金的络合物离子的解离反应式通常为：
AuH_3SiO_4~0+H_2O→Au(自然金)+H_4SiO_4+O_2
[AuCl_2]~-→Au(自然金)+Cl_2↑
[Au(HS)_2]~-→Au(自然金)+HS~-或者[Au(HS)_2]~-+CH_4+H~+→Au(自然金)+H_2S+C_(有机)
综观黔西南卡林型金矿的成矿，峨眉地幔热柱活动是矿集区金矿形成的先决条件，是它提供了金等成矿的物质来源和动力来源；同时它改造了该区沉积环境，峨眉山玄武岩浆的多次间歇喷发，区内地壳颤动频繁，使潮坪相、边缘台地相、孤立台地相、台盆相等频繁交替更迭，形成复杂的含矿系(即玄武质粘土岩、粉砂质粘土岩夹薄层凝灰质生物碎屑灰岩的沉积建造)，在扬子地台形成龙头山层序、在右江造山带形成赖子山层序的赋金地层。
黔西南卡林型金矿的形成，正是峨眉地幔热柱多期次构造活动的结果。峨眉地幔热柱活动形成黔西南卡林型金矿，其金的物质来源及成矿过程可用以下模式概括：金的主要来源：地核→地幔→地壳→近地表存在状态：气体→气-液混合相→含矿流体→固体主要通道：地幔热柱→亚热柱→幔枝→构造扩容带表现形式：构造变形→岩浆活动→变质作用→成矿作用成矿过程：幔柱活动→热水循环→热水沉积作用形成矿源层→热液叠加改造作用再富集成矿
金的最终成矿作用同时还受活化剂、活化环境等的明显控制。本文提出了黔西南卡林型金矿形成的三阶段模式：金的物质来源模式、含金建造形成模式、矿集区卡林型金矿成矿模式。
通过综合分析、研究认为黔西南卡林型金矿的形成过程是：黔西南地处濒临特提斯-喜马拉雅构造域与濒太平洋构造域的结合部位的特殊大地构造位置，峨眉地幔热柱活动持续时间漫长，在海西期东吴运动作用下，贵州最为强烈、规模较大的一次峨眉地幔热柱活动形成黔西南兴义、安龙、兴仁、贞丰一带的环境较为闭塞、潮坪-台地相及台地相与台地边缘斜坡相的过渡地带的沉积环境；同时，峨眉地幔热柱活动产生的晚二叠世早期峨眉山玄武岩浆喷发，为基性岩浆活动的高峰期，伴随着海底火山大量热水活动，喷出的成矿物质随火山气液直接热水沉积或玄武岩及火山碎屑岩发生海解释放出大量成矿物质，经热水沉积作用再结合生物吸附这些成矿物质死亡后通过有机质分解使大量的Au及其它微量元素呈极分散均一状态进入这一特殊的沉积盆地环境，随着古海平面的变化，沉积形成二叠系龙潭组包括陆源碎屑物质、碳酸盐岩物质、玉髓、有机物质及大量含矿物质的复杂的含矿煤系地层，形成紫木凼、水银洞、戈塘、泥堡、核桃树等金矿的主要含金建造(矿源层)。三叠纪时期，基本继承了前期的地质构造格局，沿坝索-册亨深断裂和坡坪同生断裂带分布的礁相带，成为南、北两大相区的分界线：北部地区基底抬升，形成水下隆起，沉积了陆表海型台地相的碳酸盐岩、细碎屑岩及粘土岩等：南部地区沉降强烈，形成了印支凹陷区，沉积了巨厚的复理石建造。另外，由于裂谷的形成和发展，在南盘江以南的广西境内，形成裂谷凹陷中心，在与坝索-册亨深断裂之间构成斜坡地带，主要包括兴义南部、册亨大部、贞丰南部以及望谟等地带，沉积了陆缘海型深水盆地相的浊积岩、凝灰浊积岩。斜坡地带往往是地球化学的转换带，而一些礁相带的凹凸弯曲部位可形成局部的封闭条件，引起成矿物质的相对聚集和沉淀。在桂西北地区的三叠纪时期，由于峨眉地幔热柱活动，形成多次火山活动，喷出的成矿物质随火山气液直接热水沉积或火山喷出岩发生海解作用带出大量的成矿物质经热水沉积作用，在黔西南南部的部分地区和部分层位中形成含金、砷、锑等背景值较高的岩石，如新苑组、许满组、边阳组等，这些层位构成烂泥沟、丫他、百地、洛帆、板其、豆芽井等陆源硅质碎屑岩型金矿的含金建造(矿源层)。
处于成岩期二叠系“大厂层”、含矿煤系地层和中三叠统浊积岩地层等含金建造(矿源层)中的Au及其它微量元素呈极分散均一状态；但在峨眉山玄武岩的多次喷溢作用下，这一地域形成含、隔水层岩石频繁交替的复杂沉积韵律构造。海水、大气降水、地下水(包括承压水、潜水、包气带水等)以及岩浆水等深渗循环不断从含金建造(矿源层)中萃取大量的Au等成矿物质形成含金硅络合物、金硫络合物等形式迁移的含矿热水，在燕山期峨眉地幔热柱再次活动作用下，由于强烈的构造运动，使热水相对封闭的平衡体系遭到破坏，在构造应力驱动下使封存在沉积盆地巨厚沉积柱中的这些含矿热水与地表水混合，在强烈热液叠加改造作用下，地球化学条件发生强烈变化，含矿热水的原有平衡被破坏，在应力释放的矿区背斜轴部、层间滑动带、断裂破碎带中这些含矿热水发生交代、充填作用，金等成矿物质随黄铁矿发生共沉淀，金被黄铁矿等吸附或包裹，形成矿体。结果形成“大厂层”中火山碎屑岩(凝灰岩)型、龙潭组煤系地层中不纯碳酸岩盐岩型、中三叠统浊积岩地层中陆源硅质碎屑岩型等三种卡林型金矿床(点)和其它元素异常、矿化。
论文最后通过室内理论研究及野外现场验证，结合成矿预测依据、区域内金的异常特征、分散流异常Au、As平均含量乘积划分、综合信息提取与分析，对于黔西南卡林型金矿的成矿预测，可初步划定Ⅰ、Ⅱ两级成矿预测远景区共7个。其中：Ⅰ级成矿预测远景区5个，包括盘县的归顺远景区、兴仁县的下山远景区、望漠县的白层-洛东远景区、包树-大观远景区和兴义市的雄武远景区。Ⅱ级成矿预测远景区2个，包括关岭县的顶云-永宁镇远景区、花江远景区。
In recent years, the region of Southwest China where the Emeishan basalts are widespread is an igneous rock province commonly accepted by the international geological circles at present time. Its formation is concerned with the product of a unique mantle dynamic process, i.e. the Emei mantle plume activity. Emei mantle plume activity and mineralization is a advanced question for study or discussion, and it is one of the hot question that geological researchers study in recent years.
The Carlin-type gold deposits in southwestern of Guizhou province considered to a body of gold triangle in Yunnan、Guizhou and Guangxi is a representative Carlin-type gold deposit in China at present time. Many units and researchers progress in deep-going investigations to it using many studying means and technology, achiever great studying result; however, now none organic combine to study between Emei mantle plume activity and a origin of Carlin-type gold deposits in southwestern of Guizhou province, about some deep levels questions, i.e. Emei mantle plume activity is how to affect regional mineralization background of Carlin-type gold deposits, how to cause hydrothermal solution, how to produce ore-forming matter, sedimentary process that hydrothermal solution is how to lead to form gold deposits etc. few someone knows to above all question at present. And, the sedimentary process of hydrothermal solution is whether or not universality, what is a dynamic pressure in whole hydrothermal solution mineralization, ore-forming fluid is how to produce and move; all the questions don't be convinced to explain in ore deposit science in recent years. In the academic thesis, the Carlin-type gold deposits in southwestern of Guizhou province is a researching sample, studies how gold deposit is formed in concentrate district of the Carlin-type gold deposits through Emei mantle plume activity in southwestern of Guizhou province. Through the research on a mechanism forming Carlin-type gold deposits in Emei mantle plume activity, may explain and answer to a great extent above questions.
The Emei mantle plume is one of the most typical mantle plume in China. According to the tridimentional velocity-texture diagram of mantle plume charted in terms of the seismological-tomographic imagery, the Emei mantle plume is a composite low-velocity plume at the 50-450-km depth, which is composed of a number of "plum flower-shaped" sub-plumes. The initial mushroom-shaped head of the mantle plume is measured at 1000-1500 km in diameter, and its tailing part is located around the area of Panzhihua, about 250 km in diameter. The occurrence of this composite low-velocity plume reflects the heterogeneity of the Emei mantle plume in both vertical and lateral directions and the characteristics of its multi-stage evolution. The activity period of the Emei mantle plume is from Late Paleozoic to Early Cenozoic, the overall evolutionary trend of magmas from old to young is: from mafic to acidic to alkaline; from eruption to intrusion; from marine facies to marine-continental alternative facies; and from mantle source to mantle source-predominating mantle/crust mixed source. The gap process is from the Devonian to the Mesozoic, its cracking evolutionary is from southeast to northwest.
The mafic-acidic magmatic activities in response to the Emei mantle plume tectonism started at the Devonian of the Late Paleozoic, extensively developed from the Permian of Late Paleozoic to the whole Mesozoic, even till the Early Mesozoic. During the early period (Late Paleozoic) large-scale mafic magmatic activity is dominant; during the late period (Mesozoic to Early Cenozoic) large-scale acidic and alkaline magmatic activities are dominant, associated with minor mafic-ultramafic magma intrusion.
Evolutionary of magmas from mafic to acidic and alkaline includes about seven activity stages. According to a peculiarity of Emei mantle plume activity, uniting a period of Emei mantle plume activity as well as a feature of Emei mantle plume activity in region, through much study and contrast, the regional mineralization of Emei mantle plume activity is divided into four mineralization series and six mineralization the second series in southwestern of china. The carlin type gold deposit is one of the important unit in southwestern, Guizhou.
In southwestern of Guizhou province, development of sedimentary stratium is well, its distribution is widespread. However, main stratium hosting gold is upper Permian series and lower Triassic series in Yangzi stratium district, middle Triassic series in Youjiang stratium district, they are separately named to Long Toushan stratotype as well as Lai Zishan stratotype. The carlin-type gold deposits may be divided into three types further in southwestern of Guizhou province, firstly micro-particle disseminated type gold deposits occurring in continental source siliceous clastic rock, secondly micro-particle disseminated type gold deposits occurring in carbonate rock , thirdly micro-particle disseminated type gold deposits occurring in volcanic clastic rock (tuff).
A sedimentary process of hydrothermal solution is very important role in a mineralization of long time to the Carlin type gold deposits. In whole period of Emei mantle plume activity, magma process is intense as well as frequent, which forms a excellent environment occurring hydrothermal solution in southwestern of Guizhou, the hydrothermal solution exist widespread in the area, and through a model of long-term cycle, it forms hydrothermal solution bearing a lot ore-forming matter. In southwestern of Guizhou, the gold of the hydrothermal solution is main migrated in form of AuH_3SiO_4~°, secondly in form of [AuCl_2]~-as well as[Au(HS)_2]~-. In the system made up ore-forming structure and cycle of hydrothermal solution, ore-bearing hydrothermal solution migrates up along with ore-controlling fault structure belt in a process of structure movement, it arrives in second ore-hosting or ore-bearing fault structural belt of shallow place or near surface of earth.. Moreover, the system of ore-forming hydrothermal solution change from closed state to part-opened or opened state, special, as a happening process concealed burst function of hydrothermal solution, due to release pressure rapidly as well as a mount of scatter and disappear of volatilizing matter, moreover, ore-forming hydrothermal solution appear out boiling, in order that much condition and parameter happens to change in ore-bearing hydrothermal solution, which leads that the system of hydrothermal solution depart from balance state rapidly, and lead to increase a density of ore-forming matter in hydrothermal solution, lead that complex compound loses stable, and SiO_2 density achieves super-saturation state, as a lots deposits of much cryptocrystalline-microcrystalline siliceous rock and basanite as well as pyrite and other sulphide bearing As, Sb, Hg etc. in hydrothermal solution stage , gold removes to form gold deposits main in the form of AuH_3SiO_4~°, secondly in form of [AuCl_2]~-as well as[Au(HS)_2]~-. Under normal conditions, resolving reaction formula of gold complex compound is:AuH_3SiO_4~0+ H_2O→Au (natural gold) + H_4SiO_4+O_2 [AuCl_2]~-→Au (natural gold) + Cl_2↑[Au(HS)_2]~-→Au (natural gold) + HS~-or [Au(HS)_2]~- + CH_4 + H~+→Au (natural gold) +H_2S + C_(organ)
As is shown from the ore-forming process of gold deposits in southwestern of Guizhou, The Emei mantle plume activity is firstly condition that gold deposit forms in ore concentrating district. It provides matter source forming gold deposit etc. and ore-forming power source; moreover, it transforms sedimentary environment in the area. According to Emeishan basalt eruption of intermission as well many times, vibration of crust is frequent in the area, which makes tidal flat facies, edge platform facies, isolated platform and basin facies change frequently, which lead to form complex ore-bearing rock , that is, a sedimentary formation containing basalt clay rock , siltstone clay rock as well as thin bed bioclastic limestone. Lead to form hosting gold formation of Long Toushan stratotype in Yang Zi platform region and Lai Zishan stratotype in You Jiang orogenic belt.
In southwestern of Guizhou, a mineralization process of Carlin-type gold deposits is a result from many times movement of Emei mantle plume activity. Its matter source and ore-forming process may be summarized by following model:
Main source of gold matter: core of the earth→mantle of the earth→crust of the earth→near the earth's surface
Existing state: gas→adding gas-liquid facies→ore-bearing fluid→solidMain channel: mantle plume→sub-mantle plume→mantle branch→ore-hosting belt Show form: deformation of structures→magam's activity→metamorphism→mineralization
Ore-forming process: mantle plume activity→hydrothermal solution's cycle→source beds forming by deposit process of hydrothermal solution→forming gold ore bodies adding reformation process of hydrothermal solution
Moreover, mineralization of gold deposits still is obviously controlled by mineralizer and mineralizing environment. In the thesis, gives three stages process model of Carlin-type gold deposits in southwestern of Guizhou: matter source model of gold deposits, forming model of gold-bearing formation, metallogenic model of Carlin-type gold deposit in the mineralizing concentrating district.
According to the deep study to mineralization in southwestern of Guizhou, is considered in following to ore-forming process of the gold deposit: As the region of Southwest Guizhou is located in an unique geotectonic setting at the juncture between the Tethys-Himalaya tectonic domain and the Pacific tectonic domain, the Emei mantle plume activity would last for a long period of time. During the Hercynian Dongwu Movement Guizhou experienced most intense tectonic activity. A larger-scale Emei mantle plume activity occurred around the areas of Xingyi, Anlong, Xingren and Zhenfeng of southwestern Guizhou since there had prevailed a relatively close environment, i.e., the sedimentary environment in a transitional zone from platform facies to platform marginal slope facies. In addition, eruption of the early Late Permian Emeishan basaltic magma caused by the Emei mantle plume activity marked the peak stage of basic magmatism. Accompanied by seafloor volcano-hydrothermal activities, on the one hand direct sediment gushing ore-forming matter with some gas and liquid of volcanic activity, on the other hand, move as well as deposit a lot of ore-forming matter carried out by ocean water dissolving process with volcanic rock, large amounts of Au, As, Hg, Sb and other trace elements found their way by deposit process of hydrothermal solution, in the form of extreme dispersion, into this sedimentary basin environment. With the variation of paleo-sea level, the Longtan Formation coal system seams that include terrigenous clastic matter, carbonated rock matter, chalcedony, organic matter and a lots ore-forming matter were formed. Which forms main gold-bearing formation or source bed like Zi mudang gold deposit, Shi Yindong gold deposit, Ge Tang gold deposit, Ni Pu gold deposit, He Taoshu gold deposit etc. Triassic Period, the region follows mainly a outline of geological structure earlier stage, the reef facies belt distributing along the Ba Suo-Ce Heng deep fault and Po Ping contemporaneous fault become a line of demarcation dividing two facies among south facies with north facies. In northern, basement is uprised, which sediments carbonate rock ,fine-clastic rock and clay rock of platform facies in continental sea; southern is subsided intensely ,leads to form Yin Zhi downwarping region, which deposits flysch formation of great thickness. In addition, according to a formation and development of rift, Guang Xi scale in south of Nan Panjiang forms a center of downwarping region of rift; which makes up a slope zone among Ba Suo-Ce Heng deep fault, which main involves a area of the southern of Xing Yi, the most part of Ce Heng, the southern of Zhen Feng, and Wang Mo etc., the area deposits turbidite rock and tuffaceous turbidite rock of deep water basin facies in continental sea type. Some slope belts often are changing belt to geochemistry peculiarity, some hollow winding place in the reef facies may form partial close condotion, which leads to collect and deposit for ore-forming matter. In Triassic Period of northwestern of Guang Xi, the Emei mantle plume activity leads to form many times volcanic activity, on the one hand direct sediment gushing ore-forming matter with some gas and liquid of volcanic activity, on the other hand, move as well as deposit a lot of ore-forming matter carried out by ocean water dissolving process with volcanic rock, which offers a mount of ore-forming matter for source bed by deposit process of hydrothermal solution. Therefore, form some rock of high goechemical background value bearing Au, As, Sb, Hg etc. at partial area as well as partial seam in the southern of southwestern of Guizhou, e.g. Xi Yuan formation, Xu Man formation, Bian Yang formation and so on, the seams make up gold-bearing formations or source beds of continental source siliceous clastic rock-type gold deposits like Lan Nigou gold deposit, Ya Ta gold deposit, Bai Di gold deposit, Luo Fan gold deposit, Ban Qi gold deposit, Dou Yajing gold deposit and so on.
In the gold-bearing formations or source beds of Da Chang bed, coal seams and strata of Permian System and turbidite strata of middle Triassic series at the diagenetic stage, Au, As, Hg and Sb and other trace elements were extremely homogeneously dispersed but in response to the Emei mantle plume activity, As, Au, Hg, Sb and other ore-forming materials were continuously extracted by earth surface water, ocean water, deeply circulating water (confined water, phreatic water, water of aeratedzone etc.) as well as magma water from the gold-bearing formations or source beds, thereafter forms ore-forming hydrothermal solutions that removes in a lots Au-Si complex compound as well as Au-S complex compound. During the Yanshanian period ,due to intensely tectonic movement, mix the hydrothermal solutions closed in plume of sedimentary in the sedimentary basin with the earth surface water, which leads to a intensive change in geochemistry condition, makes relative closed balance system of the hydrothermal solutions disrupt, under a prompt of tectonic power and adding reformation process of mixing hydrothermal solution, those ore-forming elements were transported upwards by metasomatism and cavity filling along tectonically weak loci such as folds and faults or advantage geochemical protective screen, which collects a large mount of ore-forming matter of Au and so on and forms sedimentary process of hydrothermal solutions, and ore-forming matter of gold etc. deposits with pyrite, gold is absorbed or bundled by pyrite etc. therefore, which forms gold bodies.
Result from three types Carlin-type gold deposit or mineral occurrence: volcanic clastic rock or tuff-type gold deposit in Da Chang bed, carbonate rock-type gold deposit in coal seam of Long Tan formation and continental source siliceous clastic rock-type gold deposit in turbidite strata of middle Triassic series as well as abnormalities and mineralization of other trace elements were formed.
In the thesis, finally according to theoretical research in home and spot test in open, uniting prognostic foundation as well as gold abnormalities feature in the region, dividing multiplying volume to mean content of Au、As in abnormalities of dispersion trains, extracting and analysing synthetical information, may primary divide two grades to minerogenetic prospect province orⅠ、Ⅱgrades, there are seven minerogenetic prospect provinces. That is: five minerogenetic prospect provinces toⅠgrade, they include: Gui Shun minerogenetic prospect province in Pan Xian county, Xia Shan minerogenetic prospect province in Xing Ren county, Bai Ceng-Luo Dong minerogenetic prospect province in Wang Mo county, Bao Shu-Da Guan minerogenetic prospect province in Wang Mo county and Xiong Wo minerogenetic prospect province in Xing Yi city; two minerogenetic prospect provinces toⅡgrade, they include: Ding Yun-Yong Ningzheng minerogenetic prospect province in Guan Ling county and Hua Jiang minerogenetic prospect province in Guan Ling county.
作为滇黔桂金三角主体的黔西南卡林型金矿是当前中国较有代表性的卡林型金矿。许多部门及学者运用多种研究手段和技术对它进行较为深入地研究，取得较大的研究成果；但目前还没有人真正地将峨眉地幔热柱活动与黔西南卡林型金矿的成因有机地结合起来，对峨眉地幔热柱活动是如何影响卡林型金矿的区域成矿背景、如何诱发热水、如何产生成矿物质、热水沉积作用如何导致金矿床的形成具体过程等等深层次问题，目前国内外研究较少。同时，热水沉积成矿作用在地球上是否具普遍性、整个热水沉积成矿作用的驱动力是什么、成矿流体的来源和如何运移等这些问题至今矿床学界还没有得到令人信服的解释。本论文以黔西南卡林型金矿床为例，研究在峨眉地幔热柱作用下，黔西南卡林型金矿床集中区(简称矿集区)金矿的形成过程，通过峨眉地幔热柱活动形成卡林型金矿床的机制研究，将对上述问题给予一定的解释和回答。
峨眉地幔热柱是中国典型的地幔热柱之一。据地震层析成像编制的地幔热柱三维速度结构图，揭示了峨眉地幔热柱在50～450km深度上为一复合低速柱，由若干个呈“梅花状”分布的次级亚热柱组成。其初始地幔热柱蘑菇状头部直径约1000～1500km，尾部区位于攀枝花一带，直径约250km。这一复合低速柱反映了峨眉山地幔热柱的纵向与横向不均匀性和多级演化特征。活动期为晚古生代至新生代早期。岩浆活动总体演化由基性到酸性，由喷发到侵入，由海相到陆相，物质从幔源到壳幔混合来源。裂谷作用由泥盆纪至三叠纪，从南东向北西依次开裂迁移演化。
伴随峨眉地幔热柱构造作用出现的基性-酸性岩浆活动，始于晚古生代泥盆纪，大规模发育于晚古生代二叠纪至整个中生代，可延续到新生代早期。其中，早期阶段(晚古生代)以基性岩浆大规模喷发活动为主，晚期阶段(中生代-新生代早期)以酸性及碱性岩浆大规模侵入为主，伴随少量的基性-超基性岩浆侵入活动。这种由基性到酸性和碱性的岩浆演化，共包括大约7个活动时期。根据峨眉地幔热柱活动特殊性，结合峨眉地幔热柱活动时期，以及峨眉地幔热柱区域成矿的具体特点，通过系统研究和对比，将峨眉地幔热柱活动区域成矿按区域矿床成矿系列和部分成矿亚系列进行划分，共分成4个区域矿床成矿系列、6个成矿亚系列。黔西南卡林型金矿床就是其中的重要一员。
黔西南地区的沉积地层发育良好，分布广泛。但最主要的赋金地层在扬子地层区是上二叠统和下三叠统，在右江地层区则是中三叠统，分别称之为龙头山层序和赖子山层序。黔西南地区微细浸染型金矿床(卡林型金矿床)可细分为三个亚类：陆源硅质碎屑岩微细浸染型金矿床，不纯碳酸盐岩微细浸染型金矿床，以及火山碎屑岩(凝灰岩)微细浸染型金矿床。
在漫长的卡林型金矿形成过程中，热水沉积作用起到十分重要的作用。在峨眉地幔热柱的整个活动时期，岩浆活动强烈而频繁这为黔西南酿造出一个很好的热水形成环境，热水在该区广泛存在，并且通过长期对流循环模式形成含大量成矿物质的热水，黔西南金矿中的金在热水中主要是以AuH_3SiO4_~°形式迁移，其次是[AuCl_2]~-和[Au(HS)_2]~-的迁移形式。在成矿构造-热液循环体系中，含矿热水在构造驱动下沿控矿断裂构造带迁移上升，到达浅部或近地表的次级容矿或赋矿断裂构造破碎带，含矿热水体系由相对封闭体系到半开放-开放体系，特别是伴随有热水隐爆作用发生时，压力的突然释放、气体挥发份的大量散失、成矿热液发生沸腾，伴随含矿热水的多种物理化学条件或参数的改变，导致热水体系快速远离平衡态，使热水组分的浓度增大，络合物失稳，SiO_2的浓度达到过饱和状态，主要呈AuH_3SiO_4~0、次为[AuCl_2]~-和[Au(HS)_2]~-络合物形式运移的金伴随着大量隐晶-微晶二氧化硅-似碧玉岩和热液期黄铁矿及含砷、锑、汞等硫化物的沉淀而成矿。
金的络合物离子的解离反应式通常为：
AuH_3SiO_4~0+H_2O→Au(自然金)+H_4SiO_4+O_2
[AuCl_2]~-→Au(自然金)+Cl_2↑
[Au(HS)_2]~-→Au(自然金)+HS~-或者[Au(HS)_2]~-+CH_4+H~+→Au(自然金)+H_2S+C_(有机)
综观黔西南卡林型金矿的成矿，峨眉地幔热柱活动是矿集区金矿形成的先决条件，是它提供了金等成矿的物质来源和动力来源；同时它改造了该区沉积环境，峨眉山玄武岩浆的多次间歇喷发，区内地壳颤动频繁，使潮坪相、边缘台地相、孤立台地相、台盆相等频繁交替更迭，形成复杂的含矿系(即玄武质粘土岩、粉砂质粘土岩夹薄层凝灰质生物碎屑灰岩的沉积建造)，在扬子地台形成龙头山层序、在右江造山带形成赖子山层序的赋金地层。
黔西南卡林型金矿的形成，正是峨眉地幔热柱多期次构造活动的结果。峨眉地幔热柱活动形成黔西南卡林型金矿，其金的物质来源及成矿过程可用以下模式概括：金的主要来源：地核→地幔→地壳→近地表存在状态：气体→气-液混合相→含矿流体→固体主要通道：地幔热柱→亚热柱→幔枝→构造扩容带表现形式：构造变形→岩浆活动→变质作用→成矿作用成矿过程：幔柱活动→热水循环→热水沉积作用形成矿源层→热液叠加改造作用再富集成矿
金的最终成矿作用同时还受活化剂、活化环境等的明显控制。本文提出了黔西南卡林型金矿形成的三阶段模式：金的物质来源模式、含金建造形成模式、矿集区卡林型金矿成矿模式。
通过综合分析、研究认为黔西南卡林型金矿的形成过程是：黔西南地处濒临特提斯-喜马拉雅构造域与濒太平洋构造域的结合部位的特殊大地构造位置，峨眉地幔热柱活动持续时间漫长，在海西期东吴运动作用下，贵州最为强烈、规模较大的一次峨眉地幔热柱活动形成黔西南兴义、安龙、兴仁、贞丰一带的环境较为闭塞、潮坪-台地相及台地相与台地边缘斜坡相的过渡地带的沉积环境；同时，峨眉地幔热柱活动产生的晚二叠世早期峨眉山玄武岩浆喷发，为基性岩浆活动的高峰期，伴随着海底火山大量热水活动，喷出的成矿物质随火山气液直接热水沉积或玄武岩及火山碎屑岩发生海解释放出大量成矿物质，经热水沉积作用再结合生物吸附这些成矿物质死亡后通过有机质分解使大量的Au及其它微量元素呈极分散均一状态进入这一特殊的沉积盆地环境，随着古海平面的变化，沉积形成二叠系龙潭组包括陆源碎屑物质、碳酸盐岩物质、玉髓、有机物质及大量含矿物质的复杂的含矿煤系地层，形成紫木凼、水银洞、戈塘、泥堡、核桃树等金矿的主要含金建造(矿源层)。三叠纪时期，基本继承了前期的地质构造格局，沿坝索-册亨深断裂和坡坪同生断裂带分布的礁相带，成为南、北两大相区的分界线：北部地区基底抬升，形成水下隆起，沉积了陆表海型台地相的碳酸盐岩、细碎屑岩及粘土岩等：南部地区沉降强烈，形成了印支凹陷区，沉积了巨厚的复理石建造。另外，由于裂谷的形成和发展，在南盘江以南的广西境内，形成裂谷凹陷中心，在与坝索-册亨深断裂之间构成斜坡地带，主要包括兴义南部、册亨大部、贞丰南部以及望谟等地带，沉积了陆缘海型深水盆地相的浊积岩、凝灰浊积岩。斜坡地带往往是地球化学的转换带，而一些礁相带的凹凸弯曲部位可形成局部的封闭条件，引起成矿物质的相对聚集和沉淀。在桂西北地区的三叠纪时期，由于峨眉地幔热柱活动，形成多次火山活动，喷出的成矿物质随火山气液直接热水沉积或火山喷出岩发生海解作用带出大量的成矿物质经热水沉积作用，在黔西南南部的部分地区和部分层位中形成含金、砷、锑等背景值较高的岩石，如新苑组、许满组、边阳组等，这些层位构成烂泥沟、丫他、百地、洛帆、板其、豆芽井等陆源硅质碎屑岩型金矿的含金建造(矿源层)。
处于成岩期二叠系“大厂层”、含矿煤系地层和中三叠统浊积岩地层等含金建造(矿源层)中的Au及其它微量元素呈极分散均一状态；但在峨眉山玄武岩的多次喷溢作用下，这一地域形成含、隔水层岩石频繁交替的复杂沉积韵律构造。海水、大气降水、地下水(包括承压水、潜水、包气带水等)以及岩浆水等深渗循环不断从含金建造(矿源层)中萃取大量的Au等成矿物质形成含金硅络合物、金硫络合物等形式迁移的含矿热水，在燕山期峨眉地幔热柱再次活动作用下，由于强烈的构造运动，使热水相对封闭的平衡体系遭到破坏，在构造应力驱动下使封存在沉积盆地巨厚沉积柱中的这些含矿热水与地表水混合，在强烈热液叠加改造作用下，地球化学条件发生强烈变化，含矿热水的原有平衡被破坏，在应力释放的矿区背斜轴部、层间滑动带、断裂破碎带中这些含矿热水发生交代、充填作用，金等成矿物质随黄铁矿发生共沉淀，金被黄铁矿等吸附或包裹，形成矿体。结果形成“大厂层”中火山碎屑岩(凝灰岩)型、龙潭组煤系地层中不纯碳酸岩盐岩型、中三叠统浊积岩地层中陆源硅质碎屑岩型等三种卡林型金矿床(点)和其它元素异常、矿化。
论文最后通过室内理论研究及野外现场验证，结合成矿预测依据、区域内金的异常特征、分散流异常Au、As平均含量乘积划分、综合信息提取与分析，对于黔西南卡林型金矿的成矿预测，可初步划定Ⅰ、Ⅱ两级成矿预测远景区共7个。其中：Ⅰ级成矿预测远景区5个，包括盘县的归顺远景区、兴仁县的下山远景区、望漠县的白层-洛东远景区、包树-大观远景区和兴义市的雄武远景区。Ⅱ级成矿预测远景区2个，包括关岭县的顶云-永宁镇远景区、花江远景区。
In recent years, the region of Southwest China where the Emeishan basalts are widespread is an igneous rock province commonly accepted by the international geological circles at present time. Its formation is concerned with the product of a unique mantle dynamic process, i.e. the Emei mantle plume activity. Emei mantle plume activity and mineralization is a advanced question for study or discussion, and it is one of the hot question that geological researchers study in recent years.
The Carlin-type gold deposits in southwestern of Guizhou province considered to a body of gold triangle in Yunnan、Guizhou and Guangxi is a representative Carlin-type gold deposit in China at present time. Many units and researchers progress in deep-going investigations to it using many studying means and technology, achiever great studying result; however, now none organic combine to study between Emei mantle plume activity and a origin of Carlin-type gold deposits in southwestern of Guizhou province, about some deep levels questions, i.e. Emei mantle plume activity is how to affect regional mineralization background of Carlin-type gold deposits, how to cause hydrothermal solution, how to produce ore-forming matter, sedimentary process that hydrothermal solution is how to lead to form gold deposits etc. few someone knows to above all question at present. And, the sedimentary process of hydrothermal solution is whether or not universality, what is a dynamic pressure in whole hydrothermal solution mineralization, ore-forming fluid is how to produce and move; all the questions don't be convinced to explain in ore deposit science in recent years. In the academic thesis, the Carlin-type gold deposits in southwestern of Guizhou province is a researching sample, studies how gold deposit is formed in concentrate district of the Carlin-type gold deposits through Emei mantle plume activity in southwestern of Guizhou province. Through the research on a mechanism forming Carlin-type gold deposits in Emei mantle plume activity, may explain and answer to a great extent above questions.
The Emei mantle plume is one of the most typical mantle plume in China. According to the tridimentional velocity-texture diagram of mantle plume charted in terms of the seismological-tomographic imagery, the Emei mantle plume is a composite low-velocity plume at the 50-450-km depth, which is composed of a number of "plum flower-shaped" sub-plumes. The initial mushroom-shaped head of the mantle plume is measured at 1000-1500 km in diameter, and its tailing part is located around the area of Panzhihua, about 250 km in diameter. The occurrence of this composite low-velocity plume reflects the heterogeneity of the Emei mantle plume in both vertical and lateral directions and the characteristics of its multi-stage evolution. The activity period of the Emei mantle plume is from Late Paleozoic to Early Cenozoic, the overall evolutionary trend of magmas from old to young is: from mafic to acidic to alkaline; from eruption to intrusion; from marine facies to marine-continental alternative facies; and from mantle source to mantle source-predominating mantle/crust mixed source. The gap process is from the Devonian to the Mesozoic, its cracking evolutionary is from southeast to northwest.
The mafic-acidic magmatic activities in response to the Emei mantle plume tectonism started at the Devonian of the Late Paleozoic, extensively developed from the Permian of Late Paleozoic to the whole Mesozoic, even till the Early Mesozoic. During the early period (Late Paleozoic) large-scale mafic magmatic activity is dominant; during the late period (Mesozoic to Early Cenozoic) large-scale acidic and alkaline magmatic activities are dominant, associated with minor mafic-ultramafic magma intrusion.
Evolutionary of magmas from mafic to acidic and alkaline includes about seven activity stages. According to a peculiarity of Emei mantle plume activity, uniting a period of Emei mantle plume activity as well as a feature of Emei mantle plume activity in region, through much study and contrast, the regional mineralization of Emei mantle plume activity is divided into four mineralization series and six mineralization the second series in southwestern of china. The carlin type gold deposit is one of the important unit in southwestern, Guizhou.
In southwestern of Guizhou province, development of sedimentary stratium is well, its distribution is widespread. However, main stratium hosting gold is upper Permian series and lower Triassic series in Yangzi stratium district, middle Triassic series in Youjiang stratium district, they are separately named to Long Toushan stratotype as well as Lai Zishan stratotype. The carlin-type gold deposits may be divided into three types further in southwestern of Guizhou province, firstly micro-particle disseminated type gold deposits occurring in continental source siliceous clastic rock, secondly micro-particle disseminated type gold deposits occurring in carbonate rock , thirdly micro-particle disseminated type gold deposits occurring in volcanic clastic rock (tuff).
A sedimentary process of hydrothermal solution is very important role in a mineralization of long time to the Carlin type gold deposits. In whole period of Emei mantle plume activity, magma process is intense as well as frequent, which forms a excellent environment occurring hydrothermal solution in southwestern of Guizhou, the hydrothermal solution exist widespread in the area, and through a model of long-term cycle, it forms hydrothermal solution bearing a lot ore-forming matter. In southwestern of Guizhou, the gold of the hydrothermal solution is main migrated in form of AuH_3SiO_4~°, secondly in form of [AuCl_2]~-as well as[Au(HS)_2]~-. In the system made up ore-forming structure and cycle of hydrothermal solution, ore-bearing hydrothermal solution migrates up along with ore-controlling fault structure belt in a process of structure movement, it arrives in second ore-hosting or ore-bearing fault structural belt of shallow place or near surface of earth.. Moreover, the system of ore-forming hydrothermal solution change from closed state to part-opened or opened state, special, as a happening process concealed burst function of hydrothermal solution, due to release pressure rapidly as well as a mount of scatter and disappear of volatilizing matter, moreover, ore-forming hydrothermal solution appear out boiling, in order that much condition and parameter happens to change in ore-bearing hydrothermal solution, which leads that the system of hydrothermal solution depart from balance state rapidly, and lead to increase a density of ore-forming matter in hydrothermal solution, lead that complex compound loses stable, and SiO_2 density achieves super-saturation state, as a lots deposits of much cryptocrystalline-microcrystalline siliceous rock and basanite as well as pyrite and other sulphide bearing As, Sb, Hg etc. in hydrothermal solution stage , gold removes to form gold deposits main in the form of AuH_3SiO_4~°, secondly in form of [AuCl_2]~-as well as[Au(HS)_2]~-. Under normal conditions, resolving reaction formula of gold complex compound is:AuH_3SiO_4~0+ H_2O→Au (natural gold) + H_4SiO_4+O_2 [AuCl_2]~-→Au (natural gold) + Cl_2↑[Au(HS)_2]~-→Au (natural gold) + HS~-or [Au(HS)_2]~- + CH_4 + H~+→Au (natural gold) +H_2S + C_(organ)
As is shown from the ore-forming process of gold deposits in southwestern of Guizhou, The Emei mantle plume activity is firstly condition that gold deposit forms in ore concentrating district. It provides matter source forming gold deposit etc. and ore-forming power source; moreover, it transforms sedimentary environment in the area. According to Emeishan basalt eruption of intermission as well many times, vibration of crust is frequent in the area, which makes tidal flat facies, edge platform facies, isolated platform and basin facies change frequently, which lead to form complex ore-bearing rock , that is, a sedimentary formation containing basalt clay rock , siltstone clay rock as well as thin bed bioclastic limestone. Lead to form hosting gold formation of Long Toushan stratotype in Yang Zi platform region and Lai Zishan stratotype in You Jiang orogenic belt.
In southwestern of Guizhou, a mineralization process of Carlin-type gold deposits is a result from many times movement of Emei mantle plume activity. Its matter source and ore-forming process may be summarized by following model:
Main source of gold matter: core of the earth→mantle of the earth→crust of the earth→near the earth's surface
Existing state: gas→adding gas-liquid facies→ore-bearing fluid→solidMain channel: mantle plume→sub-mantle plume→mantle branch→ore-hosting belt Show form: deformation of structures→magam's activity→metamorphism→mineralization
Ore-forming process: mantle plume activity→hydrothermal solution's cycle→source beds forming by deposit process of hydrothermal solution→forming gold ore bodies adding reformation process of hydrothermal solution
Moreover, mineralization of gold deposits still is obviously controlled by mineralizer and mineralizing environment. In the thesis, gives three stages process model of Carlin-type gold deposits in southwestern of Guizhou: matter source model of gold deposits, forming model of gold-bearing formation, metallogenic model of Carlin-type gold deposit in the mineralizing concentrating district.
According to the deep study to mineralization in southwestern of Guizhou, is considered in following to ore-forming process of the gold deposit: As the region of Southwest Guizhou is located in an unique geotectonic setting at the juncture between the Tethys-Himalaya tectonic domain and the Pacific tectonic domain, the Emei mantle plume activity would last for a long period of time. During the Hercynian Dongwu Movement Guizhou experienced most intense tectonic activity. A larger-scale Emei mantle plume activity occurred around the areas of Xingyi, Anlong, Xingren and Zhenfeng of southwestern Guizhou since there had prevailed a relatively close environment, i.e., the sedimentary environment in a transitional zone from platform facies to platform marginal slope facies. In addition, eruption of the early Late Permian Emeishan basaltic magma caused by the Emei mantle plume activity marked the peak stage of basic magmatism. Accompanied by seafloor volcano-hydrothermal activities, on the one hand direct sediment gushing ore-forming matter with some gas and liquid of volcanic activity, on the other hand, move as well as deposit a lot of ore-forming matter carried out by ocean water dissolving process with volcanic rock, large amounts of Au, As, Hg, Sb and other trace elements found their way by deposit process of hydrothermal solution, in the form of extreme dispersion, into this sedimentary basin environment. With the variation of paleo-sea level, the Longtan Formation coal system seams that include terrigenous clastic matter, carbonated rock matter, chalcedony, organic matter and a lots ore-forming matter were formed. Which forms main gold-bearing formation or source bed like Zi mudang gold deposit, Shi Yindong gold deposit, Ge Tang gold deposit, Ni Pu gold deposit, He Taoshu gold deposit etc. Triassic Period, the region follows mainly a outline of geological structure earlier stage, the reef facies belt distributing along the Ba Suo-Ce Heng deep fault and Po Ping contemporaneous fault become a line of demarcation dividing two facies among south facies with north facies. In northern, basement is uprised, which sediments carbonate rock ,fine-clastic rock and clay rock of platform facies in continental sea; southern is subsided intensely ,leads to form Yin Zhi downwarping region, which deposits flysch formation of great thickness. In addition, according to a formation and development of rift, Guang Xi scale in south of Nan Panjiang forms a center of downwarping region of rift; which makes up a slope zone among Ba Suo-Ce Heng deep fault, which main involves a area of the southern of Xing Yi, the most part of Ce Heng, the southern of Zhen Feng, and Wang Mo etc., the area deposits turbidite rock and tuffaceous turbidite rock of deep water basin facies in continental sea type. Some slope belts often are changing belt to geochemistry peculiarity, some hollow winding place in the reef facies may form partial close condotion, which leads to collect and deposit for ore-forming matter. In Triassic Period of northwestern of Guang Xi, the Emei mantle plume activity leads to form many times volcanic activity, on the one hand direct sediment gushing ore-forming matter with some gas and liquid of volcanic activity, on the other hand, move as well as deposit a lot of ore-forming matter carried out by ocean water dissolving process with volcanic rock, which offers a mount of ore-forming matter for source bed by deposit process of hydrothermal solution. Therefore, form some rock of high goechemical background value bearing Au, As, Sb, Hg etc. at partial area as well as partial seam in the southern of southwestern of Guizhou, e.g. Xi Yuan formation, Xu Man formation, Bian Yang formation and so on, the seams make up gold-bearing formations or source beds of continental source siliceous clastic rock-type gold deposits like Lan Nigou gold deposit, Ya Ta gold deposit, Bai Di gold deposit, Luo Fan gold deposit, Ban Qi gold deposit, Dou Yajing gold deposit and so on.
In the gold-bearing formations or source beds of Da Chang bed, coal seams and strata of Permian System and turbidite strata of middle Triassic series at the diagenetic stage, Au, As, Hg and Sb and other trace elements were extremely homogeneously dispersed but in response to the Emei mantle plume activity, As, Au, Hg, Sb and other ore-forming materials were continuously extracted by earth surface water, ocean water, deeply circulating water (confined water, phreatic water, water of aeratedzone etc.) as well as magma water from the gold-bearing formations or source beds, thereafter forms ore-forming hydrothermal solutions that removes in a lots Au-Si complex compound as well as Au-S complex compound. During the Yanshanian period ,due to intensely tectonic movement, mix the hydrothermal solutions closed in plume of sedimentary in the sedimentary basin with the earth surface water, which leads to a intensive change in geochemistry condition, makes relative closed balance system of the hydrothermal solutions disrupt, under a prompt of tectonic power and adding reformation process of mixing hydrothermal solution, those ore-forming elements were transported upwards by metasomatism and cavity filling along tectonically weak loci such as folds and faults or advantage geochemical protective screen, which collects a large mount of ore-forming matter of Au and so on and forms sedimentary process of hydrothermal solutions, and ore-forming matter of gold etc. deposits with pyrite, gold is absorbed or bundled by pyrite etc. therefore, which forms gold bodies.
Result from three types Carlin-type gold deposit or mineral occurrence: volcanic clastic rock or tuff-type gold deposit in Da Chang bed, carbonate rock-type gold deposit in coal seam of Long Tan formation and continental source siliceous clastic rock-type gold deposit in turbidite strata of middle Triassic series as well as abnormalities and mineralization of other trace elements were formed.
In the thesis, finally according to theoretical research in home and spot test in open, uniting prognostic foundation as well as gold abnormalities feature in the region, dividing multiplying volume to mean content of Au、As in abnormalities of dispersion trains, extracting and analysing synthetical information, may primary divide two grades to minerogenetic prospect province orⅠ、Ⅱgrades, there are seven minerogenetic prospect provinces. That is: five minerogenetic prospect provinces toⅠgrade, they include: Gui Shun minerogenetic prospect province in Pan Xian county, Xia Shan minerogenetic prospect province in Xing Ren county, Bai Ceng-Luo Dong minerogenetic prospect province in Wang Mo county, Bao Shu-Da Guan minerogenetic prospect province in Wang Mo county and Xiong Wo minerogenetic prospect province in Xing Yi city; two minerogenetic prospect provinces toⅡgrade, they include: Ding Yun-Yong Ningzheng minerogenetic prospect province in Guan Ling county and Hua Jiang minerogenetic prospect province in Guan Ling county.
引文
[1]涂光炽，地幔柱成岩成矿若干问题讨论，贵州省地二届矿产资源战略发展研讨会(内部刊物)[C]，贵阳，2005．1．
[2]李红阳，牛树银，王立峰等，幔柱构造[M]，北京，地震出版社，2002
[3]牛数银，孙爱群，邵振国等，地幔热柱多级演化及其成矿作用[M]，北京，地震社，2001
[4]邓晋福，赵海玲，莫宣学等，中国大陆根-柱构造——大陆动力学的钥匙[M]，北京，地质出版社，1996
[5]侯增谦，卢记仁、李红阳，中国西南特提斯构造演化-幔柱构造控制[J]，地球学报，1996，17(4)：439-453
[6]卢记仁，峨眉地幔热柱的动力学特征[J]，地球学报，1996，17(4)：424-438
[7]徐义刚，种孙霖，峨眉山大火成岩省：地幔柱活动的证据及其熔融条件[J]，地球化学，2001，30(1)：1-9
[8]高振敏，张乾，陶琰等，峨眉山地幔柱成矿作用分析[J]，矿物学报，2004，24 (2)：99-104
[9] Pirajno F., Ore Deposits and Mantle Plumes[M]. Dordrecht , Neth: Kluwer Acad , 2000
[10] Anderson D.L., Hotspots, basalts and the evolution of the mantle[J], Science, 1981, 213:82-89
[11] Hill R. I. .Campbell, I. H., and Griffiths, R.W., Plume tectonics and the development of stable continental crust[J], Explor. Geophys. 1991,22:185-188
[12] Coffin M. F., Eldholm, O., Large igneous provinces:dimensions and external consequence[J], Rew, Geophys.,1994,32:1-36
[13] Amdt N.T.,Czamanske,GK.,Wooden,J.L.,And Fedorenko ,V.A., mantle and crustal contributions to continental flood basalt volcanism[J], Tectonophys.,1993,223:39-52
[14]罗祖虞，滇黔桂金三角金矿地质[M]，昆明，云南民族出版社，1993
[15]李文亢，黔西南微细粒金矿床地质特征及成矿作用，中国金矿主要类型区域成矿条件文集(6)[M]，北京，地质出版社，1989
[16]刘东升，我国卡林型金矿床的地质特征及找矿方向[J]，地质与勘探，1987．第1 期
[17]万兵，滇黔桂金三角区金(银)矿床地质特征及成矿条件[J]，矿产与地质，5 (3)
[18]李存登，黔西南区微细金矿地质特征及成因[J]，矿床地质，1987，6(3)
[19]程代全，以细屑岩为容矿层金矿的成矿条件及矿床模式探讨[J]，贵州地质，1992，第4期
[20]倪师军，刘显凡，金景福等，滇黔桂三角区微细粒浸染型金矿成矿流体地球化学[M]，成都，成都科技大学出版社，1997
[21]谭运金，滇黔桂地区微细粒浸染型金矿床的矿床地球化学类型[J]，矿床地质，1994，(4)：308-321
[22]涂光炽，我国原生金矿类型的划分和不同类型金矿的远景剖析[J]，矿产与地质，1990，4(1)：1-10
[23]涂光炽，西南秦岭与西南贵州铀金成矿带及其与美国西部卡林型金矿的类似性[J]，铀矿地质，1990，6(6)：321-325
[24]涂光炽，超大型矿床的探寻与研究的若干进展[J]，地学前缘，1994，(3)
[25]涂光炽，贵金属找矿的若干问题讨论，见：陈毓川主编，当代矿产资源勘查评价的理论与方法[M]，北京：地震出版社，1999，
[26]徐义刚，地幔柱构造、大火成岩省及其地质效应[J]，地学前缘，2002，9(4)：341-352
[27]徐义刚，钟孙霖，峨眉山大火成岩省：地幔柱活动的证据及其熔融条件[J]，地球化学，2001，30(1)：1-9
[28]Chung SL, Jahn BM. Plume-lithosphrer interaction in generation of the Emeishan flood basalts at the Permina-triassic boundary[J], Geology, 1995,23:889-892
[29]卢记仁，峨眉地幔热柱的动力学特征[J]，地球学报，1996，17(4)：424-438
[30]宋谢炎，侯增谦，汪云亮等，峨眉山玄武岩的地幔热柱成因[J]，矿物岩石，2002，22(4)：27-32
[31] XU Y G, Chung SL, JahnBM, et al. Petrological and geochemical constraints on the??petrogenesis of the Permo-Triassic Emeishan flood basalts in southwestern China Lithos[J], 2001,58:145-168
[32] Zhou MF, Malpas J, Song X Y , et al. Atemporal link between the Emeishan large igneous province(SW China) and the end-guadalupian mass extinction[J] , Earth Planet Sci Lett, 2002,196:113-122
[33]汪云亮，侯增谦，修淑芝等，峨眉火成岩省地幔柱热异常初探[J]，地质论评1999，45(增刊)：876-879
[34]王登红，地幔柱及其成矿作用[M]，北京：地震出版社，1998
[35]徐义刚，梅厚钧，许继峰等，峨眉山大火成岩省中两类岩浆分异趋势及其成因[J]，科学通报，2003，48(4)：383-387
[36] Wilson, J.T., A possible origin of the Hawaiian islands[J], Can. J. Phys., 1963,41:863-870
[37] Wilson, J. T., Evidence from ocean islands suggesting movement in the earth, In "symposium on continental drift" [J], Phil. Trans.R. Soc. Lond., 1965,258:145-167
[38] Morgan W.J. Deep mantle convection plumes and plate motions[J]. Amer. Assoc. Petro.Geol.Bull., 1972,56:203-213
[39] Morgan,W.J., Convection plumes in the lower mantle[J], Nature,1971,230: 42-43
[40] Wilson, J. T.,Mantle plumes and plate motions[J], Tectonophysics, 1973, 19:149-164
[41] Maruyama,S. ,Plume tectonics[J], Jour. Geol. Soc. Japan, 1994,100(1): 24-49
[42]罗定国 地幔喷流柱构造和地球动力学新模式[J]，国外地质科技，1994，(5)：1-10
[43]王登红 热点研究评述[J]，地质科技情报，1995，14(1)：9-15
[44]邓晋福，莫宣学，赵海岭等，中国东部岩石圈根／去根作用与大陆“活化”[J]，现代地质，1994，8：349-356
[45]牛树银，罗殿文，叶东虎等，幔枝构造及其成矿规律[M]，北京地质出版社，1996
[46]王登红，地幔柱的概念、分类、演化与大规模成矿——对中国西南部的探讨[J]，地学前缘，2001，8(3)67-72
[47]李红阳，侯增谦 初论幔柱构造成矿体系[J]，矿床地质，1998，17(3)：247-255
[48] Chung S L, Jahn BM , W u G Y, Lo CH, Cong B L. 1998. The Emeishan flood basalt in WS China[C]: a mantle plume lnitration model and its connection with continental breakup and mass extinction at the Permian 桾riassic boundary Mantle Dynamics and PLate Interactions in East Asia Geodynamics. 27: 47-58
[49]Le Roex A. Chlf R A. Adair B J I. 1990. Trisan de Cunha, South Aylantic: geochemistry and petrogenesis of a basanite-phonulite lava series [J]. Petrol , 31: 779-812
[50] Cliff R A, Baker PE, MateerNJ, 1991 Geochemistry of inaccessible island volcanics[J], Chem.Geol,92 251-260
[51] Hemond C.Devey C W, Chauvel C. 1994. Source compositions and melting processes in the Society and Austral plumes (South Pacific Ocean): element and isotope (Sr. Nd. Pb. Th) geochemistry[J]. Chem Geol , 115. 7-45
[52] Weaver B I . 1991 The origin of ocean lsland basalt end-trmber composition: trace element and isotopic constrains Earth Planet[J]. Sci Lett , 104:381-397.
[53] Chauvel et al. 1992. HIMU-EM : The French Polynesian connection Earth and Planet[J]. Lett. 110: 99-119
[54]宋书炎，侯增谦，曹志敏等，峨眉大火成岩省的岩石地球化学特征及时限[J]，地质学报，2001，75(4)：498-506
[55]牛树银，孙爱群，深源流体与地幔热柱的成矿控制作用探讨，现代矿产资源评价的理论方法与应用[M]，北京，地震出版社，1998
[56]牟保磊，元素地球化学[M]，北京，北京大学出版社，1999
[57] Kaneoka I., Takaoka N. Noble-gas state in the earth's interior: some constrains on the present state[J],Chem Geol, 1985, 52:75-95
[58]刘丛强，黄智龙，许成等，地幔流体及其成矿作用——以四川冕宁稀土矿床为例[M]，北京，地质出版社，2004
[59]肖荣阁，云南中新生代地质与矿产[M]，北京，海洋出版社，1993
[60]苏文超，胡瑞忠，漆亮等，黔西南卡林型金矿床流体包裹体中微量元素研究[J]，地球化学，2001，30(6)：512-516
[61]王平安，秦岭造山带区域矿床成矿系列、构造-成矿旋回与演化[M]，北京，地质出版社，1998
[62]沈阳地质矿产研究所编，中国金矿主要类型区域成矿条件文集6，黔西南地区[M]，地质出版社，1989
[63]高振敏，李红阳，杨竹森等，滇黔地区主要类型金矿的成矿与找矿[M]，北京，地质出版社，2002
[64]王砚耕，索书田，张明发等，黔西南构造与卡林型金矿[M]，北京，地质出版社，1994
[65]贵州省地质矿产局，贵州省区域地质志[M]，北京，地质出版社，1987
[66]王砚耕，黔西南及邻区赋金层序及沉积环境[J]，岩相古地理，1990，(6)
[67]汪云亮，中国西南二叠系玄武岩微量元素地球化学和岩浆起源模式研究[J]，地球科学进展，1991，6(6)：87
[68]杨世瑜，王瑞学，矿床遥感地质问题[M]，昆明，云南大学出版社，2003
[69]毛德明，张启厚，安树仁著，贵州西部峨眉山玄武岩及其有关矿产[M]，贵阳，贵州科技出版社，1992
[70]中国地质调查局，全国主要成矿远景区矿产资源调查评价重点选区研究(10)[C]，2003
[71]韩至钧，王砚耕，冯济舟等，黔西南金矿地质与勘查[M]，贵阳，贵州科技出版社，1999
[72]冯学仕，王尚彦，贵州省区域矿床成矿系列与成矿规律[M]，北京，地质出版社，2004
[73]王砚耕，王立亭，张明发等，南盘江地区浅层地壳结构与金矿分布模式[J]，贵州地质，1995，12(2)：91-183．
[74]陈凯礼，广西金矿地质[M]，南宁，广西科技出版社，2002．
[75]贵州省地质矿产局，贵州省区域矿产志[M]，北京，地质出版社，1987
[76]何立贤，曾若兰，林立青等，汞矿带中金矿赋存规律，沈阳地质矿产研究所编，中国金矿主要类型金矿找矿方法文集[M]，北京，地质出版社，1994
[77]刘建中，贵州灰家堡金矿田Au／Ag比值特征及找矿意义[J]，贵州地质，1999，16(2)：97-102
[78]付绍洪，顾学祥，王乾等，黔西南水银洞金矿床载金黄铁矿标型特征[J]，矿??物学报，2004，24(1)：76-80
[79]刘建中，贵州水银洞金矿床矿石特征及金的赋存状态[J]，贵州地质，2003，20(1)：30-34
[80]罗孝桓，贵州贞丰烂泥沟金矿床地质特征、成矿机理及找矿，中国卡林型微细浸染型金矿床[M]，南京，南京大学出版社，1994
[81]罗孝桓，断裂构造的几何学运动学特征及其金矿体就位的控制研究[J]，贵州地质，1997，50
[82]Hugh R．Rollison著，杨学明，杨晓勇，陈双喜译，岩石地球化学[M]，中国科学技术大学出版社，2000
[83]陈豫，刘秀成，张启厚，贵州晴隆大厂锑矿床成因探讨[J]，矿床地质，1984，3(3)：1-12
[84]何立贤，曾若兰，林立青，贵州金矿地质[M]，北京，地质出版社，1993
[85]严钧平，刘平，贵州汞矿地质[M]，北京，地质出版社，1989
[86]刘平，我国主要汞矿床的辰砂硫同位素组成[J]，矿床地质，1992，11(3)：213-220
[87]陈代演，滇东黔西主要层控锑汞矿床稳定同位素研究[J]，贵州地质，1991，8(3)：227-240
[88]2000年中国科学院地球化学研究所年鉴[M]，北京，科学出版社，2001
[89] NIE Aiguo. XIE Hong. A study on Emei mantle plume activity and the origin of high-As coal in southwestern Guizhou Province[J], Chinese Journal of GEOCHEMISTRY. 2006, 25 (3): 238-244
[90]涂光炽，低温地球化学[M]，北京，科学出版社，1998
[91]陈景河，葛广福，黔西南上二叠龙潭组层控卡林型金矿床的成因及与玄武质沉凝灰岩的关系[J]，黄金地质，2004，25(增刊)：19-24
[92] Rona P A. Hydrothermal processes at seafloor spriading centers[M] .N. Y. Plenum Press ,1983.
[93] Rona P A. Hydrothermal mineralization at oceanic ridges [J]. TheCanadian Mineralogist -Seafloor hydrothermal mineralization, 1988 ,26(3): 431 - 466.
[94] Rona P A ,Scott S D. A special issue of seafloorhy drothermalmineralization: new??perspective [J]. Economic Geology, 1993 , 88(8): 1935 - 2078.
[95] Edmond J M, Von Damm KL, McDuff R E. Chemistry of hot springon the East Pacific Rise and their effluent dispersal [J]. Nature , 1982 ,279 (5863): 187-191.
[96]王涛，刘淑文，隗合明等，热水沉积矿床研究的现状与趋势[J]，地球科学与环境学报，2004，26(4)：6-10
[97] Harry H R, Robert S C. Evidence of episodic fluid, gas, andsediment venting on the Northern Gulf of Mexico continental slope[J] .Economic Geology, 1997 ,98 : 863 - 879
[98]薛春纪，祁思敬，郑明华等，热水沉积研究及相关科学问题[J]，矿物岩石地球化学同通报，2000，19(3)：155-163
[99]陈先沛，陈多福，李英等，热水沉积作用与超大型矿床，中国超大型矿床(Ⅰ)[M]，北京，科学出版社，2000
[100] Spry P G. Geochemistry and origin of coticules (spessartine-quartzrocks) associated with metamorphosed massive sulfide deposits [A] .In : Spry P G, Bryndzia L T, eds. Regional Metamorphism of Ore Deposits and Genetic Implications[C]. Holland: VSP. 1990
[101]路远发，陈开旭，战明国，羊拉地区含矿矽卡岩成因的地球化学证据[J]，地球科学，1999，24(3)：298-303
[102] Marching V. Some geochemical indication for determination between diagenetic and hydrothermal metalliferous sediments[J]. MarineGeol ,1982, 50(3): 241-256
[103]周永章，广西丹池盆地热水成因硅质岩地球化学特征[J]，沉积学报，1990，8(3)：75-83
[104]赵一阳，鄢明才，冲绳海槽海底沉积物汞异常-现代海底热水效应的“指示剂”[J]，地球化学，1994，23(2)：132-139
[105] Davidson C J, Hydrothermal geochemistry and ore genesis of sea floor volcanogenic copper bearing oxide ores[J], Econ Geol, 1992, 87(3):889-912
[106]徐跃通，尚树川，张邦花，浙江西裘铜块状硫化物矿床火山-热泉沉积成矿的地质地球化学证据[J]，地球化学，2000，29(1)：14-20
[107]杨振强，陈开旭，翟丽娜，生物成矿和热水成矿中碳来源的同位素示踪[J]，??华南地质与矿产，1999，2期：59-65
[108]张复新，喷流岩及其识别与找矿[J]，地质科技情报，1988，7(3)：67-73．
[109]薛春纪，热水沉积岩及识别标志，中国科学院矿床地球化学开放研究实验，矿床地质和矿床地球化学研究新进展[M]，兰州：兰州大学出版社，1990
[110]陈先沛，高计元，陈多福，热水沉积作用的概念和几个岩石学标志[J]，沉积学报，1992，10(3)：124-132
[111]薛春纪，马国良，秦岭泥盆纪热水沉积环境和海底热液沉积岩[J]，矿物岩石地球化学通讯，1991，(1)：46-55
[112]薛春纪，秦岭泥盆纪热水沉积[M]，西安，西安地图出版社，1997
[113]Wolf K H，层控矿床与层状矿床[M]，北京，地质出版社，1986
[114]A．J．博伊斯，爱尔兰早石炭世的快速沉降和有色金属矿化作用[J]，国外地质科技，1985，(8)：52-64
[115]薛春纪，祁思敬，南秦岭泥盆纪同生热水沉积环境的沉积学及地球化学信息[J]，西北地质，1995，16(4)：325-332
[116]涂光炽，王秀璋，陈先沛等，中国层控矿床地球化学(第三卷)[M]，北京，科学出版社，1988
[117]中国科学院黄金科技工作领导小组办公室，中国金矿研究新进展(第一卷，上卷)[M]，北京，地震出版社，1994
[118]A．M．彼列尔曼，后生地球化学[M]，北京，科学出版社，1975
[119]冉启洋，杨忠贵，兴仁县紫木凼金矿外围地区基岩含金量与地层、岩石和沉积相的关系[J]，贵州地质，1995，12(3)：208-213
[120]陈文一，刘家仁，王中刚等，贵州峨眉山玄武岩喷发期的岩相古地理研究[J]，古地理学报，2003，5(1)：17-28
[121]郭振春，贵州紫木凼金矿床地质特征及勘查实践，中国卡林型微细浸染型金矿[M]，南京，南京大学出版社，1994
[122]田毓龙，秦德先，林幼斌等，喷流热水沉积矿床研究的现状与进展[J]，昆明理工大学学报，1999，24(1)：150-156
[123]曾允孚，夏文杰，沉积岩石学[M]，北京，地质出版社，1986
[124]韩宝平，微观喀斯特机理研究[M]，北京，地质出版社，1998
[125]刘英俊，马东升，金的地球化学[M]，北京，科学出版社，1991
[126]林清，刘德汉，黔西南金矿有机质地球化学研究[J]，地球化学，1995，24(4)：402-408
[127]藤吉文，地球深部物质和能量交汇的动力过程与矿产资源的形成[J]，大地构造与成矿学，27(1)：3-21
[128]王登红，陈振宇，李建康，中新生代以来地幔柱活动的全球响应，中国大陆地球深部结构与动力学研究[M]，北京，科学出版社，2004
[129]黄智龙，陈进，韩润生等，云南会泽超大型铅锌矿床地球化学及成因——兼论峨眉山玄武岩与铅锌成矿的关系[M]，北京，地质出版社，2004
[130]藤吉文，世纪之交的国际地质盛会[J]，科学，1996，48(6)：18-20
[131]邓晋福，赵海玲，吴宗絮等，中国北方大陆下的地幔热柱与岩石圈运动[J]，现代地质，1992，16(3)：267-273
[132]涂光炽，霍明远，金的经济地质学[M]，北京，科学出版社，1991
[133]牛数银，李红阳，孙爱群等，幔枝构造理论与找矿实践[M]，北京，地震出版社，2002
[134]刘英俊，马东升，金的地球化学[M]，北京，科学出版社，1991
[135]R．W．博伊尔，金的地球化学及金矿床[M]，北京，地质出版社，1984
[136]冯少南，东吴运动的新认[J]识，现代地质，1991，5(4)：378-384
[137]秦德先，燕永峰，林幼斌等，程海断裂带玄武岩及其成矿[J]，岩土工程界，1999，6期
[138]毛德明，张启厚，安树仁，贵州西部峨眉山玄武岩及其有关矿产[M]，贵阳，贵州科技出版社，1992
[139]聂爱国，黄志勇，谢宏，黔西南地区高砷煤与金矿的成因研究[J]，湖南科技大学学报，2006，21(3)：21-25
[140]郭振春，黔西南金矿的构造控制作用探讨[J]，贵州地质，1993，34
[141]罗孝桓，烂泥沟金矿区F_3控矿断裂特征及构造成矿作用机理探讨[J]，贵州地质，1993，34
[142]陈俊华，戈塘金矿床地质特征及成矿条件，中国卡林型微细浸染型金矿[M]，南京，南京大学出版社，1994
[143] C.GCunningham et. al., Newly discovered sedimentary rock-hosted disseminated gold deposits in the People's Republic of China[J]. Economic Geology 1988,Vol.83, P: 1462-1467
[144]侯宗林，杨庆德，滇黔桂地区微细浸染型金矿成矿条件及成矿模式[J]，地质找矿论丛，1989，4(3)：1-13
[145]李九玲，微细浸染型(卡林型)金矿成矿过程中的碳和有机质的作用[J]，矿床地质，1996，15(3)
[146] B.R.Berger and W.C.Bagby ,The geology and Origin of Carlin-type gold deposits[J],Gold Metallogeny and Exploration ,Foster R.P.Blackie,1991,P:432
[147] M.B.Woitsekhowskaya and S.G Peters, Geochemical modeling of alteration and gold depositon at the Betze Depsit, Eureka County, Nevada[J], Carlin-type Gold Deposit, 1998,211-221.
[148] Fernando Henrique Bucco Tallarico, Claudio Rodrigues Coimbra and Carlos Henrique Cravo Costa, The Serra Leste sediment-hosted Au-(Pd-Pt) mineralization, Carajas Province[J], Revista Brusileira de Geocieneias, 2000,30(2): 226-229
[149]何立贤，黔西南金矿“热、液、矿”同源成矿模式，贵州地质[J]，1996
[150]曹鸿水黔西南“大厂层”形成环境及其成矿作用的探讨[J] 贵州地质 1991，8(1)：5-12
[151] Nan Junya, Liu Congqiang , Zhou Dequan, Wang Zhuming Ree geochemical study of the Permian-Triassic marine sedimentary environment in GuiZhou province[J] Chinese Journal of Geochemistry 2002,21(4): 348 -361
[152]王立亭，中国南方二叠纪岩相古地理与成矿作用[M]，北京，地质出版社，1994
[153]刘宝君，黔西南中三叠世陆棚-斜坡沉积特征[J]，沉积学报，1987，5(2)
[154]聂爱国，谢宏 峨眉山玄武岩浆与贵州高砷煤成因研究[J]，煤田地质与勘探
[2]李红阳，牛树银，王立峰等，幔柱构造[M]，北京，地震出版社，2002
[3]牛数银，孙爱群，邵振国等，地幔热柱多级演化及其成矿作用[M]，北京，地震社，2001
[4]邓晋福，赵海玲，莫宣学等，中国大陆根-柱构造——大陆动力学的钥匙[M]，北京，地质出版社，1996
[5]侯增谦，卢记仁、李红阳，中国西南特提斯构造演化-幔柱构造控制[J]，地球学报，1996，17(4)：439-453
[6]卢记仁，峨眉地幔热柱的动力学特征[J]，地球学报，1996，17(4)：424-438
[7]徐义刚，种孙霖，峨眉山大火成岩省：地幔柱活动的证据及其熔融条件[J]，地球化学，2001，30(1)：1-9
[8]高振敏，张乾，陶琰等，峨眉山地幔柱成矿作用分析[J]，矿物学报，2004，24 (2)：99-104
[9] Pirajno F., Ore Deposits and Mantle Plumes[M]. Dordrecht , Neth: Kluwer Acad , 2000
[10] Anderson D.L., Hotspots, basalts and the evolution of the mantle[J], Science, 1981, 213:82-89
[11] Hill R. I. .Campbell, I. H., and Griffiths, R.W., Plume tectonics and the development of stable continental crust[J], Explor. Geophys. 1991,22:185-188
[12] Coffin M. F., Eldholm, O., Large igneous provinces:dimensions and external consequence[J], Rew, Geophys.,1994,32:1-36
[13] Amdt N.T.,Czamanske,GK.,Wooden,J.L.,And Fedorenko ,V.A., mantle and crustal contributions to continental flood basalt volcanism[J], Tectonophys.,1993,223:39-52
[14]罗祖虞，滇黔桂金三角金矿地质[M]，昆明，云南民族出版社，1993
[15]李文亢，黔西南微细粒金矿床地质特征及成矿作用，中国金矿主要类型区域成矿条件文集(6)[M]，北京，地质出版社，1989
[16]刘东升，我国卡林型金矿床的地质特征及找矿方向[J]，地质与勘探，1987．第1 期
[17]万兵，滇黔桂金三角区金(银)矿床地质特征及成矿条件[J]，矿产与地质，5 (3)
[18]李存登，黔西南区微细金矿地质特征及成因[J]，矿床地质，1987，6(3)
[19]程代全，以细屑岩为容矿层金矿的成矿条件及矿床模式探讨[J]，贵州地质，1992，第4期
[20]倪师军，刘显凡，金景福等，滇黔桂三角区微细粒浸染型金矿成矿流体地球化学[M]，成都，成都科技大学出版社，1997
[21]谭运金，滇黔桂地区微细粒浸染型金矿床的矿床地球化学类型[J]，矿床地质，1994，(4)：308-321
[22]涂光炽，我国原生金矿类型的划分和不同类型金矿的远景剖析[J]，矿产与地质，1990，4(1)：1-10
[23]涂光炽，西南秦岭与西南贵州铀金成矿带及其与美国西部卡林型金矿的类似性[J]，铀矿地质，1990，6(6)：321-325
[24]涂光炽，超大型矿床的探寻与研究的若干进展[J]，地学前缘，1994，(3)
[25]涂光炽，贵金属找矿的若干问题讨论，见：陈毓川主编，当代矿产资源勘查评价的理论与方法[M]，北京：地震出版社，1999，
[26]徐义刚，地幔柱构造、大火成岩省及其地质效应[J]，地学前缘，2002，9(4)：341-352
[27]徐义刚，钟孙霖，峨眉山大火成岩省：地幔柱活动的证据及其熔融条件[J]，地球化学，2001，30(1)：1-9
[28]Chung SL, Jahn BM. Plume-lithosphrer interaction in generation of the Emeishan flood basalts at the Permina-triassic boundary[J], Geology, 1995,23:889-892
[29]卢记仁，峨眉地幔热柱的动力学特征[J]，地球学报，1996，17(4)：424-438
[30]宋谢炎，侯增谦，汪云亮等，峨眉山玄武岩的地幔热柱成因[J]，矿物岩石，2002，22(4)：27-32
[31] XU Y G, Chung SL, JahnBM, et al. Petrological and geochemical constraints on the??petrogenesis of the Permo-Triassic Emeishan flood basalts in southwestern China Lithos[J], 2001,58:145-168
[32] Zhou MF, Malpas J, Song X Y , et al. Atemporal link between the Emeishan large igneous province(SW China) and the end-guadalupian mass extinction[J] , Earth Planet Sci Lett, 2002,196:113-122
[33]汪云亮，侯增谦，修淑芝等，峨眉火成岩省地幔柱热异常初探[J]，地质论评1999，45(增刊)：876-879
[34]王登红，地幔柱及其成矿作用[M]，北京：地震出版社，1998
[35]徐义刚，梅厚钧，许继峰等，峨眉山大火成岩省中两类岩浆分异趋势及其成因[J]，科学通报，2003，48(4)：383-387
[36] Wilson, J.T., A possible origin of the Hawaiian islands[J], Can. J. Phys., 1963,41:863-870
[37] Wilson, J. T., Evidence from ocean islands suggesting movement in the earth, In "symposium on continental drift" [J], Phil. Trans.R. Soc. Lond., 1965,258:145-167
[38] Morgan W.J. Deep mantle convection plumes and plate motions[J]. Amer. Assoc. Petro.Geol.Bull., 1972,56:203-213
[39] Morgan,W.J., Convection plumes in the lower mantle[J], Nature,1971,230: 42-43
[40] Wilson, J. T.,Mantle plumes and plate motions[J], Tectonophysics, 1973, 19:149-164
[41] Maruyama,S. ,Plume tectonics[J], Jour. Geol. Soc. Japan, 1994,100(1): 24-49
[42]罗定国 地幔喷流柱构造和地球动力学新模式[J]，国外地质科技，1994，(5)：1-10
[43]王登红 热点研究评述[J]，地质科技情报，1995，14(1)：9-15
[44]邓晋福，莫宣学，赵海岭等，中国东部岩石圈根／去根作用与大陆“活化”[J]，现代地质，1994，8：349-356
[45]牛树银，罗殿文，叶东虎等，幔枝构造及其成矿规律[M]，北京地质出版社，1996
[46]王登红，地幔柱的概念、分类、演化与大规模成矿——对中国西南部的探讨[J]，地学前缘，2001，8(3)67-72
[47]李红阳，侯增谦 初论幔柱构造成矿体系[J]，矿床地质，1998，17(3)：247-255
[48] Chung S L, Jahn BM , W u G Y, Lo CH, Cong B L. 1998. The Emeishan flood basalt in WS China[C]: a mantle plume lnitration model and its connection with continental breakup and mass extinction at the Permian 桾riassic boundary Mantle Dynamics and PLate Interactions in East Asia Geodynamics. 27: 47-58
[49]Le Roex A. Chlf R A. Adair B J I. 1990. Trisan de Cunha, South Aylantic: geochemistry and petrogenesis of a basanite-phonulite lava series [J]. Petrol , 31: 779-812
[50] Cliff R A, Baker PE, MateerNJ, 1991 Geochemistry of inaccessible island volcanics[J], Chem.Geol,92 251-260
[51] Hemond C.Devey C W, Chauvel C. 1994. Source compositions and melting processes in the Society and Austral plumes (South Pacific Ocean): element and isotope (Sr. Nd. Pb. Th) geochemistry[J]. Chem Geol , 115. 7-45
[52] Weaver B I . 1991 The origin of ocean lsland basalt end-trmber composition: trace element and isotopic constrains Earth Planet[J]. Sci Lett , 104:381-397.
[53] Chauvel et al. 1992. HIMU-EM : The French Polynesian connection Earth and Planet[J]. Lett. 110: 99-119
[54]宋书炎，侯增谦，曹志敏等，峨眉大火成岩省的岩石地球化学特征及时限[J]，地质学报，2001，75(4)：498-506
[55]牛树银，孙爱群，深源流体与地幔热柱的成矿控制作用探讨，现代矿产资源评价的理论方法与应用[M]，北京，地震出版社，1998
[56]牟保磊，元素地球化学[M]，北京，北京大学出版社，1999
[57] Kaneoka I., Takaoka N. Noble-gas state in the earth's interior: some constrains on the present state[J],Chem Geol, 1985, 52:75-95
[58]刘丛强，黄智龙，许成等，地幔流体及其成矿作用——以四川冕宁稀土矿床为例[M]，北京，地质出版社，2004
[59]肖荣阁，云南中新生代地质与矿产[M]，北京，海洋出版社，1993
[60]苏文超，胡瑞忠，漆亮等，黔西南卡林型金矿床流体包裹体中微量元素研究[J]，地球化学，2001，30(6)：512-516
[61]王平安，秦岭造山带区域矿床成矿系列、构造-成矿旋回与演化[M]，北京，地质出版社，1998
[62]沈阳地质矿产研究所编，中国金矿主要类型区域成矿条件文集6，黔西南地区[M]，地质出版社，1989
[63]高振敏，李红阳，杨竹森等，滇黔地区主要类型金矿的成矿与找矿[M]，北京，地质出版社，2002
[64]王砚耕，索书田，张明发等，黔西南构造与卡林型金矿[M]，北京，地质出版社，1994
[65]贵州省地质矿产局，贵州省区域地质志[M]，北京，地质出版社，1987
[66]王砚耕，黔西南及邻区赋金层序及沉积环境[J]，岩相古地理，1990，(6)
[67]汪云亮，中国西南二叠系玄武岩微量元素地球化学和岩浆起源模式研究[J]，地球科学进展，1991，6(6)：87
[68]杨世瑜，王瑞学，矿床遥感地质问题[M]，昆明，云南大学出版社，2003
[69]毛德明，张启厚，安树仁著，贵州西部峨眉山玄武岩及其有关矿产[M]，贵阳，贵州科技出版社，1992
[70]中国地质调查局，全国主要成矿远景区矿产资源调查评价重点选区研究(10)[C]，2003
[71]韩至钧，王砚耕，冯济舟等，黔西南金矿地质与勘查[M]，贵阳，贵州科技出版社，1999
[72]冯学仕，王尚彦，贵州省区域矿床成矿系列与成矿规律[M]，北京，地质出版社，2004
[73]王砚耕，王立亭，张明发等，南盘江地区浅层地壳结构与金矿分布模式[J]，贵州地质，1995，12(2)：91-183．
[74]陈凯礼，广西金矿地质[M]，南宁，广西科技出版社，2002．
[75]贵州省地质矿产局，贵州省区域矿产志[M]，北京，地质出版社，1987
[76]何立贤，曾若兰，林立青等，汞矿带中金矿赋存规律，沈阳地质矿产研究所编，中国金矿主要类型金矿找矿方法文集[M]，北京，地质出版社，1994
[77]刘建中，贵州灰家堡金矿田Au／Ag比值特征及找矿意义[J]，贵州地质，1999，16(2)：97-102
[78]付绍洪，顾学祥，王乾等，黔西南水银洞金矿床载金黄铁矿标型特征[J]，矿??物学报，2004，24(1)：76-80
[79]刘建中，贵州水银洞金矿床矿石特征及金的赋存状态[J]，贵州地质，2003，20(1)：30-34
[80]罗孝桓，贵州贞丰烂泥沟金矿床地质特征、成矿机理及找矿，中国卡林型微细浸染型金矿床[M]，南京，南京大学出版社，1994
[81]罗孝桓，断裂构造的几何学运动学特征及其金矿体就位的控制研究[J]，贵州地质，1997，50
[82]Hugh R．Rollison著，杨学明，杨晓勇，陈双喜译，岩石地球化学[M]，中国科学技术大学出版社，2000
[83]陈豫，刘秀成，张启厚，贵州晴隆大厂锑矿床成因探讨[J]，矿床地质，1984，3(3)：1-12
[84]何立贤，曾若兰，林立青，贵州金矿地质[M]，北京，地质出版社，1993
[85]严钧平，刘平，贵州汞矿地质[M]，北京，地质出版社，1989
[86]刘平，我国主要汞矿床的辰砂硫同位素组成[J]，矿床地质，1992，11(3)：213-220
[87]陈代演，滇东黔西主要层控锑汞矿床稳定同位素研究[J]，贵州地质，1991，8(3)：227-240
[88]2000年中国科学院地球化学研究所年鉴[M]，北京，科学出版社，2001
[89] NIE Aiguo. XIE Hong. A study on Emei mantle plume activity and the origin of high-As coal in southwestern Guizhou Province[J], Chinese Journal of GEOCHEMISTRY. 2006, 25 (3): 238-244
[90]涂光炽，低温地球化学[M]，北京，科学出版社，1998
[91]陈景河，葛广福，黔西南上二叠龙潭组层控卡林型金矿床的成因及与玄武质沉凝灰岩的关系[J]，黄金地质，2004，25(增刊)：19-24
[92] Rona P A. Hydrothermal processes at seafloor spriading centers[M] .N. Y. Plenum Press ,1983.
[93] Rona P A. Hydrothermal mineralization at oceanic ridges [J]. TheCanadian Mineralogist -Seafloor hydrothermal mineralization, 1988 ,26(3): 431 - 466.
[94] Rona P A ,Scott S D. A special issue of seafloorhy drothermalmineralization: new??perspective [J]. Economic Geology, 1993 , 88(8): 1935 - 2078.
[95] Edmond J M, Von Damm KL, McDuff R E. Chemistry of hot springon the East Pacific Rise and their effluent dispersal [J]. Nature , 1982 ,279 (5863): 187-191.
[96]王涛，刘淑文，隗合明等，热水沉积矿床研究的现状与趋势[J]，地球科学与环境学报，2004，26(4)：6-10
[97] Harry H R, Robert S C. Evidence of episodic fluid, gas, andsediment venting on the Northern Gulf of Mexico continental slope[J] .Economic Geology, 1997 ,98 : 863 - 879
[98]薛春纪，祁思敬，郑明华等，热水沉积研究及相关科学问题[J]，矿物岩石地球化学同通报，2000，19(3)：155-163
[99]陈先沛，陈多福，李英等，热水沉积作用与超大型矿床，中国超大型矿床(Ⅰ)[M]，北京，科学出版社，2000
[100] Spry P G. Geochemistry and origin of coticules (spessartine-quartzrocks) associated with metamorphosed massive sulfide deposits [A] .In : Spry P G, Bryndzia L T, eds. Regional Metamorphism of Ore Deposits and Genetic Implications[C]. Holland: VSP. 1990
[101]路远发，陈开旭，战明国，羊拉地区含矿矽卡岩成因的地球化学证据[J]，地球科学，1999，24(3)：298-303
[102] Marching V. Some geochemical indication for determination between diagenetic and hydrothermal metalliferous sediments[J]. MarineGeol ,1982, 50(3): 241-256
[103]周永章，广西丹池盆地热水成因硅质岩地球化学特征[J]，沉积学报，1990，8(3)：75-83
[104]赵一阳，鄢明才，冲绳海槽海底沉积物汞异常-现代海底热水效应的“指示剂”[J]，地球化学，1994，23(2)：132-139
[105] Davidson C J, Hydrothermal geochemistry and ore genesis of sea floor volcanogenic copper bearing oxide ores[J], Econ Geol, 1992, 87(3):889-912
[106]徐跃通，尚树川，张邦花，浙江西裘铜块状硫化物矿床火山-热泉沉积成矿的地质地球化学证据[J]，地球化学，2000，29(1)：14-20
[107]杨振强，陈开旭，翟丽娜，生物成矿和热水成矿中碳来源的同位素示踪[J]，??华南地质与矿产，1999，2期：59-65
[108]张复新，喷流岩及其识别与找矿[J]，地质科技情报，1988，7(3)：67-73．
[109]薛春纪，热水沉积岩及识别标志，中国科学院矿床地球化学开放研究实验，矿床地质和矿床地球化学研究新进展[M]，兰州：兰州大学出版社，1990
[110]陈先沛，高计元，陈多福，热水沉积作用的概念和几个岩石学标志[J]，沉积学报，1992，10(3)：124-132
[111]薛春纪，马国良，秦岭泥盆纪热水沉积环境和海底热液沉积岩[J]，矿物岩石地球化学通讯，1991，(1)：46-55
[112]薛春纪，秦岭泥盆纪热水沉积[M]，西安，西安地图出版社，1997
[113]Wolf K H，层控矿床与层状矿床[M]，北京，地质出版社，1986
[114]A．J．博伊斯，爱尔兰早石炭世的快速沉降和有色金属矿化作用[J]，国外地质科技，1985，(8)：52-64
[115]薛春纪，祁思敬，南秦岭泥盆纪同生热水沉积环境的沉积学及地球化学信息[J]，西北地质，1995，16(4)：325-332
[116]涂光炽，王秀璋，陈先沛等，中国层控矿床地球化学(第三卷)[M]，北京，科学出版社，1988
[117]中国科学院黄金科技工作领导小组办公室，中国金矿研究新进展(第一卷，上卷)[M]，北京，地震出版社，1994
[118]A．M．彼列尔曼，后生地球化学[M]，北京，科学出版社，1975
[119]冉启洋，杨忠贵，兴仁县紫木凼金矿外围地区基岩含金量与地层、岩石和沉积相的关系[J]，贵州地质，1995，12(3)：208-213
[120]陈文一，刘家仁，王中刚等，贵州峨眉山玄武岩喷发期的岩相古地理研究[J]，古地理学报，2003，5(1)：17-28
[121]郭振春，贵州紫木凼金矿床地质特征及勘查实践，中国卡林型微细浸染型金矿[M]，南京，南京大学出版社，1994
[122]田毓龙，秦德先，林幼斌等，喷流热水沉积矿床研究的现状与进展[J]，昆明理工大学学报，1999，24(1)：150-156
[123]曾允孚，夏文杰，沉积岩石学[M]，北京，地质出版社，1986
[124]韩宝平，微观喀斯特机理研究[M]，北京，地质出版社，1998
[125]刘英俊，马东升，金的地球化学[M]，北京，科学出版社，1991
[126]林清，刘德汉，黔西南金矿有机质地球化学研究[J]，地球化学，1995，24(4)：402-408
[127]藤吉文，地球深部物质和能量交汇的动力过程与矿产资源的形成[J]，大地构造与成矿学，27(1)：3-21
[128]王登红，陈振宇，李建康，中新生代以来地幔柱活动的全球响应，中国大陆地球深部结构与动力学研究[M]，北京，科学出版社，2004
[129]黄智龙，陈进，韩润生等，云南会泽超大型铅锌矿床地球化学及成因——兼论峨眉山玄武岩与铅锌成矿的关系[M]，北京，地质出版社，2004
[130]藤吉文，世纪之交的国际地质盛会[J]，科学，1996，48(6)：18-20
[131]邓晋福，赵海玲，吴宗絮等，中国北方大陆下的地幔热柱与岩石圈运动[J]，现代地质，1992，16(3)：267-273
[132]涂光炽，霍明远，金的经济地质学[M]，北京，科学出版社，1991
[133]牛数银，李红阳，孙爱群等，幔枝构造理论与找矿实践[M]，北京，地震出版社，2002
[134]刘英俊，马东升，金的地球化学[M]，北京，科学出版社，1991
[135]R．W．博伊尔，金的地球化学及金矿床[M]，北京，地质出版社，1984
[136]冯少南，东吴运动的新认[J]识，现代地质，1991，5(4)：378-384
[137]秦德先，燕永峰，林幼斌等，程海断裂带玄武岩及其成矿[J]，岩土工程界，1999，6期
[138]毛德明，张启厚，安树仁，贵州西部峨眉山玄武岩及其有关矿产[M]，贵阳，贵州科技出版社，1992
[139]聂爱国，黄志勇，谢宏，黔西南地区高砷煤与金矿的成因研究[J]，湖南科技大学学报，2006，21(3)：21-25
[140]郭振春，黔西南金矿的构造控制作用探讨[J]，贵州地质，1993，34
[141]罗孝桓，烂泥沟金矿区F_3控矿断裂特征及构造成矿作用机理探讨[J]，贵州地质，1993，34
[142]陈俊华，戈塘金矿床地质特征及成矿条件，中国卡林型微细浸染型金矿[M]，南京，南京大学出版社，1994
[143] C.GCunningham et. al., Newly discovered sedimentary rock-hosted disseminated gold deposits in the People's Republic of China[J]. Economic Geology 1988,Vol.83, P: 1462-1467
[144]侯宗林，杨庆德，滇黔桂地区微细浸染型金矿成矿条件及成矿模式[J]，地质找矿论丛，1989，4(3)：1-13
[145]李九玲，微细浸染型(卡林型)金矿成矿过程中的碳和有机质的作用[J]，矿床地质，1996，15(3)
[146] B.R.Berger and W.C.Bagby ,The geology and Origin of Carlin-type gold deposits[J],Gold Metallogeny and Exploration ,Foster R.P.Blackie,1991,P:432
[147] M.B.Woitsekhowskaya and S.G Peters, Geochemical modeling of alteration and gold depositon at the Betze Depsit, Eureka County, Nevada[J], Carlin-type Gold Deposit, 1998,211-221.
[148] Fernando Henrique Bucco Tallarico, Claudio Rodrigues Coimbra and Carlos Henrique Cravo Costa, The Serra Leste sediment-hosted Au-(Pd-Pt) mineralization, Carajas Province[J], Revista Brusileira de Geocieneias, 2000,30(2): 226-229
[149]何立贤，黔西南金矿“热、液、矿”同源成矿模式，贵州地质[J]，1996
[150]曹鸿水黔西南“大厂层”形成环境及其成矿作用的探讨[J] 贵州地质 1991，8(1)：5-12
[151] Nan Junya, Liu Congqiang , Zhou Dequan, Wang Zhuming Ree geochemical study of the Permian-Triassic marine sedimentary environment in GuiZhou province[J] Chinese Journal of Geochemistry 2002,21(4): 348 -361
[152]王立亭，中国南方二叠纪岩相古地理与成矿作用[M]，北京，地质出版社，1994
[153]刘宝君，黔西南中三叠世陆棚-斜坡沉积特征[J]，沉积学报，1987，5(2)
[154]聂爱国，谢宏 峨眉山玄武岩浆与贵州高砷煤成因研究[J]，煤田地质与勘探