洋中脊和弧后盆地热液区热液流体B同位素组成的系统性差异

张侠; 于增慧; 翟世奎; 杨治峰; 徐婕

doi:10.3969/j.issn.0253-4193.2019.11.007

洋中脊和弧后盆地热液区热液流体B同位素组成的系统性差异

doi: 10.3969/j.issn.0253-4193.2019.11.007

张侠^{1, 2,},
于增慧^{1, 2},
翟世奎^{1, 2, ,},
杨治峰^{1, 2},
徐婕^{1, 2}

1.
中国海洋大学海洋地球科学学院，山东青岛 266100
2.
海底科学与探测技术教育部重点实验室，山东青岛 266100

基金项目: 国家重点基础研究发展计划（2013CB429702）。

详细信息

作者简介:
张侠（1991—），男，山西省榆社县人，博士研究生，主要从事海底热液成矿作用研究。E-mail：15954227127@163.com

通讯作者:
翟世奎（1958—），男，教授，博士生导师，主要从事海洋地质学研究。E-mail：zhai2000@ouc.edu.cn

中图分类号: P736.4
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出版历程
- 收稿日期: 2018-10-08
- 修回日期: 2019-05-06
- 网络出版日期: 2021-04-21
- 刊出日期: 2019-11-25

Systematic differences in boron isotope compositions between mid-ocean ridge and back-arc basin hydrothermal fluids

Zhang Xia^{1, 2
,},
Yu Zenghui^{1, 2},
Zhai Shikui^{1, 2
, ,},
Yang Zhifeng^{1, 2},
Xu Jie^{1, 2}

1.
College of Marine Geosciences, Ocean University of China, Qingdao 266100, China
2.
Key Lab of Submarine Geosciences and Prospecting Techniques, Ministry of Education, Qingdao 266100, China

摘要

摘要: 硼(B)是流体迁移元素，趋向于在热液流体中富集而成为常量元素。不同来源的B其同位素组成有着明显的区别。因此，B的含量及其同位素组成可标识热液流体(元素)的物质来源、水–岩反应程度及沉积物(元素)混入等重要过程，对海底热液活动及其成矿作用过程具有重要的示踪意义。迄今，对全球主要热液活动区热液流体中B的含量及同位素组成特征已做了大量的测试分析及研究工作，积累了丰富的资料和重要研究成果。但是，对不同地质背景(构造环境)条件下热液流体中B的含量及同位素组成特征尚缺乏系统性的对比分析，进而对造成不同环境热液流体中元素及其同位素组成的系统性差异的原因或机制尚缺乏深入的认识。本文在获取了洋中脊和弧后盆地主要热液活动区热液端元流体中B的含量及其同位素组成数据的基础上，定量估算了热液流体中B的主要来源，并对洋中脊和弧后盆地热液端元流体中B同位素组成的系统性差异进行了分析及成因探讨。结果表明，不同热液活动区热液端元流体的δ¹¹B值都具有较大的变化范围，水–岩反应过程中不同来源B的混合是热液流体B同位素组成变化的主要原因。无沉积物覆盖的洋中脊和弧后盆地热液区热液流体中的B主要为海水与基底岩石来源B的混合，弧后盆地岩浆挥发性组分对热液系统的直接贡献及两种不同地质背景下基底岩石地球化学组成与水–岩反应程度的差异是其热液端元流体B同位素组成差异的主要原因。在有沉积物覆盖的弧后盆地热液区，热液流体中B的同位素组成与前两者之间存在显著差异，具有异常低的δ¹¹B值，水–岩反应过程中沉积物来源B的加入是导致热液流体中δ¹¹B值系统性降低的主要原因，沉积物的吸附作用也在一定程度上影响了热液流体的B同位素组成。有沉积物覆盖的洋中脊热液区热液流体同样受到了沉积物来源B加入的影响，具有较低的δ¹¹B值，且相对于冲绳海槽受到了更强烈的沉积物吸附作用的影响。基于以上分析，并结合热液流体的Sr同位素组成特征，本文提出了洋中脊和弧后盆地这两大构造环境中热液流体B同位素组成系统性差异的成因模式。
- 热液流体 /
- B同位素组成 /
- 系统性差异 /
- 洋中脊 /
- 弧后盆地
Abstract: Boron is a common element in vent fluids of seafloor hydrothermal fields. Due to its typical fluid-mobility and distinct isotope compositions in different reservoirs, boron has been largely applied to trace metal sources, water/rock interaction and sediment contribution to hydrothermal fluids. Up to date, the B contents and its isotope compositions in hydrothermal fluids from the major seafloor hydrothermal fields have been studied sufficiently, but the comparisons of B behavior in different geological settings are relatively limited and the reasons causing the systematic differences in elements and isotope compositions of hydrothermal fluids are still unclear. In this paper, the sources of B in hydrothermal fluids from different geological settings were calculated based on B contents and its isotope compositions, meanwhile, the causes of systematic differences in B isotope compositions between mid-ocean ridge and back-arc basin hydrothermal fluids were discussed. Results show that the δ¹¹B values of hydrothermal end member fluids from different hydrothermal fields have large variations, which mainly results from the mixing of B from difference sources in different proportions. Boron in mid-ocean ridge and sediment-starve back-arc basin hydrothermal fluids are mainly from the mixing of seawater and basement-derived B, the contribution of magmatic volatiles to sediment-starve back-arc basin hydrothermal systems is the major causes of B isotope composition differences in these two geological settings. Moreover, the differences in geochemical compositions of basement rocks and degrees of water/rock interaction also cause the differences in B isotope compositions to some extent. While the δ¹¹B values of hydrothermal end member fluids from sediment-covered hydrothermal fields are extremely low and contribution of sediment-derived B to hydrothermal fluid is the major cause of this phenomenon. Moreover, sediment absorption also causes the B isotope variation to some extent. In sediment-covered mid-ocean ridge hydrothermal fields, the B isotope compositions of hydrothermal fluids are also influenced by the incorporation of sediment-derived B and have relatively lower δ¹¹B values. Compared with the Okinawa Trough, the degrees of sediment absorption in sediment-covered mid-ocean ridge hydrothermal fluids are more intensely. Based on these analysis, we put forward the mechanism causing systematic differences in B isotope compositions of hydrothermal fluids from mid-ocean ridge and back-arc basins.
- hydrothermal fluids /
- boron isotope compositions /
- systematic differences /
- mid-ocean ridge /
- back-arc basin

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图 1 热液流体数据取样点位置

Fig. 1 Locations of the hydrothermal fields studied in this paper

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图 2 全球主要热液活动区热液端元流体B同位素组成

Fig. 2 The δ¹¹B values of the hydrothermal end-member fluid from the major hydrothermal fields

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图 3 主要热液活动区热液端元流体δ¹¹B–B_sw/B_h相关图

B_sw、B_h分别为海水和热液端元流体中B的含量，B_sw/B_h=1代表海水端元，B_sw/B_h=0代表参与水–岩反应的岩石（+沉积物）端元

Fig. 3 The δ¹¹B–B_sw/B_h diagram of the studied hydrothermal end-member fluid

B_sw and B_h indicate the B concentrations of seawater and hydrothermal end-member fluid. B_sw/B_h=1 indicates the seawater member and B_sw/B_h=0 indicates the rock (+sediment) member

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图 4 全球主要热液活动区热液流体B-Sr同位素混合图

CLAM热液区、Guaymas海盆及Escanaba海槽由于无热液流体Sr同位素组成数据，所以未进行投图

Fig. 4 The B-Sr isotope diagram of the hydrothermal end-member fluid from the major hydrothermal fields

The CLAM, Guaymas Basin and Escanaba Trough are not plotted for lack of Sr isotope data

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图 5 洋中脊及弧后盆地热液流体B同位素组成系统性差异模式

A.无沉积物覆盖的洋中脊；B.无沉积物覆盖的弧后盆地；C.有沉积物覆盖的弧后盆地；D.有沉积物覆盖的洋中脊

Fig. 5 The schematic of the systematic differences in B isotope compositions between mid-ocean ridge and back-arc basins

A. Sediment-starve mid-ocean ridge; B. sediment-starve back-arc basins; C. sediment-covered back-arc basins; D. sediment-covered mid-ocean ridge

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表 1 主要海底热液活动区热液端元流体中B的含量及B和Sr的同位素特征值

Tab. 1 Boron concentrations and B, Sr isotope compositions of the studied hydrothermal fluid

	热液区		δ¹¹B/‰	⁸⁷Sr/⁸⁶Sr	B含量/mmol·kg^–1	数据来源
洋中脊热液区		EPR21°N	30.0～32.6	0.702 85～0.703 45	0.53	文献[4, 13, 15]
		EPR13°N	34.9～36.8	0.703 86～0.704 08	0.46	文献[22]
		SJdFR	34.5	0.703 6
		TAG	30.9	0.703 4	0.36
	Guaymas海盆	S热液区	17.4		1.60	文献[8]
			19.6		1.68
		E-Hill	16.5		1.55
		Escanaba海槽	10.1		2.16
弧后盆地热液区	Lau海盆	Kilo Moana	25.7	0.704 46	0.54	文献[16]
			27.2	0.704 45	0.51
			29.5	0.704 53	0.55
			34.3	0.704 42	0.54
		Tow Cam	30.2	0.704 39	0.61
			26.5	0.704 30	0.58
			17.7	0.704 34	0.53
		ABE	22.6	0.704 22	0.70
			25.8	0.704 15	0.83
			24.4	0.704 22	0.88
			26.1	0.704 18	0.65
		Tu’I Malina	21.5	0.703 85	0.76
			26.4	0.703 82	0.92
		Mariner	24.9	0.704 13	1.01
			25.8	0.704 19	1.11
			17.4	0.704 24	0.83
		Vai Lili	18.0	0.705 40	0.81
			27.0	0.705 60	0.61
	Mariana海槽	Alice Spring	20.2	0.703 6	0.73	文献[12-13, 15]
		Forcast Vent	23.2	0.703 8	0.64	文献[12-13, 15]
	北斐济海盆	White Lady	36.1	0.704 6	0.44	文献[12, 15]
	Manus海盆	PAC-MANUS	13.5	0.704 29	1.47	文献[12, 23]
	冲绳海槽	Jade	2.6	0.708 9	4.80	文献[8, 12, 14-15]
		Minami-Ensei	2.5	0.710 0	4.40
		CLAM	9.2		2.73
			7.0		2.77

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表 2 主要物质端元的B和Sr的含量及其同位素组成特征值

Tab. 2 The B, Sr concentrations and their isotope compositions of the major end-members

端元组分	δ¹¹B/‰	B含量 /mmol·kg^–1	⁸⁷Sr /⁸⁶Sr	Sr含量 /mmol·kg^–1
海水^{[12, 15]}	39.6	0.41	0.709 18	0.09
MORB^{[12, 33-34]}	–3	0.09	0.702 64	1.03
BABB^{[12, 35-41]}	1.5	1.1	0.703 1	1.44
OTV^{[12, 42-44]}	1.1	1.1	0.706 635	1.93
沉积物^{[12, 45-50]}	–10	6.5	0.711 7	6.7
注：MORB：洋脊玄武岩；BABB：弧后盆地玄武岩；OTV：冲绳海槽火山岩。

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