Ore-forming fluid characteristics and ore genesis of the Mahuaping tungsten-beryllium deposit in Yunnan: Constraints from fluid inclusions and H-O-He-Ar isotopes
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摘要:
云南麻花坪钨铍矿床是“三江”地区唯一一个钨和铍均达大型的矿床。该矿床的Be-W矿体产于浅变质岩中，其大面积矿化及成矿分带表现出独特的成矿特征，然而因矿区及周边均未揭露到中酸性岩浆岩体，矿床成因不明，制约了其成矿机制的深入研究和进一步的找矿勘查。本文选择该矿床不同成矿阶段的白钨矿、绿柱石、石英、萤石、方解石，通过系统的包裹体岩相学观察、显微测温、激光拉曼及H-O-He-Ar同位素分析，示踪其流体来源和演化过程，探讨其矿床成因。包裹体岩相学及测温结果显示，包裹体以含CO2包裹体及气液两相包裹体最为常见，从阶段Ⅰ到阶段Ⅳ温度为338.64~170.32℃，盐度为5.04%~2.88% NaCleqv，密度为0.70~0.92g/cm3，为中低温中低盐度低密度的H2O-CO2-NaCl体系，且流体温度和盐度均呈现逐渐降低的趋势。计算得出成矿流体的成矿压力为51.25~91.07MPa，成矿深度为3.71~5.84km。H-O同位素分析结果显示，Ⅰ阶段δ18DV-SMOW和δ18OH2O变化范围分别为-73.9‰~-89.8‰和4.42‰~5.63‰，落于岩浆水附近；Ⅱ、Ⅲ、Ⅳ阶段δ18DV-SMOW和δ18OH2O均逐渐减小，明显向大气降水漂移，显示成矿流体主要来源于岩浆水，随着成矿作用的进行，成矿流体中有越来越多的大气降水加入。Ⅰ、Ⅱ、Ⅲ阶段中包裹体3He/4He值为0.11~0.29Ra，位于地幔氦和地壳氦之间(幔源He值为1.64%~4.62%)，且地壳流体占主导地位。40Ar/36Ar值为315.5~687.0，经计算的成矿流体中大气40Ar贡献介于6.33%~56.99%，显示出成矿流体富含大气Ar来源，与大气平衡的饱和大气水参与了成矿。因此，麻花坪钨铍矿的成矿流体是富含地壳放射成因氦的饱和大气降水与富含幔源氦的深源流体两端元混合的结果，同时，深部(3500m标高)样品的He同位素明显高于浅部，暗示隐伏岩体位于深部，成矿流体由深部向浅部运移。综合分析认为，麻花坪钨铍矿床为远端岩浆热液型矿床。
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关键词:
- 钨铍矿床 /
- H-O-He-Ar同位素 /
- 成矿流体 /
- 远端岩浆热液型矿床 /
- 云南麻花坪
Abstract:The Mahuaping tungsten-beryllium deposit is the only deposit with both large scale of tungsten and beryllium reserves in the "Sanjiang" region. The Be-W ore bodies are hosted in epimetamorphic rocks, and the extensive mineralization and metallogenic zoning exhibit unique metallogenic characteristics. No intermediate-acidic magmatic rocks have been exposed in the mining area or its surrounding areas, and the genesis of the deposit remains unclear, which has hindered in-depth research and further exploration. This paper focuses on scheelite, beryl, quartz, fluorite and calcite from different metallogenic stages of the deposit to trace their sources and fluid evolution and discuss the genesis of the deposit through systematic fluid inclusion petrography, microthermometry, Laser Raman spectroscopy, and H-O-He-Ar isotopic analysis. The petrography and thermometric results of the fluid inclusions show that CO2-bearing inclusions and gas-liquid two-phase inclusions are the most common types. From Stage Ⅰ to Stage Ⅳ, the temperature ranges from 338.64℃ to 170.32℃, the salinity ranges from 5.04% to 2.88% NaCleqv, and the density ranges from 0.70g/cm3 to 0.92g/cm3, indicating a medium-low temperature, medium-low salinity, and low-density H2O-CO2-NaCl system. From the early to the late stages, both the temperature and salinity of the fluids show a gradual decreasing trend. The calculated metallogenic pressure of the ore-forming fluids ranges from 51.25MPa to 91.07MPa, and the metallogenic depth ranges from 3.71km to 5.84km. The H-O isotopic results show that in Stage Ⅰ, the δ18DV-SMOW values range from -73.9‰ to -89.8‰, and the δ18OH2O values range from 4.42‰ to 5.63‰, falling near the range of magmatic water. In Stages Ⅱ, Ⅲ and Ⅳ, both δ18DV-SMOW and δ18OH2O gradually decrease, showing a clear shift towards meteoric water, indicating that the ore-forming fluids were primarily derived from magmatic water, with an increasing contribution from meteoric water as the mineralization progressed. The 3He/4He ratios of the inclusions range from 0.11Ra to 0.29Ra, falling in between mantle helium and crustal helium ranges (with mantle-derived He values ranging from 1.64% to 4.62%), indicating crustal fluids dominate. The 40Ar/36Ar ratios range from 315.5 to 687.0, and the calculated contribution of atmospheric 40Ar to the ore-forming fluids ranges from 6.33% to 56.99%, indicating that the ore-forming fluids are rich in atmospheric Ar and that meteoric water in equilibrium with the atmosphere participated in the mineralization. Therefore, the ore-forming fluids of the Mahuaping tungsten-beryllium deposit are the result of mixing between two end-members: the meteoric water saturated with crustal radiogenic helium and the deep-sourced fluids rich in mantle-derived helium. Additionally, the He isotopes in deep-level (elevation 3500m) samples are significantly higher than those in shallow, suggesting that the concealed intrusive body is located at depth and that fluids migrated from deep to shallow. Comprehensive analysis indicates that the Mahuaping tungsten-beryllium deposit is a distal magmatic-hydrothermal deposit.
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图 1
云南麻花坪钨铍矿床大地构造位置(a，据李文昌等, 2010修编)和区域地质简图(b，据云南省地质调查院, 2011①修编)
Figure 1.
Tectonic setting map (a, modified after Li et al., 2010) and simplified geological map of the studied region (b) of the Mahuaping tungsten-beryllium deposit, Yunnan Province
图 2
麻花坪钨铍矿床地质简图(据云南省地质矿产局, 2006①)
Figure 2.
Geological sketch map of the Mahuaping tungsten-beryllium deposit
图 3
麻花坪钨铍矿床A-A′和B-B′地质剖面及采样示意图
Figure 3.
Geological sections A-A′ and B-B′ with sampling locations of the Mahuaping tungsten-beryllium deposit
图 4
麻花坪钨铍矿床矿化阶段及矿物生成次序图
Figure 4.
Mineralization stages and paragenetic sequence of the Mahuaping tungsten-beryllium deposit
图 5
麻花坪钨铍矿床不同矿化阶段矿石及矿物组合图
Figure 5.
Ore and mineral assemblage diagrams of different mineralization stages in the Mahuaping tungsten-beryllium deposit
图 6
麻花坪钨铍矿床流体包裹体显微照片
Figure 6.
Photomicrographs of fluid inclusion in the Mahuaping tungsten-beryllium deposit
图 7
麻花坪钨铍矿床流体包裹体激光拉曼位移图
Figure 7.
Laser Raman shift diagram of fluid inclusions in the Mahuaping tungsten-beryllium deposit
图 8
麻花坪钨铍矿床流体包裹体均一温度、盐度频率直方图
Figure 8.
Histograms of homogenization temperature and salinity frequency of fluid inclusions in the Mahuaping tungsten-beryllium deposit
图 9
麻花坪钨铍矿床流体包裹体温度-盐度-密度图
Figure 9.
Temperature-salinity-density diagram of fluid inclusions in the Mahuaping tungsten-beryllium deposit
图 10
麻花坪钨铍矿流体包裹体成矿流体δ18DV-SMOW-δ18OH2O图解(据Taylor, 1974; 翟建平等, 1995修编)
Figure 10.
δ18DV-SMOW vs. δ18OH2O diagrams of ore-forming fluids from fluid inclusions in the Mahuaping tungsten-beryllium deposit (modified after Taylor, 1974; Zhai et al., 1995)
图 11
麻花坪钨铍矿床He-Ar同位素图解(据Mamyrin and Tolstikhin, 1984; 胡瑞忠等, 1999修编)
Figure 11.
He vs. Ar isotope diagrams of the Mahuaping tungsten-beryllium deposit (modified after Mamyrin and Tolstikhin, 1984; Hu et al., 1999)
表 1
麻花坪钨铍矿床流体包裹体类型
Table 1.
Different types of fluid inclusions in the Mahuaping tungsten-beryllium deposit
包裹体类型 相态 气液比 均一相态 数量比 L-Ⅰ型 Laq+VH2O ＞50% 液相 1% L-Ⅱ型 Laq+VH2O 5%~20% 液相 5.5% V型 Laq+VCO2 ＞80% 气相 3% C-Ⅰ型 Laq+LCO2 — 液相 40% C-Ⅱ型 Laq+LCO2+VCO2 — 液相 50% S型 L+V+S 20%~30% 液相 0.5% 
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表 2
麻花坪钨铍矿床流体包裹体测温数据
Table 2.
Microthermometry data of fluid inclusions from Mahuaping tungsten-beryllium deposit
成矿阶段 寄主矿物 冰点温度(℃) 均一温度(℃) 盐度(% NaCleqv) Ia 白钨矿 -3.3~-3.8 268.7~296.8 5.40~6.20 绿柱石 -1.8~-2.6 258.4~280.9 3.10~4.30 萤石 -2.4~-4.8 260.3~286.3 3.87~7.59 Ib 石英 -1.2~-3.9 261.3~284.9 2.11~6.30 黑钨矿 -3.3~-4.6 272.4~338.6 5.26~7.31 Ⅱ 萤石 -1.7~-3.8 246.2~271.9 2.90~6.08 绿柱石 -2.1~-2.7 252.2~266.8 3.50~4.49 Ⅲ 萤石 -1.5~-2.6 193.4~269.3 2.57~4.30 Ⅳ 石英 -1.4~-1.8 170.3~235.6 2.30~3.10 方解石 -1.7~-1.9 182.2~211.4 2.80~3.23
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表 3
麻花坪钨铍矿不同矿化阶段H-O同位素测试结果
Table 3.
H-O isotope test results of different mineralization stages in the Mahuaping tungsten-beryllium deposit
成矿阶段 样品号 矿物 δDV-SMOW δ18OV-SMOW 平均温度 δ18O水V-SMOW (‰) (K) (‰) Ⅰa MHPKT1-3 白钨矿 -77.0 4.25 546 5.46 MHP3600-4 白钨矿 -79.0 4.00 546 5.21 MHPKT-23 石英 -73.9 12.40 546 4.46 MHPKT1-4 黑钨矿 -76.0 3.89 555 4.05 KSD-5 黑钨矿 -77.0 4.27 555 4.43 23MHP3500-5 石英 -76.7 13.2 555 5.63 Ⅰb KSD-2 石英 -80.5 12.96 555 5.39 KSD-27 石英 -77.2 12.67 555 5.10 MHP3500-7 石英 -77.8 12.35 555 4.78 MHP3500-4 石英 -89.4 12.31 555 4.74 MHP-19 石英 -89.8 12.61 530 4.42 MHP-1-2 石英 -84.6 12.76 530 4.57 Ⅱ MHPKT2+3 萤石 -92.6 — — 2.11 Ⅲ 23MHP3500-1 萤石 -100.8 — — 1.48 Ⅳ 23MHP-1 方解石 -155.2 -11.07 468 -11.55
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表 4
麻花坪钨铍矿不同矿化阶段He-Ar同位素测试结果
Table 4.
He-Ar isotope test results of different mineralization stages in the Mahuaping tungsten-beryllium deposit
样品号 成矿阶段 矿物 40Ar/36Ar 3He/4He 40Ar 4He 40Ar* 幔源He R/Ra (×10-7) (×10-8cm3STP/g) (%) MHPKT2 Ⅰa 萤石 517.2 2.66 26.8 82.20 42.87 3.01 0.19 KSD-31 Ⅰa 白钨矿 687.0 2.20 14.6 107.84 56.99 2.45 0.16 KSD-2 Ⅰb 石英 621.3 2.71 74.1 38.29 52.44 3.06 0.19 23MHP3500-5 Ⅰb 石英 512.6 2.93 102.2 70.17 42.35 3.32 0.21 23MHPKT1-4 Ⅱ 白钨矿 505.3 1.52 30.0 153.65 41.52 1.64 0.11 MHP3500-1 Ⅲ 萤石 315.5 4.02 54.3 41.65 6.33 4.62 0.29
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