2021, Vol. 37
2. 中国地质科学院地质研究所, 自然资源部深地动力学重点实验室, 北京 100037
2. Key laboratory of Deep-Earth Dynamics of Ministry of Natural Resources, Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China
三江地区位于欧亚板块与印度板块结合部位，自早古生代以来经历了一系列的裂解、汇聚、碰撞和增生等重大地质事件。南澜沧江带位于三江地区南段，带内出露保存比较完整的、典型的蛇绿混杂岩，大量与古特提斯洋洋壳俯冲、陆-陆碰撞有关的岩浆岩以及三叠纪的榴辉岩、蓝片岩等，是研究古特提斯洋演化的重要地区(张旗等，1985；莫宣学等, 1993, 1998；Peng et al., 2008, 2013；Wang et al., 2010, 2013a, 2018b, 2019a, b；Fan et al., 2015；王保弟等，2018)。近年来，南澜沧江带内陆续识别出多处十分重要的奥陶纪-二叠纪的岩浆事件。其中早古生代的岩浆事件普遍被认为与原特提斯洋的演化有关，而晚古生代(晚石炭世-二叠纪)的岩浆岩被认为与古特提斯洋演化有关。例如，昌宁-孟连蛇绿混杂岩中辉长岩、玄武岩的锆石U-Pb年龄为471~439Ma，指示这些蛇绿混杂岩的形成时代可追溯到早古生代(Wang et al., 2013a；刘桂春等，2017；孙载波等，2017)，代表了原特提斯洋壳的残余(王保弟等，2018)。惠民、曼来等地发育的奥陶纪-志留纪岩浆岩被认为与原特提斯洋的俯冲消减过程有关(毛晓长等，2012；Lehmann et al., 2013；Nie et al., 2015；Xing et al., 2017；彭智敏等，2018；Liu et al., 2019)。与以上早古生代岩浆事件不同，半坡-雅口-南联山晚石炭世-早二叠世(313~282Ma)基性-超基性杂岩被认为形成于与古特提斯洋俯冲作用有关的岛弧环境或弧后拉张环境(Hennig et al., 2009；Jian et al., 2009；Li et al., 2012；Zhai et al., 2019)。少量的二叠纪花岗闪长岩被解释为古特提斯洋俯冲过程中形成的岛弧岩浆岩(284~282Ma，Hennig et al., 2009；261~252Ma，Deng et al., 2018)。除早古生代蛇绿混杂岩外，昌宁-孟连缝合带中还发育267~272Ma的蛇绿混杂岩(Jian et al., 2009；王冬兵等，2017)。一些研究人员认为西南三江地区存在连续的原-古特提斯演化，昌宁-孟连洋盆可能在中奥陶世已经打开，并一直延续到晚二叠世(Deng et al., 2014；王保弟等，2018)。由于研究对象十分有限，早古生代至晚石炭世之间的演化过程研究程度较低，这也制约了原、古特提斯洋之间关系的研究。尽管景洪东南部出露的南光组沉积岩中保存晚泥盆世(382~366Ma)的凝灰岩夹层，为衔接原、古特提斯洋之间的构造演化提供了重要的研究对象，但由于遭受了强烈的风化改造，无法获取这些火山岩的岩石类型，成因等方面的信息(Nie et al., 2016)。最近，作者在景洪南部的南联山地区新识别出一套新鲜的晚泥盆世英安质火山岩。本研究系统报道了该套火山岩的锆石U-Pb年龄，Hf-O同位素以及全岩地球化学，探讨了岩石的成因、形成环境，并结合前人已发表资料，为南澜沧江带原、古特提斯洋之间的构造演化过程提供一些新的制约。
1 地质概况和样品采集南澜沧江带从西向东主要可分为昌宁-孟连缝合带、澜沧变质杂岩、临沧花岗岩基以及云县-景洪火山岩带四个地质单元(图 1)。昌宁-孟连缝合带代表古特提斯洋主洋盆闭合的位置，缝合带内的铜厂街、南汀河、牛井山以及曼信等地出露比较完整、典型的奥陶纪-晚二叠世(471~267Ma)的蛇绿混杂岩(张旗等，1985；Jian et al., 2009；Wang et al., 2013a；刘桂春等，2017；王冬兵等，2017；王保弟等，2018)，与蛇绿混杂岩相伴生的泥盆纪-中三叠世硅质岩中含深海放射虫组合(吴浩若和李红生，1989；Liu et al., 1991；Feng，1992；冯庆来和刘本培，1993；刘本培等，1993；Fang et al., 1994；冯庆来等, 1996, 1997；Feng et al., 1998；方宗杰等，2000)。澜沧变质杂岩主要由崇山群、大勐龙群、澜沧群和西盟群组成，榴辉岩、蓝片岩以透镜体或夹层的形式零星出露在澜沧群中(徐桂香等，2016；李静等，2017；Wang et al., 2019b)。蓝片岩、榴辉岩以及澜沧群变沉积岩均记录了246~229Ma的高压变质作用(Fan et al., 2015；王舫等，2016；Wang et al., 2019a, b，2020)。澜沧群变沉积岩中碎屑锆石年龄主要分布在600~500Ma和1200~900Ma(Zhao et al., 2017；王舫等，2017；Wang et al., 2020)。临沧花岗岩基主要由黑云母二长花岗岩和花岗闪长岩组成。黑云母二长花岗岩为主体岩性，属过铝质S型花岗岩，主要形成于235~210Ma(Peng et al., 2006, 2013；Hennig et al., 2009；孔会磊等，2012；Dong et al., 2013；王舫等，2014)。花岗闪长岩分布在花岗岩基的边部或呈不规则状、岛弧状或条带状分布在二长花岗岩中(Peng et al., 2006)，最近报道的少量花岗闪长岩的锆石U-Pb年龄为261~252Ma(Deng et al., 2018)。此外，临沧花岗岩中还存在奥陶纪S型花岗片麻岩(477~466Ma)(彭智敏等，2018)。云县-景洪火山岩位于临沧花岗岩体东侧，呈南、北向狭长带状分布(图 1)，出露安山岩、英安岩、玄武岩、流纹岩、火山角砾岩等多种类型岩石，这些火山岩原来被认为主要形成于二叠纪-三叠纪，目前报道的形成年龄主要集中在249~197Ma之间(图 1；Peng et al., 2006, 2008, 2013；Wang et al., 2010；朱维光等，2011；陈莉等，2013；韦诚等，2016；吕留彦等，2019)。除二叠纪-三叠纪火山岩外，带内还保存少量志留-泥盆纪的火山岩，例如大中河、大平掌地区429~418Ma的基性-酸性火山岩(毛晓长等，2012；Lehmann et al., 2013；Liu et al., 2019)，景洪东南部南光组碎屑沉积岩中382~366Ma的薄层状凝灰岩夹层(Nie et al., 2016)。
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图 1 东南亚构造格架图(a，据Cawood et al., 2018修改)和南澜沧江带地质简图(b) 图a中主要的缝合带：CMS-昌宁-孟连缝合带; LCSS-龙木错-双湖缝合带; IBRS-因他暖-文冬-劳勿缝合带; JASS-金沙江-哀牢山-松马缝合带. 图b数据来自: (1)本次研究; (2)王冬兵等(2016); (3)彭智敏等(2018); (4)Nie et al.(2015); (5)Xing et al.(2017); (6)Lehmann et al.(2013); (7)毛晓长等(2012); (8)Liu et al.(2019); (9)Nie et al.(2016); (10) Hennig et al.(2009) Fig. 1 Tectonic framework of southeastern Asia(a, modified after Cawood et al., 2018) and simplified geological map of the southern Lancangjiang belt, SW China Main suture zones between major blocks in Fig. 1a: CMS-Changning-Menglian suture; LCSS-Longmu Co-Shuanghu suture; IBRS-Inthanon-Bentong-Raub suture; JASS-Jinshajiang-Ailaoshan-Song Ma suture. Ages of magmatic rocks in Fig. 1b from: (1)this study; (2)Wang et al.(2016); (3)Peng et al.(2018); (4)Nie et al.(2015); (5)Xing et al.(2017); (6)Lehmann et al.(2013); (7)Mao et al.(2012); (8)Liu et al.(2019); (9)Nie et al.(2016); (10) Hennig et al.(2009) |
本文研究区位于云县-景洪火山岩带南部的南联山地区(图 1)，该地区出露岩石主要为南联山岩体和二叠纪的火山岩、沉积岩。南联山岩体主要由辉长岩和闪长岩组成，形成于298~292Ma(Hennig et al., 2009；Li et al., 2012)。二叠纪火山岩由英安岩、玄武岩和凝灰岩等岩石组成，二叠纪沉积岩岩性主要为板岩夹粉砂岩。本文所采样品位于南联山岩体东侧的一处正在施工的隧道附近，该处堆积大量隧道中开采出的新鲜岩石，包括基性-超基性岩、千枚岩，片岩以及英安质晶屑凝灰岩等(图 2a)。碎石堆旁可见二叠纪流纹岩的原地露头，岩石呈紫红色，中等风化(图 2c)。本文研究的火山岩为采自隧道口碎石堆的英安质晶屑凝灰岩，样品新鲜，呈灰白色，片麻状构造，晶屑破碎较严重，主要由石英和斜长石组成，基质主要由细粒的斜长石和石英组成(图 2b, d)。
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图 2 野外照片及显微结构照片 (a)采样碎石堆野外照片；(b)英安质晶屑凝灰岩野外照片；(c)碎石堆旁二叠纪流纹岩露头野外照片；(d)英安质晶屑凝灰岩显微照片. Pl-斜长石；Qz-石英；Amph-角闪石 Fig. 2 Representative field and microtexture photographs (a)field photograph of the sampled scree; (b)field photograph of dacitic crystal tuff; (c)field photograph of Permian rhyolite outcrop near the sampled scree; (d)photomicrographs of dacitic crystal tuff. Pl-plagioclase; Qz-quartz; Amph-amphibole |
全岩主量元素、微量元素在澳实分析检测(广州)有限公司完成。首先将新鲜、均匀的岩石样品细碎至200目。主量元素分析将粉末样品与硼酸锂-硝酸锂混合熔融，采用熔片-X射线荧光光谱法(XRF)测试，FeO采用酸消解-重铬酸钾滴定法分析，主量元素分析精度优于5%。微量元素分析将粉末样品消解后，采用美国Perkin Elmer公司生产的Elan9000型电感耦合等离子质谱仪(ICP-MS)测定，分析精度优于5%。
2.2 锆石SHRIMP定年锆石U-Pb定年在北京离子探针中心SHRIMP Ⅱ上完成。详细分析方法见Williams(1998)。测试时一次流O-2强度为3~5nA，束斑直径为25~30μm。标样M257(U=840×10-6，Nasdala et al., 2008)和Plešovice(年龄为337.1Ma，Sláma et al., 2008)分别用于锆石U含量和年龄校正。每分析3~4个未知样品数据，分析1次标准锆石Plešovice。每个分析点采用5组扫描。数据处理采用SQUID和ISOPLOT程序(Ludwig，2001)。根据实测204Pb含量校正普通铅，采用206Pb/238U年龄为锆石年龄，同位素比值和单点年龄误差均为1σ。加权平均年龄误差为95%置信度。
2.3 锆石O同位素锆石原位氧同位素分析在北京离子探针中心多接收的SHRIMP IIe上完成。氧同位素均在与测年位置具有相同内部结构的区域分析，其中已测年的颗粒，氧同位素分析在原测年点位附近。采用强度为~13.5nA的一次Cs+离子束通过加速电压15keV轰击锆石表面，束斑的直径为~25μm。分析过程中，18O和16O由两个法拉第杯同时接收，每个测试点进行两组扫描，每组扫描6次，单次扫描积分时间为10秒，总积分时间约为120秒。在两组扫描之间，仪器自动优化一次离子流和二次离子流参数。在每个分析点测试之前，调整二次离子流和测定静电计的背景噪声150秒。标准锆石Penglai(δ18O=5.31±0.10‰，Li et al., 2010)用于校正仪器的质量分馏(IMF)。每分析3个未知样品，分析1次标准锆石。本次分析Penglai的δ18O=5.29±0.10‰(n=37)。详细的分析流程见Ickert et al.(2008)。
2.4 锆石Hf同位素锆石Hf同位素测试在南京聚谱检测科技有限公司完成。锆石Hf同位素在原O同位素点位上分析。分析仪器为配备193nm ArF准分子激光剥蚀系统(型号为RESOlution LR)的多接收器型号电感耦合等离子体质谱仪(MC-ICP-MS，型号为Nu Plasma Ⅱ)。激光频率为9Hz，束斑直径为44μm，能量密度为3.5J/cm2，剥蚀时间为40秒。气溶胶由氦气送出剥蚀池，与氩气混合后进入MC-ICP-MS。测试过程中，标准锆石GJ-1、91500、Plešovice、Mud Tank以及Penglai用于检验锆石Hf同位素比值的数据质量。本次分析的GJ-1、91500、Plešovice、Mud Tank、Penglai的176Hf/177Hf比值分别为0.282008±0.000013(n=7)、0.282303±0.000019(n=5)、0.282480±0.000008(n=4)、0.282516±0.000013(n=2)和0.282904±0.000014(n=2)，与推荐值一致。计算εHf(t)值采用176Lu衰常数为1.867±10-11yr-1(Söderlund et al., 2004)，现今的球粒陨石176Hf/177Hf=0.282772、176Lu/177Hf=0.0332(Blichert-Toft and Albarède，1997)。Hf亏损地幔模式年龄(tDM1)的计算采用现今的亏损地幔176Hf/177Hf=0.28325和176Lu/177Hf=0.0384(Griffin et al., 2000)。两阶段Hf模式年龄(tDM2)计算，采用大陆地壳平均的176Lu/177Hf=0.015(Griffin et al., 2002)。
3 结果 3.1 锆石U-Pb年龄样品18YP64-1中锆石无色透明，自形，呈短柱-柱状，粒径大多为80~150μm，发育清晰的振荡环带(图 3a)。13个测试点的U含量为232×10-6~413×10-6，Th/U比值为0.48~0.72，206Pb/238U年龄为355.4~372.2Ma，加权平均年龄为362.3±3.4Ma(n=13，MSWD=1.4；表 1，图 3b)，代表样品的结晶年龄。
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图 3 样品18YP64-1中典型锆石CL图像(a)和锆石年龄谐和图(b) 图a中：红色虚线椭圆、红色实线椭圆和大的绿色圆形分别代表U-Pb年龄、O同位素和Hf同位素测试点位; 数据代表分析点号、年龄和εHf(t)/δ18O值 Fig. 3 Cathodoluminescence images and U-Pb Concordia plot of zircon from sample 18YP64-1 In Fig. 3a: The red dashed ellipses, red solide ellipses and big green circles represent the analyzed domains of zircon U-Pb age, O isotope, and Hf isotope, respectively; Numbers near zircon denote spot numbers, U-Pb ages and εHf(t)/δ18O values |
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表 1 景洪南部晚泥盆世英安质火山岩(样品18YP64-1)锆石SHRIMP U-Pb测年结果 Table 1 SHRIMP U-Pb data for zircon from Late Devonian dacitic volcanic rock(Sample 18YP64-1)form the southern Jinghong area |
对测年样品18YP64-1中15颗锆石进行了15次Hf-O同位素分析，分析结果见表 2。其中13颗锆石为已测年颗粒，Hf-O同位素分析在年龄测试点旁，与年龄测试具有相同结构的区域。另外2颗锆石为未测年颗粒。15颗锆石的176Hf/177Hf=0.282577~0.282647，εHf(t)=+0.87~+3.27，对应的tDM2=1.15~1.30Ga。这些测试点的δ18O值较集中，分布在6.31‰~7.64‰之间，平均值为6.77±0.12‰(2σ)。
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表 2 景洪南部晚泥盆世英安质火山岩(样品18YP64-1)锆石Hf-O同位素组成 Table 2 Zircon Hf-O isotope compositions of Late Devonian dacitic volcanic rock(Sample 18YP64-1)form the southern Jinghong area |
样品的主、微量元素结果见表 3。样品的SiO2含量为62.87%~66.29%，MgO含量(2.15%~ 2.49%)和Fe2O3T含量(4.95%~6.21%)相对较高，对应的Mg#值(摩尔数Mg/(Mg+FeT)×100)为44 ~ 47。样品具有高的Na2O含量(4.77%~5.51%)，低的K2O含量(1.43%~2.39%)。它们的全碱(Na2O+K2O)为6.20%~ 7.34%，Na2O/K2O比值为2.1~3.3。在TAS图解中，样品均位于英安岩区域(图 4a)，属钙碱性系列(图 4b)。样品富集轻稀土，呈右倾型配分模式(图 5a)，(La/Yb)N=8.7~11.1，具有弱的负铕异常(Eu/Eu*=0.81~0.92)。样品的Sr含量较高(285×10-6~522×10-6)，而Yb(1.38×10-6~1.70×10-6)和Y(12.5×10-6~15.3×10-6)较低，Sr/Y比值为21.9~34.1。在微量元素蛛网图中，富集Rb、Th、U、Pb，亏损Nb、Ta、Ti等高场强元素(图 5b)。
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表 3 景洪南部晚泥盆世英安质火山岩主量元素(wt%)和微量元素(×10-6)组成 Table 3 Major(wt%) and trace(×10-6)elements data for Late Devonian dacitic volcanic rocks form the southern Jinghong area |
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图 4 景洪晚泥盆世英安质火山岩TAS图解(a，底图据Le Bas et al., 1986)和SiO2-K2O图解(b，底图据Rickwood，1989) Fig. 4 TAS(a, after Le Bas et al., 1986) and SiO2 vs. K2O(b, after Rickwood, 1989)diagrams for Late Devonian dacitic volcanic rocks from the Jinghong area |
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图 5 景洪晚泥盆世英安质火山岩球粒陨石标准化稀土元素配分图和原始地幔标准化微量元素蛛网图(标准化值据Sun and McDonough, 1989) Fig. 5 Chondrite-normalized rare earth element patterns and primitive mantle-normalized trace element distributions of Late Devonian dacitic volcanic rocks from the Jinghong area(normalized values after Sun and McDonough, 1989) |
如前文所述，本文报道的英安质晶屑凝灰岩具有埃达克岩的地球化学特征，例如较高SiO2(> 56%)、Al2O3(> 15%)、Na2O(> 3.5%)、Sr(平均为384×10-6，略低于400×10-6)、Sr/Y(> 20)和相对低的Y(< 18 × 10-6)、Yb(< 1.9×10-6)(表 3、图 6a)。埃达克岩最初发现于岛弧环境，被认为直接由年轻的玄武质洋壳俯冲熔融而成(Defant and Drummond, 1990)。随后，越来越多的研究表明，具有埃达克质地球化学特征的岩石可以形成于多种构造环境，具有不同的岩石成因。目前，埃达克岩成因主要有以下3种：(1)俯冲洋壳的部分熔融(Kay，1978；Defant and Drummond, 1990；Yogodzinski et al., 1995；Wang et al., 2007)；(2)加厚下地壳的部分熔融(Atherton and Petford, 1993；Xu et al., 2002；Chung et al., 2003；Gao et al., 2004；Hou et al., 2004)；以及(3)玄武质母岩浆的高压结晶分异(Prouteau and Scaillet, 2003；Macpherson et al., 2006；Rodríguez et al., 2007；Rooney et al., 2011)。
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图 6 景洪晚泥盆世英安质火山岩Sr/Y-Y(a，底图据Defant and Drummond, 1990)、Sr/Y-SiO2(b)、La/Y-SiO2(c)和La/Sm-La(d) 石榴子石参与的高压分离结晶演化趋势据Wang et al.(2008) Fig. 6 Plots of Sr/Y vs. Y(a, after Defant and Drummond, 1990), Sr/Y-SiO2(b), La/Y-SiO2(c) and La/Sm-La(d)for Late Devonian dacitic volcanic rocks from the Jinghong area High-pressure fractional crystallization trends involving garnet after Wang et al.(2008) |
俯冲洋壳部分熔融形成的埃达克岩通常具有高的Na2O、Na2O/K2O以及与MORB相似的放射性同位素组成(Defant and Drummond, 1990；Yogodzinski et al., 1994, 1995；Aguillón-Robles et al., 2001)。加厚的地壳包括古老的地壳和玄武岩底侵形成的新生地壳。加厚的古老下地壳部分熔融一般富钾，且具有演化的放射性同位素组成(Xu et al., 2002, 2006；Gao et al., 2004)。景洪英安质火山岩的Na2O、Na2O/K2O分别为4.77%~5.51%和2.1~3.3，与俯冲洋壳部分熔融成因的埃达克岩相似，而与加厚古老下地壳部分熔融的埃达克岩不同。另一方面，临沧花岗岩中锆石具有很低的εHf(t)值(-17.5~-9.4)和古老的tDM2(1852~2358Ma)，且花岗岩中含有大量太古代-古元古代继承锆石(孔会磊等，2012；Dong et al., 2013；王舫等，2014)。临沧花岗岩中奥陶纪花岗片麻岩的εHf(t)值为-17.5~-9.4，tDM2为1488~1895Ma。澜沧变质杂岩中奥陶纪火山岩的全岩εNd(t)为-7.6，Nd模式年龄为2.1Ga(Xing et al., 2017)，锆石εHf(t)为-4.4~-3.3，tDM2为1506~1548 Ma(Nie et al., 2015)。这些演化的同位素特征和大量太古代-古元古代继承锆石暗示南澜沧江带可能存在古老的地壳物质。与上述岩浆岩不同，本文报道的景洪英安质火山岩具有较高的εHf(t)值(+0.87~+3.27)和较年轻的tDM2年龄(1.15~1.30Ga)。尽管埃达克质熔体可与地幔岩石相互作用，导致熔体的176Hf/177Hf和143Nd/144Nd比值升高，同时提高MgO、Ni和Cr含量(Yogodzinski et al., 1995；Rapp et al., 1999；Prouteau et al., 2001；Gao et al., 2004)。本文样品的Ni(7.90×10-6~9.10×10-6)、Cr(30.0×10-6~37.0×10-6)含量均很低，指示岩浆未与地幔橄榄岩发生显著的相互作用。以上结果表明景洪英安质火山岩成因可能与加厚的古老下地壳部分熔融无关。底侵、新生的玄武岩质下地壳部分熔融可形成与起源于俯冲洋壳埃达克岩相似地球化学组成的熔体(Atherton and Petford, 1993)。但样品18YP64-1中锆石的δ18O值为6.31‰~7.64‰(图 7)，平均值为6.8±0.1‰(2σ)，明显高于与幔源岩浆平衡的锆石的δ18O值(5.3±0.3‰，Valley，2003)，不支持新生玄武质下地壳熔融模式。在高压条件下，玄武岩经历石榴子石、角闪石等矿物的分离结晶可以演化成具有埃达克岩地球化学特征的中酸性熔体(Macpherson et al., 2006；Rodríguez et al., 2007；Rooney et al., 2011)。在这种情况下，岩浆的一些特征元素或元素比值会随SiO2含量的升高表现出一定的演化趋势，例如，La/Y、Sr/Y与SiO2含量均具有正的演化关系(Wang et al., 2008)。景洪英安质火山岩La/Y、Sr/Y比值未随SiO2含量的增加而增加(图 6b，c)。此外，La/Sm比值随La含量的演化趋势也不支持岩浆经历了明显的分离结晶作用(图 6d)。高硅埃达克岩被认为由俯冲板片部分熔融而成(Martin et al., 2005)，景洪英安质火山岩具有高硅埃达克岩的地球化学特征(图 8a，b)，在埃达克岩源区的地球化学判别图解中也均落在俯冲洋壳起源的埃达克岩区域(图 8c，d)。根据以上讨论，我们认为景洪英安质火山岩很可能由俯冲洋壳的部分熔融而成。
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图 7 景洪晚泥盆世英安质火山岩(样品18YP64-1)锆石εHf(t)-δ18O(‰)关系图 Fig. 7 Combined zircon Hf-O isotopes diagram for Late Devonian dacitic volcanic rocks (Sample 18YP64-1)from the Jinghong area |
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图 8 景洪晚泥盆世英安质火山岩MgO-SiO2(a，底图据Martin et al., 2005；c，底图据Wang et al., 2006)、Sr-(CaO+Na2O)(b，底图据Martin et al., 2005)和Mg#-SiO2(d，底图据Wang et al., 2006)关系图 Fig. 8 Plots of MgO vs. SiO2(a, after Martin et al., 2005; c, after Wang et al., 2006), Sr vs. CaO+Na2O(b, after Martin et al., 2005) and Mg# vs. SiO2(d, after Wang et al., 2006)for Late Devonian dacitic volcanic rocks from the Jinghong area |
锆石δ18O小于6.5‰被认为寄主岩浆中基本不含沉积岩组分，而大于6.5‰表明岩浆源区中含有或岩浆混染了富集18O的组分(Cavosie et al., 2005；Valley et al., 2005；Kemp et al., 2006)。样品18YP64-1中锆石的δ18O的平均值为6.8±0.1‰(2σ)，表明岩浆中混入了高δ18O组分(图 7)。俯冲板片中高δ18O的组分为大洋沉积物(例如，海相碳酸盐，δ18O=25‰~32‰；硅质软泥，δ18O=25‰~32‰和深海黏土，δ18O=15‰~25‰；Kolodny and Epstein, 1976)和经历低温水-岩相互作用的洋壳上层玄武质岩石(δ18O=7‰~15‰；Gregory and Taylor, 1981；Alt et al., 1986；Staudigel et al., 1995)。尽管低温水-岩相互作用导致玄武质岩石的δ18O明显升高，但不会引起Hf同位素组成的明显改变。因此，即使岩浆源区含有低温蚀变的洋壳物质，也不会明显改变俯冲洋壳起源岩浆类似MORB的Hf同位素组成。昌宁-孟连缝合带内奥陶-志留纪蛇绿混杂岩的时代为439~471Ma，其中的基性岩大多为N-MORB型(王保弟等，2018)。样品18YP64-1锆石tDM2的平均值为1195±22Ma(2σ)，远大于样品的侵位时代和蛇绿混杂岩的形成时代，暗示岩浆中混入了具有演化Hf同位素特征的组分。因此样品略高的δ18O可能不是由低温蚀变的玄武质洋壳造成的。大洋沉积物的Hf同位素特征受沉积源区控制，如前文所述，南澜沧江带可能存在古老的地壳物质，岩浆中混入来自南澜沧江带的沉积物则可形成景洪英安质火山岩的锆石Hf-O同位素特征(图 7)。与本文报告的锆石Hf-O同位素类似，长江下游被认为起源于板片熔融的早白垩世埃达克岩也具有高的δ18O值和低的εHf(t)值(Wang et al., 2013b)。此外，样品较高的Th/Yb(4.86~7.78)和(La/Sm)N(3.62 ~ 4.56)比值也支持岩浆中混入了大洋沉积物或沉积物起源的熔体(图 9)。
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图 9 景洪晚泥盆世英安质火山岩Th/Yb-Ba/La(a，据Woodhead et al., 2001)和Ba/Th-(La/Sm)N(b, 据Tatsumi，2006)图解 Fig. 9 Th/Yb vs. Ba/La(a, after Woodhead et al., 2001) and Ba/Th vs.(La/Sm)N(b, after Tatsumi, 2006)diagrams for Late Devonian dacitic volcanic rocks form the Jinghong area |
综上所述，景洪英安质火山岩由俯冲板片部分熔融而成，岩浆中混入了大洋沉积物或沉积物起源的熔体。
4.2 构造意义如前文所述，南澜沧江带发育一系列与原、古特提斯洋演化有关的岩浆作用(图 1)。本文研究显示景洪南部发育362.3±3.4Ma的英安质火山岩，介于原特提斯和古特提斯演化阶段之间，为探讨原、古特提斯之间的构造演化过程提供了重要的研究对象。本文报告的英安质火山岩具有高硅埃达克岩的地球化学特征，是俯冲洋壳部分熔融的产物，指示南澜沧江带晚泥盆世存在洋壳的俯冲作用。与本文英安质火山岩指示的构造环境相似，Nie et al.(2016)通过对景洪东南部晚泥盆世南光组沉积岩的碎屑物质、全岩地球化学进行研究，认为它们的源区来自弧岩浆岩(Nie et al., 2016)。南光组沉积岩中碎屑锆石年龄呈单峰分布，年龄峰值接近地层的沉积时代，几乎不含年龄明显老于地层沉积时代的碎屑锆石，表明南光组可能沉积于弧前盆地(Cawood et al., 2012；Nie et al., 2016)。尽管这些结果均表明晚泥盆世洋壳俯冲事件的存在，但该时期俯冲过程与原、古特提斯洋的关系仍不清楚(Nie et al., 2016)，确定它们的关系对认识原特提斯洋俯冲持续的时间以及古特提斯洋的起始俯冲时限均具有重要的意义。考虑到南澜沧江带早古生代岩浆岩的成因被认为与原特提斯洋向东的俯冲过程有关(毛晓长等，2012；Lehmann et al., 2013；Nie et al., 2015；彭智敏等，2018；Liu et al., 2019)，晚泥盆世俯冲作用可能是原特提斯洋壳消减的持续。Gehrels et al.(2011)通过对比喜马拉雅、拉萨、羌塘等地体元古代-中生代沉积岩中碎屑锆石U-Pb年龄的分布特征，认为原特提斯洋在晚志留世已经闭合。中羌塘志留纪高压麻粒岩的发现也支持原特提斯洋晚志留世的闭合(Zhang et al., 2014)。如果南澜沧江带与羌塘、柴达木-昆仑等地区经历了相似的原特提斯洋阶段的演化，南澜沧江带晚泥盆世的俯冲过程可能代表了古特提斯洋的起始俯冲(Nie et al., 2016)。值得注意的是，除昌宁-孟连蛇绿混杂岩带中的牛井山英云闪长岩外，本文报道的英安质火山岩与研究区其他时代岩浆岩的成因明显不同。景洪晚泥盆世英安质火山岩由俯冲洋壳部分熔融而成，而早古生代的惠民、曼来变火山岩、大中河和大平掌火山岩基性-酸性火山岩以及早二叠世的花岗闪长岩被认为是俯冲洋壳交代的地幔熔融的产物(Nie et al., 2015；Xing et al., 2017；Liu et al., 2019)，临沧花岗岩基中的S型花岗片麻岩由板片俯冲引起的古老地壳物质重熔(彭智敏等，2018)。Sr/Y比值和(La/Yb)N比值也支持景洪英安质火山岩的起源与其他时代岩浆岩存在差异(图 10)。岩石成因的差异暗示晚泥盆世俯冲过程可能不同于早、晚古生代的俯冲过程。此外，惠民、曼来变火山岩，临沧花岗岩及其中的早古生代S型花岗片麻岩均具有演化的同位素特征，表明云县-景洪火山岩带西侧为含古老岩石的大陆边缘。从空间分布特征来看，本文报道的英安质火山岩位于临沧花岗岩东侧，南光组沉积于景洪火山岩东南，靠近思茅陆块的一侧(图 1)。如果晚泥盆世的俯冲作用代表的是西侧原特提斯洋或古特提斯洋向东俯冲，景洪英安质火山岩应为大陆岛弧火山岩，南光组应沉积于弧后环境。景洪英安质火山岩中未见继承锆石，且锆石εHf(t)值偏高，明显与惠民、曼来变火山岩所代表的大陆岛弧岩浆岩不同。南光组中几乎不含明显早于地层沉积时代的碎屑锆石，也不支持其沉积于弧后环境(Cawood et al., 2012；Nie et al., 2016)。
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图 10 南澜沧江带古生代中-酸性岩浆岩Sr/Y(a)和(La/Yb)N(b)随形成时代的变化图 数据来自：本次研究；Hennig et al.(2009)；毛晓长等(2012)；Lehmann et al.(2013)；Nie et al.(2015)；王冬兵等(2016)；Xing et al.(2017)；彭智敏等(2018)；Liu et al.(2019) Fig. 10 Variations of Sr/Y(a) and (La/Yb)N(b)vs. ages of the Paleozoic intermediate-acid magmatic rocks in the southern Lancangjiang belt with age Data from: this study; Hennig et al.(2009); Mao et al.(2012). Lehmann et al.(2013); Nie et al.(2015); Wang et al.(2016); Xing et al.(2017); Peng et al.(2018); Liu et al.(2019) |
临沧花岗岩东侧和北侧的南光组、无量山组以及团梁子组中显生宙碎屑锆石主要的年龄峰为~362Ma、~297Ma、~270Ma和~259Ma，次要的年龄峰为480~420Ma(图 11)。这些年龄峰与带内古生代岩浆岩形成时代可以很好的对应，例如，480~420Ma的年龄峰与带内早古生代(477~418Ma)岩浆岩形成时代一致，~362Ma的年龄峰与本文报告的英安质火山岩形成时代一致。由此可见，这些碎屑锆石的年龄峰在一定程度上反应了带内古生代岩浆的活动期次。碎屑锆石分布特征指示南澜沧江带古生代岩浆活动可能具有幕式的特征，晚泥盆世的岩浆作用与早古生代以及晚石炭世-早二叠世的岩浆事件之间均存在时间间隔，不是连续的岩浆过程(图 11)。综合以上分析，景洪晚泥盆世英安质火山岩很可能不是早古生代原特提斯岛弧岩浆的延续，也不是晚石炭世-二叠纪古特提斯岛弧岩浆事件的开始，可能与另外一期独立的俯冲事件有关。
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图 11 南澜沧江带晚古生代沉积岩中显生宙碎屑锆石U-Pb年龄频率分布直方图 数据引自Nie et al.(2016); Xing et al.(2016)和王冬兵等(2018) Fig. 11 Relative probability plot of U-Pb ages for Paleozoic detrital zircon from Late Paleozoic sedimentary rocks from the southern Lancangjiang belt Data sources: Nie et al.(2016); Xing et al.(2016)and Wang et al.(2018a) |
值得注意的是，早古生代晚期(429~418Ma)大中河，大平掌基性-酸性火山岩形成于原特提斯洋向东俯冲导致的弧后拉张环境(图 12)，该过程可形成新的洋盆。相对于原、古特提斯洋俯冲作用的延续或开始，晚泥盆世的弧岩浆作用更可能与大中河，大平掌弧后洋盆打开之后的俯冲消减过程有关。弧后洋盆持续打开，形成比昌宁-孟连早古生代蛇绿混杂岩年轻、热的洋壳，年轻的洋壳俯冲熔融形成景洪晚泥盆世具有埃达克岩地球化学特征的英安质火山岩(图 12)。从空间位置来看，景洪晚泥盆世英安质火山岩位于大中河、大平掌火山岩西侧的澜沧江构造带内(半坡-雅口-南联山沿线，图 1)，暗示弧后洋盆可能由东向西俯冲。南光组出露在本文报告的景洪晚泥盆世火山岩东侧，沉积于景洪火山岩代表的岛弧岩浆岩东侧靠近洋盆弧前盆地内。打开的大中河、大平掌弧后洋盆有效的阻挡了思茅陆块碎屑物质的加入(图 12)。该模式不仅解释了景洪英安质火山岩与早古生代、二叠纪弧岩浆岩的成因差异，也很好的解释了南光组沉积岩碎屑锆石的年龄分布特征。综上所述，南澜沧江带晚泥盆世的俯冲作用很可能代表的是打开的大中河、大平掌弧后洋盆的俯冲过程。
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图 12 南澜沧江带奥陶纪-泥盆纪构造演化模式图 (a)原特提斯洋向东俯冲形成奥陶纪岩浆岩；(b)原特提斯洋向东导致志留纪弧后拉张环境，形成大中河、大平掌火山岩；(c)大中河、大平掌弧后洋盆向西俯冲导致景洪晚泥盆世岩浆活动和南光组沉积 Fig. 12 Schematic model showing tectonic evolution of the southern Lancangjiang belt during the Ordovician to Devonian (a) eastwards subduction of the Proto-Tethyan ocean produced Ordovician magmatic rocks; (b) the Dazhonghe and Dapingzhang volcanic rocks were generated in a Silurian continental back-arc extentsion setting related to the eastwards subduction of the Proto-Tethyan ocean; (c)westwards subduction of the Dazhonghe and Dapingzhang back-arc oceanic basin led to Late Devonian magmatic activities in the Jinghong area and the Nanguang Formation deposition |
在景洪南部南联山地区识别出362.3±3.4Ma的英安质火山岩，该火山岩具有高硅埃达克岩的地球化学特征，是俯冲洋壳部分熔融的产物。南澜沧江构造带晚泥盆世俯冲作用很可能指示的是打开的大中河、大平掌弧后洋盆的俯冲过程。
致谢 感谢闫臻研究员及另一位匿名审稿人提出许多宝贵修改意见，使本文的讨论更加完善；感谢北京离子探针中心刘建辉、王培智和包泽明等在锆石U-Pb年龄和O同位素测试过程中给予的帮助。
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