Migration and Emplacement of Ore-forming Fluids and Their Structural Controlling Mechanisms: An Example from Jiaojia Gold Belt in Jiaodong Peninsula

doi:10.19657/j.geoscience.1000-8527.2024.092

Abstract

Abstract:

Hydrothermal ore-forming system can be controlled by the migration and placement of ore-forming fluids induced by tectonic movement.Structure is the primary ore-controlling factor, and the migration and placement of ore-forming fluids are the core theory of tectonic ore-controlling.Multiple or single dominant factors, such as fluid pressure differences, integrated hydraulic gradients, and heat conduction, drive fluid migration within transport channels formed by faults, cracks, and pores in the surrounding rocks.Chemical reactions of fluids in structural cracks or pores, fluid mixing and immiscibility, and fluid boiling lead to changes in the physical and chemical properties of the fluids, resulting in the precipitation of ore-forming materials.Fluid migration patterns affect the form of mineralization.Fluid migrating through macroscopic faults and fractures, resembling pipeline flow, primarily forms large vein ore bodies with high mineralization.However, permeation flow, which widely develops in micron-scale cracks and pores of surrounding rock, mostly forms fine veins and disseminated ore bodies with stable mineralization grade and medium scale.The dynamic coupling between tectonic deformation, fluid pressure, and stress state leads to the temporal and spatial occurrence of the ore body.The fault valve-pumping mechanism is the most representative tectonic-fluid coupling model to explain orogenic gold mineralization.The formation and distribution of deposits in the Jiaojia gold belt are controlled by three-order fault structures.The compression-shear Jiaojia fault is a first-order ore-controlling structure, which governs the extensive hydrothermal alteration dominated by sericitization and the placement of altered rock type gold ore bodies within fracture zones.The Wangershan fault, a tensile shear structure in its footwall, serves as a secondary ore-controlling structure, where hydrothermal alteration is relatively weaker, resulting in the development transitional gold ore-body.The third-order ore-controlling structure consists of dozens of tensile-shear faults and joint systems dominated by the Baoli fault, which exhibits the weakest degree of alteration and mineralization.This structure mainly controls the occurrence of quartz vein-type gold orebodies.The study of the three-dimensional geometry of the ore-body in Sizhuang gold deposit shows that the morphological flatness of the ore-body group increase from No.I ore body to No.Ⅲ ore body.This indicates the spatial evolution of ore-forming fluid transport from infiltration to pipeline flow, and the differences in ore-body occurrence reflect changes in ore-forming fluid migration directions.Further research needs to integrate results from multidisciplinary studies, especially conducting in-depth analysis of the coupling relationship between micro-ultra-microscopic deformation fabric and ore-forming fluid behaviors.This includes constructing a multi-scale structure-fluid coupling ore-forming model that closely mimics reality and reveals the intricate processes and mechanisms of hydrothermal ore-forming system.

Key words: hydrothermal ore-forming system, migration and emplacement of ore-forming fluids, structural ore-controlling, structure-fluid metallogenic dynamics, Jiaojia gold belt

CLC Number:

ZHANG Longxiao, YANG Liqiang, YANG Wei, XIE Dong. Migration and Emplacement of Ore-forming Fluids and Their Structural Controlling Mechanisms: An Example from Jiaojia Gold Belt in Jiaodong Peninsula[J]. Geoscience, 2024, 38(04): 873-891.

Figures/Tables 11

References 129

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矿床	流体包裹体的均一温度(℃)	流体包裹体盐度特征(%)	流体组成	流体来源	成矿压力 (bar)	成矿深度 (km)	主控矿因素	资料来源
MVT密西西比河谷型铅锌矿床	75~175	20±5	富含Pb、Zn,Cu等金属元素;挥发性组分为CO₂、CH₄	海水、部分大气降水	几百到上千巴之间	1~1.8	层控	[26-27]
VMS火山成因块状硫化物矿床	100~360	5~10	富含Cu、Pb、Zn等金属元素;挥发性组分为CO₂、CH₄、N₂	海底热液:海水、岩浆热液	/	/	层控	[28-29]
浅成热液矿床	100~450	0~40	富含各种金属元素;挥发分为CO₂、H₂S、CH₄、N₂和SO₂	岩浆热液、大气降水	100~500	1~1.5	断裂系统控制	[30-31]
斑岩型Cu-Mo矿	100~900	0~60	富含Cu、Mo、Na、K、Fe等金属元素的高盐度流体	岩浆热液	几十到几百巴,有时高达1000 bar左右	1~6	断裂系统控制	[32-33]
矽卡岩型矿床	100~600	0~60	富含W、Mo、Cu、Pb、Zn等金属元素	岩浆热液、变质热液、部分大气降水	不同类型的矽卡岩矿床有着不同的成矿压力	1~4.5	褶皱、断裂构造控制	[4]
卡林型金矿	100~300	0~7	富含以Au为主的各种金属元素;主要挥发分为CO₂、H₂S	岩浆热液、变质热液、大气降水	不同类型的卡林型金矿有着不同的成矿压力	2 km左右,甚至达到数千米	层控	[34-35]
造山型金矿	150~350	0~10	富含Na、Ca、K、Mg等金属元素;为H₂O-CO₂-NaCl体系	岩浆热液、变质热液和深循环大气降水	500~1500	3~10	断裂系统控制	[3,36]
胶东型金矿	260~340	2~10	富含Na、K、Mg、Ca等金属元素;为H₂O-CO₂-NaCl-CH₄体系	深部岩浆热液与大气水混合	900~2400	2~10	断裂系统控制	[37-39]

矿床	流体包裹体的均一温度(℃)	流体包裹体盐度特征(%)	流体组成	流体来源	成矿压力 (bar)	成矿深度 (km)	主控矿因素	资料来源
MVT密西西比河谷型铅锌矿床	75~175	20±5	富含Pb、Zn,Cu等金属元素;挥发性组分为CO₂、CH₄	海水、部分大气降水	几百到上千巴之间	1~1.8	层控	[26-27]
VMS火山成因块状硫化物矿床	100~360	5~10	富含Cu、Pb、Zn等金属元素;挥发性组分为CO₂、CH₄、N₂	海底热液:海水、岩浆热液	/	/	层控	[28-29]
浅成热液矿床	100~450	0~40	富含各种金属元素;挥发分为CO₂、H₂S、CH₄、N₂和SO₂	岩浆热液、大气降水	100~500	1~1.5	断裂系统控制	[30-31]
斑岩型Cu-Mo矿	100~900	0~60	富含Cu、Mo、Na、K、Fe等金属元素的高盐度流体	岩浆热液	几十到几百巴,有时高达1000 bar左右	1~6	断裂系统控制	[32-33]
矽卡岩型矿床	100~600	0~60	富含W、Mo、Cu、Pb、Zn等金属元素	岩浆热液、变质热液、部分大气降水	不同类型的矽卡岩矿床有着不同的成矿压力	1~4.5	褶皱、断裂构造控制	[4]
卡林型金矿	100~300	0~7	富含以Au为主的各种金属元素;主要挥发分为CO₂、H₂S	岩浆热液、变质热液、大气降水	不同类型的卡林型金矿有着不同的成矿压力	2 km左右,甚至达到数千米	层控	[34-35]
造山型金矿	150~350	0~10	富含Na、Ca、K、Mg等金属元素;为H₂O-CO₂-NaCl体系	岩浆热液、变质热液和深循环大气降水	500~1500	3~10	断裂系统控制	[3,36]
胶东型金矿	260~340	2~10	富含Na、K、Mg、Ca等金属元素;为H₂O-CO₂-NaCl-CH₄体系	深部岩浆热液与大气水混合	900~2400	2~10	断裂系统控制	[37-39]