Geochronology, geochemistry of lamprophyre and evidence of mantle fluid in the western part of Xiangshan uranium orefield
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摘要:
研究目的 幔源岩浆是探讨深部动力学演化和铀成矿的研究对象，相山铀矿田基性岩脉是探讨区域岩浆演化和铀成矿的关键所在。
研究方法 本文对矿区西部煌斑岩脉进行了系统的岩石学、地质年代学和地球化学综合研究。
研究结果 本区存在3期煌斑岩，分别为134 Ma、120~125 Ma和84.5 Ma。该区煌斑岩为钠质碱性煌斑岩，富集LILE和LREE，亏损HFSE，具明显的Ta−Nb−Ti负异常，具有岛弧玄武岩和大陆地壳的微量元素特征。该区煌斑岩为部分熔融和结晶分异共同作用的产物，经历了橄榄石、单斜辉石的结晶分异作用，在岩浆上侵过程中受到明显上地壳物质的混染。该区煌斑岩形成于伸展作用下的板内拉张构造环境，未受到古太平洋板块俯冲作用的影响。其源区应为软流圈亏损地幔与岩石圈富集地幔的混合，且主要体现为软流圈亏损地幔特征。
结论 第一期煌斑岩矿岩时差大，仅为后期铀的沉淀富集提供有利条件；后两期煌斑岩矿岩时差小，不仅为相山矿田铀矿化提供了幔源流体（ΣCO2矿化剂和He），也为铀沉淀富集提供还原障。
Abstract:This paper is the result of mineral exploration engineering.
Objective Mantle−derived magma generally provied an object to reveal geodynamic evolution in the depth and uranium mineralization. The mafic dikes in the west of Xiangshan uranium deposit are regarded as a key aspect to understand the regional tectono−magmatic evolution and uranium mineralization.
Methods In this paper, the comprehensive research of petrology, geochronology and geochemistry were carried on the lamprophyre in the west of Xiangshan uranium deposit.
Results There are three stages of lamprophyre in this area, which are 134 Ma, 120–125 Ma and 84.5 Ma. The lamprophyre is sodium−alkaline lamprophyre and characterized with the enrichment of LILE and LREE, depletion of HFSE, and obvious negative anomaly of Ta–Nb–Ti. The lamprophyre is the product of partal melting from the source region and crystallisation differentiation, which experienced the crystallization differentiation of olivine and clinopyroxene as well as strong assimilation and contamination of upper crustal meterials during the magmatic intrusion. The lamprophyre was formed in the extentional entraplate tensioned tectonic environment, and was not affected by the subduction of the ancient Pacific Plate. The source region is a mixture of asthenospheric depleted mantle (main source) and lithospheric enriched mantle, which is mainly characterized by asthenospheric depleted mantle.
Conclusions The first period of lamprophyres is much older than the age of uranium mineralization, only providing favorable conditions for uranium accumulation. The later two periods of lamprophyres are closely associated with uranium deposits on space and time, possibly providing mantle hydrothemal fluids (∑CO2 and He) and a favorable reducing environment for uranium enrichment and deposition.
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图 3 相山矿田煌斑岩SiO2–(Na2O+K2O)图（a，据Rock, 1987）和K/(K+Na)–K/Al（b，据路凤香等, 1991）
Figure 3.
图 4 煌斑岩原始地幔标准化微量元素蛛网图（a，标准化数据值据Sun and McDonough, 1989）和球粒陨石标准化REE配分模式图（b，标准化数据值据Boynton, 1984）
Figure 4.
图 5 相山矿田煌斑岩同化混染判别图解207Pb/204Pb–206Pb/204Pb图解（a）和208Pb/204Pb–206Pb/204Pb图解（b）（据Zartman and Doe, 1981）
Figure 5.
表 1 煌斑岩取样位置
Table 1. Sampling locations of larmprophyre
序号 样品编号 样品位置 孔号 孔深/m 1 ZK1−2−301 ZK56-102 477.50~478.30 2 ZK1−2−303 479.05~479.80 3 ZK1−2−301 ZK52-23 483.85~484.75 4 ZK1−2−303 485.70~486.65 5 ZK1−2−307 287.25~288.15 6 ZK1−2−311 291.00~291.90 7 ZK1−2−301 ZK56-101 298.00~298.30 8 ZK1−2−303 298.60~299.00 9 ZK1−2−301 ZK84-102 448.20~448.40 10 ZK1−2−303 448.60~448.80 
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表 2 相山矿田煌斑岩全岩K−Ar稀释法年龄测试结果
Table 2. Results of whole−rock K−Ar ages of lamprophyres with the dilutional method in Xiangshan orefield
序号 样品编号 岩性 40K/10−2 40Ar/10−6 40Ar/40K 空氩/10−2 年龄/Ma 活动期次 1 ZK1−2−303 煌斑岩 2.310 0.013860 0.005028 13.0 84.5 第三期 2 ZK1−2−303 煌斑岩 1.120 0.009601 0.007185 13.7 120 第二期 3 ZK1−2−303 煌斑岩 2.053 0.018350 0.007490 6.00 125 4 ZK1−2−303 煌斑岩 2.247 0.021570 0.008047 11.2 134 第一期
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表 3 相山矿田煌斑岩主量元素（%）、微量（10−6）元素测试结果
Table 3. Analytical results of major element (%) and trace element (10−6) of lamprohyres in Xiangshan orefield
ZK1−2−301 ZK1−2−303 ZK1−2−301 ZK1−2−303 ZK1−2−307 ZK1−2−311 ZK1−2−301 ZK1−2−303 ZK1−2−301 ZK1−2−303 SiO2 51.00 44.90 44.30 42.40 42.20 53.12 47.90 54.40 51.10 49.30 TiO2 1.22 1.36 1.36 1.34 1.24 0.91 1.48 1.08 1.01 1.00 Al2O3 14.70 13.40 12.30 12.20 12.10 20.27 14.70 12.50 13.52 11.70 Fe2O3 6.95 5.80 4.25 4.85 4.90 6.00 5.20 5.25 6.45 4.50 FeO 10.40 8.81 10.40 11.60 10.00 8.79 9.23 9.15 9.03 7.13 MnO 0.12 0.17 0.19 0.19 0.24 0.19 0.18 0.14 0.13 0.18 MgO 7.22 7.50 11.20 13.60 12.60 3.50 6.35 5.66 6.89 4.85 CaO 3.82 9.51 7.14 7.64 9.05 1.09 6.68 5.27 5.48 10.20 Na2O 1.24 2.08 2.44 1.78 1.58 0.16 3.94 1.70 2.16 1.72 K2O 3.22 1.83 1.96 1.60 1.21 5.56 1.60 2.39 1.99 2.92 P2O5 0.27 0.30 0.54 0.50 0.49 0.19 0.29 0.23 0.28 0.22 LOI 6.73 9.96 7.96 7.35 9.34 3.22 7.29 7.27 2.85 10.27 Cr 256 411 341 354 359 95.40 283 179 26.30 245 Ni 128 149 172 193 166 38.20 116 93.30 11.60 96.60 Rb 154 148 124 104 39.3 125 93.10 105 145 132 Ba 603 60.70 527 706 1083 605 138 303 234 568 Th 15.30 8.53 9.76 8.68 8.62 9.34 9.18 13.70 22.40 10.70 U 5.620 5.400 2.730 1.990 2.160 2.750 9.460 3.440 7.410 3.260 Nb 22.20 21.10 16.70 13.90 14.50 12.40 19.70 18.40 15.60 16.70 Ta 1.620 1.160 0.920 0.770 0.810 0.870 1.350 1.290 1.600 1.090 Sr 142 299 480 598 744 91.50 145 174 73.40 258 Zr 239 175 252 226 226 251 197 183 127 177 Hf 6.390 4.230 5.800 5.120 5.420 6.430 5.560 4.920 4.130 4.410 Tl 1.010 0.710 0.810 0.590 0.350 0.100 0.720 0.580 0.830 0.840 Y 27.00 23.20 26.50 23.90 22.00 26.60 30.30 24.10 24.40 23.90 Li 229 165 148 154 169 82.60 154 234 64.9 145 Be 4.580 3.510 2.380 2.160 1.410 2.130 4.880 4.360 2.500 3.910 Sc 22.90 25.50 26.80 29.60 27.40 14.00 24.00 18.40 5.910 21.30 V 141 162 197 193 188 106 164 120 30.00 126 Co 34.80 33.70 42.50 46.30 37.30 16.80 34.70 28.40 5.110 27.00 Cu 72.30 37.60 50.10 46.80 38.10 65.90 95.00 59.60 12.20 62.50 Zn 104 90.0 90.20 86.60 86.40 102 86.50 87.60 43.00 68.70 Ga 19.80 21.20 16.30 17.50 15.90 17.30 25.20 16.70 17.10 14.80 Mo 1.780 1.020 0.235 0.156 0.499 0.419 2.850 2.470 2.800 1.030 Cd 0.080 0.130 0.100 0.130 0.120 0.050 0.090 0.080 0.070 0.140 In 0.080 0.060 0.060 0.050 0.060 0.050 0.060 0.050 0.060 0.050 Sb 0.400 0.690 0.190 0.170 0.480 0.300 1.270 0.610 0.510 0.830 Cs 9.530 36.70 27.50 33.20 31.10 15.00 7.190 9.490 14.00 9.040 W 6.270 4.130 2.530 1.620 0.970 2.230 6.100 4.980 4.660 4.470 Re 0.004 0.001 0.002 0.002 — 0.001 0.001 0.004 0.004 0.002 Pb 7.990 13.60 8.290 7.940 9.700 7.920 15.80 15.90 18.20 19.60 Bi 0.280 0.150 0.080 0.080 0.040 0.150 0.250 0.310 0.500 0.150 La 43.90 35.10 51.40 41.30 43.50 35.60 37.80 42.70 63.30 33.90 Ce 83.90 67.10 92.20 80.00 80.60 66.80 72.10 77.80 114.0 64.80 Pr 10.30 8.240 11.40 10.30 10.10 8.060 8.830 9.490 13.30 7.680 Nd 39.60 32.50 46.30 42.40 39.40 32.20 34.30 35.80 48.80 29.90 Sm 6.960 5.780 8.180 7.660 6.980 5.980 6.360 6.250 8.300 5.600 Eu 1.390 1.560 2.490 2.220 2.250 1.470 1.750 1.310 0.900 1.310 Gd 6.130 5.130 7.060 6.630 6.210 5.410 5.810 5.270 6.570 5.360 Tb 1.030 0.860 1.100 1.030 0.960 0.980 1.070 0.890 1.050 0.880 Dy 5.530 4.620 5.640 5.120 4.720 5.510 6.010 4.730 5.350 4.750 Er 3.180 2.540 2.860 2.550 2.530 2.920 3.590 2.640 2.690 2.520 Tm 0.490 0.390 0.440 0.380 0.360 0.480 0.540 0.400 0.440 0.400 Yb 3.070 2.560 2.900 2.340 2.460 2.950 3.530 2.570 2.650 2.440 Lu 0.630 0.610 0.630 0.540 0.620 0.600 0.590 0.680 0.760 0.610 REE 206.11 166.99 232.60 202.47 200.70 168.96 182.29 190.53 268.12 160.14 (La/Yb)N 9.64 9.24 11.95 11.90 11.92 8.14 7.22 11.20 16.10 9.37 (Gd/Yb)N 1.61 1.62 1.96 2.29 2.04 1.48 1.33 1.65 2.00 1.77 (La/Sm)N 3.97 3.82 3.95 3.39 3.92 3.74 3.74 4.30 4.80 3.81 δEu 0.65 0.88 1.00 0.95 1.04 0.79 0.88 0.70 0.37 0.73 δCe 0.95 0.95 0.92 0.93 0.93 0.95 0.95 0.93 0.95 0.97
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表 4 相山矿田煌斑岩Sr–Nd–Pb同位素组成
Table 4. Sr–Nd–Pb isotopic composition of lamprophyres in the Xiangshan orefield
ZK1−2−303 ZK1−2−303 ZK1−2−303 147Sm/144Nd 0.1075 0.1055 0.1232 143Nd/144Nd 0.5124 0.5123 0.5123 (143Nd/144Nd)i 0.5123 0.5122 0.5123 87Rb/86Sr 1.4333 1.7474 1.4815 87Sr/86Sr 0.7155 0.7144 0.7135 (87Sr/86Sr)i 0.7128 0.7113 0.7117 208Pb/204Pb 38.8060 38.8940 38.7810 207Pb/204Pb 15.6270 15.6180 15.8150 206Pb/204Pb 18.8270 18.6120 18.6270 (208Pb/204Pb)i 38.5190 38.5400 38.6300 (207Pb/204Pb)i 15.6010 15.6050 15.6050 (206Pb/204Pb)i 18.2920 18.3410 18.5320 εNd(t) −3.25 −4.76 −5.37 注：样品87Rb/86Sr比值根据微量元素含量（表2）和87Sr/86Sr测量值计算得到；样品147Sm/144Nd比值根据微量元素含量（表2）和143Nd/144Nd测量值计算得到。
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表 5 相山矿田煌斑岩同化混染微量元素比值
Table 5. Ratios of trace elements of lamprophyres assimilation and contamination in the Xiangshan orefield
相山矿田 同化混染 未同化混染 备注 Yi/Yb 1849~3488 <5000 >5000 Hart et al., 1989 Ba/Nb 15.00~74.69 >10 <10 Furman et al., 2006 La/Nb 1.92~4.06 >1 <1 (Th/Nb)N 3.39~12.05 >1 <1 夏林圻等, 2007 Nb/La 0.24~0.60 <1 ≥1 夏林圻等, 2007
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表 6 相山矿田煌斑岩构造环境判别
Table 6. Environmental discrimination of lamprophyres in Xiangshan orefield
相山矿田煌斑岩 大陆玄武岩 岛弧玄武岩 未受到大陆岩石圈混染 受大陆岩石圈混染 具古老基底 较年轻岛弧
增生地体不相容微量元素浓度 高于消减带玄武岩 高于消减带玄武岩 等同于消减带玄武岩 Nb、Ta、Ti Nb–Ta–Ti负异常 “隆起状”似OIB不相容元素配分模式 Nb–Ta–Ti负异常 Nb–Ta–Ti负异常 Nb/La 0.25~0.60 ≥1 <1 <1 εNd(t) −3.25 ~ −5.37 中等正值 低负值 高正值 高正值 87Sr/86Sr(t) 0.713485~0.714443 低—中等 中等—高 低 低 各种地球化学
判别图中位置在不利用Nb–Ta–Ti作为判别因子的图解中，仍具WPB的特性 恒定于WPB成分域中 在不利用Nb–Ta–Ti作为判别因子的图解中，仍然具有WPB的特性 恒定于弧玄武岩成分域中
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