华夏早古生代俯冲作用(Ⅰ)：来自糯垌蛇绿岩的新证据

彭松柏; 刘松峰; 林木森; 吴长峰; 韩庆森

doi:10.3799/dqkx.2016.065

华夏早古生代俯冲作用(Ⅰ)：来自糯垌蛇绿岩的新证据

doi: 10.3799/dqkx.2016.065

彭松柏^1,2,,
刘松峰^1,2,
林木森³,
吴长峰⁴,
韩庆森^1,2

1.
中国地质大学地球科学学院，湖北武汉 430074
2.
中国地质大学全球大地构造中心，湖北武汉 430074
3.
福州大学紫金矿业学院，福建福州 350108
4.
福建闽西地质大队，福建厦门 361000

基金项目:

中国地质调查局地质调查项目 12120114039201

详细信息

作者简介:
彭松柏(1963-)，男，教授，博士，主要从事岩石大地构造及蛇绿岩研究.E-mail：psongbai@aliyun.com

中图分类号: P545
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出版历程
- 收稿日期: 2016-01-16
- 刊出日期: 2016-05-15

Early Paleozoic Subduction in Cathaysia (Ⅰ): New Evidence from Nuodong Ophiolite

1.
School of Earth Sciences, China University of Geosciences, Wuhan 430074, China
2.
Center for Global Tectonics, China University of Geosciences, Wuhan 430074, China
3.
College of Zijin Minning, Fuzhou University, Fuzhou 350108, China
4.
The Western Geological Party of Fujian, Xiamen 361000, China

摘要

摘要: 早古生代加里东期造山运动(广西运动)的性质是华南大地构造演化长期争议的重大地质问题.桂东南岑溪糯垌一带奥陶纪浅变质地层中出露一套变形变质基性岩系构造岩片，主要由变枕状玄武岩、辉绿岩墙以及少量块状辉长岩和辉石岩组成.变玄武岩、变辉绿岩的SiO₂含量为49.20%~52.30%，MgO含量为6.78%~9.11%，Mg^#为55~63，TiO₂含量为1.02%~1.34%，属低钾拉斑玄武系列基性岩.稀土元素配分平坦，轻稀土亏损，(La/Sm)_N为0.72~1.05，(La/Yb)_N为0.7~1.0，无明显Eu异常，大离子亲石元素Rb、Ba、Th、U、K、Pb相对富集，高场强元素Nb、Ta、Zr、Hf、Ti平坦-略亏损，Ti/V为21.30~25.12，Nb/Th为2.1~4.2，表现出俯冲带之上(SSZ)蛇绿岩的地球化学特征.变辉绿岩LA-ICP-MS锆石U-Pb成岩年龄为437±5 Ma，表明其形成于早志留世.综合研究表明，糯垌变基性岩系应属早古生代形成于俯冲之上(SSZ)弧前构造环境的肢解蛇绿岩残片，这一发现为华南扬子克拉通与华夏地块之间存在早古生代洋盆和俯冲-增生碰撞造山提供了关键证据.
- 岑溪地区 /
- 蛇绿岩 /
- 岩石学 /
- 地球化学 /
- 早古生代洋盆 /
- 大地构造意义
Abstract: The nature of Early Paleozoic Caledonian orogeny (Guangxi movement), as one of the key geolocial problems of tectonic evolution in South China, has been controversial for a long time. In this study we report a suite of deformed and metamorphosed basic rocks in tectonic slices that are exposed in epimetamorphic Ordovician strata, located at the Nuodong in the Cenxi area of the Southeast Guangxi, South China. This suite of rock is mainly composed of metamorphic basalt, diabase dike and minor pyroxenite. Petrogeochemical data of the metabasalt and metadiabase dike show the content of SiO₂=49.20%-52.30%, MgO=6.78%-9.11%, Mg^#=55-63, TiO₂=1.02%-1.34%, indicating the low potassium tholeiitic series of basic rocks. The chondrite-normalized REE distribution patterns are flat type with light rare earths depleted, no obvious Eu anomaly, (La/Sm)_N=0.72-1.05, (La/Yb)_N=0.7-1.0, while the N-MORB normalized spider diagrams show slightly enrichment of LILEs (e.g.Rb, Ba, Th, U, K, Pb) and flat-slightly depletion of HFSEs (e.g.Nb, Ta, Zr, Hf, Ti), Ti/V=21.30-25.12, Nb/Th=2.1-4.2. The geological and petrogeochemical features imply that this series of rocks represent a dismembered ophiolites formed in supra-subduction zone (SSZ) tectonic environment.The LA-ICP-MS zircon U-Pb age of the metadiabase is 437±5 Ma, indicating that the ophiolites were formed at the Early Silurian. Based on the above comprehensive study, we propose that the Nuodong metamorphic basic rock series are Early Paleozoic ophiolite fragments formed in a forearc tectonic environment in a supra-subduction zone (SSZ). The document of the Early Paleozoic Nuodong ophiolite provides key evidence for the existence of an Early Paleozoic oceanic basin and subduction-accretionary collisional orogenesis between Yangtze craton and Cathaysia blocks in South China.
- Southeast Guangxi /
- ophiolite /
- petrology /
- geochemistry /
- Early Paleozoic oceanic basin /
- tectonic significance

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图 1 华南大地构造基本单元(a)、糯垌地区地质简图(b)和糯垌变基性岩系地质剖面(c)

图b据广西壮族自治区区域地质调查队1:5万地质图修编

Fig. 1. The tectonic framework of the South China (a), the geological sketch of Nuodong area (b) and geological section of the Nuodong metamorphic basic rock series (c)

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图 2 变玄武岩、辉绿岩及变辉石岩野外宏观和显微照片

a.枕状玄武岩野外露头；b.杏仁状玄武岩野外露头；c.变辉绿岩岩脉(岩墙)群野外露头；d.强烈韧性剪切变形形成的玄武岩与辉绿岩岩脉(岩墙)似层状构造；e.变玄武岩中变余杏仁结构(正交镜)；f.变辉绿岩中变余辉绿-辉长结构(单偏镜)；g.变辉绿岩中变余辉绿结构(正交镜)；h.变辉石岩中变余粒状结构(正交镜).矿物缩写：Prx.辉石；Hbl.角闪石；Pl.斜长石；Mag.磁铁矿；Q.石英

Fig. 2. Representative field and thin section photomicrographs of the metabasalt and metadiabase

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图 3 变玄武岩、辉绿岩岩石化学分类和岩浆岩系列判别

a.Zr/Ti-Nb/Y岩石化学分类图(Floyd and Winchester, 1975; Pearce, 1996)；b.Y-Zr岩浆系列判别图(Polat et al., 2009)

Fig. 3. Geochemical classification and magmatic series discriminant diagrams of the metabasalt and metadiabase

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图 4 变玄武岩、辉绿岩稀土元素球粒陨石标准化配分型式(a)和微量元素N-MORB标准化蛛网图(b)

Fig. 4. Chondrite-normalized REE diagram (a) and N-MORB-normalized trace elements spider-diagram of the metabasalt and metadiabase (b)

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图 5 变辉绿岩代表性锆石CL图像(a)及锆石年龄协和图(b)

Fig. 5. Representative CL images (a) and U-Pb concordia diagram for zircons of the metadiabase (b)

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图 6 变玄武岩、辉绿岩构造环境判别图

a.2Nb-Zr/4-Y判别图解(Meschede, 1986)；b.V-Ti判别图解(Shervais, 1982)；c.Th/Yb-Ta/Yb判别图解(Pearce, 1982)；d.Th/Yb-Nb/Yb判别图解(Pearce, 2008, 2014; Dilek and Furnes, 2011; Angerer et al., 2013).N-MORB.正常洋脊玄武岩；E-MORB.富集洋脊玄武岩；IAB.岛弧玄武岩；IAT.岛弧拉斑玄武岩；ICA.岛弧钙碱性玄武岩；CAB.钙碱性玄武岩；WPB.板内玄武岩；WPT.板内拉斑玄武岩；WPAB.板内碱性玄武岩；OIB.洋岛玄武岩；AB.弧玄武岩；SHO.钾玄岩；CFB.大陆溢流玄武岩；FAB.弧前玄武岩

Fig. 6. Tectonic discriminant diagrams of the metabasalt and diabase

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图 7 桂东南早古生代蛇绿岩和髙镁-镁质玄武岩-安山岩成因示意

Fig. 7. Genetic sketch of Early Paleozoic ophiolite and high magnesian-magnesian basalt-andesite in the southeastern Guangxi

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表 1 变玄武岩、辉绿岩主量元素(%)和微量元素(10^-6)组成

Table 1. Major elements (%) and trace elements (10^-6) composition of the metabasalt and metadiabase

岩性	变玄武岩			变辉绿岩
岩性	12ND03	14ND3-1	15ND1-1	12ND01	12ND02	12ND05	14ND1-1	14ND4-2
SiO₂	51.00	49.20	50.60	51.78	51.45	52.30	50.10	50.00
TiO₂	1.07	1.04	1.27	1.34	1.15	1.02	1.20	1.07
Al₂O₃	15.04	15.10	15.00	14.87	14.43	15.63	14.50	15.20
Fe₂O₃	2.41	2.24	2.57	2.61	2.75	1.98	2.49	1.84
FeO	7.25	7.63	7.89	8.20	7.55	6.65	8.34	7.68
MnO	0.18	0.19	0.17	0.16	0.17	0.13	0.18	0.18
MgO	7.59	9.11	7.22	7.09	7.54	6.78	7.46	7.75
CaO	10.63	11.70	9.48	8.07	10.21	11.30	10.15	12.10
Na₂O	3.01	2.20	3.19	4.15	2.53	2.17	2.80	2.48
K₂O	0.08	0.09	0.14	0.13	0.12	0.15	0.19	0.16
P₂O₅	0.08	0.08	0.11	0.11	0.09	0.08	0.10	0.08
LOI	0.88	0.69	0.61	0.90	1.21	1.00	0.52	0.63
Total	99.22	99.27	98.25	99.33	99.20	99.19	98.03	99.17
Mg^#	59	63	56	55	58	59	56	60
Ba	13.8	15.3	20.0	54.6	26.4	68.2	30.5	26.0
Rb	1.3	0.7	1.7	0.9	2.7	3.4	2.7	1.9
Th	0.54	0.61	0.82	0.74	0.96	0.90	0.80	0.59
Pb	0.60	2.00	1.10	0.94	0.71	0.81	1.20	1.90
Nb	2.11	2.10	3.10	2.57	2.67	1.93	3.30	2.30
Sr	83.8	92.1	80.9	64.1	85.3	122.0	104.0	91.2
Zr	57.4	60.0	69.0	74.7	69.1	62.8	72.0	60.0
Y	28.0	26.4	34.5	36.0	33.3	28.4	34.4	26.7
Cr	216	211	116	143	205	136	98	216
V	301	282	303	370	303	273	303	283
Ni	80.4	81.0	47.0	40.8	71.7	59.4	46.0	86.0
Co	46.1	52.0	51.0	48.4	44.4	47.8	45.0	54.0
Cs	0.08	0.06	0.18	0.08	0.16	0.24	0.20	0.02
Ta	0.16	0.10	0.17	0.18	0.19	0.17	0.20	0.20
Hf	1.70	1.90	2.10	2.28	2.05	1.84	2.20	1.90
U	0.23	0.19	0.31	0.23	0.17	0.16	0.19	0.23
La	2.73	3.00	4.30	3.81	4.11	3.28	4.40	3.20
Ce	7.64	7.90	10.60	9.98	9.36	8.62	10.50	8.20
Pr	1.24	1.31	1.68	1.65	1.69	1.38	1.70	1.33
Nd	6.73	6.40	7.90	8.85	8.53	7.48	8.30	6.40
Sm	2.46	2.29	2.92	3.05	2.82	2.55	2.70	2.21
Eu	0.81	0.92	1.05	1.03	0.99	0.90	1.04	0.91
Gd	3.42	3.46	4.71	4.40	4.00	3.41	4.11	3.45
Tb	0.67	0.67	0.83	0.85	0.79	0.69	0.80	0.67
Dy	4.62	4.54	5.41	5.93	5.44	4.66	5.48	4.26
Ho	0.99	0.94	1.26	1.29	1.17	0.96	1.15	0.93
Er	2.95	3.01	3.73	3.85	3.56	3.00	3.66	2.92
Tm	0.41	0.44	0.62	0.57	0.51	0.43	0.50	0.41
Yb	2.89	2.84	3.57	3.77	3.41	2.95	3.31	2.64
Lu	0.44	0.40	0.55	0.57	0.53	0.45	0.48	0.40

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表 2 变辉绿岩LA-ICP-MS锆石U-Pb测年结果

Table 2. Analyses results of LA-ICP-MS zircon U-Pb dating for the metadiabase

测点	Th(10^-6)	U(10^-6)	Th/U	同位素比值(±1σ)			年龄Ma(±1σ)
测点	Th(10^-6)	U(10^-6)	Th/U	²⁰⁷Pb/²⁰⁶Pb	²⁰⁷Pb/²³⁵U	²⁰⁶Pb/²³⁸U	²⁰⁷Pb/²⁰⁶Pb	²⁰⁷Pb/²³⁵U	²⁰⁶Pb/²³⁸U
1	1 129	963	1.17	0.054 5±0.001 3	0.538 6±0.012 9	0.071 2±0.000 7	391±49.1	437±8.5	443±4.1
2	127	167	0.76	0.069 1±0.002 4	1.141 8±0.040 5	0.119 1±0.001 5	902±72.2	773±19.2	725±8.4
3	1 245	1 879	0.66	0.056 1±0.001 3	0.541 4±0.012 1	0.069 4±0.000 6	457±50.0	439±8.0	433±3.9
4	466	550	0.85	0.056 2±0.001 9	0.566 0±0.018 6	0.072 5±0.000 8	461±106	455±12.1	451±4.5
5	214	386	0.55	0.054 5±0.002 0	0.545 2±0.019 9	0.072 0±0.000 8	391±81.5	442±13.1	448±5.0
6	186	294	0.63	0.056 6±0.002 5	0.535 6±0.023 6	0.068 3±0.000 9	476±98.1	435±15.6	426±5.4
7	395	778	0.51	0.056 4±0.001 7	0.563 2±0.015 8	0.072 0±0.000 6	478±32.4	454±10.3	448±3.8
8	426	465	0.92	0.055 7±0.001 7	0.544 1±0.017 4	0.069 9±0.000 7	443±68.5	441±11.4	435±4.1
9	742	1178	0.63	0.055 1±0.001 4	0.524 5±0.013 4	0.068 3±0.000 6	417±54.6	428±8.9	426±3.8
10	535	672	0.80	0.055 2±0.001 8	0.535 3±0.016 8	0.069 7±0.000 8	420±76.8	435±11.1	434±4.5
11	116	666	0.17	0.121 0±0.003 0	5.825 3±0.137 6	0.345 4±0.003 1	1 972±43.8	1 950±20.5	1 912±14.9
12	333	711	0.47	0.054 9±0.001 6	0.535 7±0.015 7	0.070 1±0.000 7	409±66.7	436±10.4	437±4.2
13	497	523	0.95	0.055 8±0.002 0	0.529 8±0.018 1	0.068 4±0.000 8	443±79.6	432±12.0	427±4.6
14	351	467	0.75	0.064 3±0.002 1	0.996 7±0.043 4	0.109 1±0.002 9	750±69.3	702±22.1	668±16.8
15	299	618	0.48	0.053 6±0.002 1	0.532 2±0.021 7	0.071 4±0.000 9	354±90.7	433±14.4	445±5.5
16	828	838	0.99	0.053 9±0.001 9	0.532 6±0.017 7	0.071 4±0.000 8	369±84.3	434±11.7	444±4.8
17	315	469	0.67	0.052 7±0.001 8	0.580 9±0.019 4	0.079 3±0.001 0	317±75.9	465±12.4	492±5.8
18	285	461	0.62	0.106 5±0.002 6	4.444 6±0.107 5	0.299 8±0.002 9	1 740±44.8	1 721±20.1	1 690±14.5
19	1 167	1 016	1.15	0.055 6±0.001 5	0.538 0±0.014 0	0.069 6±0.000 7	435±59.3	437±9.3	434±4.2
20	371	647	0.57	0.056 0±0.001 8	0.533 9±0.016 8	0.068 9±0.000 6	454±67.6	434±11.1	429±3.8

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