Genesis of Mesozoic alkaline granites and biotite granites in Nigeria and its significance for tin-polymetallic prospecting
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摘要:
尼日利亚中生代环状杂岩中产出丰富的含锡(铌钽)等多金属的花岗岩, 其中与成矿相关且占主体的2种岩石类型是碱性花岗岩和黑云母花岗岩, 前者具有含碱性暗色矿物过碱质特征, 后者具有含黑云母过铝质特征。前人对2种共生的岩石对锡(铌钽)成矿作用可能的制约机制还未深入探讨, 综合分析前人研究资料, 为理解非造山A型花岗岩锡(铌钽)成矿作用提供新视角, 进一步明确找矿方向。2种岩石绝大多数在侏罗纪侵位, 但在同一杂岩体中, 碱性花岗岩锆石结晶普遍稍早于黑云母花岗岩, 且前者分异程度稍弱于后者。碱性花岗岩是起源于富集地幔岩浆在极端分离结晶作用下的产物, 但此过程中有部分地壳物质的混染。过铝质黑云母花岗岩并非与造山型过铝质花岗岩一样来自地壳物质的熔融, 它更可能是来自于碱性花岗岩同一母岩浆演化的另一个混染了更多地壳物质的晚期分支。与俯冲背景的成锡花岗岩一样, 尼日利亚锡多金属富集主要与弱过铝质黑云母花岗岩有关, 受岩浆后期出溶流体的显著影响。碱性花岗岩对锡(铌钽)元素的富集程度, 大致代表了未受出溶流体影响时共生黑云母花岗岩的锡(铌钽)含量。成矿物质来源为泛非基底围岩, 元素的富集成矿主要被分离结晶和流体出溶行为控制。尼日利亚不成矿环状杂岩体中, 黑云母花岗岩和碱性花岗岩的锡(铌钽)含量都偏低, 两者的Sn含量范围为4×10-6~13×10-6; 而对于成矿杂岩体, 两者锡(铌钽)含量基本高于不成矿杂岩体, 但其中与成矿密切相关的黑云母花岗岩锡(铌钽)含量反而较碱性花岗岩偏低, 其中碱性花岗岩Sn含量范围为21×10-6~205×10-6, 黑云母花岗岩Sn含量范围为10×10-6~62×10-6, 表明熔体中成矿元素含量高低及后期流体出溶是决定能否成矿的关键。因此, 高锡(铌钽)含量杂岩体中具有较低Sn含量的黑云母花岗岩是寻找锡多金属矿的第一选择。
Abstract:There are tin(niobium and tantalum)polymetallic granites in the Mesozoic ring complexes in Nigeria. The two main series are alkaline granite and biotite granite. The former is mainly characterized by alkaline mafic minerals and the latter is mainly peraluminous series. The possible restriction mechanism of the two main series on tin(niobium and tantalum)mineralization has not been deeply discussed by predecessors. The comprehensive analysis of previous research data in this paper provides a new perspective for understanding the tin(niobium-tantalum)mineralization of non-orogenic A-type granite and further defines the prospecting direction. Two series both emplaced during the Jurassic. In one complex, the alkaline granite crystallized slightly earlier than the biotite granite and the former is slightly weaker in the degree of differentiation than the latter. Alkaline granites were formed through fractional crystallization of enriched mantle-derived magma and contaminated with a small amount of crustal material. Peraluminous biotite granites unlikely came from the melting of crustal material like orogenic peraluminous granites. Peraluminous biotite granites were more likely to come from the same primitive magma as the alkaline granite but belong to another branch contaminated with more crustal material. However, like the ore-forming granites in the subduction background, the tin-polymetallic enrichment is mainly related to the weakly peraluminous biotite granite in Nigeria, which is significantly affected by the exsolution of fluids during the late-magmatic stage. The enrichment of tin(niobium and tantalum)elements in some alkaline granites roughly represent the content of tin(niobium and tantalum)in the paragenetic biotite granites that had been not affected by fluids. The ore-forming materials were mainly from Pan-African basement rocks, and the enrichment of elements is mainly controlled by the fractional crystallization and fluid exsolution. The content of tin(niobium and tantalum)in the unmineralized ring complexes in Nigeria is relatively low in biotite granite and alkaline granite, whose Sn content range from 4×10-6 to 13×10-6. As for the mineralized ring complexes, the content of tin(niobium and tantalum)is higher than that of the unmineralized complexes. However, the content of tin(niobium and tantalum)in the biotite granite closely related to mineralization is lower than that of the alkaline granite. Sn content range of these alkaline granites and biotite granites are from 21×10-6 to 205×10-6 and 10×10-6 to 62×10-6, respectively. The above evidence shows that the content of ore-forming elements in the melt and the later exsolution of hydrothermal fluids are the key factors to determine the mineralization. Therefore, the biotite granite with low tin(-niobium and tantalum)content in the ring complexes with corresponding high ore-forming elements is the first choice for searching for tin polymetallic deposits.
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Key words:
- alkaline granite /
- anorogenic /
- Jurassic /
- West Africa /
- niobium and tantalum /
- tin-polymetallic deposit
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图 1 尼日利亚构造划分和稀有金属成矿带简图(据Obaje，2009修改)
Figure 1.
图 2 尼日利亚环状杂岩和锡-铌钽矿点地质简图(据Kinnaird, 1981修改)
Figure 2.
图 3 尼日利亚Ririwai杂岩体地质简图(据Girei et al., 2019修改)
Figure 3.
图 5 尼日利亚Kudaru杂岩体地质简图(据Kamaunji et al., 2020修改)
Figure 5.
图 6 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗岩SiO2-(Na2O+K2O)图解(尼日利亚数据据Girei et al., 2019；2020；Amuda et al., 2020；Kamaunji et al., 2020；Ahmed et al., 2021; 马来西亚数据据Cao et al., 2020；Du et al., 2020；Liu et al., 2020；缅甸数据据Li et al., 2018；底图据Middlemost，1994)
Figure 6.
图 7 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩SiO2-K2O图解(数据来源同图 6，底图据Peccerillo et al., 1976)
Figure 7.
图 8 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩A/CNK-A/NK图解(数据来源同图 6)
Figure 8.
图 9 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩稀土元素配分模式图(数据来源和图 6相同，标准化数据来自Sun et al., 1989)
Figure 9.
图 10 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩微量元素蛛网图(数据来源同图 6，标准化数据据Sun et al., 1989)
Figure 10.
图 11 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩(Zr+Nb+Ce+Y)-(Na2O+K2O)/CaO图解和10000Ga/Al-Y图(数据来源同图 6，底图据Whalen et al., 1987)
Figure 11.
图 12 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩Ta-Nb/Ta变异图解(数据来源同图 6，底图据Ballouard et al., 2020)
Figure 12.
图 13 尼日利亚Kudaru、Ririwai、Amo、Jos、Pankshin、Zaranda、Ropp、Dutsen Wai和Mada花岗质岩Nd和Hf同位素图解(数据据Dada et al., 1995；Dickin et al., 1991；Girei et al., 2019；2020；Kamaunji et al., 2020；Ahmed et al., 2021)
Figure 13.
图 14 尼日利亚Kudaru、Ririwai、Dutsen Wai、Ropp、Zaranda和Mada花岗质岩Ta-Sn(a)和Nb-Sn(b) 微量元素协变图(数据来源同图 6)
Figure 14.
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