胶北太古宙早期锆石U-Pb定年及Hf同位素研究：华北克拉通古老陆壳增生及再循环的证据

引用本文

刘建辉, 刘福来, 丁正江, 刘平华, 王舫. 2014. 胶北太古宙早期锆石U-Pb定年及Hf同位素研究：华北克拉通古老陆壳增生及再循环的证据. 岩石学报,30(10): 2941-2950 复制到剪切板

LIU JH, LIU FL, DING ZJ, LIU PH and WANG F. 2014. U-Pb dating and Hf isotope study of Early Archean zircons from the Jiaobei Terrane, North China Craton: Evidence for growth and recycling of ancient continental crust. Acta Petrologica Sinica,30(10): 2941-2950 (in Chinese with English abstract) 复制到剪切板

胶北太古宙早期锆石U-Pb定年及Hf同位素研究：华北克拉通古老陆壳增生及再循环的证据

刘建辉¹, 刘福来¹, 丁正江^2,3, 刘平华¹, 王舫¹

1. 中国地质科学院地质研究所, 北京 100037;
2. 吉林大学地球科学学院, 长春 130061;
3. 山东省第三地质矿产勘查院, 烟台 264000

2014-1-2 收稿, 2014-3-20 改回.

基金项目：本文受科技部973项目（2012CB416603）、中国地质科学院地质研究所基本科研业务经费（J1214、J1005）和中国地质调查局地质大调查项目（1212011120150）联合资助。

第一作者简介：刘建辉，男，1978年生，副研究员，主要从事构造地质学和同位素年代学研究，Email: liujianhui1999@163.com

摘要：古老陆壳物质的发现与鉴别是探索地球早期陆壳形成与演化历史的重要内容之一，锆石U-Pb年龄结合Hf同位素研究是该研究的重要手段。本文通过对胶北地体内一个长英质副片麻岩中的锆石开展系统的原位U-Pb定年和微量、稀土元素分析，获得了多个太古宙早期的锆石。根据这些锆石的阴极发光图像、Th/U比值及稀土元素球粒陨石标准化配分模式，它们具有典型岩浆锆石的特征，其中2个分析点给出了3413Ma和3400Ma （~3.4Ga）的锆石U-Pb年龄，7个分析点给出3547±19Ma （MSWD=1.16）的锆石U-Pb年龄，指示太古宙早期的陆壳岩浆事件;结合华北克拉通其它地区的类似研究结果，暗示华北克拉通可能曾经存在比现今出露面积更大的太古宙早期的古老陆壳。这些古老锆石的Hf同位素分析显示，它们的ε_Hf（t）值在-6.19~0.95之间，平均为-2.54，两阶段Hf模式年龄在3737~4353Ma之间，平均值为~4.1Ga，远大于锆石的U-Pb年龄，指示华北克拉通存在~4.1Ga的地壳增生作用及古老陆壳（>3.55Ga）的再循环。

关键词：古老陆壳再循锆石Hf同位素碎屑锆石U-Pb定年胶北地体华北克拉通

U-Pb dating and Hf isotope study of Early Archean zircons from the Jiaobei Terrane, North China Craton: Evidence for growth and recycling of ancient continental crust

LIU JianHui¹, LIU FuLai¹, DING ZhengJiang^2,3, LIU PingHua¹, WANG Fang¹

1. Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China;
2. College of Earth Sciences, Jilin University, Changchun 130061, China;
3. Exploration Institute of Geology and Mineral Resources, Yantai 264000, China

Abstract: Identification and discovery of ancient continental crust is an important part of exploring the crustal evolutionary history of the early Earth, and zircon U-Pb age combined with zircon Hf isotope analysis is the major method of the research. In this study, we have conducted in situ U-Pb dating,rare earth element concentrations and Hf isotope analyses on detrital zircons from one felsic paragneiss sample collected from the Jiaobei Terrane, and many Early Archean detrital zircons have been identified. They are igneous origin on the base of analyses of their CL images, Th/U ratios and chondrite normalized REE patterns. The result of the U-Pb analyses indicates that two zircons yield ~3.40Ga (3413Ma and 3400Ma), and other seven zircons yield a weighted mean ²⁰⁷Pb/²⁰⁶Pb age of 3547±19Ma (MSWD=1.16), suggesting that two magmatic events took place at ~3.40Ga and 3.55Ga, respectively, combined with similar reports of other places in the North China Craton, implying that the Early Archean continental crust is much larger than present exposure of ancient continental crust. Most of these ancient detrital zircons have generally negative ε_Hf(t) values from -6.19~0.95 (average=-2.54), two-stage Hf model ages of 3737~4353Ma (average=~4.1Ga) which are much older than their U-Pb ages, implying the recycling of ancient continental crust (>3.55Ga) and crustal growth prior to 4.1Ga in the North China Craton.

Key words: Ancient continental crust recycling Detrital zircon U-Pb dating Jiaobei Terrane North China Craton

1 引言华北克拉通是全球几个保留有老于~3.8Ga地壳物质的克拉通之一，其早期大陆地壳的形成与演化是地球科学研究中最重要的科学问题之一。目前华北克拉通出露的太古宙岩石主要是~2.5Ga的花岗质(TTG)岩石，其次是~2.7Ga的花岗质(TTG)岩石(Jahn et al., 1988，2008; Guan et al., 2002; Kroner et al., 2005; Wan et al., 2010; 董晓杰等，2012; 马铭株等，2013; Yang et al., 2013)，另外在胶北出露有大面积的~2.9Ga的TTG岩石(Jahn et al., 2008; 刘建辉等，2011; Liu et al., 2013a)。然而，华北克拉通太古宙早期的地壳岩石出露非常有限，主要在辽宁鞍山及冀东地区少量出露(Liu et al., 1992，2008; Song et al., 1996; Zhou et al., 2007; Wu et al., 2008)，这归因于两种可能，一是在太古宙早期，陆壳增生就非常有限；另一种可能是由于后期强烈的岩浆活动及构造运动，使地球最初形成的大陆地壳很难保存下来，其中保留下来的古老地壳岩石为华北克拉通早期大陆地壳的形成及演化历史提供了有限而重要的信息。此外，变质表壳岩中古老的碎屑锆石及晚期侵入岩中捕虏的继承性锆石记录了早期大陆地壳形成及演化历史，是研究地球早期大陆地壳形成及演化的重要途径(Wu et al., 2005，2008; 多吉等，2007; Diwu et al., 2013)，因此，通过对这些锆石的U-Pb年代学分析及Hf同位素分析，能为地球早期大陆地壳形成与演化提供重要的证据和信息。

图 1 华北克拉通构造单元划分(a，据Zhao et al., 2005修改)及胶北地区地质简图与采样位置(b，据山东省地质矿产局，1991; Zhou et al., 2008a，Liu et al., 2013a修改)
YB-阴山地块；KB-孔兹岩带；WB-西部块体；TNCO-中部造山带；EB-东部块体；JLJB-胶-辽-吉带 Fig. 1 Tectonic subdivisions of the North China Craton(a，modified after Zhao et al., 2005) and simplified geological map of the Jiaobei Terrane(b，modified after BGMRS，1991; Zhou et al., 2008a; Liu et al., 2013a)
YB-Yinshan Block; KB-Khondalite Belt; WB-Western Block; TNCO-Trans-North China Orogen; EB-Eastern Block; JLJB-Jiao-Liao-Jiao Belt

本文应用LA-ICP-MS锆石U-Pb原位定年技术首次在胶北一个长英质副片麻岩样品中测定出大量太古宙早期碎屑锆石，结合锆石阴极发光图像及锆石微区原位微量、稀土元素分析，对胶北太古宙早期锆石开展了系统的年代学分析；同时应用锆石原位Hf同位素分析技术对这些太古宙早期锆石开展了原位Hf同位素研究，研究结果为华北克拉通古老陆壳的存在、增生与再循环提供了重要的证据。 2 地质背景及样品

胶北地体是指位于郯庐断裂以东，五莲-烟台断裂以北的地区，在大地构造上位于华北克拉通的东缘，胶-辽-吉构造带的西南端，紧邻苏鲁超高压带(图 1a)。该地体主要由太古宙花岗质(TTG)片麻岩、变质基性-超基性岩及表壳岩，古元古代花岗岩类及变质基性岩，古元古代高级变质的粉子山群及荆山群，低级变质的芝罘群，以及新元古代低级变质的蓬莱群等寒武纪变质-变形基底，中生代花岗岩类及中-新生代沉积地层组成(图 1b)(山东省地质矿产局，1991; 卢良兆，1996; 唐俊等，2004; 周喜文等，2004; Jahn et al., 2008; Zhou et al., 2008a，b; 李旭平等，2011; Liu et al., 2013a，b)。

太古宙花岗质(TTG)片麻岩主要在栖霞附近呈穹窿状大面积出露，主要包括~2.9Ga，~2.7Ga及~2.5Ga三期岩浆事件，并经历了~2.5Ga和~1.86Ga两期变质热事件(Jahn et al., 2008; Zhou et al., 2008a; 刘建辉等，2011; Liu et al., 2013a)；这些片麻岩普遍遭受强烈剪切变形作用，定向构造发育，常形成条纹和条带状构造，内部流柔褶皱发育(刘建辉等，2011)。在TTG片麻岩内部，斜长角闪片麻岩、黑云母变粒、黑云斜长片麻岩及变质基性-超基性岩呈大小不等的透镜体或不规则脉状体产出，同样显示遭受强烈剪切变形，深熔混合岩化作用强烈(刘建辉等，2011；刘平华等， 2011a，b，2012)。古元古代花岗岩类出露面积较小，呈零星分布，根据其侵位时间及变形作用，可划分为构造前变形花岗质片麻岩类及构造后末变形的花岗岩类，它们可与辽-吉地区的古元古代花岗岩类对比(Liu et al., 2014)。胶北地体内古元古代孔兹岩系(包括粉子山群、荆山群)不整合于TTG片麻岩之上，其具有3.34~2.20Ga的碎屑锆石U-Pb年龄(Wan et al., 2006)。这些组成胶北地体早前寒武变质基底的岩石，经历了高角闪岩相-麻粒岩相变质作用，具有顺时针P-T演化路径(刘文军等，1998; 周喜文等，2004; 刘平华等， 2010，2013; 王舫等，2010; Tam et al., 2011，2012a，b，c; Liu et al., 2013c)，并伴随普遍的深熔作用。变质锆石U-Pb年代学研究表明，其变质作用的时间约为1.85~1.95Ga(Zhou et al., 2008b; Tam et al., 2011，2012a，b; 刘福来等，2012; Liu et al., 2013c)，其中高压麻粒岩相峰期变质时间约在1.85~1.90Ga之间(刘平华等， 2011a，b; Liu et al., 2013c)。芝罘群主要分布在芝罘岛，碎屑锆石U-Pb年代学分析结果显示其沉积时代应晚于约1.8Ga(Liu et al., 2013b)。新元古代蓬莱群是一套绿片岩相-低角闪岩相的浅变质岩系(山东省地质矿产局，1991; Zhou et al., 2008a)，目前，对于其形成的构造背景、沉积时间及属性仍有争议(Li et al., 2007; Zhou et al., 2008a; 初航等，2011)。

图 2 样品QX2-4b的野外照片及显微照片
Pl-斜长石；Kfs-钾长石；Qtz-石英；Bt-黑云母 Fig. 2 Photographs of outcrops and photomicrographs of the sample QX2-4b
Pl-plagioclase; Kfs-K-feldspar; Qtz-quartz; Bt-biotite

本文用于锆石U-Pb定年及Hf同位素分析的样品QX2-4b为浅色中细粒长英质副片麻岩，采自莱阳北西留镇东采矿坑(图 1b)。岩石呈灰白色，弱片麻状、条带状构造(图 2a)，不等粒变晶结构，主要矿物组合为：石英(45%)+斜长石(30%)+钾长石(20%)，以及少量黑云母，石英及长石呈他形，弱定向排列，可见斜长石残斑(图 2b)。周边有古元古代~2.1Ga变质辉长岩(刘平华等，2013)，太古宙花岗质片麻岩及古元古代荆山群，由于出露不好，其与其它岩体的产出关系不清。 3 分析方法

LA-ICP-MS锆石U-Pb原位定年及锆石微区微量、稀土元素分析在中国地质大学(北京)地学实验中心元素地球化学实验室进行。分析仪器采用由美国New Wave Research公司生产的激光剥蚀进样系统(UP193SS)和美国AGLENT科技有限公司生产的Agilent 7500型四级杆等离子体质谱仪联合构成的激光等离子质谱仪。分析时采用10Hz的激光频率，193nm的激光波长，36μm的激光束斑直径，激光预剥蚀时间和剥蚀时间分别为5s和45s，U、Th、Pb元素积分时间为20ms，其它元素积分时间为15ms。年龄计算时以标准锆石91500为外标进行同位素比值校正，以TEM为监控盲样；元素含量以国际标样NIST612为外标，Si为内标计算；普通铅校正与Andersen(2002)方法相同，数据采用Glitter 4程序进行处理。

锆石Hf同位素测试在中国地质科学院矿产资源研究所国土资源部成矿作用与资源评价重点实验室Neptune多接收等离子质谱和New Wave UP213紫外激光剥蚀系统(LA-MC-ICP-MS)上进行，锆石Hf同位素分析在U-Pb年龄分析点原位进行，实验过程中采用He作为剥蚀物质载气，激光剥蚀束直径采用55μm，激光剥蚀时间约为27s。测定时选用锆石国际标样GJ-1作为参考物质。相关仪器运行条件及详细分析流程与侯可军等(2007)相同。分析过程中锆石标样GJ-1的¹⁷⁶Hf/¹⁷⁷Hf测试加权平均值为0.282012±17(2SD，n=24)，与文献报道值(Elhlou et al., 2006; 侯可军等，2007)在误差范围内完全一致。在ε_Hf(t)计算时，球粒陨石的¹⁷⁶Hf/¹⁷⁷Hf比值为0.282772，¹⁷⁶Lu/¹⁷⁷Hf比值为0.0332(Blichert-Toft and Albarede， 1997)。在单阶段Hf模式年龄(t_DM)计算时，亏损地幔的¹⁷⁶Hf/¹⁷⁷Hf比值和¹⁷⁶Lu/¹⁷⁷Hf比值分别为0.28325和0.0384(Griffin et al., 2000)；在两阶段Hf模式年龄(t_DM(Hf2))计算时，下地壳、平均地壳与亏损地幔的f_Lu/Hf比值分别为-0.32、-0.5482及0.1566(Amelin et al., 1999; Griffin et al., 2000，2002)。¹⁷⁶Lu的衰变常量选用1.867×10^-11 year^-1(Soderlund et al., 2004; Amelin，2005)；相关计算中锆石的U-Pb年龄选择单点²⁰⁷Pb/²⁰⁶Pb年龄，相关计算公式参考吴福元等(2007) 4 分析结果 4.1 锆石U-Pb定年

该样品锆石主要呈紫红色或黄褐色；晶形以半自形或他形为主，少量为自形晶，锆石形态多样，以短柱状及椭圆状锆石为主，显示了一定的磨圆作用及机械破碎。CL图像显示它们既有具岩浆韵律环带的岩浆锆石，也有无明显内部结构的变质增生边或变质锆石(图 3)。在锆石形态及内部结构分析基础上，采用LA-ICP-MS法对该样品的40个锆石进行原位U-Pb年龄测试及微量、稀土元素分析。分析结果显示，锆石²⁰⁷Pb/²⁰⁶Pb年龄在1861~3583Ma之间(表 1)，包括1个1861Ma(点1)的古元古代变质年龄；3个约2.1~2.2Ga(点12、30及37)岩浆锆石年龄，它们与胶北古元古代花岗质岩石的侵位年龄一致(Liu et al., 2014)；另外18个分析点给出了2524±28Ma(MSWD=0.82)的²⁰⁷Pb/²⁰⁶Pb加权平均年龄(图 4a)，这些分析点具有较高的Th/U比值(表 1)，重稀土相对富集，轻稀土相对亏损，具有明显的负Eu异常和明显的正Ce异常(图 4b)，显示出典型岩浆锆石的稀土配分曲线模式(Hoskin and Schaltegger， 2003; Liu et al., 2010)，结合锆石的内部结构，其应代表胶北约2.5Ga的岩浆事件年龄；除了约2.5Ga的岩浆锆石年龄外，同时也获得了约2.5Ga的变质事件年龄(如点32)；另外4个锆石分析点(点16、20、29及40)分别给出了2770Ma、2754Ma、2756Ma及2739Ma的²⁰⁷Pb/²⁰⁶Pb年龄，它们应代表胶北约2.7Ga的岩浆事件年龄。

图 3 样品QX2-4b代表性太古宙早期锆石及其它锆石阴极发光图像、²⁰⁷Pb/²⁰⁶Pb年龄及ε_Hf(t)值 Fig. 3 Representative cathodoluminescence(CL)images of Early Archean and others zircons from the sample QX2-4b with ²⁰⁷Pb/²⁰⁶Pb ages and ε_Hf(t)values

图 4 样品QX2-4b的锆石U-Pb年龄谐和图(a)及锆石分析微区球粒陨石标准化稀土元素配分曲线(b，c) Fig. 4 U-Pb concordia diagram(a) and chondrite-normalized REE patterns(b，c)of different zircons from the sample QX2-4b

表 1 胶北样品QX2-4b的LA-ICP-MS锆石U-Pb数据表Table 1 The LA-ICP-MS zircon U-Pb isotopic data of the sample QX2-4b from the Jiaobei Terrane

测点号	含量(×10^-6)			同位素比值						年龄(Ma)
测点号	Th	U	Pb	Th/U	²⁰⁷Pb ²³⁵U	1σ	²⁰⁶Pb ²³⁸U	1σ	²⁰⁷Pb ²⁰⁶Pb	1σ	²⁰⁶Pb ²³⁸U	1σ	²⁰⁷Pb ²³⁵U	1σ	²⁰⁷Pb ²⁰⁶Pb	1σ
QX24B-01	316	878	329	0.36	5.28331	0.13377	0.33659	0.0046	0.11382	0.00278	1870	22	1866	22	1861	26
QX24B-02	66	41	28	1.58	10.50443	0.29871	0.46857	0.00697	0.16256	0.00454	2477	31	2480	26	2482	28
QX24B-03	183	223	175	0.82	18.48131	0.47188	0.5972	0.00824	0.22441	0.00554	3019	33	3015	25	3013	24
QX24B-04	29	86	75	0.34	27.39653	0.72115	0.6928	0.00992	0.28676	0.00734	3393	38	3398	26	3400	24
QX24B-05	324	362	286	0.89	18.52219	0.47511	0.5904	0.00814	0.22749	0.00564	2991	33	3017	25	3034	24
QX24B-06	151	193	118	0.78	11.26428	0.29959	0.48248	0.00678	0.16929	0.00438	2538	29	2545	25	2551	26
QX24B-07	15	25	15	0.61	11.51618	0.39712	0.48746	0.00818	0.17131	0.00591	2560	35	2566	32	2570	35
QX24B-08	276	379	222	0.73	10.57062	0.27623	0.47186	0.00651	0.16245	0.00411	2492	29	2486	24	2481	26
QX24B-09	40	56	34	0.70	11.00643	0.32013	0.48454	0.00725	0.16472	0.00471	2547	31	2524	27	2505	29
QX24B-10	68	83	51	0.81	11.13548	0.30914	0.48075	0.00693	0.16796	0.00456	2531	30	2535	26	2537	28
QX24B-11	251	320	195	0.78	11.34899	0.30345	0.48489	0.00676	0.16972	0.00441	2549	29	2552	25	2555	26
QX24B-12	279	333	163	0.84	7.30014	0.19781	0.39069	0.00546	0.13549	0.00357	2126	25	2149	24	2170	28
QX24B-13	374	391	400	0.96	31.09207	0.82467	0.72519	0.01005	0.3109	0.008	3515	38	3522	26	3525	24
QX24B-14	121	248	242	0.49	33.04355	0.87984	0.74265	0.01031	0.32265	0.00833	3580	38	3582	26	3583	24
QX24B-15	85	187	172	0.45	30.03508	0.80599	0.7094	0.00991	0.30702	0.008	3456td>	37	3488	26	3506	25
QX24B-16	112	117	83	0.96	14.35584	0.39739	0.53863	0.00764	0.19327	0.00522	2778	32	2774	26	2770	27
QX24B-17	61	136	83	0.45	13.07075	0.36357	0.5177	0.00735	0.18308	0.00497	2689	31	2685	26	2681	28
QX24B-18	63	119	89	0.53	18.85134	0.52306	0.60013	0.00852	0.22778	0.00616	3030	34	3034	27	3037	27
QX24B-19	58	178	97	0.32	10.94286	0.30467	0.47813	0.00674	0.16596	0.0045	2519	29	2518	26	2517	28
QX24B-20	375	459	312	0.82	14.02088	0.38555	0.53137	0.0074	0.19134	0.00512	2747	31	2751	26	2754	27
QX24B-21	61	136	129	0.45	31.85416	0.89004	0.73057	0.01039	0.31617	0.00861	3536	39	3546	28	3551	26
QX24B-22	87	771	398	0.11	10.76332	0.29818	0.47407	0.00659	0.16464	0.00444	2501	29	2503	26	2504	28
QX24B-23	20	83	45	0.24	10.99544	0.32326	0.47796	0.00697	0.16682	0.00481	2518	30	2523	27	2526	30
QX24B-24	256	275	171	0.93	11.24323	0.31775	0.48309	0.0068	0.16877	0.00465	2541	30	2544	26	2545	29
QX24B-25	207	338	196	0.61	10.90427	0.3082	0.47895	0.00672	0.16509	0.00455	2523	29	2515	26	2508	29
QX24B-26	68	130	74	0.52	11.06418	0.32392	0.48043	0.0069	0.167	0.00479	2529	30	2529	27	2528	30
QX24B-27	113	278	263	0.41	32.00062	0.91136	0.7334	0.01031	0.3164	0.00878	3546	38	3550	28	3552	27
QX24B-28	438	367	235	1.20	11.07487	0.31873	0.47504	0.00669	0.16906	0.00475	2506	29	2529	27	2548	30
QX24B-29	41	87	55	0.47	14.05343	0.41481	0.53191	0.00768	0.19159	0.00554	2749	32	2753	28	2756	30
QX24B-30	91	135	66	0.68	7.6981	0.23513	0.40054	0.00583	0.13937	0.00418	2172	27	2196	27	2219	33
QX24B-32	47	615	312	0.08	10.67255	0.31197	0.47053	0.00663	0.16448	0.0047	2486	29	2495	27	2502	30
QX24B-33	89	179	161	0.50	27.81943	0.81902	0.69746	0.00994	0.28923	0.00832	3411	38	3413	29	3413	28
QX24B-34	39	38	25	1.01	11.39377	0.38121	0.48673	0.00774	0.16974	0.00564	2557	34	2556	31	2555	35
QX24B-35	133	405	359	0.33	30.23671	0.89082	0.69836	0.00986	0.31396	0.00904	3414	37	3495	29	3540	28
QX24B-36	272	220	144	1.23	11.17428	0.33888	0.48191	0.00691	0.16814	0.005	2536	30	2538	28	2539	32
QX24B-37	368	246	134	1.50	7.1095	0.21873	0.3894	0.00561	0.13239	0.004	2120	26	2125	27	2130	34
QX24B-38	241	649	355	0.37	10.8104	0.3275	0.47647	0.00678	0.16452	0.00488	2512	30	2507	28	2503	32
QX24B-39	84	175	166	0.48	32.1165	0.9755	0.7245	0.01041	0.32144	0.00956	3513	39	3554	30	3577	29
QX24B-40	167	118	89	1.41	13.84536	0.42815	0.52952	0.00767	0.1896	0.00575	2739	32	2739	29	2739	32

表 1 胶北样品QX2-4b的LA-ICP-MS锆石U-Pb数据表Table 1 The LA-ICP-MS zircon U-Pb isotopic data of the sample QX2-4b from the Jiaobei Terrane

除了以上胶北地区主要的早前寒武纪岩浆-变质事件锆石年龄外，本次测试获得了大量太古宙早期的锆石²⁰⁷Pb/²⁰⁶Pb年龄(表 1)，其中9个分析点(点4、13、14、15、21、27、33、35及39)的锆石年龄>3.4Ga，为古太古代年龄(表 1)，这些锆石呈柱状或椭圆状，以半自形或他形为主，CL图像呈暗色调，有的显示了韵律环带或梳状环带，有的则无明显的韵律环带(图 3)。锆石U-Pb及稀土、微量元素分析显示它们具有较高的Th/U比值(表 1)，重稀土相对富集，轻稀土相对亏损，具有明显的负Eu异常和明显的正Ce异常(图 4c)，显示出典型岩浆锆石的特征；这些分析点中7个给出3547±19Ma(MSWD=1.16)的²⁰⁷Pb/²⁰⁶Pb加权平均年龄(图 4a)，我们将其解释为太古宙早期的岩浆事件年龄。 4.2 锆石Hf同位素分析

本次测试对样品QX2-4b的36个锆石进行了Hf同位素分析，锆石的Hf同位素分析结果如表 2和图 5所示。所有锆石分析点的¹⁷⁶Lu/¹⁷⁷Hf比值小(绝大部分小于0.002)，表明锆石形成以后具有较低的放射成因Hf的积累。具有古太古代锆石U-Pb年龄(>3.3Ga)的分析点的¹⁷⁶Hf/¹⁷⁷Hf比值分布于0.280433~0.280655之间，其它锆石的¹⁷⁶Hf/¹⁷⁷Hf比值分布于0.280879~0.281444之间(表 2及图 5a)。以锆石单点²⁰⁷Pb/²⁰⁶Pb年龄计算的ε_Hf(t)值在-12.25~9.56之间，其中10个古太古代锆石的ε_Hf(t)值在-6.19~0.95之间，平均值为-2.54(表 2及图 5b)。两阶段Hf模式年龄(t_DM(Hf2))在2416~4353Ma之间，其中古太古代锆石的两阶段Hf模式年龄在3737~4353Ma之间，平均值为4101Ma，两阶段Hf模式年龄均大于锆石单点的²⁰⁷Pb/²⁰⁶Pb年龄(表 2及图 5c)。

表 2 胶北样品QX2-4b的LA-MC-ICP-MS锆石原位Hf同位素数据Table 2 The LA-MC-ICP-MS zircon in situ Hf isotopic data of the sample QX2-4b from the Jiaobei Terrane

Spot No.	Age (Ma)	¹⁷⁶Yb ¹⁷⁷Hf	¹⁷⁶Lu ¹⁷⁷Hf	¹⁷⁶Hf ¹⁷⁷Hf	2σ	ε_Hf(0)	ε_Hf(t)	2σ	t_DM(Ma)	t_DM(Hf2)(Ma)	2σ	t_DM(Hf)^C (Ma)	f_Lu/Hf
QX2-4b 01	2482	0.046014	0.000756	0.281168	0.000020	-56.72	-2.32	0.72	2883	3398	27	3128	-0.98
QX2-4b 02	3013	0.212873	0.003797	0.281217	0.000032	-55.00	5.20	1.13	3058	3108	47	3080	-0.89
QX2-4b 03	3400	0.027144	0.000496	0.280655	0.000025	-74.85	0.95	0.88	3546	3737	33	3637	-0.99
QX2-4b 04	3034	0.076776	0.001435	0.280879	0.000019	-66.94	-1.48	0.69	3330	3697	26	3501	-0.96
QX2-4b 05	2551	0.098590	0.001683	0.281271	0.000024	-53.07	1.30	0.84	2811	3131	33	2960	-0.95
QX2-4b 06	2570	0.005416	0.000109	0.281244	0.000015	-54.02	3.52	0.54	2734	2952	20	2839	-1.00
QX2-4b 07	2481	0.109993	0.002273	0.281345	0.000031	-50.47	1.39	1.09	2753	3076	43	2900	-0.93
QX2-4b 08	2505	0.034688	0.000620	0.281079	0.000026	-59.86	-4.72	0.92	2992	3621	35	3291	-0.98
QX2-4b 09	2537	0.039414	0.000734	0.281356	0.000025	-50.06	5.66	0.89	2627	2743	34	2682	-0.98
QX2-4b 10	2555	0.030629	0.000520	0.281444	0.000024	-46.96	9.56	0.86	2495	2416	33	2457	-0.98
QX2-4b 11	3525	0.095941	0.001500	0.280580	0.000019	-77.52	-1.27	0.69	3742	4010	26	3867	-0.95
QX2-4b 12	3583	0.062383	0.001130	0.280560	0.000021	-78.22	0.24	0.77	3733	3921	29	3821	-0.97
QX2-4b 13	3506	0.046181	0.000783	0.280503	0.000023	-80.25	-2.72	0.81	3776	4121	30	3939	-0.98
QX2-4b 14	2770	0.018978	0.000392	0.281132	0.000023	-57.98	3.62	0.83	2904	3079	31	2988	-0.99
QX2-4b 15	2681	0.043985	0.000866	0.281274	0.000024	-52.97	5.76	0.87	2748	2833	33	2788	-0.97
QX2-4b 16	3037	0.020603	0.000384	0.280905	0.000024	-66.02	1.69	0.85	3206	3427	32	3312	-0.99
QX2-4b 17	2517	0.043410	0.001098	0.281353	0.000020	-50.18	4.46	0.73	2657	2834	28	2740	-0.97
QX2-4b 18	2754	0.032033	0.000631	0.281140	0.000022	-57.72	3.07	0.78	2912	3115	29	3009	-0.98
QX2-4b 19	3551	0.052472	0.000918	0.280483	0.000019	-80.94	-2.71	0.66	3815	4150	25	3973	-0.97
QX2-4b 20	2504	0.032783	0.000711	0.281059	0.000018	-60.58	-5.62	0.64	3027	3699	24	3346	-0.98
QX2-4b 21	2526	0.032085	0.000614	0.281385	0.000020	-49.04	6.65	0.73	2580	2650	28	2613	-0.98
QX2-4b 22	2545	0.062081	0.001227	0.281112	0.000022	-58.69	-3.69	0.80	2995	3559	31	3259	-0.96
QX2-4b 23	2508	0.044979	0.000777	0.281152	0.000018	-57.31	-2.35	0.65	2907	3419	25	3150	-0.98
QX2-4b 24	2528	0.015091	0.000349	0.281116	0.000021	-58.58	-2.45	0.74	2923	3440	28	3171	-0.99
QX2-4b 25	3552	0.048965	0.000890	0.280497	0.000020	-80.46	-2.13	0.70	3794	4102	26	3939	-0.97
QX2-4b 26	2548	0.097092	0.001766	0.281282	0.000023	-52.71	1.46	0.81	2803	3115	32	2948	-0.95
QX2-4b 27	2756	0.027532	0.000610	0.281126	0.000022	-58.20	2.67	0.77	2929	3151	29	3035	-0.98
QX2-4b 28	2502	0.019956	0.000383	0.281291	0.000017	-52.36	3.15	0.61	2691	2937	23	2809	-0.99
QX2-4b 29	3413	0.048672	0.000820	0.280468	0.000019	-81.48	-6.19	0.66	3825	4353	25	4075	-0.98
QX2-4b 30	2555	0.037493	0.000628	0.281108	0.000022	-58.86	-2.60	0.80	2955	3471	30	3201	-0.98
QX2-4b 31	3540	0.047264	0.000788	0.280451	0.000018	-82.07	-3.79	0.66	3844	4234	24	4029	-0.98
QX2-4b 32	3373	0.064142	0.001011	0.280577	0.000022	-77.63	-3.67	0.78	3699	4112	29	3894	-0.97
QX2-4b 33	2539	0.146929	0.002380	0.281418	0.000029	-47.87	5.07	1.02	2657	2796	40	2720	-0.93
QX2-4b 34	2503	0.133667	0.002088	0.280939	0.000024	-64.81	-12.25	0.84	3304	4268	33	3747	-0.94
QX2-4b 35	3577	0.053194	0.000919	0.280433	0.000020	-82.72	-3.91	0.72	3882	4269	27	4065	-0.97
QX2-4b 36	2739	0.025806	0.000478	0.280950	0.000018	-64.44	-3.74	0.65	3154	3693	24	3411	-0.99

表 2 胶北样品QX2-4b的LA-MC-ICP-MS锆石原位Hf同位素数据Table 2 The LA-MC-ICP-MS zircon in situ Hf isotopic data of the sample QX2-4b from the Jiaobei Terrane

图 5 样品QX2-4b锆石Hf同位素分析
(a)-¹⁷⁶Lu/¹⁷⁷Hf比值对¹⁷⁶Hf/¹⁷⁷Hf比值及变化；(b)-锆石²⁰⁷Pb/²⁰⁶Pb年龄对ε_Hf(t)值及变化；(c)-两阶段Hf模式年龄直方柱状图 Fig. 5 Zircon Hf isotopic composition of the sample QX2-4b
(a)-¹⁷⁶Lu/¹⁷⁷Hf-¹⁷⁶Hf/¹⁷⁷Hf variations;(b)-zircon ²⁰⁷Pb/²⁰⁶Pb age-ε_Hf(t)variations;(c)-histograms of the two-stage Hf model ages

5 讨论与结论

古老陆壳物质的发现与鉴别是探索地球早期地壳形成与演化历史的重要内容之一，锆石U-Pb年龄结合Hf同位素研究是该研究的重要手段。本次对胶北地体内一个长英质副片麻岩样品的LA-ICP-MS锆石U-Pb定年结果显示，~2.5Ga岩浆锆石是该样品最主要的锆石组份，同时也有~2.7Ga岩浆锆石，~1.85Ga及~2.5Ga两期变质锆石，除了以上胶北地区常见的岩浆-变质热事件年龄外，还包含有大量太古宙早期的锆石U-Pb年龄(图 4a及表 1)。根据锆石阴极发光图像、Th/U比值及稀土元素球粒陨石标准化配分模式(图 3、图 4c及表 1)，这些太古宙早期的锆石大部分具有典型岩浆锆石的特征，表明它们的锆石U-Pb年龄代表岩浆事件年龄，它们分别是~3.4Ga(3413Ma及3400Ma两个数据)及3.55Ga(7个U-Pb分析点给出3547±19Ma，MSWD=1.16)两期岩浆事件(图 4a及表 1)，此外，胶北中生代花岗岩中捕掳有大量类似年龄的继承锆石(Wang et al., 1998)，这表明在胶北地体中可能存在太古宙早期的古老地壳。此外，除了在辽宁鞍山地区发现~3.8Ga的大陆地壳岩石外，还在冀东、胶北、蚌埠、河南焦作及信阳、秦岭、内蒙固阳等地发现大量太古宙早期(>3.2Ga)的古老碎屑锆石或继承/残余锆石(Liu et al., 1992，2008; Song et al., 1996; Wang et al., 1998，2007; 靳克等，2003; Zheng et al., 2004; 简平等，2005; Wu et al., 2005，2008; Gao et al., 2006; Wan et al., 2006; Zhou et al., 2007; Diwu et al., 2013)，这些研究结果表明，华北克拉通可能曾经存在比现今出露面积更大的太古宙早期的古老陆壳。

锆石Hf同位素被证明是一种示踪岩浆源区，岩石成因及约束地壳增生演化极佳的方法(Kinny and Maas， 2003; 吴福元等，2007)。岩浆锆石的结晶年龄通常被理解为寄主岩石形成的时间，而锆石Hf同位素模式年龄则代表原岩物质从亏损地幔抽取的时间(Amelin et al., 2000; Griffin et al., 2000; 吴福元等，2007)；正的锆石ε_Hf(t)值指示来自新生地壳的重熔，而负的ε_Hf(t)值则表明来自老地壳的部分熔融(Kinny and Maas， 2003)；锆石U-Pb测年揭示了胶北可能存在~3.4Ga及~3.55Ga太古宙早期的古老陆壳岩石。这些太古宙早期锆石的Hf同位素分析显示，它们的ε_Hf(t)值在-6.19~0.95之间，除两个分析点具较小的正ε_Hf(t)值(0.95及0.24)外，其它分析点均具有负的的ε_Hf(t)值；两阶段Hf模式年龄在3737~4353Ma之间，平均值为4101Ma，远大于锆石结晶年龄(表 2)，表明胶北太古宙早期(~3.4Ga和~3.55Ga)碎屑锆石的源区岩石形成于古老陆壳物质的再循环；也暗示华北克拉通在~4.1Ga之前就存地壳增生作用。

致谢中国地质大学(北京)苏犁教授和于红、张红雨、李弦博士在锆石LA-ICP-MS定年和微量、稀土元素分析中提供了帮助；中国地质科学院矿产资源研究所侯可军博士、郭春丽副研究员在锆石原位Hf同位素测试分析中提供了帮助；中国科学院地质与地球物理研究所纪伟强副研究员在锆石Hf同位素计算及解释过程中提供了帮助；两位论文评审人审阅全文并提出宝贵的修改意见；在此一致表示感谢。

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岩石学报 2014, Vol. 30 Issue (10): 2941-2950	PDF