胶东福禄地金矿成矿流体来源和演化特征：来自流体包裹体和H-O同位素证据

王江波; 黄鑫; 宋倩; 高涛; 杨君玺; 李泗龙; 毛光周; 吴霞; 邵玉宝; 王勇军; 崔凯; 王笑丛; 刘洋

doi:10.19509/j.cnki.dzkq.tb20250167

胶东福禄地金矿成矿流体来源和演化特征：来自流体包裹体和H-O同位素证据

doi: 10.19509/j.cnki.dzkq.tb20250167

王江波^{1, 2,},
黄鑫^{1, 3, ,},
宋倩¹,
高涛²,
杨君玺²,
李泗龙¹,
毛光周⁴,
吴霞⁵,
邵玉宝¹,
王勇军¹,
崔凯¹,
王笑丛⁶,
刘洋⁷

1.
山东省煤田地质规划勘察研究院，济南市院士工作站，济南 250104
2.
山东恒邦冶炼股份有限公司，山东烟台 264000
3.
吉林大学地球科学学院，长春 430074
4.
山东科技大学地球科学与工程学院，山东青岛 266590
5.
山东省煤田地质局物探测量队，济南 250104
6.
山东省地矿工程勘察院，山东省地质矿产勘查开发局八〇一水文地质工程地质大队，济南 250014
7.
中国地质大学（武汉）资源学院，武汉 430074

基金项目: 山东省自然科学基金项目（ZR2023QD172）；山东省煤田地质局科研专项项目（鲁煤地科字﹝2023﹞33号）；山东省地勘基金项目（鲁勘字﹝2022﹞32号；鲁勘字﹝2025﹞18号）

详细信息

作者简介:
王江波：E-mail：839966746@qq.com

通讯作者:
E-mail：705018182@qq.com

中图分类号: P618.51；P592
计量
- 文章访问数: 109
- PDF下载量: 22
- 被引次数: 0
出版历程
- 收稿日期: 2025-04-14
- 录用日期: 2025-09-02
- 修回日期: 2025-07-05
- 网络出版日期: 2026-06-24

Source and evolutionary characteristics of ore-forming fluids in Fuludi gold deposit, Jiaodong Peninsula: Evidence from fluid inclusions and H-O isotopes

1.
Shandong Institute of Coalfield Geological Planning and Exploration, Jinan Academician Workstation, Jinan 250104, China
2.
Shandong Hengbang Smelting Co., Ltd., Yantai Shandong 264000, China
3.
School of Earth Sciences, Jilin University, Changchun 430074, China
4.
College of Earth Science and Engineering, Shandong University of Science and Technology, Qingdao Shandong 266590, China
5.
Geophysical Survey Team of Shandong Coalfield Geological Bureau, Jinan 250104, China
6.
Shandong Geological and Mineral Engineering Survey Institute, 801 Hydrogeological Engineering Geological Brigade of Shandong Geological and Mineral Exploration and Development Bureau, Jinan 250014, China
7.
School of Earth Resources, China University of Geosciences (Wuhan), Wuhan 430074, China

More Information

Author Bio:
E-mail：839966746@qq.com

Corresponding author: E-mail：705018182@qq.com

摘要

摘要:
胶东福禄地金矿位于牟平−乳山金成矿带，现有矿床成因研究较为薄弱。为了查明该矿床成矿流体来源与完整演化过程，结合矿区地质特征，开展流体包裹体显微测温、激光拉曼光谱及氢−氧（H-O）同位素综合分析，探讨成矿流体来源与金矿物沉淀机制。依据石英脉穿插关系与共生矿物组合，将成矿作用划分为4个阶段：乳白色石英阶段（Ⅰ）、烟灰色石英+黄铁矿阶段（Ⅱ）、烟灰色石英+多金属硫化物主成矿阶段（Ⅲ）、石英+方解石成矿末期阶段（Ⅳ）。矿石石英中发育纯液相水溶液（L型）包裹体、气液两相（L+V型）包裹体；L+V型包裹体贯穿全部成矿阶段，粒径3～10 μm，形态以长条状、椭圆状、不规则状为主，整体液相占比约80%；L型包裹体仅见于Ⅲ阶段，粒径5～15 μm、多呈椭圆形。激光拉曼分析显示流体主体为CO₂−H₂O体系，伴生CH₄、N₂且组分存在阶段性差异。成矿早期Ⅰ、Ⅱ阶段流体性质稳定，均一温度180.0～240.0 ℃，盐度峰值9.0%～17.0%；主成矿Ⅲ阶段流体发生沸腾，温盐度明显下降，均一温度160.0～200.0 ℃，盐度11.0%～15.0%；末期Ⅳ阶段温盐度进一步降低，均一温度120.0～180.0 ℃，盐度3.0%～11.0%。H-O同位素测试得到δD为−87.0‰～−72.4‰，石英δ¹⁸O为9‰～14‰，计算获得流体水δ¹⁸O_H₂O为−3.98‰～1.82‰。成矿流体以岩浆水与变质水混合为主体，并存在深部幔源组分参与；成矿过程中大气降水持续混入流体体系，流体温压不断降低，叠加流体沸腾、挥发分逸出等作用，造成Au（HS）₂⁻络合物失稳，驱动成矿物质快速沉淀。综合判定，福禄地金矿为典型的中低温、低盐度热液脉型金矿床。
- 福禄地金矿 /
- 成矿流体 /
- 流体包裹体 /
- H−O同位素 /
- 激光拉曼 /
- 水岩反应
Abstract:
Objective
The Fuludi gold deposit is located in the middle segment of the Muping-Rushan gold metallogenic belt, Jiaodong Peninsula, a world-class gold concentration area with substantial gold resources. Previous geological studies on deposits in this belt have mainly focused on gold deposits in its southern and northern sections, while the origin and ore-forming fluid evolution of Fuludi gold deposit have long remained poorly understood. Controversies still exist over the source of ore-forming fluids in the Muping-Rushan belt, with three mainstream viewpoints: Mantle-derived fluid, mixed magmatic fluid and meteoric water, and mixed magmatic water and metamorphic water. Geographically, the Fuludi gold deposit acts as a key link connecting the northern and southern parts of the metallogenic belt. However, previous studies have only carried out basic geological surveys and divided its mineralization stages, and systematic studies on ore-forming fluids have long been lacking. This study aims to clarify the source, spatiotemporal evolution of ore-forming fluids, and gold precipitation mechanism of the Fuludi gold deposit.
Methods
Combined with detailed field and microscopic geological characteristics, this study selected quartz samples from four different mineralization stages to conduct a comprehensive analysis, including fluid inclusion microthermometry, laser Raman spectroscopy, and hydrogen-oxygen (H-O) isotope testing. It systematically analyzed the petrographic characteristics of fluid inclusions, physicochemical parameters of ore-forming fluids, fluid compositions, and isotopic compositions, so as to constrain the fluid source and gold metallogenesis.
Results
According to the cross-cutting relationships of quartz veins and paragenetic mineral assemblages, four mineralization stages were divided: Milky quartz stage (Stage Ⅰ), smoky quartz+pyrite early mineralization stage (Stage Ⅱ), smoky quartz+polymetallic sulfide main mineralization stage (Stage Ⅲ), and quartz+calcite late mineralization stage (Stage Ⅳ). Two types of fluid inclusions were identified in quartz: Pure liquid (L-type) aqueous fluid inclusions and gas-liquid two-phase (L+V-type) fluid inclusions. The L+V-type inclusions occurred throughout all four stages, with particle sizes of 3−10 μm and showing elongated, oval, and irregular shapes. Their liquid-phase proportion gradually increased from Stage Ⅰ to Stage Ⅳ, ultimately reaching approximately 80%. The L-type inclusions only developed in Stage Ⅲ, with a particle size of 5−15 μm and mostly oval shapes. Laser Raman analyses revealed that the ore-forming fluid belonged to the CO₂-H₂O-NaCl system, and its components varied significantly at different stages. CH₄ was detected in Stage Ⅰ, no CH₄ existed in Stage Ⅱ, N₂ appeared in Stage Ⅲ, and only CO₂ and H₂O were found in Stage Ⅳ. Microthermometric results showed that the early Stage Ⅰ and Stage Ⅱ had stable physicochemical conditions, with homogenization temperatures ranging from 180.0 °C to 240.0 °C and salinity peaks of 9.0%−17.0%. Fluid boiling occurred at the main Stage Ⅲ, accompanied by obvious decreases in temperature (160.0-200.0 °C) and salinity (11.0%−15.0%). At the late Stage Ⅳ, temperature (120.0-180.0 °C) and salinity (3.0%−11.0%) decreased further. H-O isotope results showed that δD values ranged from −87.0‰ to −72.4‰, and δ¹⁸O values of quartz were 9.0‰-14.0‰. Calculated by oxygen isotope fractionation equation, the δ¹⁸OH₂O of ore-forming fluid was −3.98‰ to 1.82‰.
Conclusion
The ore-forming fluids are dominated by mixed magmatic water and metamorphic water, and are also accompanied by mantle-derived components originating from volatile degassing of enriched mantle. Meteoric water continuously mixed into the fluid system during mineralization. With the gradual decrease of temperature and pressure, combined with fluid boiling and escape of volatile CO₂, the physicochemical properties of fluids change significantly. These processes broke the stability of ${\mathrm{Au}}({\mathrm{HS}})_2^- $ complexes, which are the main transport carrier of gold, and led to the rapid precipitation of gold and polymetallic minerals. Comprehensive geological and geochemical evidence indicates that the Fuludi gold deposit is a typical medium- to low-temperature, low-salinity quartz vein-type hydrothermal gold deposit controlled by NNE-trending faults. This study fills the research gap on ore-forming fluids in Fuludi gold deposit, and provides reliable geological evidence for regional metallogenic theory and further prospecting work.
- Fuludi gold deposit /
- ore-forming fluid /
- fluid inclusion /
- H-O isotope /
- laser Raman spectroscopy /
- water-rock interaction

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图 1 胶东牟平−乳山成矿带地质图^[4]

Figure 1. Geological map of Mouping-Rushan metallogenic belt in Jiaodong Peninsula

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图 2 福禄地金矿矿区地质图

Figure 2. Geological map of Fuludi gold mining area

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图 3 福禄地金矿不同成矿阶段手标本照片

a. 乳白色石英+少量黄铁矿（Ⅰ）；b. 黄铁矿+烟灰色石英（Ⅱ）；c. 多金属硫化物+烟灰色石英（Ⅲ）；d～f. 成矿各阶段接触关系。Ⅰ～Ⅳ. 成矿阶段编号；Py. 黄铁矿；Qtz. 石英；Gn. 方铅矿；Cal. 方解石；下同

Figure 3. Hand specimen photographs of different mineralization stages of Fuludi gold deposit

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图 4 福禄地金矿黄铁矿及共生矿物背散射电子（BSE）图像

a. 乳白色石英中少量黄铁矿（Ⅰ）；b. 大量黄铁矿产于石英中（Ⅱ）；c. 石英脉中黄铁矿与闪锌矿共生（Ⅲ）；d. 方解石脉与石英黄铁矿共生（Ⅳ）。Sp. 闪锌矿；Lm. 褐铁矿；下同

Figure 4. Backscattered electron (BSE) images of pyrite and associated minerals in Fuludi gold deposit

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图 5 福禄地金矿石英中流体包裹体显微镜下特征

a. L+V型包裹体（Ⅰ）；b. L+V型包裹体（Ⅱ）；c. L+V型包裹体和L型包裹体（Ⅲ）；d. L+V型包裹体（Ⅳ）。L. 纯液相；L+V. 气液两相

Figure 5. Microscopic characteristics of fluid inclusions in quartz of Fuludi gold deposit

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图 6 福禄地金矿石英中流体包裹体均一温度T与盐度w(NaCl)直方图（各子图共用纵坐标，刻度区间独立设置）

Figure 6. Histograms of homogenization temperature and salinity of fluid inclusions in quartz from Fuludi gold deposit

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图 7 福禄地金矿床不同阶段流体包裹体拉曼光谱分析结果

Figure 7. Raman spectroscopy analysis results of fluid inclusions at different stages of Fuludi gold deposit

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图 8 福禄地金矿石英δD-δ¹⁸O同位素组成图^[31]

Figure 8. Isotope composition of quartz δD-δ¹⁸O in Fuludi gold deposit

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表 1 福禄地金矿主要矿物生成顺序

Table 1. Main mineral formation sequence of Fuludi gold deposit

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表 2 福禄地金矿各阶段矿物组合和矿化特征

Table 2. Mineral assemblages and mineralization characteristics at each stage of Fuludi gold deposit

成矿阶段	矿物组合及特征
乳白色石英阶段（Ⅰ）	矿物组合为石英+黄铁矿，石英主要为乳白色，颗粒较大，体积分数约90%，黄铁矿以团块状为主零星分布在石英之中，该阶段是金的早期成矿阶段，矿化较弱，但形成了含金石英脉的主体
黄铁矿−烟灰色石英阶段（Ⅱ）	矿物组合为黄铁矿+石英，多见角砾状或网脉状烟灰色石英，黄铁矿呈它形与石英共生，细粒至粗粒，体积分数约在60%以上，该阶段产生较为强烈的金富集矿化，是金矿形成过程的早期阶段
多金属硫化物−烟灰色石英阶段（Ⅲ）	矿物组合为烟灰色石英+黄铁矿+黄铜矿+方铅矿+闪锌矿，多见它形细粒黄铁矿与多金属硫化物共生赋存于石英脉中，金矿物赋存于各矿物的晶体裂隙、间隙中，以裂隙金为主，该阶段为主要成矿阶段，大多独立形成多金属硫化物脉或叠加在前期破碎石英脉中，形成富矿体
石英−方解石阶段（IV）	矿物组合为白色石英+方解石+黄铁矿，方解石主要呈脉状或条带状充填在石英脉中，可见少量黄铁矿，该阶段接近成矿尾声，基本不含金

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表 3 福禄地金矿石英中流体包裹体测温结果

Table 3. Microthermometric results of fluid inclusions in quartz from Fuludi gold deposit

成矿阶段	样品编号	冰点温度/℃	均一温度/℃	盐度w(NaCl)/%	测量数量/个
Ⅰ	FB16	−8.1～−5.4	178.8～238.1	10.99～17.61	8
Ⅰ	FB18	−7.5～−5.4	187.6～229.6	10.99～16.07	5
Ⅱ	FB13-1	−7.7～−4.8	188.7～235.7	9.18～16.58	8
Ⅱ	FB13-2	−9.1～−4.6	148.2～219.2	9.62～20.28	8
Ⅲ	FB8-1	−8.2～−5.5	165.3～198.8	11.22～17.88	4
	FB8-2	−8.0～−6.0	176.4～182.3	12.39～17.35	4
	FB10-1	−7.5～−5.5	168.2～205.1	11.22～16.07	4
	FB10-2	−6.0～−4.2	167.2～191.1	8.30～12.39	5
Ⅳ	FB2-2	−1.8～−0.4	129.4～168.4	0.72～3.35	4
	FB3	−6.2～−4.1	127.3～177.1	8.08～12.87	3
	FB5	−7.6～−4.6	165.7～187.8	9.18～16.33	3

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表 4 福禄地金矿床氢氧同位素组成

Table 4. Hydrogen-oxygen isotope compositions of Fuludi gold deposit

样品编号	δD/‰	δ¹⁸O/‰	均一温度T/℃	$\delta^{18}{\mathrm{O}}_{{\mathrm{H}}_{2}{\mathrm{O}}} $/‰	成矿阶段
FLD16	−72.4	14	190	1.64	I
FLD18	−77.5	12.9	210	1.82	I
FLD13	−76.9	12.6	180	−0.46	II
FLD8-1	−80.7	11.6	180	−1.46	III
FLD18-2	−87.0	9.0	200	−2.70
FLD10	−74.9	12.2	195	0.18
FLD2	−76.9	11.5	150	−3.98	IV
FLD3	−82.9	11.8	195	−0.22
FLD5	−84.5	12.8	190	0.44

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