Zirzon U-Pb age and petrogenisis of plagiogranite porphyry in Changlingzi, Hexigten Banner, Inner Mongolia and its collision orogeny
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摘要:
内蒙古克什克腾旗长岭子斜长花岗斑岩位于大兴安岭锡林浩特增生杂岩带内。本文对长岭子斜长花岗斑岩进行了主微量元素地球化学以及锆石U-Pb年代学和Lu-Hf同位素研究。长岭子斜长花岗斑岩锆石206Pb/238U加权平均年龄为（248.1±4.7）Ma，是早三叠世岩浆活动的产物；继承锆石除外，样品中锆石具有正的εHf（t）值（5.78~12.41），二阶段模式年龄TDM2分别为914~488 Ma。长岭子斜长花岗斑岩具有较高的SiO2、Na2O和Al2O3含量以及较低的Fe2O3、MgO和CaO含量，属于偏铝质-过铝质的低钾-钙碱性系列I型花岗岩，富集Rb、K、U、Th、Pb、Sr等大离子亲石元素，亏损Nd、Ta、Ti等高场强元素。同时，斜长花岗斑岩具有高Sr低Y以及高Sr/Y比等特点，具有典型的埃达克质岩石特征，形成于加厚下地壳的部分熔融。综合上述地球化学特征，本文认为长岭子斜长花岗斑岩来源于加厚新生下地壳的部分熔融，表明早三叠世兴蒙地区并非岛弧的环境，而是处于碰撞造山环境，古亚洲洋在该时期已经闭合。
Abstract:The Changlingzi plagiogranite porphyry is located in the Xilinhot Late Paleozoic Accretion Complex within the Da Hinggan Mountains. This study is focused on the zircon U -Pb isotopic geochronology, Hf isotopic composition analysis and geochemistry of the Changlingzi plagiogranite porphyry. Zircon crystals from the plagiogranite porphyry yielded weighted average 206Pb/238U age of (248.1±4.7)Ma. The zircons from this porphyry have positive εHf(t) values from 5.78 to 12.41, with TDM2(Hf) ages from 914 to 488Ma. The plagiogranite porphyry has high content of SiO2, Na2O and Al2O3, and low content of TiO2, MgO and CaO, showing a metaluminous-peraluminouslow-K to calc-alkaline affinity, with LREE enrichment and HREE depletion, suggesting I-type granite. In addition, the plagiogranite porphyry has high Sr and low Y values as well as high Sr/Y ratios (74.5~103.4), indicating that the plagiogranite porphyry belongs to adakite. It is suggested that the plagiogranite porphyry was formed by partial melting of the thickened newborn lower crust. And in Early Triassic, Xing' an-Mongolian orogenic belt was in a collisionorogeny tectonic setting, indicating that the Paleo-Asian Ocean had been closed in this period.
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1. 引言
能源与环境问题一直是困扰世界各国可持续发展的重大问题，进入21世纪，节能减排、开发新能源和走可持续发展道路受到越来越多的关注（刘凯等，2017）。地球是个巨大的热库，其内核（地核）的温度高达约6000℃（汪集旸等，2012）。地核与地表巨大的温差使得地球在不断地向外（大气层）散发着热量，同时地壳内部放射性衰变热、势能转换热、摩擦热等也在不断生成与供给（Clauser，2005）。而在当前的技术经济和地质环境条件下，可以从地壳表面下一定深度内科学、合理地开发出来的地下岩石中的地热能量和地热流体中的热能量及其伴生的有用组分被称之为地热资源（孔维臻，2013）。地热资源是一种极具竞争力的清洁可再生能源，很大程度上可以缓解因大量使用化石能源所造成严重的空气污染问题（马伟斌等，2016），按其成因和产出条件可分为水热型和干热岩型，利用方式分为直接利用和发电两种。
断裂构造对地热田分布具有直接的控制作用（苗可等，2012），因为它是地热水主要储存和运移通道，要掌握地热水的赋存特征，必须掌握断裂的产状及展布特征。江西省会昌县坝背地区地处武夷山和南岭余脉地带，受太平洋构造域的制约，晚侏罗世发生大规模岩浆侵入和火山喷发（燕山期），早白垩世晚期以后发生了强烈的伸展作用，强烈的地壳运动形成密集的断裂构造，成为地下热源导热构造带，并在断裂带附近形成地热异常区。区内有分布于会昌盆地东侧大富足岩体内的河草坑铀矿田和桂坑岩体中的铀矿化（蔡煜琦等，1997），说明区内具有放射性衰变热的持续供给来源。
地下的热作用能明显改变岩石的地球物理性质，构造带、地热田的生储盖等不同部位均具有较明显的电性差异（Wright et al., 1985），地热区电阻率的空间分布不仅受围岩性质的影响，还与勘探对象——热水的分布直接有关（切列缅斯基，1982）。总体上，随着温度的升高，电阻率在不断的降低，可见在地热田勘查中，低阻体成为最重要的寻找目标，由于它的直接指示作用和地热田不同部位电性差异明显，电法和电磁法也就成为地热资源勘探中最直接有效的方法技术（曾昭发等，2012）。直流电测深法、高密度电法、激发极化法、瞬变电磁法等都不乏成功的范例，而CSAMT更是因为其抗干扰能力强、探测深度大、横向分辨率高、受高阻层屏蔽作用影响小等优点，越来越多地被应用到地热勘查中（周仕新，2013）。为了查明会昌县坝背勘查区各断裂构造的产状、规模及深部变化特征，为寻找地热水钻孔布置提供依据，遵循从已知到未知，由浅至深的勘探原则，项目组首先在已知温泉位置布置3条高密度试验测线，确定地球物理方法在该测区的有效性和导水断层的形态、主要物性参数等，接着在已知温泉位置以南布置4条高密度测线，然后在高密度电阻率法资料初步解释成果的基础上再施工CSAMT。
2. 地质概况
会昌县坝背区域上地处武夷山和南岭余脉地带，属低山丘陵地区，地势由西南向东北倾斜，境内峰峦起伏。勘查区最高点在南部海拔标高约389.9 m，最低点海拔标高约190 m，最大相对高差近200 m。工作区及周边地球物理工作程度低，未开展过系统的地球物理工作。区域地质概况详细论述如下（图 1）。
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图 1 坝背地区区域地质、勘探范围及测线布置图Figure 1. Regional geology, exploration limits and survey line layout of Babei area2.1 地层
勘查区内地层岩性特征由新到老分别为第四系（Qh1），上白垩统周田组（K2z）、茅店组（K2m2），下白垩统鸡笼嶂组（K1j）、震旦系桃溪岩组（Pt32 - 3 tx）。其中Qh1主要分布在河水两岸及山间沟谷附近，成因类型为冲积作用，岩性具有二元结构，上部为黄褐色、褐色亚黏土、亚砂土，厚度1.0~2.5m；下部为砂砾石层，砾石成分为石英砂岩，粒径一般2~4 cm，大者达10 cm，结构松散，厚度1.5~3.5 m，总厚度2.5~ 6.0 m。K2z大面积出露勘查区内，为紫红色中厚层状钙质粉砂岩夹薄层细砂岩，下部为紫红色细粒石英砂岩，厚度170~450 m。K2m2大面积出露勘查区西侧，为紫红色巨厚层状砾岩夹钙质粉砂岩、泥岩及粗砂岩，砾石成分以晶屑凝灰岩为主，厚度300~ 800 m。K1j出露于勘查区东北侧，为杂色流纹质熔结凝灰岩，厚度大于200 m。Pt32-3tx小面积出露勘查区北东角，为勘查区褶皱基底，岩性主要为杂色黑云斜长变粒岩、石英片岩，厚度大于400m。这些地层的成分与结构特征无疑为地热水的存储提供了良好条件。
2.2 岩浆岩
勘查区出露岩浆岩来自两个不同时期，出露面积都较大。一是分布于勘查区北东角印支期晚三叠世罗珊序列（T3γt）黑云母、二云母花岗岩；二是分布于勘查区南东角加里东期早志留世汤湖序列（S1gnγ-ξγ）二长、正长花岗岩。
2.3 地质构造
本区的区域大地构造单元在加里东期为中南武夷山褶皱带（江西省区域地质志，1984），之后受太平洋构造域的制约，晚侏罗世发生大规模岩浆侵入和火山喷发（燕山期），在武夷山隆起地带形成一系列的NE、NNE向火山岩盆地，到早白垩世晚期以后，受太平洋板块北北西向左行走滑影响，发生了强烈的伸展作用，盆地由坳陷转为断陷，沉积了巨厚的红色碎屑岩系，不整合地叠覆于火山岩盆地之上。
2.4 地球物理特征
周田组为紫红色中厚层状钙质粉砂岩夹薄层细砂岩，紫红色细粒石英砂岩其视电阻率小于200 Ω·m。茅店组为紫红色巨厚层状砾岩夹钙质粉砂岩、泥岩及粗砂岩，砾石成分以晶屑凝灰岩为主其视电阻率为300~400 Ω·m。鸡笼嶂组为杂色流纹质熔结凝灰岩其视电阻率400~600 Ω·m。震旦系桃溪岩组，为勘查区褶皱基底，岩性主要为杂色黑云斜长变粒岩、石英片岩，其视电阻率大于800 Ω·m。断裂破碎带多系充水，其电阻率相对围岩较低，在视电阻率断面图上多呈现低阻特征，异常等值线密集或扭曲。这就为电法探测断裂破碎带提供了物性条件。
3. 数据采集及处理
3.1 测网布置
勘探区地球物理测线的布置安排在地表调查后，根据地表地质调查情况来确定地球物理测线的起止点。因勘探区内及相邻勘探区均没开展过地球物理工作，进一步了解地球物理方法在该测区的有效性和导水断层的形态、主要物性参数等，为勘查区地球物理参数的设置和地球物理资料的解释工作提供依据，在勘探区外已知的车心出露点布设一条高密度电阻率测量线，编号为S1线，测线长度为0.3 km。由于车心热水泉出露点走向长约50 m，方位为北东10°左右，S1线施工完后视电阻率断面图反映不够明显，因此在S1线南约240 m处布置了长750 m的S2线，方位角为69°；在与车心热水泉出露点走向斜交处布置了长590 m的S3线，方位角为344°，同时将S1线延长到750 m，受地形限制其方位角调整为93°，3条测线极距均为10 m。然后根据地表地质调查情况在勘探区内共布置4条高密度测线，线距500 m，极距10 m。由北向南分别为G1线、G2线、G3线和G4线，每条测线长约1.65 km，方位角为102°。G1测线东侧遇有陡坎、悬崖等障碍物影响布线，因此，实际布线时G1测线往南偏移150 m左右（图 1）。
在高密度电阻率法资料的初步解释成果的基础上，确定在勘探范围内重点勘探区开展可控源音频大地电磁测深工作，由于在勘探区中部有一由西南-北东走向的220 kV的高压电线，对可控源音频大地电磁测深的野外测量数据采集数据质量会有一定的影响，故勘探区内根据实际情况布置了5条可控源音频大地电磁测深测线，测线由南向北、由西向东分别为K1线、K2线、K3线、K4线、K5线。线距在300~500 m，长度在300~840 m，点距30 m，方位角为92°。K2线、K4线、K5线基本上与高密度电阻率法测线重合（图 1）。
3.2 数据采集
高密度电阻率法使用的仪器是重庆奔腾数控技术研究所生产的WDJD-3型和WGMD-1型高密度电阻率测量系统。在试验线S1线布置了两个排列同时用高密度电阻率法α1排列装置和α2排列装置进行测量，经对资料的分析认为采用高密度电阻率法α1排列装置进行测量效果更佳，因而决定高密度电阻率测量工作采用α1排列装置（图 2），电极距10 m，60根电极，排列长度590 m。
CSAMT投入的仪器设备为加拿大凤凰公司的V8网络化多功能电法仪，为保证工作质量，在测量之前标定了仪器和磁棒，并进行了一致性测试，测试结果均符合规范要求。CSAMT测点点距30 m，频率范围1~9600 Hz，有效探测深度大于2.0 km。采集方式为标量模式，接收端和发射端工作示意图如图 3。本项目布设了2个场源，一号场源极距为1316 m，最小收发距为9810 m，在第一天工作结束后，发现频率在100 Hz左右进入近场并且数据信躁比大，于是对发射场源进行了调整，并通过增大收发距，加大供电极距，增大供电电流来保证数据质量。最终选定二号场源位置，极距为2079 m，最小收发距为13269 m，最大供电电流17A。
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图 3 CSAMT法V8（一主一辅）网络化野外作业方式示意图Figure 3. Schematic diagram of field operation mode of CSAMT method using V8 (one main and one auxiliary) network本次可控源音频大地电磁法测量水平方向电场（MN）平行于场源（AB），水平磁场垂直于场源布设。共设计55个频点，工作频带为1~9600 Hz（表 1），频点间隔均匀分布，高、中频段适度加密。
表 1 CSAMT工作频率Table 1. CSAMT working frequency list
3.3 数据质量评价
本项目共获得高密度电阻率法测量坐标测点261个，质量检查点21个，质量检查点占测点总数7.4%，高密度电阻率法测点数据没有废点，检查点相对均方误差均小于5%，数据质量良好；可控源音频大地电磁测点82个，质量检查点5个，质量检查点占测点总数5.7%，不存在三类点，检查点相对均方误差均小7%，数据质量良好。
3.4 数据处理
高密度电法野外采集的数据传入计算机后，对每个排列所测数据经软件（RES2DINV）进行必要的一些编辑，对个别畸变点进行剔除（图 4）。由于测线地形相差大，因此在进行二维反演时必须进行地形改正，本次计算选用Schwarz-Christoffel变换法作地形改正计算。然后使用有限差分法进行反演得到每个排列的视电阻率断面图，根据反演结果所得的视电阻率断面图，进行破碎带等地质体的初步划分。然后对每个排列所测的数据进行数据拼接得到整条测线的数据，经一系列处理后，得到整条测线的视电阻率断面图。
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图 4 G1线1排列数据圆滑处理前（a）后（b）对比图Figure 4. The contrast diagram of Permutation1, Line G1 data (a) and that processed by smoothing (b)CSAMT数据处理以测线为单位进行，数据预处理使用的软件为加拿大凤凰公司配套软件CMT Pro Version，通过加载数据；核对点位、极距等信息；查看数据质量来完成预处理过程，最后输出*.AVG文件用于反演。数据反演软件为CSAMT-SW，过程包括：测线记录型文件-（D File）、点位偏差校正*-J*、剔除跳点*-ED*、曲线平滑*-S2*（图 5）、删除近场频点*-WR*、删除坏道数据（重复点数据）*- WC*、静态位移校正、Bostick反演生成*.DMT文件等，最终绘制成图。
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图 5 未经平滑处理（a）、（c）和处理后（b）、（d）视电阻率和相位曲线对比图Figure 5. The contrast diagram of apparent resistivity and phase curve (a), (c) and that processed by smoothing (b), (d)4. 电阻率模型分析
高密度视电阻率断面图是以实测数据经数据处理后按点（线）排列方式形成的地表以下不同深度的视电阻率值绘制而成。纵轴为标高，横轴为测点对应距离，剖面方向为102°（图 6、图 7）。通过已收集的钻孔资料可知地下热水是通过岩层裂隙涌向地面的，高密度电阻率法试验S3线就通过了该裂隙带，它在视电阻率断面图上反映为低阻区，据此对全区各线进行解释。鉴于高密度电阻率法的探测深度低于CSAMT，由高密度电阻率法推断的断裂或破碎带在深部的发育和延伸情况还需要CSAMT做进一步的追踪。
CSAMT的主要参数为卡尼亚视电阻率，由实测正交电、磁信号振幅计算而来，与常规电法中视电阻率的意义相同，主要反映勘探体积内岩（矿）石的综合导电性能。图 8为实测数据经处理后按点（线）排列方式形成的地表以下不同深度的卡尼亚视电阻率值绘制而成。纵轴为标高，横轴为测点对应距离，剖面方向为92°。各勘探线CSAMT二维反演电阻率断面图解译如下。
由K1线CSAMT二维反演电阻率断面图（图 8）可看出，剖面内推断的基底起伏大，基底以上地层呈不规则分布。剖面0~480 m，标高-250 m以上；剖面750~840 m，标高240~-50 m为高阻区，推断为白垩纪晚期茅店组砂砾岩。高阻体以下至基底界面区域存在明显的低阻异常带，剖面90~360 m，标高在-396~-550 m、埋深在682~814 m视电阻率值异常低，为低阻异常区，编为1号低阻异常区。剖面660~840 m，标高在-82~-176 m，埋深在396~491 m视电阻率值异常偏小，为低阻异常区，编为2号低阻异常区。剖面120 m附近，标高在230~150 m处视电阻值与两侧差异明显，推测此处有一断裂构造，结合地质资料和G1线高密度视电阻率断面图将该断裂命名为F3，该断裂构造将0~480 m的高阻错断。剖面480 m处两侧电阻率值差异显著，推断该位置有一断裂，结合地质资料和G1线高密度视电阻率断面图（图 7）将该断裂命名为F1，此构造深切至基底。剖面750 m处电阻率差异大且地层错动，推断该处有一断裂构造，此构造深切基底，且造成切割部位发生一定的凹陷，两侧则抬升的现象，结合地质资料和G1线高密度视电阻率断面图将该断裂命名为F4。
K2剖面内推断的基底起伏较小，基底以上地层呈不规则分布。剖面0~480 m处，标高在250~130 m和剖面0~270 m处，标高在-50~-170 m为高阻区，这2个高阻区认为系同一电性层被断裂F3错断所致，推断其高阻区为白垩纪晚期茅店组砂砾岩。剖面180~360 m处，标高在-200~-462 m，埋深在490~758 m视电阻率值异常偏小，存在一明显的低阻异常区，为1号低阻异常区往南的延伸。剖面390 m处电阻率两侧的差异大，延伸深，基底略微凹陷，推断存在一断裂构造，结合G1线高密度视电阻率断面图推断为F4断层往南的延伸。K3剖面内推断的基底起伏大，基底以上地层呈不规则分布；剖面0~240 m处，标高在-292~-584 m，埋深在532~ 826 m视电阻率值异常小，为低阻异常区，同样为1号低阻异常区在该处的表现。剖面120~180m处，标高在160~-220 m为高阻区，推断为白垩系晚期茅店组砂砾岩，该砂砾岩近直立，底部被F3断裂错断。剖面270~300 m处两侧的电阻率差异大，推断该位置存在一断裂构造，构造近乎直立，结合地质资料和G2线高密度视电阻率断面图推测为F4在该处的表现，基底凹陷明显。
K4剖面内推断的基底起伏明显，剖面中部位置基底隆起。剖面0~180 m处，标高120~-800 m和240~300 m处，标高50~-50 m为高阻区，这2个高阻区有错动，推断存在一断裂构造，结合地质资料和G1线高密度视电阻率断面图将该断裂命名为F5。K5剖面内推断的基底起伏平缓，基底以上地层分层明显，各种岩性在横向上分布较均匀，地表至标高-500 m范围内存在三层次高阻，其间夹杂2层厚度50~100 m的低阻区，推断此区域为白垩系茅店组砂砾岩，剖面上部的低阻区编为3号低阻异常区，3号低阻异常区顶、底标高186~131 m，埋深在95~156 m。在剖面中部的低阻区编为4号低阻异常区，4号低阻异常区顶、底标高-82~-316 m，埋深在368~600 m。剖面90~150 m处从表层到基底电性层均有错动，推断该位置存在一断裂构造，结合地质资料和G2线高密度视电阻率断面图将该断裂命名为F5。
5. 解释与讨论
区内断裂主要由一系列北北东或北东及近东西或北西向规模不等的逆冲、斜冲断层和推滑-推覆断裂构造组成，这些密集的（断裂）成为地下热源导热构造带，并在断裂带附近形成地热导常区。通过对电阻率模型的解释获得了测区高阻基底埋深在750~1250 m，基底起伏较大；同时确定了大断层F1、F3、F4、F5的性质和产状（图 8）。F1正断层分布在测区北部边缘，走向为弧形，总体为北西向，倾向为西—西南，倾角73°，断层深切至基底，为测区内导热构造。F3逆断层分布在测区西部，走向为北东向，倾向南东，倾角55°~65°，测区内走向长1800 m。F4正断层分布在测区中东部，走向在G4线— K3线为近南北向，在K3线—K1线为北东向，倾向西—北西，倾角86°，测区内走向长1800 m，深切至基底，为测区内导热构造。F5逆断层分布在测区东部，走向在G4线—G3线为近南北向，在G3线~G1线为北东向，倾向由东转南东，倾角82°，测区内走向长1300 m，深切至基底面。
本区以侵蚀构造低山地形为主，地势上东高西低，植被繁茂，构造裂隙水发育。地下水主要赋存于断裂破碎带和构造裂隙中，富水性极不均一。地下水总体运动方向由南东向北西径流，一部分在车心村的西部（温泉地）排泄于地表，另一部分沿深部构造径流出勘查区。
联合K1、K2、K3剖面图中来看，1号异常区基本上分布在以K1（270 m处）—K2（240 m处）—K3（180 m处）连线为轴线的左右两侧各约100 m范围内，东部为北东向的高阻条带，为F4深大断裂构造的反映。1号异常区在4个低阻异常区内范围最大，长约1000 m，宽约240 m，高约200 m，由南往北的走向特征为北东转向北西，是地热水赋存最为可能的区域，建议在K1线360 m处布设钻孔进行验证，孔深约800 m，满足深大断裂和基底对低阻区的深度控制。
6. 结论
（1）通过高密度和CSAMT电阻率勘测推断出F4、F1构造深切至基底界面，为深大断裂，是温泉主要的导水导热构造。
（2）依据工作区的电性结构特点，厘定了基底的岩性界面，刻画了基底面的起伏情况。
（3）根据CSAMT二维反演的断面图上的低阻异常，圈定了4个低阻异常区，其中1号异常范围最大，为本区含水有利区，亦是寻找地热水的直接依据，建议在K1线360 m处布设钻孔进行验证，孔深约800 m。
（4）验证了高密度和CSAMT电阻率法在坝北区域地热探测中的有效性，为类似地区地热勘查提供了一定的借鉴。
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图 1 中国东北大地构造简图（a，据陈衍景等, 2012; Chen et al., 2016修改）及黄岗—甘珠尔庙地区地质简图（b，据芮宗瑶等, 1994修改）
Figure 1. Simplified tectonic map of Northeast China (a, modified after Chen et al., 2012, 2016);Sketch geological map of the Huanggang–Ganzhuermiao area (b, modified after Rui et al., 1994)
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图 2 长岭子研究区地质简图（据内蒙古山金地质矿产勘查有限公司❶修改）
Figure 2. Geological map of the Changlingzi area (after Inner Mongolia Shandong Gold Geological and Mineral Exploration Co. Ltd.❶)
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图 3 长岭子斜长花岗斑岩岩相学特征
a—斜长花岗斑岩手标本照片；b—斜长花岗斑岩中斜长石斑晶发生绢云母化，可见聚片双晶，基质主要为长英质（正交偏光）；c—斜长花岗斑岩中正长石斑晶，可见典型的卡式双晶（正交偏光）；d—斜长花岗斑岩中正长石斑晶（单偏光）；e—斜长花岗斑岩中角闪石斑晶，角闪石被绿帘石交代（正交偏光）；f—斜长花岗斑岩中黑云母斑晶（单偏光）；Q—石英；Pl—斜长石；Or—正长石；Hb—角闪石；Bi—黑云母
Figure 3. Petrographic characteristics of the plagiogranite porphyry in Changlingzi area
a-Hand specimen photo of the plagiogranite porphyry; b-The feldspar phenocrysts with sericitizationin in plagiogranite porphyry, polysynthetic twin observed in feldspar and the matrix being predominantly felsic (crossed nicols); c-The orthoclase phenocrysts in the plagiogranite porphyry with carlsbad twin observed in orthoclase (crossed nicols); d-The orthoclase phenocrysts in the plagiogranite porphyry (plainlight); e-The hornblende phenocrysts in the plagiogranite porphyry, the hornblende replaced by epidote (crossed nicols); f-The biotite phenocryst in the plagiogranite porphyry (plainlight); Q-Quartz; Pl-Plagioclase; Or-Orthocalse; Hb-Hornblende; Bi-Biotite
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图 4 长岭子斜长花岗斑岩SiO2-(Na2O + K2O)图解（a，据Le Maitre, 2002）、A/CNK-A/NK图解（b，据Maniar and Piccoli, 1989）和SiO2-K2O图解（c，据Rickwood, 1989）
Figure 4. SiO2-(Na2O + K2O) (a, after Le Maitre, 2002), ACNKANK (b, after Maniar and Piccoli, 1989) and SiO2-K2O (c, after Rickwood, 1989) diagrams for plagiogranite porphyries in Changlingzi area
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图 5 长岭子研究区斜长花岗斑岩球粒陨石标准化稀土元素配分曲线（a）和原始地幔标准化微量元素蛛网图（b）（球粒陨石标准化值和原始地幔标准化值据Sun and McDonough, 1989）
Figure 5. Chondrite-normalized REE patterns (a) and primitive mantle normalized trace element spider diagrams (b) for plagiogranite porphyries in Changlingzi area (chondrite normalization values and primitive mantle normalization values after Sun and McDonough, 1989)
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图 6 长岭子研究区斜长花岗斑岩锆石CL图像（a）和LA-ICP-MS锆石U-Pb年龄谐和图（b, c）
Figure 6. Cathodoluminescent images (a) and LA-ICP-MS zircon U-Pb concordia diagrams (b, c) for plagiogranite porphyry in Changlingzi area
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图 7 长岭子斜长花岗斑岩K2O-Na2O图解（据Collins et al., 1982）
Figure 7. K2O-Na2O diagram for plagiogranite porphyry in Changlingzi area (after Collins et al., 1982)
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图 8 长岭子斜长花岗斑岩锆石εHf(t)-t图解
（阴影部分代表兴蒙造山带东段中生代花岗岩和辉长岩，虚线框部分代表燕山地区岩浆岩；数据来源：兴蒙造山带东段和燕山地区岩浆岩锆石εHf(t)范围据Yang et al., 2006；中生代火山岩据张超等（2014）和谭皓元等（2017）；林西组据朱俊宾等（2017）；大石寨组据张健（2012）和作者未发表数据；宝音图群据孙立新等（2013）；白垩纪花岗岩据杨奇荻等（2014）、周振华等（2011）和Zhou ZH et al., 2012；侏罗纪花岗岩据杨奇荻等（2014）、刘伟等（2007）和Liu et al., 2009；二叠纪花岗岩据Wang et al., 2017）
Figure 8. Zircon εHf(t)-t diagram for plagiogranite porphyry in Changlingzi area
(The shaded part represents the Mesozoic granites and gabbros in the eastern segment of the Xingmeng orogenic belt, and the dotted section \ represents the magmatic rocks in the Yanshan area)Data sources: Xing'an-Mongolian Orogenic belt and Yanshan area zircon εHf(t) range after Yang et al., 2006; Mesozoic volcanic rocks after Zhang et al., 2014 and Tan et al., 2017; the Linxi Formation after Zhu et al., 2017; the Dashizhai Formation after Zhang, 2012 and the authors'unpublished data; the Baoyintu Group after Sun et al., 2013; Cretaceous granite after Yang et al., 2014 and Zhou et al., 2011, 2012; Jurassic granite after Yang et al., 2012 and Liu et al., 2007, 2009; Permian granite after Wang et al., 2017)
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图 9 长岭子斜长花岗斑岩Sr/Y-Y图解（a, 据Martin, 1999）和（La/Yb）N-YbN图解（b, 据Defant et al., 1990）
Figure 9. Sr/Y-Y (a, after Martin, 1999) and (La/Yb)N-YbN (b, after Defant et al., 1990) diagrams of the plagiogranite porphyry in Changlingzi area
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图 10 长岭子斜长花岗斑岩SiO2-Mg#（a）图解和SiO2-MgO图解（b）（据Wang et al., 2006）
Figure 10. SiO2-Mg# (a) diagram and SiO2-MgO diagram (b) for the plagiogranite porphyry in Changlingzi area (after Wang et al., 2006)
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图 11 长岭子斜长花岗斑岩Nb−Y（a）, Ta−Yb（b）, Rb−(Y+Nb)（c）和Rb−(Yb+Ta)（d）图解（据Pearce et al., 1984, 1996；）
数据来源：三叠纪花岗岩类据李锦轶等, 2007；石玉若等, 2007；张维等, 2010; 叶栩松等, 2011;张万益等, 2012;刘建峰等, 2014; 吴荣泽等, 2015;张海华等, 2015;李晓海等, 2016
Figure 11. Nb−Y (a), Ta−Yb (b), Rb−(Y+Nb) (c) and Rb−(Yb+Ta) (d) diagram (after Pearce et al., 1984, 1996) of plagiogranite porphyries in Changlingzi area
Data sources: Triassic granitoids after Li et al., 2007; Shi et al., 2007; Zhang et al., 2010; Ye et al., 2011; Zhang et al., 2012; Liu et al., 2014; Wu et al., 2015; Zhang et al., 2015 and Li et al., 2016
表 1 长岭子斜长花岗斑岩全岩主量元素（%）和微量元素（10−6）分析结果
Table 1 Major (%) and trace(10−6) elements compositions of the plagiogranite porphyries in Changlingzi area
下载: 导出CSV
表 2 长岭子斜长花岗斑岩锆石LA−ICP−MS U−Pb定年分析结果
Table 2 LA−ICP−MS Zircon U−Pb analysis for the plagiogranite porphyry in Changlingzi area
下载: 导出CSV
表 3 长岭子研究区斜长花岗斑岩锆石Lu−Hf同位素分析结果
Table 3 Zircon Lu−Hf isotope analysis for the plagiogranite porphyry in Changlingzi area
下载: 导出CSV
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