Petrogenesis and Geological Significance of Highly Differentiated A⁃Type Granites in Bankeng Pluton, Nanling Region, South China
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摘要:
我国稀土资源丰富，其中华南离子吸附型稀土矿床独具特色，其时空分布特征显示其形成与华南中生代花岗岩密切有关，但内在成因联系仍缺乏深刻认识.对南岭半坑花岗岩（半坑稀土矿床的成矿母岩）开展了岩相学、锆石和磷灰石年代学、岩石地球化学、锆石Hf同位素和全岩Sr⁃Nd⁃Li同位素等综合研究.半坑花岗岩中岩浆锆石、岩浆磷灰石的U⁃Pb年代学分析结果分别为185.5~194.0 Ma和~189.2 Ma，表明其侵位形成于早侏罗世.矿物组成主要由长英质矿物（Q+Ab+ Or≥95%）组成，镁铁质暗色矿物仅有少量黑云母（< 5%）；岩石地球化学特征呈现高SiO2（75.93%~77.48%）、富K2O（5.27%~5.55%）、低MgO（0.09%~0.14%）、贫MnO（0.02%~0.03%），较高的锆饱和温度（801~847 ℃）和高Zr+Nb+Ce+Y含量（360×10‒6~534×10‒6）和10 000×Ga/Al比值（3.2~4.2）等，表明其具有高分异A型花岗岩的属性.Sr⁃Nd⁃Hf⁃Li同位素特征（（87Sr/86Sr）i=0.704 477~0.712 715，εNd（t）=-5.0~-5.2，εHf（t）=-6.8~+1.4，δ7Li=-0.88‰~6.65‰）表明其岩浆源区可能为中元古代古老地壳物质熔融并侵位于地壳浅部的富集轻稀土的火成岩.半坑花岗岩呈现A2型花岗岩属性（Y/Nb=1.21~2.09），结合区域同期的双峰式侵入岩、火山岩组合和A型花岗岩共同指示其形成于早侏罗世伸展构造背景.结合与半坑花岗岩同期的南岭地区A型花岗岩的成因认识，认为早侏罗世深部软流圈上涌产生的热异常，引起壳‒幔岩浆源区富稀土岩石的部分熔融形成更加富集稀土的A型花岗质熔体，可能是华南离子吸附型轻稀土矿床成矿母岩形成的重要机制之一.富轻稀土的半坑花岗岩与富重稀土的足洞花岗岩的成因对比表明轻稀土型成矿母岩的形成主要受控于岩浆源区与伸展构造背景，而岩浆结晶分异程度和外部流体交代作用对重稀土型成矿母岩的形成更为关键.
Abstract:The rare earth element (REE) resources are rich in China, among which the ion-adsorbed REE deposit in South China is unique. Its spatial and temporal distribution characteristics indicate that its formation is closely related to the Mesozoic granites in South China, but the internal genetic relationship is still not deeply understood. A comprehensive study on the Bankeng granite in the Nanling (the ore-forming parent rock of Bankeng REE deposit) has been carried out, including petrography, zircon and apatite chronology, lithogeochemistry, zircon Hf isotopes and whole-rock Sr⁃Nd⁃Li isotopes. The U⁃Pb dating of magmatic zircon and magmatic apatite in the Bankeng granites yield ages of 185.5-194.0 Ma and 189.2 Ma respectively, indicating that the emplacement occurred in the Early Jurassic. They are mainly composed of felsic minerals (Q+Ab+Or≥95%), with only a small amount of biotite (< 5%) in the mafic dark minerals. Their geochemical characteristics show high SiO2 (75.93%-77.48%), rich K2O (5.27%-5.55%), low MgO (0.09%-0.14%), and poor MnO (0.02%-0.03%), as well as a high zircon saturation temperature (801-847 ℃), high Zr+Nb+Ce+Y content (360×10‒6-534×10‒6), and a 10 000×Ga/Al ratio (3.2-4.2), which are similar to the highly differentiated A-type granites. The Sr⁃Nd⁃Hf⁃Li isotopic characteristics ((87Sr/86Sr)i=0.704 477-0.712 715, εNd(t)=-5.0-(-5.2), εHf(t)=-6.8-(+1.4), δ7Li=-0.88‰-6.65‰) indicate that the magma source may be REE-rich igneous rocks from Mesoproterozoic recycled ancient crust that was intruded into the shallow crust. The Bankeng granites exhibits A2-type granite properties (Y/Nb=1.21-2.09), combined with the regional contemporaneous bimodal intrusive rocks, volcanic rock suites and A-type granitoids, indicating they formed in the Early Jurassic extensional tectonic setting. Combined with the genetic understanding of A-type granite in the Nanling at the same time as Bankeng granites, this paper suggests that the thermal anomaly generated by the upwelling of deep asthenosphere in the Early Jurassic caused partial melting of REE-rich rocks in the crust-mantle magmatic source area to form more REE-enriched A-type granitic melt, which may be one of the important mechanisms for the petrogenesis of ore-forming parent rocks of the ion-adsorbed light REE deposits in South China. The genetic correlation between the LREE-riched Bankeng granites and the HREE-riched Zudong granites shows that the petrogenesis of the LREE-type ore-forming parent rocks is mainly related to their magma source region and extensional tectonic setting, while the degree of magma crystallization differentiation and the external fluid metasomatism are more critical for the petrogenesis of the HREE-type ore-forming parent rocks.
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图 1 华南中生代花岗岩与离子吸附型稀土矿床的空间分布
据Jiang et al.（2022）和 Chu et al.（2024）修改. 底图来自自然资源部标准地图服务系统，底图审图号为GS（2016）1569号
Fig. 1. Map showing the distribution of Mesozoic granites and ion-adsorbed rare earth element deposits in South China
图 2 江西省龙南地区地质简图
据江西省重工业局和广东省地质局，1970，区域地质矿产调查报告（龙南幅，1∶200 000）
Fig. 2. Geological sketch map of the Longnan area, Jiangxi
图 3 半坑花岗岩岩石学特征
a.半坑黑云母钾长花岗岩风化壳照片；b.手标本照片；c.单偏光显微照片；d.正交偏光显微照片. 矿物代号：Q.石英；Kfs.钾长石；Mc.微斜长石；Bt.黑云母；Zrn.锆石；Aln.褐帘石；Ap.磷灰石；Ep.绿帘石
Fig. 3. Petrological characteristics of the Bankeng granite
图 4 半坑花岗岩中锆石矿物特征与U⁃Pb年龄
a.锆石透射光照片；b.锆石阴极发光照片，实线圆代表LA-MC-ICPMS U-Pb年龄激光束斑位置，虚线圆代表LA-MC-ICPMS Hf同位素激光束斑位置；c.锆石稀土配分曲线，球粒陨石标准数据分别引自Boynton（1984）；d.锆石U-Pb年龄
Fig. 4. Mineral characteristics of zircon in the Bankeng granite and its U⁃Pb age
图 5 半坑花岗岩中磷灰石矿物特征与U⁃Pb年龄
a.磷灰石透射光照片；b.磷灰石阴极发光照片，实线圆代表LA-ICPMS U-Pb年龄激光束斑位置；c.磷灰石稀土配分曲线，球粒陨石标准数据分别引自Boynton（1984），I型、S型花岗岩稀土曲线区域据Sha and Chappell（1999）；d.磷灰石U⁃Pb年龄
Fig. 5. Mineral characteristics of apatite in the Bankeng granite and and its U⁃Pb age
图 7 半坑花岗岩的主量元素特征
a.（Na2O+K2O）vs. SiO2（底图据Middlemost，1994）；b. K2O vs.SiO2（底图据Peccerillo and Taylor，1976）；c.A/NK vs.A/CNK（底图据Maniar and Piccoli，1989）；d.FeOT/（FeOT+MgO）vs. SiO2（底图据Frost et al.， 2001）. 1.南岭J1辉长‒辉绿岩（数据来自Li et al.， 2003；Xie et al.， 2005；Hsieh et al.， 2008；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015；Wang et al.， 2015；Gan et al.， 2017a；Zhang et al.， 2018；Yang et al.， 2021）；2.南岭J1正长岩（数据来自Li et al.， 2003；Chen et al.， 2005；He et al.， 2010；Yang et al.， 2021）；3.南岭J1 A型花岗岩（数据来自Li et al.， 2003；Chen et al.， 2005；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015，2017，2022；甘成势等，2016；Gan et al.， 2017b，2022；Zhou et al.， 2018；Yang et al.， 2021；Zhao et al.， 2021）；4.半坑花岗岩（本文数据）
Fig. 7. Major element characteristics of the Bankeng granite
图 8 （a）球粒陨石标准化的稀土元素配分图与（b）原始地幔标准化的微量元素蛛网图
球粒陨石、原始地幔标准数据分别引自Boynton（1984）和Sun and McDonough（1989）. 1.南岭J1 A型花岗岩（数据来自Li et al.， 2003；Chen et al.， 2005；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015，2017，2022；甘成势等，2016；Gan et al.， 2017b，2022；Zhou et al.， 2018；Yang et al.， 2021；Zhao et al.， 2021）；2.半坑花岗岩（本文数据）
Fig. 8. (a) Chondrite-normalized REE patterns and (b) primitive-mantle-normalized trace element patterns
图 9 半坑花岗岩Sr⁃Nd同位素特征
图a底图据Jiang et al.， 2017. 1.南岭J1辉长‒辉绿岩（数据来自Li et al.， 2003；Xie et al.， 2005；Hsieh et al.， 2008；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015；Wang et al.， 2015；Gan et al.， 2017a；Zhang et al.， 2018；Yang et al.， 2021）；2.南岭J1正长岩（数据来自Li et al.， 2003；Chen et al.， 2005；Yang et al.， 2021）；3.南岭J1 A型花岗岩（数据来自Li et al.， 2003；Chen et al.， 2005；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015，2017，2022；甘成势等，2016；Gan et al.， 2017b，2022；Zhou et al.， 2018；Yang et al.， 2021；Zhao et al.， 2021）；4.半坑花岗岩（本文数据）
Fig. 9. Sr⁃Nd isotope characteristics of the Bankeng granite
图 10 半坑花岗岩Li同位素特征
1.地幔岩石（数据来自Magna et al.， 2006；Lai et al.，2015）；2.下地壳岩石（数据来自Teng et al.， 2008）；；3.中地壳岩石（数据来自Teng et al.， 2008）；4.上地壳岩石（数据来自Sauzéat et al.， 2015）；5.碱性A型花岗岩（数据来自Teng et al.， 2009）；6.铝质A型花岗岩（数据来自Teng et al.，2009）；7.半坑花岗岩（本文数据）
Fig. 10. Li isotopes characteristics of the Bankeng granite
图 11 半坑花岗岩的岩石成因判别图解
a.锆饱和温度Tzr据Watson and Harrison，1983计算，I型、S型和A型Tzr据King et al.， 2001；b.据Whalen et al.， 1987；c.据吴福元等，2017；d.底图据Wang et al.， 2012. 1.南岭J1 A型花岗岩（数据来自Li et al.，2003；Chen et al.， 2005；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015，2017，2022；甘成势等，2016；Gan et al.， 2017b，2022；Zhou et al.， 2018；Yang et al.， 2021；Zhao et al.， 2021）；2.半坑花岗岩（本文数据）
Fig. 11. Petrogenetic discrimination diagrams of the Bankeng granite
图 12 A型花岗岩分类图解
底图据Eby（1992）. 1.南岭J1 A型花岗岩（数据来自Li et al.， 2003；Chen et al.， 2005；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015，2017，2022；甘成势等，2016；Gan et al.， 2017b，2022；Zhou et al.， 2018；Yang et al.， 2021；Zhao et al.， 2021）；2.半坑花岗岩（本文数据）
Fig. 12. Classification diagram of A-type granite
图 13 成矿母岩中稀土含量与岩浆分异程度的相关关系
1.南岭J1 A型花岗岩（数据来自Li et al.， 2003；Chen et al.， 2005；He et al.， 2010；Zhu et al.， 2010；Jiang et al.， 2015，2017，2022；甘成势等，2016；Gan et al.， 2017b，2022；Zhou et al.， 2018；Yang et al.， 2021；Zhao et al.， 2021）；2. 半坑花岗岩（本文数据）；3.足洞花岗闪长岩（数据来自Fan et al.， 2023）；4.足洞二云母花岗岩（数据来自Fan et al.， 2023）；5足洞白云母碱长花岗岩（数据来自Li et al.， 2019；Fan et al.， 2023）
Fig. 13. The correlation between the REEY contents in the ore-forming parent rock and the differentiation degree of magma
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