南岭九嶷山地区砂子岭岩体成因与构造属性:来自锆石U-Pb年代学、岩石地球化学及Sr、Nd、Hf同位素证据

李剑锋; 付建明; 马昌前; 卢友月; 程顺波; 马丽艳; 秦拯纬

doi:10.3799/dqkx.2019.013

南岭九嶷山地区砂子岭岩体成因与构造属性:来自锆石U-Pb年代学、岩石地球化学及Sr、Nd、Hf同位素证据

doi: 10.3799/dqkx.2019.013

李剑锋^1,2,3, ,,
付建明^1, , ,,
马昌前²,
卢友月¹,
程顺波¹,
马丽艳¹,
秦拯纬¹

1.
中国地质调查局武汉地质调查中心, 湖北武汉 430205
2.
中国地质大学地球科学学院, 湖北武汉 430074
3.
辽宁师范大学城市与环境学院, 辽宁大连 116029

基金项目:

中国地质调查局项目"南岭成矿带中西段地质矿产调查" 121201009000150002

详细信息

作者简介:
李剑锋(1986-), 男, 助理研究员, 博士后, 主要从事矿床学研究工作

通讯作者:
付建明

中图分类号: P597
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- 被引次数: 0
出版历程
- 收稿日期: 2019-05-25
- 刊出日期: 2020-02-15

Petrogenesis and Tectonic Setting of the Shaziling Pluton in Jiuyishan Area, Nanling: Evidence from Zircon U-Pb Geochronology, Petrogeochemistry, and Sr-Nd-Hf Isotopes

Li Jianfeng^{1,2,3
,
,},
Fu Jianming^{1
, ,
,},
Ma Changqian²,
Lu Youyue¹,
Cheng Shunbo¹,
Ma Liyan¹,
Qin Zhengwei¹

1.
Wuhan Center of Geological Survey, China Geological Survey, Wuhan 430205, China
2.
Faculty of Earth Sciences, China University of Geosciences, Wuhan 430074, China
3.
College of Urban and Environmental Science, Liaoning Normal University, Dalian 116029, China

摘要

摘要: 九嶷山地区砂子岭岩体作为南岭花岗岩带的有机组成部分，对其主要岩石类型开展了年代学研究，系统的LA-ICP-MS锆石定年结果表明，含斑中细粒花岗闪长岩成岩年龄为151.9±1.1 Ma、152.1±1.1 Ma，中细粒斑状二长花岗岩成岩年龄为154.1±1.2 Ma；确定其成岩年代为燕山早期，而不是以前普遍认为的印支期.岩石地球化学分析显示，砂子岭岩体具有富硅碱贫钙镁、K₂O/Na₂O为1.37~2.65、准铝-过铝质（0.93~1.09），FeO^*/MgO比值大（5.43~15.33，平均7.14）等特点；岩石稀土含量介于186.75×10^-6~413.17×10^-6之间，明显高于世界花岗岩均值，稀土元素配分曲线呈右倾轻稀土富集型，具明显铕负异常，δEu值为0.095~0.224；岩石富集Ga、Y、Nb、Zr、Hf等大离子高场强元素及亏损Ni、Cr、Eu、Ti、V、P、Sr等元素，Ga/Al比值为245×10^-6~582×10^-6（平均值350×10^-6）、Zr+Nb+Ce+Y为256.8×10^-6~630.7×10^-6（平均值441.95×10^-6），显示A型花岗岩地球化学属性，形成于伸展构造体系的造山后环境.Sr、Nd、Hf同位素显示砂子岭岩体具较高Sr同位素初始值（I_Sr=0.716 03~0.718 17），较低的ε_Nd（t）（-6.8~-7.4）、ε_Hf（t）（4.8~-14.2）值特点；揭示其源区为地壳杂砂岩/泥质岩的部分熔融，成岩过程中有地幔物质的贡献；钕、铪模式年龄较接近，分别为1 498~1 546 Ma与1 061~1 756 Ma，暗示其源岩从地幔储库中脱离的时间为中元古代.结合南岭地区地质演化史，中生代九嶷山地区恰处于板块拼合带及太平洋板块弧后伸展的构造背景之下，具发生过岛弧岩浆作用、构造相对薄弱且存在大量具较高Lu-Hf、Sm-Nd同位素比值新生地壳物质的特点；地幔对流与软流圈上涌引发源区部分熔融形成具有类似同位素组成特征的A型花岗岩，即为砂子岭及九嶷山复式岩体的成因.
- A型花岗岩 /
- 锆石U-Pb年代学 /
- 同位素 /
- 地球化学 /
- 构造背景 /
- 砂子岭 /
- 南岭
Abstract: A study of LA-ICP-MS zircon U-Pb dating for Shaziling pluton composed of granodiorites and monzogranites from Jiuyishan area considered as a part of Nanling granite belt was carried out. The results of chronology indicate that the Shaziling pluton was formed during the early Yanshanian (151.9±1.1-154.1±1.2 Ma) instead of the Indosinian. The analyses of geochemistry indicate that the Shaziling pluton was characterized by rich silicon-alkali and poor calcium-magnesium with K₂O/Na₂O ratios of 1.37-2.65, Al₂O₃ of 0.93-1.09 and FeO^*/MgO ratios of 5.43-15.33 (average 7.14); The content of rare earth elements in the range of 186.75 to 413.17×10^-6 is significantly higher than the those of world average granite, which shows the right-leaning distribution of enriched light rare earth elements with obvious negative anomaly of Eu and δEu values of 0.095-0.224. These rocks are enriched in large ion lithophile elements (LILEs, e.g., Ga, Y, Nb, Zr, and Hf) and relatively depleted in high field strength elements (HFSEs, e.g., Ni, Cr, Eu, Ti, V, P, and Sr), with Ga/Al ratios of (245~582)×10^-6 (average 350×10^-6) and Zr+Nb+Ce+Y of (256.8-630.7)×10^-6 (average 441.95×10^-6), similar to geochemical features of A-type granites, which indicates the Shaziling pluton formed in the post- orogenic environment of the extensional tectonic system. Sr, Nd and Hf isotopes show that the Shaziling pluton has higher initial Sr isotope values of 0.71603 to 0.71817, lower ε_Nd(t) values of -6.8 to -7.4 and ε_Hf(t) values of 4.8 to -14.2, revealing that the source area occurred partial melting of crustal graywacke/pelite with a contribution of mantle materials during the diagenesis. Nd and Hf are relatively close in mode ages, with 1 498-1 546 Ma and 1 061-1 756 Ma, respectively, suggesting that the source rocks separated from the mantle reservoir during the Mesoproterozoic. Combined with the geological evolution of Nanling area that was in the tectonic setting of plate juncture zone and post-arc extension of Pacific plate, magmatism occurred in the Mesozoic Jiuyishan area in which the structure is relatively weak and there are a lot of new crustal materials with higher Lu/Hf and Sm/Nd isotope ratios. The Shaziling and Jiuyishan complex massif, similar to isotopic composition of A-type granites was formed by partial melting of the source area caused by mantle convection and upwelling of asthenosphere.
- A-type granites /
- zircon U-Pb dating /
- isotope /
- geochemistry /
- tectonic setting /
- Shaziling /
- Nanling

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图 1 九嶷山地区地质简图

图a中S、M、N分别为南岭南、中、北花岗岩带；1.白垩系；2.石炭系；3.泥盆系；4.寒武系；5.震旦系；6.志留纪花岗岩；7.中侏罗世花岗岩；8.中侏罗世碎斑熔岩；9.中侏罗世英安/流纹(斑)岩；10.岩相界线；11.地质界线；12.不整合界线；13.断层；14.取样位置

Fig. 1. Simplified geological map of Jiuyishan

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图 2 砂子岭岩体(a)、暗色包体(b)、(c)及显微照片(d)、(e)、(f)

a.样品12D72采样位置，见有椭圆-不规则状暗色包体；b.暗色包体；c. 13D13采样点，寄主岩石为中细粒斑状二长花岗岩；d.含斑中细粒花岗闪长岩(12D72，正交偏光)；e.斜长石环带(12D72，正交偏光)；f.中细粒斑状二长花岗岩(12D72，正交偏光)；矿物代码: Hb.角闪石; Bi.黑云母; Pl.斜长石; Q.石英.

Fig. 2. Shaziling rock mass (a) MME (b)、(c) and its microscopic photos (d)、(e)、(f)

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图 3 研究区岩浆岩锆石U-Pb年龄谐和图和锆石阴极发光(CL)图像

Fig. 3. Magmatite Zircon U-Pb Concordia diagrams for the CL images in the study area

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图 4 砂子岭岩体Na₂O+K₂O/SiO₂(a)、K₂O-SiO₂图解(b)和A/NK-A/KNC图解(c)

Fig. 4. The Na₂O+K₂O/SiO₂(a)、K₂O-SiO₂ (b) and A/NK-A/KNC diagram (c) of Shaziling rock mass

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图 5 砂子岭岩体REE配分图(a)和微量元素蛛网图(b)

Fig. 5. Chondrite-normalized REE patterns and primitive mantle-normalized spidergrams of Shaziling

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图 6 砂子岭岩体ε_Nd(t)-I_sr、ε_Hf(t)-Age、CaO/(MgO+FeO)-Al₂O₃/(MgO+FeO)及Rb/Sr-Rb/Ba图解

Fig. 6. ε_Nd(t)-I_sr、ε_Hf(t)-Age、CaO/(MgO+FeO)-Al₂O₃/(MgO+FeO) and Rb/Sr-Rb/Ba diagrams of Shaziling

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图 7 砂子岭岩体(10 000×Ga/Al)vs(FeO^*/MgO)/Ce /[(Na₂O+K₂O)/CaO]、(Zr+Nb+Ce+Y)vs(FeO^*/MgO)、Nb-Y-Ce及Nb-Y-Ga判别图解(底图据Whalen et al., 1987)

Fig. 7. (10 000×Ga/Al)vs(FeO^*/MgO)/Ce/[(Na₂O+K₂O)/CaO]、(Zr+Nb+Ce+Y)VS(FeO^*/MgO)、Nb-Y-Ce and Nb-Y-Ga discrimination diagrams of Shaziling rock mass

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表 3 砂子岭岩体Sr-Nd同位素数据

Table 3. Nd-Sr-Pb isotopic data for Xishan volcanic-intrusive complex rocks

样号	Rb(10^-6)	Sr(10^-6)	⁸⁷Rb/⁸⁶Sr	⁸⁷Sr/⁸⁶Sr	误差2σ	I_(Sr)	ε_Sr(0)	ε_Sr(t)	f_Rb/Sr	Sm(10^-6)	Nd(10^-6)	¹⁴⁷Sm/¹³⁴Nd	¹⁴³Nd/¹⁴⁴Nd	误差2σ	I_Nd	ε_Nd(t)	T_2DM	f_Sm/Nd
D116-1	290.1	86.9	9.652	0.737 82	0.000 001	0.716 28	473.0	169.9	115.71	9.180	36.55	0.151 9	0.512 215	0.000 012	0.512 059	-7.36	1 541	-0.23
D117-1	196.1	135.2	4.188	0.726 79	0.000 009	0.717 44	316.4	186.4	49.64	10.290	49.53	0.125 7	0.512 190	0.000 070	0.512 061	-7.32	1 542	-0.36
D118-1	188.6	137.6	3.959	0.726 39	0.000 003	0.717 55	310.7	187.9	46.87	10.310	51.17	0.121 8	0.512 183	0.000 060	0.512 058	-7.38	1 546	-0.38
12D72	166.8	145.2	3.318	0.724 86	0.000 005	0.717 59	289.0	188.4	39.12	14.370	86.74	0.100 2	0.512 168	0.000 010	0.512 067	-7.27	1 537	-0.49
12D73	222.1	120.0	5.347	0.727 74	0.000 001	0.716 03	329.9	166.3	63.66	9.417	48.29	0.118 0	0.512 210	0.000 040	0.512 091	-6.80	1 498	-0.40
13D13	196.3	118.2	4.799	0.728 68	0.000 004	0.718 17	343.2	196.7	57.03	11.790	64.36	0.110 8	0.512 180	0.000 060	0.512 068	-7.25	1 535	-0.44

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表 4 砂子岭岩体Hf同位素数据

Table 4. Hf isotopic data for Xishan volcanic-intrusive complex rocks

测点号	¹⁷⁶Hf/¹⁷⁷Hf	2σ	¹⁷⁶Lu/¹⁷⁷Hf	¹⁷⁶Yb/¹⁷⁷Hf	ε_Hf(0)	Age	ε_Hf(t)	2σ	T_DM	2σ	T_2DM	2σ
12D72-01	0.282 624	0.000 013	0.000 806	0.025 352	-5.2	153	-2.0	0.5	886	38	1 326	60
12D72-02	0.282 445	0.000 019	0.000 858	0.026 673	-11.5	151	-8.3	0.7	1 137	52	1 726	83
12D72-03	0.282 630	0.000 014	0.001 153	0.036 333	-5.0	152	-1.8	0.5	885	39	1 313	62
12D72-04	0.282 463	0.000 010	0.001 318	0.042 661	-10.9	151	-7.8	0.3	1 127	28	1 691	44
12D72-05	0.282 513	0.000 019	0.001 392	0.043 024	-9.1	151	-6.0	0.7	1 057	53	1 577	84
12D72-06	0.282 816	0.000 013	0.001 095	0.034 853	1.6	154	4.8	0.4	620	36	894	57
12D72-07	0.282 744	0.000 011	0.001 654	0.052 192	-1.0	152	2.2	0.4	733	32	1 061	49
12D72-08	0.282 603	0.000 012	0.000 951	0.030 035	-6.0	155	-2.7	0.4	918	33	1 371	53
12D72-09	0.282 557	0.000 009	0.000 865	0.027 294	-7.6	152	-4.3	0.3	980	26	1 475	42
12D72-10	0.282 593	0.000 008	0.001 011	0.027 185	-6.3	151	-3.1	0.3	934	24	1 397	38
12D72-11	0.282 278	0.000 017	0.000 630	0.015 328	-17.5	153	-14.2	0.6	1 362	47	2 097	75
12D72-12	0.282 600	0.000 020	0.000 940	0.024 645	-6.1	434	3.2	0.7	922	55	1 212	88
12D72-13	0.282 600	0.000 013	0.000 853	0.021 819	-6.1	151	-2.9	0.5	921	37	1 381	59
12D72-14	0.282 607	0.000 009	0.000 991	0.026 542	-5.8	151	-2.6	0.3	914	26	1 365	42
12D72-15	0.282 557	0.000 013	0.000 650	0.016 865	-7.6	151	-4.4	0.5	975	38	1 475	60
12D72-16	0.282 507	0.000 010	0.000 899	0.023 017	-9.4	154	-6.1	0.4	1 052	28	1 588	45
12D72-17	0.282 560	0.000 012	0.000 864	0.022 860	-7.5	152	-4.3	0.4	977	34	1 469	54
12D72-18	0.282 620	0.000 011	0.000 662	0.017 171	-5.4	151	-2.1	0.4	888	32	1 335	51
12D72-19	0.282 431	0.000 015	0.000 696	0.018 064	-12.1	154	-8.8	0.5	1 152	42	1 756	67
12D72-20	0.282 672	0.000 008	0.000 835	0.021 963	-3.5	154	-0.2	0.3	818	23	1 216	37

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