2021, Vol. 37
2. 中国科学院深地科学卓越创新中心, 广州 510640;
3. 中国科学院大学, 北京 100049;
4. 南方海洋科学与工程广东省实验室, 珠海 519000
2. CAS Center for Excellence in Deep Earth Science, Guangzhou 510640, China;
3. University of Chinese Academy of Sciences, Beijing 100049, China;
4. Southern Marine Science and Engineering Guangdong Laboratory, Zhuhai 519000, China
自Chappell and White (1974)定义了以变沉积岩为源区的S型花岗岩及变火成岩为源区的I型花岗岩以及后来定义的代表碱性、无水、形成于非造山背景下A型花岗岩(Loiselle and Wones, 1979)以来，花岗岩的I-S-A型划分方案被普遍接受(Gao et al., 2016; 吴福元等, 2007)。角闪石、堇青石或碱性暗色矿物可以分别作为I型、S型或A型花岗岩的有效识别标志(吴福元等, 2007)。但对于不含有这些标志性矿物的花岗岩，一般根据其全岩主微量特征来判断其岩石类型，如S型花岗岩由富铝变沉积岩的部分熔融形成，因此过铝质特征被作为S型花岗岩的判别指标，然而过铝质特征并非S型花岗岩所独有，澳大利亚Lachlan褶皱带中超过一半的I型花岗岩同样为过铝质(Chappell et al., 2012)。这是因为I型花岗质岩浆角闪石和辉石的分离结晶也可以形成过铝质花岗岩(吴福元等, 2017)。此外，SiO2-P2O5和SiO2-A/CNK等判别图也被用来区分I、S型花岗岩，但也存在较大的不确定性(Gao et al., 2016)。花岗岩全岩主微量元素组成不仅受源区组成控制，也受到岩浆过程如部分熔融、同化混染等过程的影响，常常无法有效限制其源区组成。全岩的Sr-Nd同位素及锆石的Hf同位素主要反映的是源岩在地壳中存留时间，例如，亏损的Sr-Nd-Hf同位素特征表明花岗岩可能是新生下地壳部分熔融形成的I型花岗岩(Zhou et al., 2018)，也可能是新生的上地壳物质由于构造作用被迅速剥蚀掩埋而后发生熔融形成的S型花岗岩(Dan et al., 2014)。因此仅通过对岩石的全岩主微量元素或者放射性成因同位素(如Sr-Nd)组成来确定花岗岩类型可能会产生错误的结论。锆石氧同位素组成不受部分熔融和结晶分异过程的影响，是识别I、S型花岗岩的理想地球化学指标(Gao et al., 2016; Kemp et al., 2007)。如果源岩为遭受过地表低温水岩反应的变沉积岩，部分熔融形成的熔体具有高氧同位素特征；相反，以未经历地表沉积循环的变火成岩为源区部分熔融形成的熔体具有较低的氧同位素。
位于中国云南西部的腾冲地块发育大量早白垩世花岗岩(130~110Ma)(戚学祥等, 2011; Cao et al., 2019; Fang et al., 2018; He et al., 2020; Qi et al., 2019; Zhang et al., 2018a, b; Zhu et al., 2015, 2020)。这些花岗岩有的具有角闪石，属于典型I型花岗岩；但其中也有部分花岗岩不具有角闪石，也不具有堇青石或碱性暗色矿物等特征矿物，但具有高硅(68.67%~77.90%)、高钾、弱到强过铝质的特点，被认为是S型花岗岩(陈永清等, 2013; 杨启军等, 2006; Cao et al., 2014)或高分异I型花岗岩(Zhu et al., 2015)。前者认为这些花岗岩形成于碰撞造成的挤压背景下，源区主要为上地壳硬砂岩，而后者则认为形成于俯冲背景下，源区主要为中下地壳及少量的幔源物质。如前所述，由于缺乏矿物学标志，前人对这些高硅、过铝质花岗岩的成因类型判断主要依靠全岩主微量元素，缺乏足够的依据，无法有效的限制其源区特征及构造背景。本文首次对腾冲地块早白垩世高硅过铝质花岗岩进行锆石氧同位素研究，发现这些花岗岩普遍具有相对较低的氧同位素组成，表明其源区组成主要以基性下地壳为主，并结合花岗岩的矿物学特征、全岩主微量元素和Sr-Nd同位素特征，确定了这些花岗岩属于高分异I型花岗岩，它们可能形成于班公湖-怒江洋闭合后的板片折返或板片断离背景，而非之前认为的是沉积物为主的源区在碰撞挤压背景下的熔融产物。
1 地质背景和样品描述腾冲地块位于青藏高原东南缘，东以高黎贡剪切带(或龙陵-瑞丽断裂带)与保山地块相隔，西以密支那缝合带与西缅地块相隔(图 1)。在早古生代腾冲地块位于冈瓦纳大陆边缘，于中生代拼合到欧亚大陆(Liu et al., 2019a; Metcalfe, 2013)。腾冲地块最古老的地质单元为古-新元古代高黎贡山群，由片麻岩、片岩、硅质岩、大理岩和板岩等组成，普遍经历绿片岩-角闪岩相变质作用，向南可与缅甸的Mogok群相连(陈福坤等, 2006; 李再会等, 2012a)，但最新的研究表明该群也出露一些早古生代(518~476Ma)、中生代(128~109Ma)和新生代(55~50Ma)花岗岩(Ma et al., 2014; Qi et al., 2019; Wang et al., 2013; Xu et al., 2012; Zhang et al., 2018a)。上覆沉积盖层主要包括：石炭纪碎屑沉积岩、二叠纪-三叠纪浊积岩和新生代陆相火山岩、河湖相碎屑沉积岩。腾冲地块缺失侏罗-白垩纪地层，可能与中特提斯洋的俯冲，腾冲与保山的碰撞有关(戚学祥等, 2011)。腾冲地块主要发育五期岩浆作用，包括寒武-奥陶纪(510~470Ma)(崔晓琳等, 2017; Wang et al., 2013)、二叠-三叠纪(245~206Ma)(从峰等, 2010; 黄志英等, 2013; Shi et al., 2016)、早白垩世(130~110Ma)(Cao et al., 2019; He et al., 2020; Qi et al., 2019; Xie et al., 2020; Zhang et al., 2018a, b)、晚白垩世(77~65Ma)(唐婉丽等, 2018; 徐容等, 2018; Cao et al., 2016; Wu et al., 2019)和古新世-始新世(65~40Ma)(Cheng et al., 2020; Liu et al., 2019b; Zhao et al., 2019)。此外，腾冲地块同样广泛发育着新近纪以来的火山岩(17.84~0.09Ma)(丁磊磊等, 2018; 林木森等, 2017; 张诗启等, 2017; Cheng et al., 2020; Xu et al., 2018a)。
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图 1 滇西腾冲地块构造地质简图 BNS-班公湖-怒江缝合带；TC-腾冲地块；BS-保山地块；IC-印支地块 Fig. 1 Simplified tectonic map of the Tengchong terrane in western Yunnan Province BNS-Bangong-Nujiang Suture; TC-Tengchong terrane; BS-Baoshan terrane; IC-Indochina terrane |
腾冲早白垩世岩浆岩主要分布在地体东缘，以中酸性为主，由数个岩体组成，出露面积在500km2以上(李再会等, 2012b)。本次研究的样品采自明光、勐连和小棠-芒东三个早白垩世岩体(图 1)。岩体侵入高黎贡山群中，岩石类型主要包括二长花岗岩、正长花岗岩及白云母花岗岩。矿物组成较为单一，主要包括：钾长石(30%~50%)、斜长石(10%~40%)、石英(20%~40%)、黑云母(3%~5%)和白云母(0~3%)，副矿物主要有锆石和磷灰石，不含角闪石、堇青石和碱性暗色矿物(图 2)。
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图 2 腾冲地块早白垩世花岗岩样品显微镜下照片 (a)白云母花岗岩；(b)二长花岗岩. Pl-斜长石；Qz-石英；Ms-白云母；Kfs-钾长石 Fig. 2 Photomicrographs of the Early Cretaceous granites from the Tengchong terrane (a) muscovite granite; (b) monzogranite. Pl-plagioclase; Qz-quartz; Ms-muscovite; Kfs-K-feldspar |
全岩主微量元素分析测试在武汉上谱分析科技有限责任公司分析测试中心完成。主量元素分析采用波长色散X射线荧光光谱仪(XRF型号：Axios MAX)测试，测试过程中使用外标和重复样综合控制测试质量，平行测定了BHVO-2、GSP-2、W-2A、GBW07103和GBW07316等标准物质，分析精度优于5%。微量元素分析利用Agilent 7700e ICP-MS完成，测试过程采用内标、重复样和外标综合控制测试质量的方法，以元素In为内标，平行测定空白样以及AGV-2、BHVO-2、BCR-2和RGM-2等标准物质, 分析精度约为5%~10%。全岩Sr-Nd同位素分析测试在中国科学院广州地球化学研究所同位素地球化学国家重点实验室MC-ICP-MS仪器上完成，将小于180目的样品粉末，用1：1的HF+HNO3在Teflon容器中低温溶解，利用AG-50W-8X柱分离出Sr和REEs，利用HDEHP阳离子交换柱分离出Nd和其他稀土元素，然后将分离出的Sr和Nd溶液用2%的HNO3稀释至适当浓度进行上机测试。分别用87Sr/86Sr=0.1194和146Nd/144Nd=0.7219对87Sr/86Sr和146Nd/144Nd的测定值标准化。
2.2 锆石SIMS U-Pb定年和氧同位素分析锆石SIMS U-Pb定年和氧同位素分析测试均在中国科学院广州地球化学研究所同位素地球化学国家重点实验室完成，测试仪器为CAMECA IMS 1280-HR型二次离子质谱仪。锆石U-Pb定年测试采用O2-为一次离子源，离子流强度为~10nA，加速电压为-13kV，束斑为椭圆形，大小为20×30μm，详细分析过程参考(Xu et al., 2019)。使用标准锆石Plesovice(Sláma et al., 2008)对样品Pb/U同位素比值进行校正，标准锆石SA01(Huang et al., 2020)用于监控分析结果可靠性。锆石氧同位素分析时使用133Cs一次离子源，加速电压10kV，电流强度为~2nA，束斑大小直径约为20μm。仪器质量分馏(IMF)校正采用标准锆石Penglai(δ18O=5.31±0.10‰)(Li et al., 2010)。标准锆石SA01(δ18O=6.16±0.26‰)用于监控测试结果的准确度。详细分析过程参考文献(Yang et al., 2018)。
3 分析结果 3.1 SIMS锆石U-Pb年龄和氧同位素3个岩体中各选取6个花岗岩样品进行锆石SIMS U-Pb定年测试及氧同位素测试，分析数据分别见表 1和表 2。所有样品中的锆石具有较一致的晶型，大部分呈自形-半自形的柱状，长100~200μm，长宽比一般为2：1~3：1，具有岩浆结晶环带(图 3)Th/U变化范围为0.4~3.7，为典型的岩浆成因锆石(Belousova et al., 2002)。
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表 1 腾冲地块早白垩世花岗岩锆石U-Pb SIMS分析结果 Table 1 Zircon U-Pb SIMS analytical results for Early Cretaceous granites in the Tengchong terrane |
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表 2 腾冲地块早白垩世花岗岩锆石氧同位素分析结果 Table 2 Zircon Oxygen isotope analytical results for Early Cretaceous granites in the Tengchong terrane |
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图 3 腾冲地块早白垩世花岗岩锆石阴极发光图像(圆圈代表U-Pb定年位置及氧同位素分析位置) Fig. 3 Cathodoluminescence (CL) images for zircons from the Early Cretaceous granites in the Tengchong terrane (The circle show the positions for U-Pb dating and O isotope analysis) |
明光岩体2个二长花岗岩样品18TC85和18TC74分别测试了16个点和14个点U-Pb数据，其中去除样品18TC85中2个误差较大的点后，2个样品给出的谐和年龄分别为122.2±1.1Ma(图 4a)和122.1±0.50Ma(图 4b)。勐连岩体1个白云母花岗岩样品18TC64和1个二长花岗岩样品17LL41分别测试了20个点和16个点，给出的谐和年龄分别为115.56±0.45Ma(图 4d)和114.37±1.1Ma(图 4c)。小棠-芒东岩体1个正长花岗岩样品18TC19和1个二长花岗岩样品18TC20分别测试了15个点，给出的谐和年龄分别为112.47±0.45Ma(图 4e)和115.16±0.46Ma(图 4f)。
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图 4 腾冲地块早白垩世花岗岩锆石U-Pb谐和图 Fig. 4 Zircon U-Pb concordia diagrams from the Early Cretaceous granites in the Tengchong terrane |
完成年龄测试后，抛去剥蚀坑后在测年锆石颗粒相同位置进行氧同位素分析。其中明光岩体2个样品共30粒锆石的δ18O变化范围为6.5‰~7.8‰(图 5a)，平均值为7.1‰。勐连岩体2个样品共36粒锆石的δ18O变化范围为6.0‰~7.5‰(图 5b)，平均值为6.7‰。小棠-芒东岩体2个样品共30粒锆石的δ18O变化范围为6.2‰~7.2‰(图 5c)，平均值为6.6‰。
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图 5 腾冲地块早白垩世花岗岩锆石氧同位素特征 Fig. 5 Zircon O isotopes from the Early Cretaceous granites in the Tengchong terrane |
表 3列出了3个岩体共11个样品的主微量元素测试结果。这3个岩体的主量元素组成具有以下一致特征：(1)富硅，SiO2含量为69.2%~77.4%，具有较高的分异指数(DI)(83~96)，与北拉萨地块察隅高分异花岗岩(82~92)(朱弟成等, 2009)以及华南佛冈高分异花岗岩(82~94)(Li et al., 2007)相当, 表明岩体经历了较高程度的分异演化作用；(2)弱过铝-强过铝质，A/CNK值变化于1.03~1.23(平均值为1.09)；(3)高钾钙碱性，在SiO2-K2O的地球化学判别图解中，样品均显示为高钾钙碱性(图 6a)；(4) 较低的镁、铁、磷含量，可能指示了高程度的分异演化特征(表 3)。
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表 3 腾冲地块早白垩世花岗岩全岩主量元素(wt%)和微量元素(×10-6)分析结果 Table 3 Composition of major (wt%) and trace (×10-6) elements for Early Cretaceous granites in the Tengchong terrane |
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图 6 腾冲地块早白垩世花岗岩全岩地球化学图解 (a) SiO2-K2O图解；(b) (Zr+Nb+Ce+Y)-FeOT/MgO图解 Fig. 6 Geochemical diagrams of the Early Cretaceous granites in the Tengchong terrane (a) SiO2 vs. K2O diagram; (b) Zr+Nb+Ce+Y vs. FeOT/MgO diagram |
各岩体的稀土总量总体较低(∑REE=71.1×10-6~292.6×10-6)(表 3)。在球粒陨石标准化稀土元素配分图中(图 7a)，各岩体均表现出轻稀土相对富集(∑LREE=61.7×10-6~279.1×10-6)，重稀土相对亏损(∑HREE=9.5×10-6~30.0×10-6)，LREE/HREE=3.9~20.6，(La/Yb)N=3.0~37.4，铕负异常较为明显(δEu=0.13~0.69)，在原始地幔标准化微量元素蜘蛛图中(图 7b)，所有样品均不同程度富集大离子亲石元素Rb、Th、Pb和K，亏损高场强元素Nb、P、Ti。
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图 7 腾冲地块早白垩世花岗岩球粒陨石标准化稀土元素分布图(a)和原始地幔标准化微量元素蛛网图(b)(标准化值据Sun and McDonough, 1989) Fig. 7 Chondrite-normalized REE distributions (a) and primitive mantle-normalized trace-element spidergram (b) for the Early Cretaceous granites in the Tengchong terrane (normalization values after Sun and McDonough, 1989) |
3个岩体的Sr-Nd同位素基本一致，具体见表 4。小棠-芒东岩体的(87Sr/86Sr)i=0.71079~0.72125，εNd(t)=-7.70~-7.57；明光岩体的(87Sr/86Sr)i=0.70923~0.71022，εNd(t)=-9.13~-6.95；勐连岩体的(87Sr/86Sr)i=0.70624~0.70896，εNd(t)=-8.9~-4.73。研究样品均具有较老的二阶段Nd同位素模式年龄(1297~1662Ma)。
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表 4 腾冲地块早白垩世花岗岩全岩Sr-Nd同位素分析结果 Table 4 Whole-rock Sr-Nd isotopic compositions of the Early Cretaceous granites in the Tengchong terrane |
就所研究的3个岩体而言，它们具有不同于A型花岗岩的岩相学和地球化学特征，主要包括：(1)不含A型花岗岩的特征矿物，碱性暗色矿物(吴福元等, 2007)；(2)较低的FeOT/MgO比值(平均为5.7)以及较低的10000×Ga/Al比值(平均为2.2)，区别于典型的A型花岗岩(FeoT/MgO>10，10000×Ga/Al>2.6)(Whalen et al., 1987)；(3)具有相对低的锆饱和温度(平均为760℃)，不具有A型花岗岩显著的高温(>800℃)特征(King et al., 1997)。这些花岗岩具有较高的铝饱和指数，与变沉积岩部分熔融形成S型花岗岩相似(Chappell, 1999)。目前更多的学者根据花岗岩的SiO2与P2O5、Rb与Th、或Rb与Y含量的相关性来判断I型或S型花岗岩(Clemens, 2003)。在SiO2-P2O5图解中3个所研究的岩体样品以及杨启军等(2006)所定义的“S型花岗岩”样品均表现出I型花岗岩具有的相关关系(图 8a)。但值得注意的是，仅通过SiO2-P2O5和Rb-Y、Rb-Th等相关关系来区分I型或S型花岗岩是不够充分的(汪洋, 2008; Broska et al., 2004; Gao et al., 2016)。有些典型的S型花岗岩，如南非的Cape Granite Suite同样表现出SiO2-P2O5的负相关关系(Gao et al., 2016)。如前所述，锆石O同位素组成可以用来有效区分I型或S型花岗岩，所研究的3个岩体的花岗岩平均锆石氧同位素值(6.5‰~7.5‰)(图 5)，远低于典型的华南S型花岗岩(8‰~12‰)(Fu et al., 2015; Jiao et al., 2015)，以及澳大利亚拉克伦褶皱带S型花岗岩(8.0‰~11.0‰)(Kemp et al., 2007)。此外这3个岩体的花岗岩的锆石氧同位素与腾冲地块同时期典型的I型花岗岩(含角闪石)的锆石氧同位素值(6.1‰~7.8‰)(未发表数据)十分一致，并且它们的全岩Nd同位素同样可与这些典型的I型花岗岩对比(-10.5~-5.16)。以上证据基本排除了本文所研究的样品为S型花岗岩的可能。结合这3个岩体的花岗岩样品均具有高的SiO2含量，高的分异指数(DI=83~96)，以及不同程度的Eu的负异常(δEu=0.13~0.69)(表 3)，在Zr+Nb+Ce+Y-(FeOT/MgO)判别图(图 6b)解中位于高分异花岗岩区域，综合判断，我们认为3个岩体均属于高分异的I型花岗岩。
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图 8 腾冲地块早白垩世花岗岩哈克图解 Fig. 8 Harker diagrams of the Early Cretaceous granites in the Tengchong terrane |
高分异I型花岗岩的成因主要包括：(1)来自幔源的基性岩浆与长英质岩浆混合形成混源岩浆并在后期发生分离结晶作用(Karsli et al., 2010; Zhu et al., 2009a)；(2)由于幔源分异的基性岩浆底侵，导致下地壳物质发生部分熔融，并发生分离结晶作用(Chappell et al., 2012; Topuz et al., 2010)；(3)幔源的基性岩浆发生分离结晶(Chen and Arakawa, 2005; Wyborn et al., 2001)。腾冲早白垩世高分异I型花岗岩具有较为富集Sr-Nd的同位素组成，说明它们不可能是幔源基性岩浆分离结晶的产物。锆石平均δ18O值变化于6.5‰~7.0‰(图 5)，略高于与幔源岩浆平衡的锆石δ18O值(5.3±0.3‰)(Valley et al., 2005), 低于上地壳平均δ18O值(9.7±1.3‰)(Simon and Lécuyer, 2005), 与下地壳平均值(7.0‰)(Kempton and Harmon, 1992)以及具有高镁(Mg#>70)特征的下地壳镁铁质麻粒岩捕虏体氧同位素(6.7±0.6‰)(Kempton and Harmon, 1992)十分接近，结合古老的Nd模式年龄(1297~1662Ma)(表 4)，暗示它们可能是古老镁铁质大陆下地壳部分熔融的产物。低钾玄武质岩石熔融产生的中性-酸性熔体具有低钾及低的K2O/Na2O值(< 1)，而中钾-高钾玄武质岩熔融则会产生更偏酸性及高钾及高的K2O/Na2O值(>1)的熔体(Sisson et al., 2005)。本次研究的样品具有高的K2O含量(>4.2%)，高的K2O/Na2O值(>1.1)，符合源岩为中钾-高钾玄武质岩石的特征(图 9)。因此，本文认为这些高分异花岗岩的源区是以中钾-高钾玄武质岩石为主的腾冲古老基底物质。
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图 9 花岗岩源区判别图解(据Jiang et al., 2018) Fig. 9 Discrimination diagrams for the magma source of the granites (after Jiang et al., 2018) |
研究的花岗岩样品经历了高程度的结晶分异作用，其中SiO2与CaO和Al2O3的负相关(图 8b, e)及Sr、Ba和Eu的亏损(图 7b)指示斜长石和钾长石的分离结晶，SiO2与P2O5的负相关(图 8a)及P的亏损(图 7b)指示磷灰石的分离结晶，SiO2与MgO和Fe2O3的负相关(图 8c, d)可能指示镁铁矿物(角闪石，黑云母)的分离结晶，SiO2与TiO2的负相关(图 8f)及Ti的亏损(图 7b)指示富钛矿物的分离结晶。值得注意的是，研究的样品中存在一些锆石具有十分低的氧同位素(6.0‰~6.3‰), 低于下地壳平均值(7.0‰)(Kempton and Harmon, 1992)，甚至低于富镁的下地壳麻粒岩捕虏体(6.7±0.6%)(Kempton and Harmon, 1992)，略高于与幔源岩浆平衡的锆石δ18O值(5.3±0.3‰)(Valley et al., 2005)。此外，3个岩体的Nd同位素(-9.1~-4.7)也具有较大的变化范围，以上证据表明来自幔源物质参与了成岩作用。尽管在研究的高分异花岗岩中未发现暗色包体的存在，但是在同时期的腾冲早白垩世I型花岗岩中有大量包体的报道(从峰等, 2011; Zhang et al., 2018a)，这些包体具有较寄主岩更亏损的同位素特征(从峰等, 2011)。熔融实验表明镁铁质下地壳在没有地幔物质参与的情况下其部分熔融产生的熔体的镁值(Mg#)总是小于40(Rapp and Watson, 1995)，然而同时期的腾冲地块存在许多具有高Mg#(>40)特征的中酸性岩(Qi et al., 2019; Zhu et al., 2017b)。综合以上证据，我们将本次研究的高分异I型花岗岩的成因解释为：来自幔源的岩浆底侵至镁铁质下地壳使其部分熔融并与壳源的岩浆混合随后发生分离结晶作用所形成。
4.3 构造意义腾冲地块东缘发育大量早白垩世岩浆岩，呈近南北向展布，岩石类型主要为花岗岩、花岗闪长岩、闪长岩及包体，锆石年代学研究表明这些中酸性岩的形成时代在130~110Ma之间(从峰等, 2011; 戚学祥等, 2011; 杨启军等, 2006; Cao et al., 2019; Fang et al., 2018; He et al., 2020; Qi et al., 2019; Zhang et al., 2018a; Zhu et al., 2017a, b)。这些早白垩世岩浆岩的形成时的构造环境仍然存在较大争议。前人提出的构造成因模式主要包括：(1)班公湖-怒江洋闭合导致拉萨-腾冲地块与羌塘-保山地块碰撞所引发的地壳增厚熔融(杨启军等, 2006; Cao et al., 2014; Xu et al., 2012)；(2)班公湖-怒江洋的向南(Qi et al., 2019; Zhu et al., 2017b)或向北(Cao et al., 2019; Fang et al., 2018)的俯冲背景；(3)碰撞后背景，包括俯冲板片断离(Zhang et al., 2018a; Zhu et al., 2017a)和板片后撤(He et al., 2020)。Xu et al. (2012)认为这些强过铝质花岗岩为S型，形成于板块碰撞导致的地壳增厚背景，幔源的贡献是十分有限的。如前所述，这些所谓的“S型花岗岩”其实为高分异的I型花岗岩，而且其形成过程中有幔源岩浆参与。此外，新的研究发现了越来越多的具有正的锆石εHf(t)值的早白垩世I型花岗岩(He et al., 2020; Zhang et al., 2018a; Zhu et al., 2017b)，表明了地幔物质对腾冲早白垩世岩浆活动有着不可忽视的作用。
腾冲地块与西藏陆块群如拉萨地块和羌塘地块之间的对应关系一直存在着争议。Liu et al. (2016)通过年代学及锆石Hf-O同位素研究认为班公湖-怒江缝合带向东南延伸至缅甸境内的密支那蛇绿岩带(腾冲地块以西)。在这种构造模式下，腾冲地块与保山地块一样同属于Sibumasu地块的一部分，与西羌塘地块相连(Metcalfe, 2013)。然而，腾冲地块具有与拉萨地块相似的岩浆活动历史、地层学及古生物学特征(Liao et al., 2015; Zhang et al., 2019; Zhao et al., 2016)，我们新的碎屑锆石年代学和同位素分析研究表明保山地块和腾冲地块古-中生代具有不同的碎屑锆石源区，分别为西羌塘地块和拉萨地块的东南延伸(周美玲, 2019)。腾冲地块东缘早白垩世岩浆活动具有与拉萨地块北部岩浆岩带相似的地球化学特征及年代学特征(Qi et al., 2019; Xie et al., 2016)。根据地层学，构造学，岩浆岩及变质岩资料，Zhu et al. (2016)提出了班公怒江洋双向俯冲模式，认为持续的双向俯冲最终导致班公湖-怒江洋在~140Ma的闭合，其中向南(或向西)俯冲的洋壳由于重力不稳定性发生板片折返(130~120Ma)，并最终断离(120~110Ma)。最近，Xie et al. (2020)通过对腾冲地块早白垩世岩浆岩的Nd-Hf同位素研究认为腾冲地块早白垩世晚期岩浆活动(122~112Ma)具有比早期的岩浆活动(132~122Ma)更多的地幔物质加入，并认为这两期岩浆活动指示腾冲-保山地块碰撞后，由洋壳板片折返向洋壳板片断离的构造背景转换。本次研究的1个较年轻的样品(112Ma)具有相对高的Nd同位素值(εNd(t)=-4.7)，并且两个较年轻的勐连和小棠芒东岩体的锆石氧同位素值(平均为6.6‰和6.7‰)具有比较老的(122Ma)明光岩体低的锆石氧同位素值(平均为7.1‰)，以上这些同位素变化规律均指示幔源物质明显增加，进一步支持Zhu et al. (2016)和Xie et al. (2020)所提出的构造模式。结合前人的研究，我们认为较老(122Ma)的明光高分异I型花岗岩可能与腾冲-保山地块碰撞后的板片折返背景相关，较年轻(115~112Ma)的勐连和小棠-芒东高分异I型花岗岩则与板片断离相关。这一构造背景跟拉萨地块北缘同期相似，支持腾冲地块是拉萨地块的东南延伸这一认识。
5 结论(1) 明光、勐连及小棠-芒东岩体主要包括二长花岗岩、白云母花岗岩和正长花岗岩，高精度SIMS锆石U-Pb定年结果表明它们形成于114~122Ma，δ18O变化于6.5‰~7.0‰，是典型的I型花岗岩锆石氧同位素特征，属于高分异I型花岗岩。
(2) 全岩主微量、全岩Sr-Nd同位素表明这些具有高硅、富钾、弱过铝-强过铝质花岗岩源区为古老的高钾-中钾玄武质下地壳。
(3) 腾冲早白垩世岩浆作用可能形成于腾冲与保山之间的中特提斯洋闭合后，特提斯洋板片发生折返或断离的构造背景，跟拉萨地块北缘演化历史高度一致，表明腾冲陆块是拉萨陆块的东南向延伸。
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