2022, Vol. 38
2. 中国地质科学院地球深部探测中心, 北京 100037;
3. 中国地质科学院地质力学研究所, 北京 100081
2. SinoProbe Center, Chinese Academy of Geological Sciences, Beijing 100037, China;
3. Institute of Geomechanics, Chinese Academy of Geological Sciences, Beijing 100081, China
祁连造山带作为一个典型的加里东期造山带(黄汲清等，1977；宋述光，1997；张建新等, 1997, 1998)是华北板块与柴达木地块之间经过碰撞、汇聚、造山作用形成的复合造山带。现今的祁连造山带位于青藏高原东北缘，呈北西西向展布，北以河西走廊盆地为界与华北板块相邻，南以宗务隆山北缘断裂与柴达木地块相隔，西端则被阿尔金断裂截切，东端可延伸至六盘山一带(图 1)。祁连造山带由北向南依次由北祁连缝合带、中祁连地块和南祁连增生杂岩三个构造单元组成(Song et al., 2017; Zhang et al., 2017a；宋述光等，2019)，其构造演化经历了早古生代的造山运动(Yin and Harrison, 2000；宋述光等，2004; Xiao et al., 2009；宋述光, 2009；Song et al., 2013, 2014；Wu et al., 2017), 并形成了北祁连蛇绿岩带(王荃和刘雪亚，1976；肖序常等，1978；Song et al., 2013；李冰等, 2016, 2017)、柴北缘超高压变质带(杨经绥等, 1998, 2000；张建新等，2002；Yin et al., 2007；宋述光等, 2013, 2015)和大量的碰撞前、同碰撞和碰撞后的岩浆岩(Gehrels et al., 2003；Yang et al., 2012)；中生代伸展作用导致侏罗纪和白垩纪伸展盆地的广泛发育(Vincent and Allen, 1999; Chen et al., 2003; Yin et al., 2008a, b; Zuza and Yin, 2016)；新生代以来，受青藏高原东北缘的地壳缩短、挤压变形(Gehrels et al., 2003；Yin et al., 2007；Zuza and Yin, 2016；Zaza et al., 2018)和大规模走滑断裂运动的影响(Duvall et al., 2013; Zuza and Yin, 2016；Li et al., 2019)，导致一系列北西向逆冲断裂和走滑断裂发育，并形成了现今的盆-山构造地貌格局(张会平等，2012；戚帮申等，2013；Zhang et al., 2017b)。
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图 1 祁连造山带大地构造位置图(a)和区域构造简图(b)(据Song et al., 2013；Zhang et al., 2017a修改) Fig. 1 Tectonic location (a) and regional geologic map (b) of Qilian orogen (modified after Song et al., 2013; Zhang et al., 2017a) |
南祁连增生杂岩带作为祁连造山带的构造单元之一(Song et al., 2017；Zhang et al., 2017a)，夹持于中祁连地块和宗务隆构造带之间。由于该区域是“祁-秦增生杂岩带”的重要组成部分(Song et al., 2017)，同时也是研究祁连造山带与柴达木地块之间构造演化与盆山耦合关系的关键地区之一(陈宣华等，2010)，近年来受到了国内外学者的广泛关注。尤其是柴北缘超高压变质带榴辉岩的发现，促进了祁连山造山带构造演化的研究，取得了大量研究成果(杨经绥等，1998；张建新等, 1999, 2008；Song et al., 2004；吴才来等，2004；宋述光等，2011)。但前人对南祁连增生杂岩带早古生代以来的构造热演化历史研究相对较少，且缺少相对准确的年代学数据约束。本文在南祁连增生杂岩带哈拉湖南侧的阿腊郭勒花岗岩体采取了4个二长花岗岩样品，对其进行了LA-ICP-MS锆石U-Pb、岩石主微量元素、锆石和磷灰石裂变径迹的测试分析；在此基础上，结合野外地质调查和构造演化特征，揭示南祁连哈拉湖地区早古生代花岗岩类岩浆侵入事件及其构造热演化历史。
1 区域地质概况南祁连增生杂岩带呈北西西向位于中祁连南缘断裂与宗务隆-青海南山断裂之间，西端在阿克塞一带与阿尔金走滑断裂相交，东端则尖灭于临夏西一带。研究区位于哈拉湖南部地区(图 1b，图 2)，该区出露的最老地层为古元古界斜长片麻岩、片岩和大理岩等，大面积出露地层为志留系的杂砂岩和板岩，同时分布石炭系海陆过渡相沉积和中生代陆相碎屑沉积，新生代地层则发育了新近系红层和第四系沉积。区域内发育一系列新生代北西西向逆冲断层和近南北向的走滑断层。
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图 2 南祁连哈拉湖南部地区地质构造简图 Fig. 2 Geological sketch map of the southern Hala Lake area in southern Qilian |
阿腊郭勒岩体位于青海省德令哈市以北约50km处，该岩体侵入于志留系巴龙贡噶尔组(Sb)地层中，出露面积约2200km2，为南祁连增生杂岩带内出露面积最大的侵入岩体之一。该岩体形态呈扁平状，长轴延伸大于100km，指向北西西向，与区域内构造方向相一致(图 2)。该岩体呈岩基状产出，沿加里东褶皱带复背斜轴部侵入巴龙贡噶尔组围岩中，北部被二叠系紫红色砾岩夹砂岩呈不整合覆盖。岩体主要由黑云母二长花岗岩组成，岩体与围岩接触界线较清楚，围岩蚀变显著，具有同化混染现象。
2 样品采集与分析方法 2.1 样品采集及岩石学特征本次工作在南祁连增生杂岩带哈拉湖南部的阿腊郭勒岩体采集了4个二长花岗岩样品(B1133、B1137、B1139和B1144)，用于锆石U-Pb、全岩地球化学、锆石和磷灰石裂变径迹的测试分析(表 1)。
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表 1 二长花岗岩样品信息及测试分析方法 Table 1 Summary of samples and analytical methods |
野外观察，岩体呈灰白色，球形风化，块状构造。镜下，采集的岩样呈半自形粒状、似斑状结构(图 3a，c)；矿物组成主要包括碱性长石(35%~40%)、斜长石(25%~30%)、石英(20%~25%)、黑云母(8%~10%)和白云母(3%~4%)；副矿物可见磁铁矿、锆石、磷灰石。其中，碱性长石多为他形粒状，可见条纹长石和微斜长石，似斑状；斜长石呈半自形柱状，可见聚片双晶，轻微的绢云母化；石英多为他形粒状；黑云母则呈自形片状，边部绿泥石化(图 3b，d)。
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图 3 岩石样品野外露头照片(a、c)与正交偏光镜下显微照片(b、d) 矿物缩写：Bt-黑云母；Kfs-钾长石；Ms-白云母；Pl-斜长石；Qtz-石英 Fig. 3 Field outcrop (a, c) and microscopic photographs under crossed polars (b, d) of samples Mineral abbreviations: Bt-biotit; Kfs-potassium feldspar; Ms-muscovite; Pl-plagioclase; Qtz-quartz |
样品经人工破碎后，按常规重力和磁选方法分选，并在双目镜下挑选出锆石。将待测样品锆石颗粒、数粒锆石标准M257和TEM置于环氧树脂制靶，用于透射、反射、阴极发光CL和U-Pb定年分析。锆石阴极发光在北京锆年领航科技有限公司日立HITACHIS3000-N型扫描电子显微镜上完成。
锆石U-Pb定年在中国地质科学院矿产资源研究所自然资源部成矿作用与资源评价重点实验室完成，所用仪器为Finnigan Neptune型MC-ICP-MS及与之配套的NewwaveUP213激光剥蚀系统。激光剥蚀所用斑束直径为30μm，频率为10Hz，能量密度约为2.5J/cm2，以He为载气。LA-MC-ICPMS激光剥蚀的采样应用单点剥蚀的方式，锆石U-Pb定年以锆石GJ-1为外标，U、Th含量以锆石M127(U=923×10-6；Th=439×10-6；Th/U=0.475，Nasdala et al., 2008)为外标进行校正。测试过程中，每测定5个点重复测定1个标样锆石GJ1对所获数据进行校正，同时测量一个标样锆石Plesovice，以观察仪器的状态和测试的重现性。所有标样锆石测试值的重现性均在1%(2σ)左右。数据处理采用ICPMS DataCal程序(Liu et al., 2008)；测量过程中绝大多数测点的206Pb/204Pb>1000，故未进行普通铅校正；204Pb由离子计数器检测，204Pb含量异常高的分析点可能受包体等普通Pb的影响，对204Pb含量异常高的分析点在计算时剔除；锆石年龄谐和图用Isoplot程序获得, 表达式中所列单个数据点的误差均为1σ，加权平均年龄具95%的置信度。详细实验测试过程可参见侯可军等(2009)。
2.3 岩石地球化学分析样品的全岩主量及微量元素测试在中国地质科学院国家地质实验测试中心完成。主量元素含量由PW4400型X射线荧光光谱仪测定，FeO的检测方法依据GB/T 14506.14—2010，其它主要氧化物的检测方法依据GB/T 14506.28—2010。主量元素的测试分析误差在1%~5%之间。稀土及微量元素含量由PE300D型等离子质谱仪测定，检测方法依据GB/T 14506.30—2010，其分析误差范围在5%以内。
2.4 锆石、磷灰石裂变径迹分析将筛选和分离出的磷灰石和锆石单矿物颗粒分别用环氧基树脂和聚四氟乙丙烯透明塑料片将磷灰石和锆石矿粒固定，制作成光薄片，并研磨抛光揭示矿物颗粒内表面。磷灰石样片在恒温21℃的5.5N HNO3溶液中蚀刻20s以揭示自发径迹；锆石样片在210℃下，使用KOH+NaOH高温熔融物蚀刻20~35h揭示自发径迹(Yuan et al., 2003, 2006)。将低铀白云母片(＜4×10-9) 作为外探测器盖在光薄片上，紧密接触矿粒内表面，与CN5(磷灰石)和CN2(锆石)标准铀玻璃(Bellemans et al., 1995)一并接受热中子辐照(Yuan et al., 2006)，照射工作在中国原子能科学研究院的原子反应堆进行。然后在25℃条件下的40% HF中蚀刻白云母外探测器20min揭示诱发径迹。最后需要在高精度光学显微镜100倍干物镜下观测统计裂变径迹。应用IUGS推荐的Zeta常数标定法计算出裂变径迹中心年龄。实验中根据标准磷灰石矿物的测定，加权平均得出Zeta常数值(Hurford and Green, 1983; Hurford, 1990)。本次实验获得的锆石样品和磷灰石样品的Zeta常数分别为90.9±2.8y/cm2和410±17.6y/cm2。磷灰石中裂变径迹退火存在各向异性(Green et al., 1986)，选择平行c轴的柱面来测定水平封闭径迹长度、自发径迹密度和诱发径迹密度。
2.5 热历史模拟为了进一步探讨阿腊郭勒岩体花岗岩体及南祁连增生杂岩带的热历史演化过程，本文利用HeFTy v1.9.3软件(Ketcham et al., 2005)及Ketcham et al.(2007)的Multi-kinetic退火模型，同时加入Dpar值作为约束参数进行磷灰石样品的热历史模拟。每个样品的模拟次数均为10000次，通过多次模拟得出可接受的和好的拟合结果，以及最佳模拟曲线。模拟结果的评价标准为GOF检测：当GOF≥0.05, 模拟曲线被认为是可接受的；当GOF≥0.5，模拟曲线被认为是好的模拟曲线(Ketcham, 2005)。基于磷灰石样品裂变径迹的参数(径迹年龄、长度和Dpar值等)，每次模拟设定如下约束条件：(1)初始温度设置在实测锆石裂变径迹年龄对应的封闭温度区间(200±20℃)；(2) 实测磷灰石裂变径迹年龄的时间，使样品处于部分退火带(PAZ；110~60℃)的温度区间；(3)现今状态使样品处于20±5℃地表温度。
3 分析结果 3.1 LA ICP-MS锆石U-Pb定年二长花岗岩样品B1133中锆石颗粒大小均匀、自形、透明、短柱-长柱状，长约100~250μm，宽约50~100μm，发育岩浆振荡环带(图 4a)。在276颗锆石上进行了25点分析(表 2)，其U、Th含量分别为164×10-6~1619×10-6和53×10-6~ 573×10-6，Th/U比值介于0.12~1.02之间，说明测试颗粒均为岩浆型锆石。其中18个测点十分谐和且聚集成簇(图 5)，206Pb/238U年龄的加权平均值为425.8±1.0Ma(MSWD=0.68)，代表该岩体的结晶年龄在中志留世。点2(693±7Ma)、12(2034±14Ma)、24(737±128Ma)的表面年龄明显偏老，分析点位置同时覆盖了岩浆震荡环带的锆石核及其外部锆石幔(图 4)，可能反映捕获性锆石核与岩浆阶段锆石幔的混合年龄。点17(479±5Ma)、点18(474±6Ma)和点21(490±5Ma)虽然谐和性较好，但明显偏老，而且早于柴北缘超高压变质带的形成时间(440~420Ma；Song et al., 2014)，因此推测是捕获的早期岩浆锆石。
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图 4 二长花岗岩锆石阴极发光(CL)图像及测点位置 Fig. 4 Representative CL images and sites of analyzed points of zircons of monzonitic granites |
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表 2 二长花岗岩LA-ICP-MS锆石U-Pb同位素年龄测定结果 Table 2 LA-ICP-MS zircon U-Pb data of monzonitic granites |
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图 5 二长花岗岩LA-ICP-MS锆石U-Pb谐和图 Fig. 5 Concordia diagrams of LA-ICP-MS zircon U-Pb from monzonitic granites |
二长花岗岩样品B1139中锆石颗粒大小均匀、自形、透明、短柱-长柱状，长约100~250μm，宽约50~100μm，具有明显的岩浆振荡环带(图 4b)。在279颗锆石上进行了29点分析(表 2)，其U、Th含量分别为158×10-6~738×10-6和57×10-6~393×10-6，Th/U比值介于0.16~1.06之间，说明测试颗粒均为岩浆型锆石。其中21个测点十分谐和且聚集成簇(图 5)，其206Pb/238U年龄的加权平均值为429.5±1.0Ma(MSWD=1.30)，代表了该岩体的结晶年代为中志留世。点2(435±5Ma)由于谐和度较低，不予采用。点4、5、15、18、22、25独立成簇且较谐和，206Pb/238U年龄的加权平均值为463.4±3.7Ma(MSWD=3.7)，该年龄明显偏老，同样早于柴北缘超高压变质带的形成时间(440~420Ma；Song et al., 2014)，推测是捕获的早期岩浆锆石。点28(751±8Ma)明显偏老，分析点位同时覆盖了锆石核及其外部锆石幔，可能反映捕获性锆石核与岩浆阶段锆石幔的混合年龄。
3.2 岩石地球化学特征南祁连增生杂岩带哈拉湖南部阿腊郭勒岩体二长花岗岩样品的主量元素和微量元素分析结果见表 3。可以看出，样品具有高SiO2(72.06%~76.51%)、富Al2O3(13.07%~13.29%)、富碱(ALK=6.68%~8.02%)的特征，并且相对富K2O(4.09%~5.05%，K2O/Na2O=1.14~2.36)，过铝质(A/CNK=1.08~1.11)，属于高钾钙碱性系列(图 6)。样品(B1133、B1137和B1139)的稀土总量较高(ΣREE=152.1×10-6~247.1×10-6)，轻稀土富集，(La/Yb)N比值较高(12.07~17.93)，Eu负异常明显(δEu=0.20~0.24, 图 7a)。样品B1144的稀土总量则较低为36.31×10-6，轻稀土不够富集，(La/Yb)N比值很低(1.53)，Eu负异常明显(δEu=0.05, 图 7a)。样品球粒陨石标准化稀土元素配分曲线呈现左高右低的L型，同时具有极强的负Eu异常，显示出明显的“V”字型样式。
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表 3 二长花岗岩主量元素(wt%)和微量元素(×10-6)分析结果 Table 3 Analysis results of the major (wt%) and trace (×10-6) elements of the monzonitic granites |
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图 6 二长花岗岩主量元素特征图 (a)岩浆岩TAS图解(Middlemost, 1994；Le Maitre, 2002)；(b)SiO2-K2O分类图解(Rickwood, 1989)；(c)AFM分类图解(Irvine and Baragar, 1971)；(d)A/CNK-A/NK图解(Maniar and Piccoli, 1989) Fig. 6 Diagrams showing major element features of the monzonitic granites (a) TAS diagram of magmatic rocks (Middlemost, 1994; Le Maitre, 2002); (b) SiO2 vs. K2O diagram (Rickwood, 1989); (c) AFM diagram (Irvine and Baragar, 1971); (d) A/CNK vs. A/NK diagram (Maniar and Piccoli, 1989) |
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图 7 二长花岗岩球粒陨石标准化稀土元素配分图(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 patterns (a) and primitive mantle-normalized trace element spider diagrams (b) for the monzonitic granites (normalization values after after Sun and McDonough, 1989) |
二长花岗岩样品的原始地幔标准化微量元素蛛网图显示(图 7b)，岩石相对富集大离子亲石元素(Cs、Rb、K、Th、U)，强烈亏损大离子亲石元素(Ba、Sr)和高场强元素(Nb、Ta、Ti、Zr)。Nb、Ta、Ti的亏损以及Zr的相对富集表明岩石的源区中应以陆壳成分为主，而P的亏损和K的富集则反映出阿腊郭勒岩体具有大陆地壳的性质。Rb、Th富集也是上地壳岩石的特点，Ba、Sr、Ti的亏损可以说明成岩过程中斜长石、磷灰石、钛铁矿发生了分离结晶。因此，南祁连增生杂岩带阿腊郭勒岩体的二长花岗岩可能源于壳源物质部分熔融，并且产出于同碰撞的构造环境(图 8)。
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图 8 二长花岗岩Rb-(Y+Nb)图解(a)和Rb-(Yb+Ta)图解(b)(据Pearce et al., 1984) Syn-COLG-同碰撞型花岗岩；VAG-火山弧型花岗岩；WPG-板内型花岗岩；ORG-洋脊型花岗岩 Fig. 8 Diagrams of the Rb vs. Yb+Nb (a) and Rb vs. Yb+Ta (b) of the monzonitic granites (after Pearce et al., 1984) Syn-COLG-syn-collision granite; VAG-volcanic arc granite; WPG-within-plate granite; ORG-ocean ridge granite |
二长花岗岩样品的锆石和磷灰石裂变径迹测年结果见表 4。结果表明：样品B1133和B1139的锆石裂变径迹(ZFT)年龄分别为133±7Ma(±1σ)和186±10Ma(± 1σ)(表 4)，明显小于岩浆侵入年龄(425.8±1.0Ma和429.5±1.0Ma；见表 1和图 4)，处于早侏罗世至早白垩世时期。样品测试的锆石颗粒数分别为35和28，满足实验要求。同时，2个二长花岗岩样品锆石裂变径迹的P(χ2)值均为0(表 4)，表示各单颗粒年龄相对分散，径迹年龄采用中心年龄(Sobel et al., 2006a, b)。单颗粒年龄放射图和直方图显示(图 9)，样品B1133的单颗粒年龄离散度为18%，峰值年龄分别为127.2±5Ma(91.4±4.8%)和243±19Ma(8.6±4.8%)。样品B1139的单颗粒年龄离散度为17%，峰值年龄分别为161.1±8.2Ma(64±12%)和235±15Ma(36±12%)。
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表 4 二长花岗岩样品的锆石和磷灰石裂变径迹年龄 Table 4 Zircon- and apatite-fission tracks data of the monzonitic granites |
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图 9 二长花岗岩锆石裂变径迹年龄辐射图(左)和直方图(右) 左为放射图，其左侧坐标为误差范围，右侧坐标为年龄，横坐标上为相对误差经度，图中圆点为所测试颗粒，直观标明中心年龄、离散度、P(χ2)检验值；右为单颗粒年龄直方图，直观标明样品号和测试颗粒数、曲线为拟合中心年龄趋势 Fig. 9 Zircon fission track age radio plots (left) and histograms (right) of monzonitic granites The left panels are the ZFT radial plots, in which the left, right and horizontal axises indicate age error, ZFT ages and relative error, respectively; the blue circles resprent each measured age; also shown are sample name, central age, dispersion, and chi-squre value, respectively. The right panels are single grain age histogram, the blue curve shows the trend of the fitting center age |
样品的磷灰石裂变径迹(AFT)的年龄分别为85±4Ma(±1σ，B1133)和82± 5Ma(± 1σ，B1139)，为晚白垩世早期。样品测试的磷灰石单颗粒数分别为30和34，其P(χ2)值为0，小于5%，表示各单颗粒年龄相对分散，磷灰石裂变径迹年龄同样采用中心年龄(Sobel et al., 2006a, b)。单颗粒年龄放射图和直方图显示(图 10)，样品B1133的单颗粒年龄离散度为17%，峰值年龄分别为77.9±2.8Ma(65.3±6%)和98.8±6.7Ma(34.7 ± 6%)。样品B1139的单颗粒年龄离散度为20%，峰值年龄分别为71.1±4.8Ma(63 ± 15%)和104.2±8.2Ma(37±15%)，表明样品自早白垩世晚期以来经历了多期热事件的影响。
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图 10 二长花岗岩磷灰石裂变径迹年龄辐射图(左)和直方图(右) 说明见图 9 Fig. 10 Apatite fission track age radio plots (left) and histograms (right) of monzonitic granites See Fig. 9 for caption note |
样品的磷灰石围限平均径迹长度(MTL)分别为14.1±1.6μm和13.8±1.9μm(表 4)，且围限径迹测试条数均超过100条，表明数据质量较好。该径迹平均长度小于原始径迹长度(16.3±0.9μm；陈刚等，2005)，也小于快速冷却至地表温度的裂变径迹平均长度(14.5~15.5μm；Green et al., 1989)。与结晶C轴平行的裂变径迹蚀象的最大直径(Dpar)的平均值分别是2.18和2.12(表 4)，但样品的磷灰石裂变径迹年龄辐射图显示，Dpar值稍有分散。样品B1133的Dpar值分布为1.61~2.57μm，样品B1139的Dpar值分布则为1.24~2.92μm，这可能与花岗岩样品数据采集的偏差有关。为了进一步分析样品Dpar值的离散度，本文将2个磷灰石裂变径迹样品的Dpar值与平均径迹长度的关系进行了进一步分析(图 11)。结果显示，样品B1133和B1139的Dpar值分布并未呈现出较明显的不同动力学性质的区间，Dpar值均主要集中在1.8~2.6μm，说明样品中的各组分经历了相同或相似的隆升过程(图 11)。
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图 11 磷灰石裂变径迹样品的平均径迹长度与Dpar值的关系 Fig. 11 Mean track lengths plotted against Dpar value of the AFT samples |
在任何一地表岩石的长期隆升剥蚀过程中，在由外探测器裂变径迹定年分析中获得的样品径迹年龄可能不具有简单的地质意义，而代表其长期处于部分退火带(PAZ)或者缓慢隆升突破部分退火带的过程(Gleadow and Brown, 2000；张志诚和王雪松，2004)。封闭径迹长度及其分布记录了岩石经历的最高古地温及热历史过程, 是裂变径迹分析中最重要的参数。裂变径迹长度的差异记录了不同样品经历的时间-温度信息，利用径迹年龄和径迹长度，选择一定的退火模型，进行热历史的反演模拟，可以揭露出样品表观年龄下定量的、更详尽的热演化信息，为区域构造热演化历史分析提供更多的依据(张志诚和王雪松，2004；Ketcham et al., 2007)。
样品B1133和B1139的热历史模拟结果显示，所有样品的GOF(拟合度)检测均大于0.5，模拟质量较高且较为可信。南祁连地区阿腊郭勒岩体经历了3期冷却历史：早白垩世以来，自锆石裂变径迹部分退火带隆升至磷灰石裂变径迹部分退火带的顶部；经过晚白垩世至古新世的构造平静阶段后；于始新世早期以来的再次进入快速隆升阶段(图 12)。
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图 12 二长花岗岩的热历史模拟图 左侧为时间-温度模拟曲线，紫红色和绿色区域分别代表可接受的和好的拟合结果，黑色实线代表最佳拟合时间-温度曲线，直观标明测试年龄颗粒数、实测径迹年龄、模拟径迹年龄、径迹年龄GOF值、可接受的模拟曲线数和好的曲线数；ZFT age为锆石裂变径迹年龄. 右侧为样品内径迹长度直方图，直观标明测试径迹条数、实测径迹长度、模拟径迹长度和平均径迹长度GOF值 Fig. 12 Thermal history models of monzonitic granites The left panels are modeled time-temperature path: the purple and green areas represent good and acceptable fits, respectively; the dark black curve indicates the best fit; Also shown are sample name, numbers of analysed single grain, measured fission track ages, modeled fission track ages, GOF (Good of fit) value, number of acceptable fits, and number of good fits, respectively.The right panels are modeled mean track length distribution histogram: Also shown are sample name, numbers of measured track length, measured mean track length, modeled mean track length and its GOF value, respectively |
锆石U-Pb定年结果显示，哈拉湖南部的二长花岗岩B1133和B1139的侵位年龄分别为425.8±1.0Ma(MSWD=0.68)和429.5±1.0Ma(MSWD=1.30)，表明阿腊郭勒岩体形成于中志留世。
前人的研究表明：由于祁连洋洋壳的俯冲，祁连山到柴北缘地区在520~440Ma主要发育岛弧岩浆作用(Song et al., 2013, 2014, 2017；Xia et al., 2003, 2012)，而在440~360Ma则主要发育与大陆碰撞和碰撞后的造山带垮塌有关的岩浆作用(Song et al., 2014；Wang et al., 2014；宋述光等，2019)。前人在南祁连地区获得的花岗岩类侵入年龄的峰值主要集中在446~440Ma(吴才来等，2001；Gehrels et al., 2003；卢欣祥等，2007；张照伟等, 2012)，且岩石地球化学特征显示南祁连增生杂岩带存在该时期的洋壳俯冲环境下岛弧岩浆活动形成的Ⅰ型花岗岩(罗志文等，2015)，证明其与祁连洋闭合早期大洋俯冲作用导致的岛弧岩浆活动密切相关。而本文获得的哈拉湖南部阿腊郭勒岩体的LA-ICP-MS锆石U-Pb年龄显示该岩体的侵位时代为中志留世(425~429Ma)，岩石地球化学特征显示阿腊郭勒岩体的二长花岗岩可能源于壳源物质部分熔融，且产出于同碰撞的构造环境，并且南祁连-柴北缘地区在同时期(440~420Ma)发生了大陆深俯冲引起的超高压变质作用(Song et al., 2014)，表明该期岩浆事件是与祁连洋洋壳俯冲结束后的柴北缘大陆碰撞过程中的岩浆活动有关，代表了柴北缘超高压变质带大陆俯冲折返过程中大陆地壳的深熔作用(宋述光等, 2013, 2015)。该结果也与柴北缘绿梁山和锡铁山地区的花岗岩形成的时代与构造环境相一致(孟繁聪和张建新，2008；Yang et al., 2020)。
4.2 南祁连哈拉湖南部地区早白垩世以来的冷却历史南祁连哈拉湖地区阿腊郭勒岩体二长花岗岩样品的锆石和磷灰石裂变径迹年龄及热历史模拟结果表明，南祁连哈拉湖南部地区自早白垩世以来经历了至少3个阶段的冷却历史：(1)早白垩世以来的快速隆升阶段；(2)晚白垩世-古新世的构造平静阶段；(3)始新世早期以来的快速隆升阶段。
中生代中晚期的构造活动影响了青藏高原北缘及东北缘的大部分地区(Vincent and Allen, 1999；Jolivet et al., 2001；Chen et al., 2003；李海兵等, 2004, 2006；Yin et al., 2007, 2008a, b；蒋荣宝等，2008；Cheng et al., 2019; Zhang et al., 2020; Wang et al., 2022)，南祁连增生杂岩带哈拉湖南部地区早白垩世以来也发育了一期快速冷却的事件(图 12)。该期构造活动反映了白垩纪的地壳隆升，与该区缺失白垩纪地层相一致，是一次区域性的隆升事件。地震剖面显示柴北缘和南祁连地区发育早白垩世逆冲断层(Zhang et al., 2020)，而祁连山北缘榆木山地区则发育有系列早白垩世早期的走滑双重构造、逆冲推覆和飞来峰构造(陈宣华等，2019；Wang et al., 2022)，这些变形均说明早白垩世早期的区域性挤压构造活动规模巨大。同时，阿尔金断裂东段地区在100~120Ma和~82Ma发育的两期岩浆活动(李海兵等，2004)，河西走廊地区早白垩世碎屑岩层序地层及沉积特征则较好地记录了早白垩世祁连山隆升过程(唐玉虎等，2008；梅冥相和苏德辰, 2014a, b；郭荣涛等, 2015, 2016)。祁连山白垩纪早期的快速隆升可能主要受拉萨地块与欧亚板块沿班公湖-怒江缝合带碰撞远程效应的影响(Vincent and Allen, 1999；Jolivet et al., 2001；李海兵等，2004；Cheng et al., 2019)，并初步构成了青藏高原雏形的东北部边界。
前人用磷灰石裂变径迹方法获得的南祁连地区的隆升过程表明，南祁连地区经历了晚白垩世-古新世期间短暂的构造夷平阶段后，于始新世早期再次转入快速隆升阶段(Qi et al., 2016；戚帮申等，2016)。柴达木盆地中新生代沉积岩的碎屑磷灰石裂变径迹方法也同样获得了54~47Ma的快速剥蚀与沉积记录，南祁连山和柴北缘地区则为此提供了沉积物源(Jian et al., 2018)。南祁连地区始新世的区域性构造运动最终导致哈拉湖地区早期发育的夷平面在34Ma的解体(贾丽云等，2018)。同时，中祁连地区、阿尔金北缘山脉和党河南山在约40Ma的快速冷却剥蚀(Jolivet et al., 2001；孙岳等，2014；Li et al., 2020)，以及始新世晚期-渐新世河西走廊盆地和中祁连木里盆地内火烧沟组(E2-3h)与上覆白杨河组(E3N1b)均呈微角度不整合接触(戴霜等，2005；戚帮申等，2013)，这些证据均显示出青藏高原北部在始新世-渐新世存在构造变形与隆升。同时，青藏高原东北缘新生代陆内变形过程所导致的地壳增厚使得南祁连增生杂岩带的地壳厚度达到了区域内的最大值(Gao et al., 1999)，并具有向南北两侧(柴达木盆地和中祁连地块)逐渐减薄的趋势，因此南祁连增生杂岩带应该是祁连山地区新生代以来最早发生地壳缩短的关键地区(Gao et al., 1999；He et al., 2018；Huang et al., 2021)。祁连山在新生代早期的挤压变形可能与早古生代祁连洋闭合时向南俯冲的化石俯冲带作为先存构造薄弱带而导致的印度与欧亚板块碰撞的远程效应有关(Chen et al., 2020；Li et al., 2021)。受这一系列强烈构造活动的影响，祁连山及其周缘地区主要以系列逆冲断层的形式协调青藏高原向北东方向的生长(Tapponnier et al., 1990；Burchfiel et al., 1991；Vincent and Allen, 1999；Zhang et al., 2004；Yuan et al., 2013；Zuza and Yin, 2016；Allen et al., 2017；Li et al., 2019)，同时也开启了青藏高原东北缘自印度板块和欧亚板块碰撞以来的初始隆升与地壳增厚(Meyer et al., 1998; Lease et al., 2012; Zuza and Yin, 2016；Zuza et al., 2018)。
4.3 南祁连哈拉湖南部地区构造热演化历史构造热年代学以构造地质学理论为指导，可以为大陆内部不同块体的构造变形时间、山体抬升和盆地沉降速率等提供精细的年代与热作用制约(王瑜，2004)。其中，矿物封闭温度是认识地质体形成与剥露作用的热演化历史的重要依据(陈宣华等，2010)。矿物年龄的封闭温度取自前人有关实验资料：锆石U-Pb年代学封闭温度取>900℃(Cherniak and Watson, 2001, 2003)，锆石裂变径迹法的封闭温度为240~210℃(Zaun and Wagner, 1985；Bernet et al., 2009)，磷灰石裂变径迹法封闭温度为110~60℃(Gleadow and Duddy, 1981；Ketcham et al., 2007)。将不同方法的测年数据、封闭温度和地温梯度联系在一起形成热年代学曲线，并结合区域构造演化特征，揭示南祁连增生杂岩带哈拉湖南部地区的热演化历史和山脉隆升过程。
根据南祁连哈拉湖地区阿腊郭勒岩体二长花岗岩的LA-ICP-MS锆石U-Pb年龄、岩石地球化学特征、锆石和磷灰石裂变径迹年龄和热历史模拟结果，并结合区域构造演化特征，得到该地区的构造热年代学演化历史曲线图(图 13)。结果表明，该区域在中志留世(425~429Ma)发生了一期与祁连洋洋壳俯冲结束后的大陆碰撞过程有关的岩浆侵位过程，并伴随有榴辉岩相超高压变质作用(宋述光等，2013；Song et al., 2014)，在晚志留世-早泥盆世期间受强烈的造山运动影响而快速冷却，使得志留纪残余海盆相复理石建造和泥盆纪磨拉石不整合的沉积覆盖于基岩之上(Zuza et al., 2018)。自晚泥盆世至侏罗纪，南祁连地区进入了陆表海和海陆交互相沉积的构造平稳阶段，岩体进入缓慢冷却阶段。自早白垩世以来，该地区再次进入快速隆升阶段，并初步构成了青藏高原雏形的东北部边界。经过晚白垩世-古新世短暂的构造平静期，受印度板块与欧亚板块挤压作用远程效应的影响，祁连山地区以发育一系列褶皱、逆冲断层、走滑断层和区域地层角度不整合的方式协调青藏高原向北东方向的隆升与扩展。
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图 13 南祁连哈拉湖地区早古生代岩浆侵入事件和构造热演化历史图解(据陈宣华等，2010；Chen et al., 2015) a、b、c、d分别为冷却速率0.1℃/Myr、1℃/Myr、10℃/Myr和100℃/Myr线；其余虚线为推测冷却曲线 Fig. 13 Temperature-time-depth diagram showing the tectonic thermal evolution history of the Early Paleozoic intrusive magmatism in Hala Lake area, southern Qilian (modified after Chen et al., 2010, 2015) a, b, c, d indicate the cooling rate of 0.1℃/Myr, 1℃/Myr, 10℃/Myr and 100℃/Myr, respectively. The bold dashed line represents speculative cooling curve |
通过南祁连增生杂岩带哈拉湖地区阿腊郭勒岩体的LA-ICP-MS锆石U-Pb年龄、岩石地球化学特征、锆石和磷灰石裂变径迹年龄以及热历史模拟结果，结合前人研究成果得出如下结论：
(1) 锆石U-Pb定年结果和岩石地球化学特征显示，南祁连增生杂岩带哈拉湖南部阿腊郭勒岩体的二长花岗岩(B1133和B1139)侵位年龄分别为425.5±1.0Ma(MSWD=0.68)和429.5±1.0Ma(MSWD=1.30)，代表了阿腊郭勒岩体的侵入时代，表明南祁连哈拉湖地区在中志留世发生一期岩浆侵入事件。岩石地球化学特征显示该岩体具有壳源花岗岩特征，且产出于同碰撞的构造环境，说明该期岩浆事件是与祁连洋洋壳俯冲结束后的柴北缘地区大陆碰撞过程中的岩浆活动有关。
(2) 锆石和磷灰石裂变径迹年龄、热历史模拟结果和区域构造变形特征显示，哈拉湖地区自早白垩世以来经历了至少3个阶段的冷却历史：早白垩世以来的快速隆升阶段；晚白垩世-古新世的构造平静阶段；始新世早期以来的快速隆升阶段。
(3) 揭示了南祁连哈拉湖地区在中志留世-晚泥盆世的区域深成岩浆侵入和快速隆升过程、晚泥盆世-侏罗纪的构造平稳与缓慢冷却阶段以及早白垩世以来的中低温冷却和快速隆升的构造热演化历史。
致谢 LA-ICP-MS锆石U-Pb测年分析得到了中国地质大学(北京)邵浩浩硕士和中国地质科学院苗慧心硕士的帮助；图件绘制工作得到了中国地质科学院丁伟翠高级工程师和徐盛林助理研究员的指导与帮助；锆石和磷灰石裂变径迹测试由中国地质大学(北京)袁万明教授协助完成；北京大学宋述光教授和另外一位匿名审稿专家的细致审稿，给本文提出了诸多建设性意见；作者对他们谨表衷心感谢。
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