江西大湖塘中生代花岗岩的成因与构造指示意义:年代学、矿物化学、地球化学与Lu-Hf同位素制约
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摘要
江西大湖塘地区发育多期次与钨、铜、钼多金属成矿关系密切的中生代花岗岩。本文对该地区出露的似斑状黑云母二长花岗岩和黑云母花岗斑岩进行矿物化学、岩石地球化学、锆石U-Pb年代学和Lu-Hf同位素研究。其中似斑状黑云母二长花岗岩样品的成岩年龄分别为145.6±1.4 Ma(昆山岩体)、148.4±2.4 Ma(燕子崖岩体中部)和145.7±2.9 Ma(燕子崖岩体边部);黑云母花岗斑岩成岩时代为143.7±2.4 Ma(狮尾洞岩体),四者的继承锆石均来自新元古代花岗岩源区。岩石地球化学特征显示主量元素特征相似,似斑状黑云母二长花岗岩和黑云母花岗斑岩普遍高硅(SiO_2分别为72.37%～73.33%和70.16%～73.8%);富铝,二者铝饱和指数A/CNK分别为1.23～1.47和1.30～3.02,均属过铝质高钾钙碱性系列,而稀土、微量元素特征存在明显差异,其中似斑状黑云母二长花岗岩轻重稀土分馏明显,(La/Yb)_N平均为26.18,Eu负异常明显,稀土元素配分曲线呈明显右倾型,富集大离子亲石元素(LILE)Cs、Rb、Th、U、K、Pb,亏损高场强元素(HFSE)Zr、Nb、Ti、Y,低Ba、Sr;而黑云母花岗斑岩轻重稀土分馏不显著,(La/Yb)_N平均为9.76,Eu负异常明显,稀土元素配分曲线呈"海鸥型",并显示"M"型四分组效应,微量元素富集LILE,亏损HFSE。似斑状黑云母二长花岗岩的锆石ε_(Hf)(t)值为-7.39～-5.19,两阶段模式年龄(T_(DM2))为1.53～1.67 Ga。综合分析表明,大湖塘晚侏罗世似斑状黑云母二长花岗岩应产于古太平洋板块向华南板块俯冲的构造背景之下,由中上地壳的新元古代黑云母花岗闪长岩部分熔融形成;而早白垩世黑云母花岗斑岩形成于古太平洋板块向华南板块俯冲—俯冲后伸展的构造转换背景之下,由于软流圈地幔上涌,诱发上地壳新元古代黑云母二长花岗岩部分熔融,且在结晶分异过程中还受到富Cl流体的交代。
The Dahutang area in Jiangxi Province developed multiple-phased granitiods during the Late Mesozoic, which are closely associated with W-Cu-Mo mineralization. This paper performed the study of mineral chemistry, geochemistry, zircon U-Pb chronology and Lu-Hf isotope for porphyric-like biotite monzogranite and biotite granite porphyry from the study area. The results show that the porphyric-like biotite monzogranite formed at 145.6±1.4 Ma(Kunshan Pluton), 148.4±2.4 Ma(in the center of Yanziya Pluton) and 145.7±2.9 Ma(the edge of Yanziya Pluton), and the biotite granite porphyry formed at 143.7±2.4 Ma(Shiweidong Pluton). All the captured zircons in four samples were derived from the surrounding granitoids of Neoproterozoic. The geochemical characteristics show that the porphyric-like biotite monzogranite and biotite granite porphyry are similarly high in SiO_2(72.37%～73.33% and 70.16%～73.8%, respectively), rich in Al with the aluminum saturation index A/CNK of 1.23～1.47 and 1.30～3.02, respectively; suggesting a high high-K calc-alkaline series. Rare earth and trace elements analyses show distinct differences between the porphyric-like biotite monzogranite and biotite granite porphyry. The porphyric-like biotite monzogranite is characterized by distinct HREE and LREE fractionation with an average(La/Yb)_Nof 26.18 and obvious right leaning of REE distribution patterns, apparent negative Eu anomaly, enrichment in LILE(Cs, Rb, Th, U, K and Pb) and depletion in HFSE(Zr, Nb, Ti and Y), and low Ba and Sr. However, the biotite granite porphyry shows weak fractionation of LREE and HREE, with an average(La/Yb)_N of 9.76, apparent Eu negative anomaly, "sea gull"-type REE patterns, and "M"-type four group effect, enrichment in LILE and depletion in HFSE. The ε_(Hf)(t) of the porphyric-like biotite monzogranite has a range of-7.39～-5.19, with a two-stage model age(T_(DM2)) of 1.53～1.67 Ga. Comprehensive analysis shows that the porphyric-like biotite monzogranite of Late Jurassic in the Dahutang area may be originated from partial melting of the Neoproterozoic biotite-granodiorite in middle-upper crust in the tectonic background of subduction of the Paleo-Pacific Plate into the South China Plate; while the biotite granite porphyry of Early Cretaceous originated from partial melting of the Neoproterozoic biotite-monzogranite in upper crust due to upwelling of the asthenosphere mantle in a tectonic transition background from subduction of the Paleo-Pacific Plate into the South China Plate to post-subduction extension. Besides, the biotite granite porphyry was replaced by Cl-rich fluids during the process of crystallization differentiation.
The Dahutang area in Jiangxi Province developed multiple-phased granitiods during the Late Mesozoic, which are closely associated with W-Cu-Mo mineralization. This paper performed the study of mineral chemistry, geochemistry, zircon U-Pb chronology and Lu-Hf isotope for porphyric-like biotite monzogranite and biotite granite porphyry from the study area. The results show that the porphyric-like biotite monzogranite formed at 145.6±1.4 Ma(Kunshan Pluton), 148.4±2.4 Ma(in the center of Yanziya Pluton) and 145.7±2.9 Ma(the edge of Yanziya Pluton), and the biotite granite porphyry formed at 143.7±2.4 Ma(Shiweidong Pluton). All the captured zircons in four samples were derived from the surrounding granitoids of Neoproterozoic. The geochemical characteristics show that the porphyric-like biotite monzogranite and biotite granite porphyry are similarly high in SiO_2(72.37%～73.33% and 70.16%～73.8%, respectively), rich in Al with the aluminum saturation index A/CNK of 1.23～1.47 and 1.30～3.02, respectively; suggesting a high high-K calc-alkaline series. Rare earth and trace elements analyses show distinct differences between the porphyric-like biotite monzogranite and biotite granite porphyry. The porphyric-like biotite monzogranite is characterized by distinct HREE and LREE fractionation with an average(La/Yb)_Nof 26.18 and obvious right leaning of REE distribution patterns, apparent negative Eu anomaly, enrichment in LILE(Cs, Rb, Th, U, K and Pb) and depletion in HFSE(Zr, Nb, Ti and Y), and low Ba and Sr. However, the biotite granite porphyry shows weak fractionation of LREE and HREE, with an average(La/Yb)_N of 9.76, apparent Eu negative anomaly, "sea gull"-type REE patterns, and "M"-type four group effect, enrichment in LILE and depletion in HFSE. The ε_(Hf)(t) of the porphyric-like biotite monzogranite has a range of-7.39～-5.19, with a two-stage model age(T_(DM2)) of 1.53～1.67 Ga. Comprehensive analysis shows that the porphyric-like biotite monzogranite of Late Jurassic in the Dahutang area may be originated from partial melting of the Neoproterozoic biotite-granodiorite in middle-upper crust in the tectonic background of subduction of the Paleo-Pacific Plate into the South China Plate; while the biotite granite porphyry of Early Cretaceous originated from partial melting of the Neoproterozoic biotite-monzogranite in upper crust due to upwelling of the asthenosphere mantle in a tectonic transition background from subduction of the Paleo-Pacific Plate into the South China Plate to post-subduction extension. Besides, the biotite granite porphyry was replaced by Cl-rich fluids during the process of crystallization differentiation.
引文
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