峨眉地幔热柱活动与贞丰水银洞金矿床形成关系研究
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摘要
中国卡林型金矿主要产于“滇黔桂”、“川甘陕”及“滇西”地区,其中以“滇黔桂”为主体。“滇黔桂”、“川甘陕”及“滇西”地区均位于峨眉地幔热柱活动区。黔西南地区金矿是“滇黔桂”金三角的主体,其中以贞丰水银洞金矿最具代表性:该矿床金矿矿石品位高、矿体厚度及矿石品位变化系数小,是我国第一个Ⅰ类勘探类型金矿床。该矿床已达特大型规模,为亚洲最大的金矿床。选择水银洞金矿为研究对象,对于探索蛾眉地幔热柱活动对该矿床的形成及对区域成矿的控制有重大理论意义和现实意义。
全文共分五章,首先介绍地幔柱理论的起源及峨眉地幔热柱的活动特征,其次论述峨眉地幔热柱活动形成区域地质背景;再次,阐述水银洞金矿床地质特征;最后探讨峨眉地幔热柱活动形成水银洞金矿床的成因机制。本论文取得以下认识和成果:
(1)水银洞金矿床位于灰家堡金、汞、铊矿矿田带东段,是黔西南金矿矿集区发现较晚、规模较大、品位较高的隐伏岩金矿床;矿床赋存于上二叠统龙潭组煤系地层及其与下伏的茅口组石灰岩之上的炭硅质岩(俗称“大厂层”)中,矿床由若干矿体组成,多个矿层垂直空间上下重叠,受灰家堡背斜严格控制:金矿体在背斜核部向两翼300m范围内产出;单个矿体呈层状、似层状、透镜状、扁豆状,顺层产于地层中,矿体产状与围岩产状一致;该地层中岩石普遍含有百分之几到百分之几十的玄武质火山碎屑;矿体主要赋存于生物碎屑灰岩中,为金的主要载体;矿石矿物有黄铁矿、毒砂及硅酸盐矿物等,其中黄铁矿是金的主要载体,含金量占各种矿石矿物含金量的89%以上。含金黄铁矿有四种类型:草莓状黄铁矿、细粒黄铁矿、粗粒黄铁矿及生物碎屑黄铁矿,其中以生物碎屑状黄铁矿含金最高;金矿物相分析及电子探针分析结果显示,金主要呈包裹金形式存在于热液期含砷黄铁矿中;
(2)峨眉地幔热柱是中国典型的地幔热柱之一。其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;
(3)峨眉地幔热柱活动形成含矿岩浆:地幔热柱边部温度比轴部低,深大断裂也不如轴部发育,减压熔融效应不明显,形成部分熔融程度小的岩浆。金在岩浆演化中是不相容元素,它在熔体中的浓度随部分熔融程度的增大而减小。所以金在这种小部分熔融程度岩浆中易于富集;
(4)海西-印支期峨眉地幔热柱活动产生多条深大断裂,这些深大断裂不仅是峨眉山玄武岩喷溢的通道,也是深部含矿热液及天水深渗及上升的通道。它沟通了地球深部与浅部之间的物质及能量交换。其中峨眉地幔热柱边部的深大断裂是富金岩浆运移的主要通道;
(5)海西-印支期峨眉地幔热柱活动造成岩石圈穹状隆起,明显改变了中国西南地区沉积格局。在贵州西部表现为掀斜式抬升,龙潭期在贞丰、兴仁及安龙一带沉积环境由开阔碳酸盐台地沉积环境变为局限的潮坪-泻湖至局限碳酸盐台地沉积环境。峨眉山玄武岩通过喷发-沉积进入这一局限的沉积盆地内,形成初步富金的含矿建造(矿源层);峨眉地幔热柱的脉动式活动,造成峨眉山玄武岩多次喷发及海水频繁进退,在上二叠统龙潭组地层中形成含、隔水层岩石频繁交替多层矿源层。
(6)海西-印支期至燕山期,峨眉地幔热柱长期活动形成区域热异常,大气降水、海水、地下水及岩浆水等深渗循环不断从峨眉山玄武岩、“大厂层”、含矿建造中萃取大量的Au等成矿物质形成金硅络合物、金硫络合物等形式迁移的成矿热液。
(7)燕山期峨眉地幔热柱再次强烈活动,在形成灰家堡背斜过程中,产生大规模的断裂构造及层间滑脱构造,大量的含矿热液通过断裂构造沿着层间滑动面及层间破碎带向灰家堡背斜核部迁移。当构造应力进一步加大,在灰家堡背斜核部产生成矿期逆冲断层及层间破碎带,成矿体系从封闭变成开放,应力突然得以释放,含矿热液的物理化学条件改变,导致热液体系快速远离平衡态,使络合物失稳,金伴随着大量隐晶-微晶二氧化硅-似碧岩和热液期黄铁矿及含砷、锑、汞等硫化物的沉淀而成矿形成水银洞金矿床。
(8)初步建立了水银洞金矿床的蛾眉地幔热柱成矿模式:峨眉地幔热柱在海西-印支期强烈活动,一方面改变了中国西南地区沉积格局,造成水银洞沉积环境由开阔碳酸盐台地沉积环境变为局限的潮坪-泻湖至局限碳酸盐台地沉积环境;另一方面,峨眉地幔热柱边部形成富金岩浆,并沿峨眉地幔热柱边部的同生深大断裂上升,通过喷发-沉积作用方式进入潮坪-泻湖至局限碳酸盐台地沉积环境。在蛾眉地幔热柱的脉动式活动作用下,造成多次峨眉山玄武岩喷发和海水频繁进退,在上二叠统龙潭组地层中形成具含、隔水层岩石频繁交替的复杂岩性组合的多层含矿建造(矿源层);海西-印支期至燕山期,峨眉地幔热柱长期活动形成区域热异常,大气降水、海水、地下水及岩浆水等深渗循环不断从峨眉山玄武岩、“大厂层”及含矿建造中萃取大量的Au等成矿物质形成金硅络合物、金硫络合物等形式迁移的成矿热液;燕山期峨眉地幔热柱再次强烈活动,在形成灰家堡背斜过程中,产生大规模的断裂构造及层间滑脱构造,大量的含矿热液通过断裂构造沿着层间滑动面及层间破碎带向灰家堡背斜核部迁移。当构造应力进一步加大,在灰家堡背斜核部产生成矿期纵向逆冲断层及层间破碎带,成矿体系从封闭变成开放,应力突然得以释放,含矿热液的物理化学条件改变,导致热液体系快速远离平衡态,使络合物失稳,金伴随着大量隐晶-微晶二氧化硅-似碧岩和热液期黄铁矿及含砷、锑、汞等硫化物的沉淀而成矿,形成水银洞金矿床
Chinese carlin-type gold deposits are mainly located in the "Yunnan -Guizhou -Guangxi", "Sichuan-Gansu-Shanxi" and the west of Yunnan region, which are located in the area of Emei mantle plume activity. The gold deposit in west of Guizhou is most prominent in "Yunnan-Guizhou-Guangxi". .Shuiyingdong gold deposit is the representative among those gold deposits: the gold ore is high-grade,is few affected by geologic structure which after metallogenesis. It is the first I -type exploration in china,and it is the super-large gold deposit. The deposit is hosted in the coal measures strata in the upper Permian Longtan Formation and the carbonaceous silicalite above the subjacent limestone of Permian Maokou Formation, which composed of a number of orebody, multiple ledge overlapped vertical space from top to bottom, the orebodies locate the high point of geological structure. The single orebody is stratiform, atoid structure, lentoid, lenticular, existed in strata, its occurrence is consistent with the adjacent rock . Study Shuiyindong gold deposit which is helpful understand the genesis of mantle plume structure of the deposit. And rich the regional metallogenic theory that have practical significance. there also are significanc to rich the mantle plume theory.
The full text is divided into five chapters. First, introduce the theory of mantle plume and the activity characteristics of the Emei mantle plume, followed by discuss that Emei mantle plume activity form regional geological background; again, introduce the geological characteristics of Shuiyindong gold deposit; Finally dicuss the genesis of the Shuiyindong gold deposit under the activity of the Emei mantle plume. And get the following recognise and results:
(1) Emei mantle plume is one of the typical mantle plume in China. The magmatic activity began in the Devonian, Late Paleozoic. large-scale development in the Late Paleozoic Permian to the entire Mesozoic, may continue into the early Cenozoic. On the early stage (Late Paleozoic),The activity of the Emei mantle plume cause large scale eruption of Mafic magma.0n the late stage (Mesozoic - early Cenozoic), The activity of the Emei mantle plume cause the large-scale invasion of the acidic and alkaline magma ,accompanied by a small number of basic - ultrabasic magma invasive activity.
(2) The activity of the Emei mantle plume formed the gold-rich parent magma: the temperature of the mantle plume edge is lower than the cener of the mantle plume. deep fault is not developmented than the axis of the mantle plume, decompression melting is also developmented than the axis of the mantle plume. small degrees of partial melting of the parent magma is formed in edge of the mantle plume. gold are incompatible elements in the magmatic evolution,so the concentration of the gold in the small degree of partial melting of is more richer;
(3) Hercynian-Indosinian Emei mantle plume generated a number of faults, the deep fault is not only the eruption of Emeishan basalt channel, but also the channel of the deep hydrothermal ore-day and the water deeply Filtrated and raised channel. It communicate between the deep earth and the shallow with the material and the energy exchange. the deep fault of Emei mantle plume is the main channel of gold-rich magma migration;
(4)Emei mantle plume activity caused the dome-like uplift ofthe lithospheric, significantly changed the deposition pattern of China's southwestern region. It is tilting-style uplift at the western Guizhou, parts of south-west of Guizhou (including Shuiyingdong) the carbonate platform depositional environment become limited tidal flat - lagoon depositional environment in parts of south-west of Guizhou (including Shuiyingdong). the Emeishan basalt come into the the limited basin by eruption-sediment, formed the initial source of the gold-rich layer; Emei mantle plume pulsating activity, caused many times of eruptions of Emeishan basalt, formed the formation of many source of ore layer. in the Upper Permian Longtan;
(5) The rate of Geothermal wanning and the radioactive heat can not explain the abnormal heat in southwest Guizhou. The long-term activity of the Emei mantle plume caused heat in southwest of Guizhou, provide heat source for the formation of gold deposits;
(6)Shuiyindong gold deposit is strictly located by the Huijiabao anticline, Gold body is located in 300 meters Range of the anticline core to the scope of the two wings, Many Orebodies overlap upperly and lowely. produced in the Permian Longtan Formation conformitily in different shap of Layered, like layered, lens, lentil-shaped. Ore formation is mainly the Permian Longtan central and lower Formation. The rock of the formation generally contain a few percent to tens percent of basaltic pyroclastic. The main ore body occurs in limestones of biological which is the Carriers of gold. Ore mineral are Pyrite, Arsenopyrite and Silicate minerals etc. Pyrite is the mainly Carriers of gold which pyrite contain more than 89% gold in a variety of gold-bearing ore minerals. There are four types of Gold-bearing pyrite: Strawberry-shaped pyrite, Fine-grained pyrite, Coarse-grained pyrite and Bio-clastic pyrite. Bio-clastic pyrite is the hignest gold-bearing type. The results of the Gold mineral phase analysis and Electron microprobe analysis Reveal that gold is mainly located in hydrothermal period Arsenic pyrite;
(7) Yanshanian the activity of the Emei mantle plume modified the source of ore in the process of the formation of Huijiabao anticline, in the atmospheric precipitation, water and construction of magma under the action of water, actived, transfered the the mineral from the wings of the anticline to the core, concentration, and form the "floor control-type" ore body and the "fracture-type" ore body: the upper part of the Longtan Formation, because of the fracture of the upper strata, communicated between the contact with the outside world, the ore-bearing fluid rapid acceed to fracture in the formation, formed relatively low grade gold "fracture-type" ore body; for the hydrothermal gold-bearing strata in the lower part of Longtan Formation, because the balance of the ore-bearing hydrothermal system is not breaked heavly, gold quality sedimented in the limited range (anticline core) formed the higher grade "stratabound-type" ore body;
(8) The main genesis of Shuiyindong gold has the following three aspects: first, Emei mantle plume activity,in the edge o mantle plume forme the gold-rich magma; second, gold-rich magma erupted and spilled belong the deep fault in the edge of Emei mantle plume ,then sedimented in a relatively isolated tidal flat - lagoon environment that is conducive to the preservation of gold; Third, because of the block of coal and clayr, the hydrothermal in the lower part in Longtan group formed the ore rich body in a relatively limited space (anticline core) through filling etc;
(9) build the mantle plume mineralization model of the Shuiyingdong gold deposit Preliminary: Emei mantle plume strongly activite in the Hercynian -Indosinian:On the one hand, the activite changed the pattern of deposition in southwest of China, the depositional environment of Shuiyindong is changed from carbonate plat to a limited tidal flat - lagoon sediment, On the other hand, formed the gold-rich magma in the Emei mantle plume edge.the gold-rich magma Raise along the deep fault in the edge of the Emei mantle plume, the gold-rich magma go into the Tidal flat-lagoon by Eruption-sedimentation, under the Emei mantle plume pulsely activity, Emeishan basalt erupted many times and Frequent advance and retreat of sea water, formed a limestone + seam (or clay rocks) Combination of complex lithology Multi-storey Source of ore. Yanshanian Emeishan mantle plume active strongly once again, in the process of form Huijiabao Anticline, under the affect of the Abnormal heat , Tectonic stress and Ore-bearing fluid, Transformed the source bed, the gold migrate along the dimensions of to the core of the Huijiabao anticline. The Tectonic stress increase Gradually, formed Ore-forming stage fracture in the The upper part of the Longtan Formation. Because of the Ore-forming stage fracture can not connected the ore-bearing fluid in the the lower part of the source of ore. on the one hand, change conditions of the "floor control-type" ore fluid system,caused the sediment of the gold mineral in a limited space,formed the "layer-control-type" body; . On the other hand, the Ore-forming stage fracture connected the the upper part of the ore fluids in the upper source of ore,, the ore-bearing fluids go fast into the ore-forming period of rapid fracture, formed the" stratabound-type "ore body in the upper strata.
全文共分五章,首先介绍地幔柱理论的起源及峨眉地幔热柱的活动特征,其次论述峨眉地幔热柱活动形成区域地质背景;再次,阐述水银洞金矿床地质特征;最后探讨峨眉地幔热柱活动形成水银洞金矿床的成因机制。本论文取得以下认识和成果:
(1)水银洞金矿床位于灰家堡金、汞、铊矿矿田带东段,是黔西南金矿矿集区发现较晚、规模较大、品位较高的隐伏岩金矿床;矿床赋存于上二叠统龙潭组煤系地层及其与下伏的茅口组石灰岩之上的炭硅质岩(俗称“大厂层”)中,矿床由若干矿体组成,多个矿层垂直空间上下重叠,受灰家堡背斜严格控制:金矿体在背斜核部向两翼300m范围内产出;单个矿体呈层状、似层状、透镜状、扁豆状,顺层产于地层中,矿体产状与围岩产状一致;该地层中岩石普遍含有百分之几到百分之几十的玄武质火山碎屑;矿体主要赋存于生物碎屑灰岩中,为金的主要载体;矿石矿物有黄铁矿、毒砂及硅酸盐矿物等,其中黄铁矿是金的主要载体,含金量占各种矿石矿物含金量的89%以上。含金黄铁矿有四种类型:草莓状黄铁矿、细粒黄铁矿、粗粒黄铁矿及生物碎屑黄铁矿,其中以生物碎屑状黄铁矿含金最高;金矿物相分析及电子探针分析结果显示,金主要呈包裹金形式存在于热液期含砷黄铁矿中;
(2)峨眉地幔热柱是中国典型的地幔热柱之一。其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;
(3)峨眉地幔热柱活动形成含矿岩浆:地幔热柱边部温度比轴部低,深大断裂也不如轴部发育,减压熔融效应不明显,形成部分熔融程度小的岩浆。金在岩浆演化中是不相容元素,它在熔体中的浓度随部分熔融程度的增大而减小。所以金在这种小部分熔融程度岩浆中易于富集;
(4)海西-印支期峨眉地幔热柱活动产生多条深大断裂,这些深大断裂不仅是峨眉山玄武岩喷溢的通道,也是深部含矿热液及天水深渗及上升的通道。它沟通了地球深部与浅部之间的物质及能量交换。其中峨眉地幔热柱边部的深大断裂是富金岩浆运移的主要通道;
(5)海西-印支期峨眉地幔热柱活动造成岩石圈穹状隆起,明显改变了中国西南地区沉积格局。在贵州西部表现为掀斜式抬升,龙潭期在贞丰、兴仁及安龙一带沉积环境由开阔碳酸盐台地沉积环境变为局限的潮坪-泻湖至局限碳酸盐台地沉积环境。峨眉山玄武岩通过喷发-沉积进入这一局限的沉积盆地内,形成初步富金的含矿建造(矿源层);峨眉地幔热柱的脉动式活动,造成峨眉山玄武岩多次喷发及海水频繁进退,在上二叠统龙潭组地层中形成含、隔水层岩石频繁交替多层矿源层。
(6)海西-印支期至燕山期,峨眉地幔热柱长期活动形成区域热异常,大气降水、海水、地下水及岩浆水等深渗循环不断从峨眉山玄武岩、“大厂层”、含矿建造中萃取大量的Au等成矿物质形成金硅络合物、金硫络合物等形式迁移的成矿热液。
(7)燕山期峨眉地幔热柱再次强烈活动,在形成灰家堡背斜过程中,产生大规模的断裂构造及层间滑脱构造,大量的含矿热液通过断裂构造沿着层间滑动面及层间破碎带向灰家堡背斜核部迁移。当构造应力进一步加大,在灰家堡背斜核部产生成矿期逆冲断层及层间破碎带,成矿体系从封闭变成开放,应力突然得以释放,含矿热液的物理化学条件改变,导致热液体系快速远离平衡态,使络合物失稳,金伴随着大量隐晶-微晶二氧化硅-似碧岩和热液期黄铁矿及含砷、锑、汞等硫化物的沉淀而成矿形成水银洞金矿床。
(8)初步建立了水银洞金矿床的蛾眉地幔热柱成矿模式:峨眉地幔热柱在海西-印支期强烈活动,一方面改变了中国西南地区沉积格局,造成水银洞沉积环境由开阔碳酸盐台地沉积环境变为局限的潮坪-泻湖至局限碳酸盐台地沉积环境;另一方面,峨眉地幔热柱边部形成富金岩浆,并沿峨眉地幔热柱边部的同生深大断裂上升,通过喷发-沉积作用方式进入潮坪-泻湖至局限碳酸盐台地沉积环境。在蛾眉地幔热柱的脉动式活动作用下,造成多次峨眉山玄武岩喷发和海水频繁进退,在上二叠统龙潭组地层中形成具含、隔水层岩石频繁交替的复杂岩性组合的多层含矿建造(矿源层);海西-印支期至燕山期,峨眉地幔热柱长期活动形成区域热异常,大气降水、海水、地下水及岩浆水等深渗循环不断从峨眉山玄武岩、“大厂层”及含矿建造中萃取大量的Au等成矿物质形成金硅络合物、金硫络合物等形式迁移的成矿热液;燕山期峨眉地幔热柱再次强烈活动,在形成灰家堡背斜过程中,产生大规模的断裂构造及层间滑脱构造,大量的含矿热液通过断裂构造沿着层间滑动面及层间破碎带向灰家堡背斜核部迁移。当构造应力进一步加大,在灰家堡背斜核部产生成矿期纵向逆冲断层及层间破碎带,成矿体系从封闭变成开放,应力突然得以释放,含矿热液的物理化学条件改变,导致热液体系快速远离平衡态,使络合物失稳,金伴随着大量隐晶-微晶二氧化硅-似碧岩和热液期黄铁矿及含砷、锑、汞等硫化物的沉淀而成矿,形成水银洞金矿床
Chinese carlin-type gold deposits are mainly located in the "Yunnan -Guizhou -Guangxi", "Sichuan-Gansu-Shanxi" and the west of Yunnan region, which are located in the area of Emei mantle plume activity. The gold deposit in west of Guizhou is most prominent in "Yunnan-Guizhou-Guangxi". .Shuiyingdong gold deposit is the representative among those gold deposits: the gold ore is high-grade,is few affected by geologic structure which after metallogenesis. It is the first I -type exploration in china,and it is the super-large gold deposit. The deposit is hosted in the coal measures strata in the upper Permian Longtan Formation and the carbonaceous silicalite above the subjacent limestone of Permian Maokou Formation, which composed of a number of orebody, multiple ledge overlapped vertical space from top to bottom, the orebodies locate the high point of geological structure. The single orebody is stratiform, atoid structure, lentoid, lenticular, existed in strata, its occurrence is consistent with the adjacent rock . Study Shuiyindong gold deposit which is helpful understand the genesis of mantle plume structure of the deposit. And rich the regional metallogenic theory that have practical significance. there also are significanc to rich the mantle plume theory.
The full text is divided into five chapters. First, introduce the theory of mantle plume and the activity characteristics of the Emei mantle plume, followed by discuss that Emei mantle plume activity form regional geological background; again, introduce the geological characteristics of Shuiyindong gold deposit; Finally dicuss the genesis of the Shuiyindong gold deposit under the activity of the Emei mantle plume. And get the following recognise and results:
(1) Emei mantle plume is one of the typical mantle plume in China. The magmatic activity began in the Devonian, Late Paleozoic. large-scale development in the Late Paleozoic Permian to the entire Mesozoic, may continue into the early Cenozoic. On the early stage (Late Paleozoic),The activity of the Emei mantle plume cause large scale eruption of Mafic magma.0n the late stage (Mesozoic - early Cenozoic), The activity of the Emei mantle plume cause the large-scale invasion of the acidic and alkaline magma ,accompanied by a small number of basic - ultrabasic magma invasive activity.
(2) The activity of the Emei mantle plume formed the gold-rich parent magma: the temperature of the mantle plume edge is lower than the cener of the mantle plume. deep fault is not developmented than the axis of the mantle plume, decompression melting is also developmented than the axis of the mantle plume. small degrees of partial melting of the parent magma is formed in edge of the mantle plume. gold are incompatible elements in the magmatic evolution,so the concentration of the gold in the small degree of partial melting of is more richer;
(3) Hercynian-Indosinian Emei mantle plume generated a number of faults, the deep fault is not only the eruption of Emeishan basalt channel, but also the channel of the deep hydrothermal ore-day and the water deeply Filtrated and raised channel. It communicate between the deep earth and the shallow with the material and the energy exchange. the deep fault of Emei mantle plume is the main channel of gold-rich magma migration;
(4)Emei mantle plume activity caused the dome-like uplift ofthe lithospheric, significantly changed the deposition pattern of China's southwestern region. It is tilting-style uplift at the western Guizhou, parts of south-west of Guizhou (including Shuiyingdong) the carbonate platform depositional environment become limited tidal flat - lagoon depositional environment in parts of south-west of Guizhou (including Shuiyingdong). the Emeishan basalt come into the the limited basin by eruption-sediment, formed the initial source of the gold-rich layer; Emei mantle plume pulsating activity, caused many times of eruptions of Emeishan basalt, formed the formation of many source of ore layer. in the Upper Permian Longtan;
(5) The rate of Geothermal wanning and the radioactive heat can not explain the abnormal heat in southwest Guizhou. The long-term activity of the Emei mantle plume caused heat in southwest of Guizhou, provide heat source for the formation of gold deposits;
(6)Shuiyindong gold deposit is strictly located by the Huijiabao anticline, Gold body is located in 300 meters Range of the anticline core to the scope of the two wings, Many Orebodies overlap upperly and lowely. produced in the Permian Longtan Formation conformitily in different shap of Layered, like layered, lens, lentil-shaped. Ore formation is mainly the Permian Longtan central and lower Formation. The rock of the formation generally contain a few percent to tens percent of basaltic pyroclastic. The main ore body occurs in limestones of biological which is the Carriers of gold. Ore mineral are Pyrite, Arsenopyrite and Silicate minerals etc. Pyrite is the mainly Carriers of gold which pyrite contain more than 89% gold in a variety of gold-bearing ore minerals. There are four types of Gold-bearing pyrite: Strawberry-shaped pyrite, Fine-grained pyrite, Coarse-grained pyrite and Bio-clastic pyrite. Bio-clastic pyrite is the hignest gold-bearing type. The results of the Gold mineral phase analysis and Electron microprobe analysis Reveal that gold is mainly located in hydrothermal period Arsenic pyrite;
(7) Yanshanian the activity of the Emei mantle plume modified the source of ore in the process of the formation of Huijiabao anticline, in the atmospheric precipitation, water and construction of magma under the action of water, actived, transfered the the mineral from the wings of the anticline to the core, concentration, and form the "floor control-type" ore body and the "fracture-type" ore body: the upper part of the Longtan Formation, because of the fracture of the upper strata, communicated between the contact with the outside world, the ore-bearing fluid rapid acceed to fracture in the formation, formed relatively low grade gold "fracture-type" ore body; for the hydrothermal gold-bearing strata in the lower part of Longtan Formation, because the balance of the ore-bearing hydrothermal system is not breaked heavly, gold quality sedimented in the limited range (anticline core) formed the higher grade "stratabound-type" ore body;
(8) The main genesis of Shuiyindong gold has the following three aspects: first, Emei mantle plume activity,in the edge o mantle plume forme the gold-rich magma; second, gold-rich magma erupted and spilled belong the deep fault in the edge of Emei mantle plume ,then sedimented in a relatively isolated tidal flat - lagoon environment that is conducive to the preservation of gold; Third, because of the block of coal and clayr, the hydrothermal in the lower part in Longtan group formed the ore rich body in a relatively limited space (anticline core) through filling etc;
(9) build the mantle plume mineralization model of the Shuiyingdong gold deposit Preliminary: Emei mantle plume strongly activite in the Hercynian -Indosinian:On the one hand, the activite changed the pattern of deposition in southwest of China, the depositional environment of Shuiyindong is changed from carbonate plat to a limited tidal flat - lagoon sediment, On the other hand, formed the gold-rich magma in the Emei mantle plume edge.the gold-rich magma Raise along the deep fault in the edge of the Emei mantle plume, the gold-rich magma go into the Tidal flat-lagoon by Eruption-sedimentation, under the Emei mantle plume pulsely activity, Emeishan basalt erupted many times and Frequent advance and retreat of sea water, formed a limestone + seam (or clay rocks) Combination of complex lithology Multi-storey Source of ore. Yanshanian Emeishan mantle plume active strongly once again, in the process of form Huijiabao Anticline, under the affect of the Abnormal heat , Tectonic stress and Ore-bearing fluid, Transformed the source bed, the gold migrate along the dimensions of to the core of the Huijiabao anticline. The Tectonic stress increase Gradually, formed Ore-forming stage fracture in the The upper part of the Longtan Formation. Because of the Ore-forming stage fracture can not connected the ore-bearing fluid in the the lower part of the source of ore. on the one hand, change conditions of the "floor control-type" ore fluid system,caused the sediment of the gold mineral in a limited space,formed the "layer-control-type" body; . On the other hand, the Ore-forming stage fracture connected the the upper part of the ore fluids in the upper source of ore,, the ore-bearing fluids go fast into the ore-forming period of rapid fracture, formed the" stratabound-type "ore body in the upper strata.
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