广东凡口铅锌矿床成矿机制与成矿模式
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摘要
广东凡口铅锌矿床是我国著名的大型-超大型铅锌矿床,隶属广东省韶关市仁化县辖区,位于华夏地块粤北曲仁盆地的北缘,在我国矿产资源中占有极其重要的地位。
多年来,国内外众多学者从不同角度,采用不同手段,对该矿床做了大量研究并积累了丰富的基础资料,并对矿床的成矿作用、控矿条件等提出不少认识,然就其成矿物质来源,矿床成因机制等关键地质问题的研究仍显薄弱。本文以矿床学、层控矿床学、地球化学等现代成矿理论为指导,以野外地质观察为基础,重点从地球化学的角度进行深入研究,探讨了该矿床的成矿物质来源、控矿因素、矿床成因、成矿作用过程,最终建立了综合成矿模式。
大量基础地质资料研究显示,凡口矿区主要出露寒武系、泥盆系、石炭系、二叠系等地层。区内褶皱、断裂构造发育,构造控矿特征明显,主要有NWW向、NW向、NNE向及NE向断裂带等。沉积地层形成以后,在石炭系壶天群(C2ht)和泥盆系天子岭下亚组(D3ta)之间的部分或全部的地层缺失,形成几米到几十米不等碎裂泥质物或劈理化岩层(即“破乱层”),北部大体呈NWW向。之后是NW向断裂带(前人认为NW向断裂带就是指F203)形成,在矿区南部的活动有可能与NWW向断裂带复合,F203可能就是二者的复合断裂,F203发育持续时间长,贯穿整个成矿期,在成矿期后仍有活动。之后为NNE向断裂带的发育,出现了F1-F1o等断层,为矿区主要的导矿容矿构造。NE断裂带为NNE断裂带的更次一级构造,包括Flo0、Flo1、F102、F104等断层,该组断层与NNE向断裂带的交汇处是矿体形成的理想场所。
赋矿围岩及矿石的微量元素及稀土元素特征显示,Fe主要来自矿区上部的碳酸盐岩地层；后期热液使矿区的含矿地层体系发生不同程度的蚀变,影响了地层中微量元素和稀土元素的分布；不同层位的岩层稀土元素分布特征相似,说明矿区各地层受到同种性质热液作用的影响。
碳、氧、锶同位素研究显示,凡口矿区奥陶系(O)δ13C=-6.5%o,δ18O=14.9‰,碳、氧值最低,主要受陆源碎屑物质的影响；石炭系(C2ht) δ13C=2.17‰,δ18O值=21.9‰,碳、氧值最高,主要受地层岩性的影响；泥盆系为主要成矿层位,碳、氧、锶值随着地层蚀变程度减弱而逐渐降低,说明其除了岩性及海相沉积旋回的影响,主要受后期热液作用的影响。
铅、硫同位素研究显示,矿石中的铅同位素主要来源于上地壳物质,围岩铅与矿石铅应属同源；矿石中的硫主要来自海水硫酸盐。黄铁矿、闪锌矿和方铅矿的硫同位素分布规律为：δ34S黄铁矿>δ34S闪锌矿>δ34S方铅矿。
流体包裹体研究显示,浅色闪锌矿流体包裹体均一温度集中在110-170℃区间,高于200℃的流体包裹体较少,冰点温度为-2.1～-1.4℃,盐度约为3wt%NaCl,含有少量的NaCl;深色闪锌矿均一温度主要在110-150℃和110-250℃两个区间,冰点温度为-0.2--0.1℃,盐度为0.18wt%～0.35wt%NaCl,基本不含NaCl。方解石中流体包裹体的均一温度分布较广,为170-310℃,盐度较高,主要在14wt%NaCl左右,也有盐度较低的流体,几乎不含NaCl,与形成闪锌矿低盐度流体区间相同。流体包裹体成分主要为H2O(液相)-H2O(气相)、NaCl-H2O体系,未发现NaCl的子结晶,含少量CH4等有机成分,以及HCl、CO等气体,成矿作用过程有机质参与成矿,但参与程度较小。
凡口矿床的成矿年代基本在86.8-138Ma,该阶段形成地层为白垩纪红层,对应于燕山运动晚期,该阶段形成的地层为白垩纪红层。凡口铅锌矿床的形成虽然与岩浆活动无关,但该时期与华南地区广泛发育红层盆地时代相对应,且凡口矿区的赋矿地层发生了白云石化作用,也正好与区域上发生的大面积白云石化相对应,矿区底部含铅锌的成矿流体可能这号来源于区域的红层盆地卤水。
综合研究显示,凡口矿床形成于一个大的热液成矿期,该成矿期分为三个成矿阶段：早期成矿阶段主要以块状黄铁矿为主,铅锌含量极少；主成矿阶段值方铅矿闪锌矿阶段,伴随少量黄铁矿的形成；晚期成矿阶段以粗粒亮黄色黄铁矿的出现为标志,主要是成矿期残余热液作用的产物。成矿流体主要有两大类：第一类为矿区底部的盆地卤水,可能来源于区域白垩系红层的盆地卤水；第二类为矿区上部碳酸盐岩中的原地层水,主要来源于大气降水。两类流体在特定的条件下,合适的场所相遇,金属元素发生反应,生成金属硫化物沉淀,最终形成巨大的铅锌矿体。
将凡口铅锌矿床与典型MVT铅锌矿床对比分析显示,二者具有众多的相似特征,但凡口矿床具有成矿温度较高、有机质参与少、坍塌角砾岩少见、胶状或草莓状矿石结构不发育等特点与MVT铅锌矿床不同。综合来讲,凡口矿床应属于非典型的MVT铅锌矿床,只是具有其特殊性。
The Fankou lead-zinc deposit is a famous large-extra large scale lead-zinc deposit where located in Shaoguan of Guangdong Province, China. The tectonic located at the north of Quren in North Guangdong. It is play an extremely vital role in the mineral resources.
Over the years, many scholars researched the deposit, using different methods and different angles, and accumulated a wealth of basic information, and proposed form the mineralization and ore-controlling conditions of the deposit, but its sources of minerals, deposit genesis mechanism research remains unclear. Based on study of minerals deposit, stratabound ore deposits, geochemical and other modern metallogenic theory as the instruction, on the basis of field geological observation, focused research from geochemistry, and probes into the source of ore-forming materials, ore-controlling factors, genesis of deposit and mineralization process, comprehensive metallogenic model is established finally.
A large number of basic geological information show that, Stratums of Cambrian, Devonian, Carboniferous and Permian developed in the ground in Fankou mining area. Fankou mining area included NWW, NW, NNE and NE fault belts. After the formation of the sedimentary strata, loss of part or all of the stratums in between C2ht and D3ta, lack of them formed several to dozens of meters fragmentation mud or cleavage of strata, which is named as "The broken layers", and it is the upper boundary in Fankou deposit. The northern range is generally NWW to lack of stratum; then NW trending fault zone (former NW trending fault zone is referred to as F203) formation, NW trending fault zone may be in the south area of the mine activities associated with the NWW trending fault zone compound, Fracture F203composed of NWW and NW trending fault zone. The NW fault belt is a lower boundary of mining area, between the formation of ore bodies should be two.F203development NNE to the secondary fracture zone, there was F1～F10fault, the fault is the main ore-bearing structure of ore. NE fault zone as a NNE fault zone more secondary structures, including F100, F101, F102, F104fault, the fault and NNE trending fault zone interchange is an ideal place for the formation of ore bodies.
Trace and rare earth elements of rock and ore shows that, the element of Fe mainly come from carbonate of mining area. The stratums of Fankou mining area of alteration in different degree due to late hydrothermal, affected the values of trace and rare earth elements, Similar characteristics of the different stratums indicated layers of Fankou mining area are affactd by same properties hydrothermal.
Stable isotope showed that, the813C value is-6.5‰and δ18O value is14.9%o with Ordovician, it is the lowest of all and mainly affected by terrigenous detrital materials. The δ13C value is2.17‰and δ18O value is21.9%o with Carboniferous, it is greater than other stratums and affected by lithology. Devonian as the main metallogenic formation, From deep to shallow, the values of carbon, oxygen and strontium are decreased along with hydrothermal alteration weaken, its in addition to the impacts of lithology and marine sedimentary cycle, mainly affected by the late hydrothermal process.
The lead isotopes in ores are mainly originated from ancient crustal material. The lead isotopes are the mixture of multiple sources, Surrouding rocks similar with the source. The sulfur of the ore came from sulfates in the seawater, and experienced the reduction of organic matter. The relative abundance of pyrite, sphalerite, and galena is:δ34S value of pyrite> δ34S value of sphalerite>δ34S value of galena.
The ore-forming fluid temperature concentrated in110～150℃and160～210℃, Fluid inclusions of light brown sphalerite, homogenization temperature is109℃in average, and usually low salinity(<4wt%NaCl). The main content of the fluid is H2O (liquid)-H2O (gaseous), NaCl-H2O, not found Sodium chloride crystal, and organic matter such as CH4, HCl, CO, a few of organic matters involved in mineralizationg.
The formation of Fankou lead-zinc deposit is closely related to the regional dolomitization. The time of ore-forming is basically during86.8～90.7Ma, it corresponds to the period which red bed basin was widely developed in Southern China. Further, and the ore-bearing stratums are dolomitized, which is also correspond to the large scale dolomitization in this region.
This study suggests that Fankou lead-zinc deposit is mainly formed during a period of hydrothermal mineralization. There are three metallogenic stages:early, main and late metallogenic stage. Early stage is mainly the formation of pyrite ore body and nearly absent of lead-zinc, main stage is the formation of lead-zinc ore body with pyrite, late stage is marked by the presence of coarse grained bright yellow colored pyrite, produced by the effect of hydrotherm of late mineralization period. Two main categories of ore-forming fluid in Fankou lead-zinc deposit:the first is the deep fluid at the bottom of the mining area, which is possibly originated from the basin brine of regional Cretaceous red strata. The second is the original formation water in carbonate rocks in upper part of the mining area, mainly from atmospheric water. The two types of fluid meet at specific condition at proper place, the metallic elements of two fluids were responsed, caused aggregation and concentrate. Finally, they formed giant ore body.
Fankou lead-zinc deposit and MVT deposit have many similarities,but the differences are higher temperature, lesser organic matter, fewer collapse breccia, fewer colloidal from texture than MVT deposit. But geological and geochemical characteristics, ore-forming fluid transport, sulphides deposition are similar with MVT deposit, Fankou lead-zinc deposit as a whole belongs to this model of MVT deposit.
多年来,国内外众多学者从不同角度,采用不同手段,对该矿床做了大量研究并积累了丰富的基础资料,并对矿床的成矿作用、控矿条件等提出不少认识,然就其成矿物质来源,矿床成因机制等关键地质问题的研究仍显薄弱。本文以矿床学、层控矿床学、地球化学等现代成矿理论为指导,以野外地质观察为基础,重点从地球化学的角度进行深入研究,探讨了该矿床的成矿物质来源、控矿因素、矿床成因、成矿作用过程,最终建立了综合成矿模式。
大量基础地质资料研究显示,凡口矿区主要出露寒武系、泥盆系、石炭系、二叠系等地层。区内褶皱、断裂构造发育,构造控矿特征明显,主要有NWW向、NW向、NNE向及NE向断裂带等。沉积地层形成以后,在石炭系壶天群(C2ht)和泥盆系天子岭下亚组(D3ta)之间的部分或全部的地层缺失,形成几米到几十米不等碎裂泥质物或劈理化岩层(即“破乱层”),北部大体呈NWW向。之后是NW向断裂带(前人认为NW向断裂带就是指F203)形成,在矿区南部的活动有可能与NWW向断裂带复合,F203可能就是二者的复合断裂,F203发育持续时间长,贯穿整个成矿期,在成矿期后仍有活动。之后为NNE向断裂带的发育,出现了F1-F1o等断层,为矿区主要的导矿容矿构造。NE断裂带为NNE断裂带的更次一级构造,包括Flo0、Flo1、F102、F104等断层,该组断层与NNE向断裂带的交汇处是矿体形成的理想场所。
赋矿围岩及矿石的微量元素及稀土元素特征显示,Fe主要来自矿区上部的碳酸盐岩地层；后期热液使矿区的含矿地层体系发生不同程度的蚀变,影响了地层中微量元素和稀土元素的分布；不同层位的岩层稀土元素分布特征相似,说明矿区各地层受到同种性质热液作用的影响。
碳、氧、锶同位素研究显示,凡口矿区奥陶系(O)δ13C=-6.5%o,δ18O=14.9‰,碳、氧值最低,主要受陆源碎屑物质的影响；石炭系(C2ht) δ13C=2.17‰,δ18O值=21.9‰,碳、氧值最高,主要受地层岩性的影响；泥盆系为主要成矿层位,碳、氧、锶值随着地层蚀变程度减弱而逐渐降低,说明其除了岩性及海相沉积旋回的影响,主要受后期热液作用的影响。
铅、硫同位素研究显示,矿石中的铅同位素主要来源于上地壳物质,围岩铅与矿石铅应属同源；矿石中的硫主要来自海水硫酸盐。黄铁矿、闪锌矿和方铅矿的硫同位素分布规律为：δ34S黄铁矿>δ34S闪锌矿>δ34S方铅矿。
流体包裹体研究显示,浅色闪锌矿流体包裹体均一温度集中在110-170℃区间,高于200℃的流体包裹体较少,冰点温度为-2.1～-1.4℃,盐度约为3wt%NaCl,含有少量的NaCl;深色闪锌矿均一温度主要在110-150℃和110-250℃两个区间,冰点温度为-0.2--0.1℃,盐度为0.18wt%～0.35wt%NaCl,基本不含NaCl。方解石中流体包裹体的均一温度分布较广,为170-310℃,盐度较高,主要在14wt%NaCl左右,也有盐度较低的流体,几乎不含NaCl,与形成闪锌矿低盐度流体区间相同。流体包裹体成分主要为H2O(液相)-H2O(气相)、NaCl-H2O体系,未发现NaCl的子结晶,含少量CH4等有机成分,以及HCl、CO等气体,成矿作用过程有机质参与成矿,但参与程度较小。
凡口矿床的成矿年代基本在86.8-138Ma,该阶段形成地层为白垩纪红层,对应于燕山运动晚期,该阶段形成的地层为白垩纪红层。凡口铅锌矿床的形成虽然与岩浆活动无关,但该时期与华南地区广泛发育红层盆地时代相对应,且凡口矿区的赋矿地层发生了白云石化作用,也正好与区域上发生的大面积白云石化相对应,矿区底部含铅锌的成矿流体可能这号来源于区域的红层盆地卤水。
综合研究显示,凡口矿床形成于一个大的热液成矿期,该成矿期分为三个成矿阶段：早期成矿阶段主要以块状黄铁矿为主,铅锌含量极少；主成矿阶段值方铅矿闪锌矿阶段,伴随少量黄铁矿的形成；晚期成矿阶段以粗粒亮黄色黄铁矿的出现为标志,主要是成矿期残余热液作用的产物。成矿流体主要有两大类：第一类为矿区底部的盆地卤水,可能来源于区域白垩系红层的盆地卤水；第二类为矿区上部碳酸盐岩中的原地层水,主要来源于大气降水。两类流体在特定的条件下,合适的场所相遇,金属元素发生反应,生成金属硫化物沉淀,最终形成巨大的铅锌矿体。
将凡口铅锌矿床与典型MVT铅锌矿床对比分析显示,二者具有众多的相似特征,但凡口矿床具有成矿温度较高、有机质参与少、坍塌角砾岩少见、胶状或草莓状矿石结构不发育等特点与MVT铅锌矿床不同。综合来讲,凡口矿床应属于非典型的MVT铅锌矿床,只是具有其特殊性。
The Fankou lead-zinc deposit is a famous large-extra large scale lead-zinc deposit where located in Shaoguan of Guangdong Province, China. The tectonic located at the north of Quren in North Guangdong. It is play an extremely vital role in the mineral resources.
Over the years, many scholars researched the deposit, using different methods and different angles, and accumulated a wealth of basic information, and proposed form the mineralization and ore-controlling conditions of the deposit, but its sources of minerals, deposit genesis mechanism research remains unclear. Based on study of minerals deposit, stratabound ore deposits, geochemical and other modern metallogenic theory as the instruction, on the basis of field geological observation, focused research from geochemistry, and probes into the source of ore-forming materials, ore-controlling factors, genesis of deposit and mineralization process, comprehensive metallogenic model is established finally.
A large number of basic geological information show that, Stratums of Cambrian, Devonian, Carboniferous and Permian developed in the ground in Fankou mining area. Fankou mining area included NWW, NW, NNE and NE fault belts. After the formation of the sedimentary strata, loss of part or all of the stratums in between C2ht and D3ta, lack of them formed several to dozens of meters fragmentation mud or cleavage of strata, which is named as "The broken layers", and it is the upper boundary in Fankou deposit. The northern range is generally NWW to lack of stratum; then NW trending fault zone (former NW trending fault zone is referred to as F203) formation, NW trending fault zone may be in the south area of the mine activities associated with the NWW trending fault zone compound, Fracture F203composed of NWW and NW trending fault zone. The NW fault belt is a lower boundary of mining area, between the formation of ore bodies should be two.F203development NNE to the secondary fracture zone, there was F1～F10fault, the fault is the main ore-bearing structure of ore. NE fault zone as a NNE fault zone more secondary structures, including F100, F101, F102, F104fault, the fault and NNE trending fault zone interchange is an ideal place for the formation of ore bodies.
Trace and rare earth elements of rock and ore shows that, the element of Fe mainly come from carbonate of mining area. The stratums of Fankou mining area of alteration in different degree due to late hydrothermal, affected the values of trace and rare earth elements, Similar characteristics of the different stratums indicated layers of Fankou mining area are affactd by same properties hydrothermal.
Stable isotope showed that, the813C value is-6.5‰and δ18O value is14.9%o with Ordovician, it is the lowest of all and mainly affected by terrigenous detrital materials. The δ13C value is2.17‰and δ18O value is21.9%o with Carboniferous, it is greater than other stratums and affected by lithology. Devonian as the main metallogenic formation, From deep to shallow, the values of carbon, oxygen and strontium are decreased along with hydrothermal alteration weaken, its in addition to the impacts of lithology and marine sedimentary cycle, mainly affected by the late hydrothermal process.
The lead isotopes in ores are mainly originated from ancient crustal material. The lead isotopes are the mixture of multiple sources, Surrouding rocks similar with the source. The sulfur of the ore came from sulfates in the seawater, and experienced the reduction of organic matter. The relative abundance of pyrite, sphalerite, and galena is:δ34S value of pyrite> δ34S value of sphalerite>δ34S value of galena.
The ore-forming fluid temperature concentrated in110～150℃and160～210℃, Fluid inclusions of light brown sphalerite, homogenization temperature is109℃in average, and usually low salinity(<4wt%NaCl). The main content of the fluid is H2O (liquid)-H2O (gaseous), NaCl-H2O, not found Sodium chloride crystal, and organic matter such as CH4, HCl, CO, a few of organic matters involved in mineralizationg.
The formation of Fankou lead-zinc deposit is closely related to the regional dolomitization. The time of ore-forming is basically during86.8～90.7Ma, it corresponds to the period which red bed basin was widely developed in Southern China. Further, and the ore-bearing stratums are dolomitized, which is also correspond to the large scale dolomitization in this region.
This study suggests that Fankou lead-zinc deposit is mainly formed during a period of hydrothermal mineralization. There are three metallogenic stages:early, main and late metallogenic stage. Early stage is mainly the formation of pyrite ore body and nearly absent of lead-zinc, main stage is the formation of lead-zinc ore body with pyrite, late stage is marked by the presence of coarse grained bright yellow colored pyrite, produced by the effect of hydrotherm of late mineralization period. Two main categories of ore-forming fluid in Fankou lead-zinc deposit:the first is the deep fluid at the bottom of the mining area, which is possibly originated from the basin brine of regional Cretaceous red strata. The second is the original formation water in carbonate rocks in upper part of the mining area, mainly from atmospheric water. The two types of fluid meet at specific condition at proper place, the metallic elements of two fluids were responsed, caused aggregation and concentrate. Finally, they formed giant ore body.
Fankou lead-zinc deposit and MVT deposit have many similarities,but the differences are higher temperature, lesser organic matter, fewer collapse breccia, fewer colloidal from texture than MVT deposit. But geological and geochemical characteristics, ore-forming fluid transport, sulphides deposition are similar with MVT deposit, Fankou lead-zinc deposit as a whole belongs to this model of MVT deposit.
引文
[1]Tikkanen, G. D.,1986, World resources and supply of lead and zinc, in Bush, W. R., ed., Economics of Internationally Traded Minerals:Society of Mining Engineers, Inc., p. 242-250.
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