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云南建水煌斑岩年代学和地球化学及其构造意义

刘娇, 周洋, 谢德根, 纪星星, 李德威

刘娇, 周洋, 谢德根, 纪星星, 李德威. 云南建水煌斑岩年代学和地球化学及其构造意义[J]. 中国地质, 2016, 43(6): 1977-1991. DOI: 10.12029/gc20160609
引用本文: 刘娇, 周洋, 谢德根, 纪星星, 李德威. 云南建水煌斑岩年代学和地球化学及其构造意义[J]. 中国地质, 2016, 43(6): 1977-1991. DOI: 10.12029/gc20160609
LIU Jiao, ZHOU Yang, XIE De-gen, JI Xing-xing, LI De-wei. Geochronology, geochemistry and geological implications of the lamprophyre in Jianshui, east Yunnan Province[J]. GEOLOGY IN CHINA, 2016, 43(6): 1977-1991. DOI: 10.12029/gc20160609
Citation: LIU Jiao, ZHOU Yang, XIE De-gen, JI Xing-xing, LI De-wei. Geochronology, geochemistry and geological implications of the lamprophyre in Jianshui, east Yunnan Province[J]. GEOLOGY IN CHINA, 2016, 43(6): 1977-1991. DOI: 10.12029/gc20160609

云南建水煌斑岩年代学和地球化学及其构造意义

基金项目: 

中国地质调查局“云南1:5万龙朋等六幅区域地质调查” 1212011220400

详细信息
    作者简介:

    刘娇, 女, 1990年生, 硕士, 构造地质学专业; E-mail:740327245@qq.com

    通讯作者:

    李德威, 男, 1962年生, 教授, 博士生导师, 构造地质学专业; E-mail:dewei89@sina.com

  • 中图分类号: P588.13

Geochronology, geochemistry and geological implications of the lamprophyre in Jianshui, east Yunnan Province

Funds: 

Supported by programs from China Geological Survey: 1:50000 Regional Geological Survey of Longpeng in Yunnan 1212011220400

More Information
    Author Bio:

    LIU Jiao, female, born in 1990, master, majors in structural geology; E-mail:740327245@qq.com

    Corresponding author:

    LI De-wei, male, born in 1962, Professor, majors in structural geology; E-mail:dewei89@sina.com

  • 摘要:

    华南大陆内部燕山期的岩浆事件可分为2期:燕山早期180~150 Ma,燕山晚期140~80 Ma。而处于扬子板块西南缘的滇黔贵等地,仅见有第二期晚白垩世中酸性侵入岩与相关成矿作用,缺乏第一期岩浆活动的时间记录。本文在滇东建水地区首次发现了麦地村煌斑岩,对其进行高精度LA-ICP-MS锆石U-Pb定年和主微量元素测试分析。结果显示煌斑岩的锆石U-Pb年龄为(158.4±2.4)Ma(MSWD=4.2),为晚侏罗世的产物,补充了该区较为空白的第一期岩浆热事件。麦地村煌斑岩不相容元素明显高于原始地幔,表现出不同程度的富集,大离子亲石元素Rb、Ba、Ce等富集程度不明显,高场强元素中U、Ta、Pb等表现出一定程度富集,LREE相对富集,HREE相对亏损,不具有Nb-Ta-Ti负异常的俯冲型配分曲线特征,具有明显的OIB型洋岛玄武岩稀土元素配分特征,为板内伸展环境下的产物。滇东地区发育中生代时期的NNE构造,早期NNE向褶皱叠加有后期同方向正断层。早期褶皱表现为SEE-NWW挤压应力作用下的构造特征,后期断层表现出同方向张应力作用下的特征。煌斑岩正是由于该区发生挤压之后伴随着一期应力松弛调整,伸展减压作用诱发地幔物质部分融熔,来自于深处的软流圈地幔流体与岩石圈地幔发生交代作用,形成富集型地幔,交代富集的岩石圈地幔局部受热、部分熔融,发生上升侵位。煌斑岩的侵位时间即是滇东地区中生代从挤压向伸展转换的起始时间。

    Abstract:

    The magmatic event of Yanshanian period in South China has been divided into two stages:Early Yanshanian (180-150Ma) (J2-J3) and Late Yanshanian (140-80Ma) (K1-K2). However, there exist only the data concerning Cretaceous mineralization associated with acidic intrusive rocks, but the record of the early magmatic events on the southwest margin of the Yangtze Plate has not been seen. In this paper, the authors newly discovered Maidicun lamprophyre in Jianshui area of eastern Yunnan. The U-Pb age of the zircon is 158.4±2.4 Ma (MSWD=4.2), and hence it is obvious that the lamprophyre was formed in the Late Jurassic, corresponding to the first stage of the thermal event in southeast China. The values of incompatible elements are significantly higher than those of the primitive mantle of Maidicun lamprophyre, showing different degrees of enrichment. The LILE (Rb, Ba, Ce) enrichment is not obvious, HFSE (U, Ta, Pb) show some enrichment, and Nb, Ti, Zr, Hf don't show significant enrichment and losses. LREE/HREE ratios are in the range of 5.65-6.07, averagely 5.89, (La/Yb)N ratios are in the range of 7-12, indicating LREE enrichment and HREF relative losses. It has no negative anomalies of Nb-Ta-Ti and shows REE characteristics of OIB-type oceanic island basalts, and the Maidicun lamprophyre was formed under the condition of intraplate extension. NNE-trending structures were developed in the study area during the Mesozoic, and the early NNE-trending folds were superposed by late normal faults in the same direction. The fold axial surface is mainly SE-trending and partly NW-trending, indicating tectonic characteristics in response to SEE-NWW trending extrusion stress. Faults are mostly high-angle normal faults in the NW-SE direction, showing that they were influenced by EW-trending tensile stress. The lamprophyre's intrusion was mainly controlled by the action of deep asthenosphere mantle, from which the fluid experienced metasomatism with lithosphere mantle in response to partial diapering of asthenosphere and the stretch of lithosphere in eastern Yunnan in the Late Jurassic period, followed by the formation of the enriched mantle. And this kind of enriched mantle was partially heated, melted and migrated upward for emplacement finally. The intrusion age of the lamprophyre (Late Jurassic 158 Ma) is the starting time of extension in the study area.

  • 华南地区位于特提斯构造域与太平洋构造域的交汇部位,在中生代经历了挤压与伸展等多期次的构造应力体制转换,长期受到地学界的广泛关注和研究,并取得了较大的进展。不同的学者分别从构造变形[1-4],岩浆及成矿事件[5-11]等方面对华南地区的多期次构造运动进行过详细的剖析。总体来说,在构造变形上,华南大陆内部存在宽约1300 km的NNE向褶皱逆冲推覆系统,表现出NWW-SEE向挤压的应力体制;但在华南的岩浆系统、盆岭构造及变质穹隆等现象上却表现出了NWW-SEE向伸展构造的应力体制[4, 12]。研究区位于华南大陆西南缘,区内NNE褶皱被后期同方向正断层叠加改造现象显著,与华南大陆整体的构造变形具有相似性。这种区域上从挤压向伸展转换的起始时间在不同地区争议较大。在岩浆活动上,前人对华南各个时期的构造岩浆事件的解释存在较多观点:太平洋板块的俯冲及挤压后伸展[13],印支期陆陆碰撞后造山伸展[14],超级地幔柱[15-16],软流圈上涌[17-18]等。虽然对于这些事件的形成机理众说纷纭,但是在岩浆活动期次上,较一致地认为华南在燕山期存在两期大规模的构造岩浆成矿事件:燕山早期180~150 Ma,燕山晚期140~80 Ma[19-20]。对处于扬子板块西南缘的滇黔桂等地,研究程度较高的仅是第二期晚白垩世区域伸展构造及中酸性侵入岩[21-22],缺乏第一期岩浆事件的时间记录[23]。本文在滇东建水地区新发现的麦地村煌斑岩的年龄刚好补充了该区较为空白的第一期岩浆事件。因此对新发现的煌斑岩脉进行详细的年代学和地球化学分析,结合区域地质资料,探讨该区煌斑岩形成时代、形成环境及岩浆成因,进一步探讨其构造意义显得尤为重要。

    研究区位于云南省东南部建水县,大地构造位置处于扬子板块西南缘,西临红河断裂,东南为加里东褶皱带,其中NW向建水-石屏断裂和NNE向师宗-弥勒断裂的南端经过该区,并在该区交汇(图 1-a)。研究区地层出露较多,从中元古代昆阳群的变形基底至上新世茨营组的沉积盖层几乎均有出露(图 1-c)。在岩浆活动上,研究区主要发育石炭纪和二叠纪火山岩及麦地村煌斑岩等次火山岩(图 1-b),各期岩浆岩的形成时间不一致,并受不同的构造环境控制,有着各自不同岩石组合、地化特征及岩石成因。

    图  1  云南建水岩浆岩分布图及构造背景图
    1-石炭纪火山岩;2-二叠纪火山岩;3-三叠纪火山岩;4-侏罗纪基性岩体;5-侏罗纪中酸性岩体;6-白垩纪中酸性岩体;7-麦地村煌斑岩;8-断层倾向玫瑰花图;9-南华系;10-泥盆-二叠系;11-石炭-二叠系;12-石炭-二叠系玄武岩;13-三叠-侏罗系;14-新近系-第四系;15-正断层;16-逆断层;17-角度不整合;18-向斜;19-背斜;20-剖面
    Figure  1.  The distribution of magmatic rocks and tectonic map of background in Jianshui, Yunnan Province
    1-Carboniferous volcanic rocks; 2-Permian volcanic rocks; 3-Triassic volcanic rocks; 4-Jurassic basic rock mass; 5-Jurassic intermediate-acid rock; 6-Cretaceous intermediate-acid rock; 7-Maidicun lamprophyre; 8-Rose diagram of fault dip; 9-Nanhuan; 10-Devonian-Permian; 11-Carboniferous-Permian; 12-Carboniferous-Permian basalt; 13-Triassic-Jurassic; 14-Neogene-Quaternary; 15-Normal fault; 16-Reverse fault; 17-Divergent unconformity; 18-Synclinal fold; 19-Anticlinal fold; 20-Section

    通过野外地质调查,研究区发育多组NNE、NWW和EW向构造,野外明显可见NWW向和EW向断层截切NNE向构造的现象(图 1-c)。其中NWW向和EW向断层多为右行平移性质,部分具有正断层性质,认为是喜山期的产物。NNE向构造可分为两期,先期为褶皱,后期为高角度的正断层,代表了挤压和伸展2期构造应力的叠加。

    研究区内发育不同尺度的NNE向褶皱,褶皱总体走向为NNE向(19°~41°),大部分褶皱轴面倾向SEE(107°~131°),少数褶皱轴面倾向NWW(288°~309°),表现为SEE-NWW挤压应力下的构造特征。参与褶皱变形的地层主要为泥盆系-中三叠统(D-T2)地层(图 2-a)。在他广村地区可见上三叠统-下侏罗统(T3s-JL1)地层(图 2-b)随褶皱发生了变形及倒转。纵观区域上参与褶皱变形的最年轻地层为下侏罗统禄丰群一段砂泥岩(JL1),因此该褶皱作用的发生时间必然晚于早侏罗世,为中新生代的产物。

    图  2  云南建水县曲溪蚂蚁新寨-利民乡实测构造地层剖面PM1(a),云南石屏县白石岩-他广村实测构造地层剖面PM2(b)
    1-灰岩;2-白云岩;3-泥岩;4-粉砂岩;5-粉砂质泥岩;6-石英砂岩;7-泥盆系;8-石炭系;9-二叠系;10-三叠系;11-上三叠统舍资组二段;12-侏罗系禄丰群一段
    Figure  2.  The measured structural stratigraphic section from Mayixinzai to Liminxing, Yunnan Province (PM1); the measured structural
    stratigraphic section from Baishiyan to Tagguangcun, Yunnan Province (PM2) 1-Limestone; 2-Dolomite; 3-Mudstone; 4-Siltstone; 5-Silty mudstone; 6-Quartz sandstone; 7-Devonian; 8-Carboniferous; 9-Permian; 10-Triassic; 11-Dhezi strata; 12-Lufeng strata

    研究区发育多组NNE(22°~35°)向断层,断层倾向SEE(112°~127°)和NWW(280°~305°)两个方向,倾角较陡(65°~83°),为NNE高角度正断层(图 1-c),在灰岩的断层面上大多可见有近于直立的擦痕线理。这些断层叠加于先期NNE向褶皱变形之上,几乎在研究区侏罗纪之前的所有地层中均有记录。多组次级断层组合成小的地堑和阶梯式正断层表现出明显的SEE-NWW向张应力作用下伸展构造的特征。

    煌斑岩在野外呈脉状产出,总体呈NE向展布,走向为46°~51°,可见有NEE向的枝脉沿着早期断层裂隙产出,脉宽约1~4 m,长为100~800 m。新鲜煌斑岩颜色为灰绿色、灰黄色,岩石中气孔、杏仁构造较为发育,杏仁体为无色透明的方解石颗粒。围岩为中泥盆统曲靖组二段(D2q2)生物碎屑灰岩。煌斑岩与围岩接触界线清晰可见,接触处可见有灰岩发生一定程度的烘烤变形(图 3),与围岩呈明显的侵入接触关系。

    图  3  与围岩接触处烘烤变形(镜头方向290°)
    D2q2-中泥盆统曲靖组二段
    Figure  3.  Deformation of baking of the contact with surrounding rocks (lens direction 290°)
    D2q2-Middle Devonian two stages of Qujing Formation

    镜下斑状结构明显,可见有圆球形的气孔状构造,气孔中充填物为方解石。作为斑晶的暗色矿物虽然发生了明显的碳酸盐化和绿泥石化,但其晶型仍然完整可见,为全自形-自形结构。其中斑晶含量为15%~20%,大小为0.3~1.2 mm,斑晶多为角闪石(5%)和辉石(15%)。角闪石斑晶可见呈菱形的六边形,部分角闪石为长柱状或是长板状;辉石斑晶其横切面为近正方形的八边形,多数为短柱状,少数辉石斑晶虽然发生了绿泥石化,但仍残留原有的环带结构(图 4)。基质中以斜长石、碱性长石、方解石、针状磷灰石等浅色矿物为主。

    图  4  辉石斑晶中残留的环带结构(正交光)
    Cc-方解石Ab-钠长石Aug-普通辉石
    Figure  4.  Residual girdle structure of pyroxene phenocryst (crossed nicols)
    Cc-Calcite Ab-Albite Aug-Augite

    本文选取采自于麦地村煌斑岩一条主脉体的新鲜样品进行锆石U-Pb定年。地理位置为102°47′ 38″E,23°32′58″N。锆石单矿物分离由河北省区域地质调查研究所承担。锆石制靶和阴极发光等图像采集在武汉上谱分析科技有限责任公司完成。选择环带和晶形较好的锆石,且在无包体、无裂缝的部位圈定做微区原位分析。LA-ICP-MS锆石U -Pb定年在中国冶金地质总局山东局测试中心完成,定年设备为Thermo X2等离子质谱仪,激光剥蚀系统使用GeoLas pro 193nm激光器。激光剥蚀采用的斑束直径为30 μm,频率为10 Hz,每个分析点的气体背景采集时间为20 s,信号采集时间为40 s。详细试验过程参见[24]

    在CL图像中锆石可分为2类(图 5):一类锆石形态不完整,阴极发光强度较大;另一类锆石形态完整,多为自形结构,主要为短柱状和长柱状。锆石的长宽比为1~3,粒径大小为60~250 μm。锆石内部振荡环带清晰可见,环带间距较窄,部分锆石具有清晰的扇形分带结构。该煌斑岩的锆石中Th值介于68×10-6~484.5×10-6,平均含量为297.22×10-6,U值介于207.1×10-6~951.5×10-6,平均为595.05×10-6,Th/U比值介于0.14~0.71,平均为0.5,仅有两颗锆石Th/U比值小于0.4,说明这些锆石主要为岩浆锆石[25]表 1)。

    图  5  麦地村煌斑岩部分锆石阴极发光图
    Figure  5.  Cathodoluminescence image of the zircons
    表  1  建水地区麦地村煌斑岩锆石LA-ICP-MS U-Pb测年分析结果表
    Table  1.  LA-ICP-MS U-Pb zircon dating results of Maidicun lamprophyre from Jianshui area
    下载: 导出CSV 
    | 显示表格

    在24个测点数据中,其中有4颗锆石测点其206Pb/238U加权平均年龄为(254±4.3) Ma(MSWD=1.19,协和度大于90%);其他20颗锆石测点其206Pb/ 238U加权平均年龄为(158.4±2.4) Ma(MSWD=4.2,协和度大于90%)(图 6)。前者年龄锆石主要为第一类岩浆锆石,多不完整,代表早期的岩浆活动,通过对比发现该锆石年龄与峨眉山火成岩喷发的热事件年龄一致[26]。后者年龄锆石对应第二类锆石,晶型完整,且时代最年轻,其年龄应代表煌斑岩的形成时代,可见该麦地村煌斑岩形成于晚侏罗世。

    图  6  煌斑岩锆石的谐和年龄
    Figure  6.  Zircon concordia age for the lamprophyre

    本次用于全岩分析的8件样品,分别采自于野外的三条煌斑岩脉体,选取较为新鲜的,杏仁体不发育的岩石样品,进行切样、送样。样品的主量、微量、稀土元素化学分析在武汉岩矿综合测试中心完成。主量元素测定方法为X-射线荧光熔片法(XRF),微量和稀土元素分析仪器均为电感耦合等离子体质谱仪(ICP-MS)。用于对比分析的焦溪岭煌斑岩,其Rb-Sr年龄为136 Ma,地化数据取自贾大成等[27]

    从8件岩石样品的地化数据可见各岩石样品的主量元素值变化较大(表 2),岩石中SiO2含量为39.84%~48.14%,平均为43.26%,为超基性-基性岩类;TiO2含量为1.50%~1.71%,表现出弱的高钛特征(TiO2>1.46%,Ti/Y>350),这与镜下所见煌斑岩中含有的钛铁矿、磁铁矿等相吻合。通过数据相关性分析发现CO2和CaO的含量较高,且两者呈明显的正相关关系(相关系数为0.965),这与手标本及镜下所见的含方解石细脉和碳酸盐蚀变等是一致的。该煌斑岩碱质含量与烧失量呈明显的负相关关系(图 7),可见随着岩石矿物发生蚀变,钾钠含量发生一定量的流失。因此在岩石分类上,本文选择使用岩石蚀变不活泼元素(Ti、Zr、Y、Nb)来进行分类判别,在Zr/TiO2-Nb/Y判别图解中(图 8),麦地村煌斑岩主体落入碱性玄武岩范围内,唯有一件样品(80-6-3)可能由于岩石蚀变程度不同而落入亚碱性玄武岩范围内。

    表  2  建水县麦地村煌斑岩主量元素(%)、微量(10-6)元素测试结果
    Table  2.  Major (%) and trace element (10-6) analytical results for Maidicun lamprophyre from Jianshui area
    下载: 导出CSV 
    | 显示表格
    图  7  Na2O+K2O-LOI图解
    Figure  7.  Na2O+K2O-LOI diagrams
    图  8  岩石Nb/Y-Zr/TiO2分类图解[28]
    Figure  8.  Zr/Ti-Nb/Y diagrams[28]

    由于岩石蚀变过程中存在碱质的带入和带出,而Na、K、Ca、Mg等作为活泼元素也较易受到蚀变作用的影响,因此本文着重讨论受蚀变作用影响较小的微量元素及稀土元素。

    在原始地幔标准化蛛网图中(图 9-b),麦地村煌斑岩的不相容元素明显高于原始地幔,表现出不同程度的富集,大离子亲石元素Rb、Ba、Ce等富集程度并不明显,高场强元素U、Ta、Pb等表现出一定程度富集,Nb、Ti、Zr、Hf等未见有明显的富集和亏损,HREE相对亏损,麦地村煌斑岩与焦溪岭煌斑岩类似,同具有与洋岛玄武岩(OIB)相似的微量元素特征。

    图  9  球粒陨石标准化稀土配分图[29]及原始地幔标准化微量元素蛛网图[30]
    JXL-焦溪岭煌斑岩; MDC-麦地村煌斑岩; OIB-洋岛玄武岩; N-type MORB-正常洋脊玄武岩
    Figure  9.  Chondrite-normalized REE patterns[29] and primitive mantle-normalized trace element spider diagrams[30]
    JXL-Jiaoxiling lamprophyre; MDC-Maidicun lamprophyre; OIB-Ocean Island Basalts; N-type MORB-Normal type mid-oceanic ridges basalts

    麦地村煌斑岩稀土元素总量较低,介于93×10-6~105×10-6,略低于OIB型洋岛玄武岩,明显高于洋中脊和原始地幔含量,其中LREE含量为79×10-6~127×10-6,HREE含量为13×10-6~22×10-6,LREE/ HREE为5.65~6.07,平均为5.89,(La/Yb)N介于7~12,轻稀土元素相对富集,重稀土元素相对亏损,明显存在轻重稀土元素分馏。(La/Sm)N为2.5~3.8,(Gd/Yb)N介于2.0~2.7,表明轻重稀土元素内部分馏程度不大。δEu为0.77~0.99,所有样品均具有轻微的负Eu异常,暗示在岩浆演化过程中存在不明显的斜长石的分离结晶作用。δCe介于0.53~0.93,表现出微小的负Ce异常,暗示在成岩过程之后发生过不均等的岩石蚀变作用。在球粒陨石标准化配分曲线中,所有样品的稀土配分曲线整体形态基本一致(图 9-a),都表现为LREE富集,HREE相对亏损的右倾型特征,与OIB型洋岛玄武岩稀土配分特征最为相似。

    本文使用高精度LA-ICP-MS对麦地村煌斑岩进行锆石U-Pb定年,获得该煌斑岩的形成年龄为(158.4±2.4) Ma。从背景区域上来看,虽然在滇东整个区域上并未见有该时代煌斑岩详细的年龄记录,但在相关地质调查报告中可见该区有煌斑岩和碱性岩类侵位于泥盆、石炭和三叠纪地层中的证据,且在后期白垩纪侵位的岩石中发现有该期岩石的俘虏体❶❷,这些地质事实间接限定了该区煌斑岩形成于三叠纪之后,白垩纪之前。通过本文所得煌斑岩的测年数据,结合前人[31-35]对于区域上蚀变矿物、岩浆矿物和变质矿物的测年结果,证实在华南川滇黔等地确实存在燕山期早期(150~180 Ma)的构造热事件,本文探讨的麦地村煌斑岩则为该时期构造热事件的产物。

    ❶段向东.云南省落水洞幅F48E001002地质图说明书:1:5万[R].云南地质矿产勘查开发局区域地质矿产调查大队. 1999.

    ❷胡荣民.云南省官厅幅G48E004003地质图说明书:1:5万[R].云南省地质矿产勘查开发局区域地质调查所.1996.

    煌斑岩作为一种独立的基性岩类,以其具有特殊的煌斑结构命名,含角闪石、云母等含水矿物,富含碱质和挥发分。对煌斑岩主流的成因模式可分为3种:(1)交代富集地幔的部分熔融(交代物质可能来自于下部软流圈的流体或是俯冲洋壳脱水形成的流体)[36];(2)基性岩浆的分离结晶或是陆壳混染[37];(3)地幔物质的小比例部分熔融[38]

    本文研究的麦地村煌斑岩具有相对较高的烧失量(8.02%~12.45%),煌斑岩中CO2与CaO之间存在明显的正相关,而碱质与烧失量之间具有显著的负相关性,其他氧化物与LOI之间相关性显著,弱的负Ce异常及岩相学特征等均表明该煌斑岩形成后经历过低温蚀变作用的影响。研究表明Nb、Ta和Zr、Hf这2对元素由于具有相近的地球化学性质,其比值很难随着分离结晶和部分熔融等岩浆过程改变。麦地村煌斑岩Nb/Ta比值为7~14,平均为11.3,Zr/Hf比值为37~39,平均为37.74,原始地幔(Nb/ Ta=17.5;Zr/Hf=36.3),大陆地壳值(Nb/Ta≈12~13;Zr/Hf≈11)[32],可见麦地村煌斑岩Nb/Ta接近于大陆地壳,可能是由于少量地壳物质混染造成Nb的亏损[39-40],Zr/Hf略大于原始地幔,通常认为偏高的Zr/ Hf同源区小体积的碳酸盐流体交代富集过程有关[41]。以上特征均表明煌斑岩在上升侵位过程中发生了部分程度的地壳混染。

    在判断岩石分离结晶和部分熔融的趋势图解中(图 10),各个样品La/Sm,La/Yb与La之间存在明显的相关性,清楚地表现出煌斑岩为部分熔融条件下的产物。但镜下可见煌斑岩中存在明显的斑晶,地球化学特征显示煌斑岩Mg#(0.42~0.48)、Ni(135× 10-6~183×10-6)、Cr(259×10-6~315×10-6)相对于原始地幔岩浆(Mg#0.7~0.83、Ni>400×10-6~500×10-6、Cr>500×10-6[42]含量较低,表明在原始地幔出熔之后经历过小程度的橄榄石或是单斜辉石的分异结晶作用。微小的负Eu异常也表现出不明显的斜长石分异结晶。因此认为该煌斑岩在形成过程中,存在橄榄石、单斜辉石和斜长石等的分异结晶作用,同时也存在源区岩浆的部分熔融。

    图  10  麦地村煌斑岩La-La/Sm与La-La/Yb图解
    Figure  10.  La-La/Sm diagram and La-La/Yb diagram

    由以上分析可见麦地村煌斑岩的形成过程:在其源区发生过低程度的部分熔融,经历了橄榄石、单斜辉石和斜长石等的分离结晶作用,在岩浆上升侵位过程中受到少量地壳物质的混染,并在地表发生过一定程度的热液蚀变作用。

    原始地幔的富集主要存在2种形式:(1)俯冲流体的交代富集;(2)深部软流圈流体的交代富集。俯冲流体交代富集的岩石圈地幔的明显特征是富集大离子亲石元素和轻稀土元素而强烈亏损高场强元素,具有显著的Ta-Nb-Ti负异常[43]。本文煌斑岩弱富集大离子亲石元素和亲稀土元素,高场强元素异常不明显,Ta、Ti均无亏损,并未表现出弧环境下俯冲流体交代富集的特征。

    由于强不相容元素(Th、U、Nb、Ta、La、Zr)具有相似的全岩配分系数,在部分熔融和分异结晶中一般不会造成这些元素的强烈分异,因此可以直接应用这些元素的比值来描述源区特征[40, 44]。通过对比,麦地村煌斑岩的Zr/Nb为5.68,La/Nb为1.06,Th/Nb为0.14,Th/La为0.14,Th/U为2.79,其比值均与Sun[30]统计的OIB型玄武岩的值较为接近(Zr/ Nb=5.8,La/Nb=0.77,Th/Nb=0.08,Th/La=0.11,Th/ U=3.92)。在La/Nb-Zr/Nb地幔源区判别图解中麦地村煌斑岩和焦溪岭煌斑岩同落入OIB型洋岛玄武岩内(图 11-a),在Th/La-Th/Nb判别图解中麦地村煌斑岩落入原始地幔区(图 11-b),说明该岩石样品同时具有OIB型洋岛玄武岩和原始地幔的源区特征。通过前人利用Zr/Y和Ti/Y比值划分的低钛和高钛玄武岩的判别方法,麦地村煌斑岩Zr/Y比值为5.7~7.0,Ti/Y比值为480~561,表现出一定的高钛玄武岩特征,为OIB型软流圈地幔特征[45]。该讨论结果与贾大成对蕉溪岭煌斑岩所做的同位素物源示踪结果一致。

    图  11  Zr/Nb-La/Nb图解、Th/Nb-Th/La图解[46]
    Figure  11.  Zr/Nb-La/Nb diagram, Th/Nb-Th/La diagram[46]

    在多个构造环境判别图解中(图 12),麦地村煌斑岩较为一致地落入板内碱性玄武岩范围内,焦溪岭煌斑岩也主要落入板内环境范围内。一般认为,碱性岩和煌斑岩均形成于岩石圈伸展构造背景中。通过上述对麦地村煌斑岩的微量元素的比较发现该煌斑岩同时具有OIB型洋岛玄武岩特征。因此认为麦地村煌斑岩为板内伸展条件下的产物,其形成同洋岛玄武岩的热点模式具有一定的相似性。

    图  12  构造环境判别图解[47-48]
    Figure  12.  Tectonic environment discrimination diagram[47-48]

    滇东地区位于扬子板块西南缘,其濒临于特提斯构造域,距离太平洋构造域较远,但从其地层、构造和岩浆活动等特征来看,其具有与华南内陆几乎相同的特征:在地层上滇东地区记录了扬子地台和华南加里东褶皱带西南缘的沉积演化;在构造上滇东地区同样记录了华南内部中生代时期特有的NNE向挤压-伸展的构造变形;在岩浆活动上,滇东南地区发育华南内部普遍存在的晚中生代的中酸性岩体。

    印支期古特提斯洋陆转换之后,华南地区进入到一个相对稳定的陆内环境。经历了205~180 Ma的构造岩浆宁静期之后,华南大陆开始发生多期次的构造变形[19, 49-50]及岩浆活动[51],形成出露面积达到240000 km2的花岗岩、基性岩体及火山岩等。华南中生代基性岩种类繁多,包括呈侵入状态产出的辉绿岩、辉长辉绿岩、辉长岩、煌斑岩等,还包括呈喷发状态产出的玄武质安山岩-玄武岩及与中酸性岩呈双峰式产出的的基性火山岩等[50, 52]。酸性岩更是以多种类型的花岗岩、正长岩、碱长岩、流纹岩、安山岩等为特征[53-54]。其形成时间跨度较大,从180~80 Ma均可见,形成地域范围较广,从华南内陆至东南沿海均有分布。大部分学者将136 Ma作为华南构造岩浆活动的转折期[55-56],认为136 Ma为华南大规模伸展构造的起始时间,但仍然不可否认,在此之前的中晚侏罗世华南大陆经历过一期挤压后伸展的构造运动[6-7, 19, 57-58]

    在华南内部广泛存在NNE向褶皱逆冲系,根据该褶皱冲断带区域沉积间断、被卷入的地层、与上覆地层角度不整合关系及后期岩体的侵位,将该期挤压变形发生时间限定于J2-J3(175~160 Ma)[2, 59-60]。华南地区广泛存在NNE向的断陷盆地和伸展穹窿,表现出NWW-SEE向张应力的作用特征[5, 33],根据构造与岩体的侵位和切割关系[58-59]限定该伸展变形的发生时间为早白垩世(K1)。

    麦地村煌斑岩所在背景区域上,明显可见NNE向断层叠加改造先期同方向褶皱现象,显示出挤压与伸展转换的应力特征。煌斑岩明显不具有Nb-Ta -Ti负异常的俯冲环境特征,显示出了典型的OIB型洋岛玄武岩的特征,为板内伸展背景下的产物。由此可见在中晚侏罗世(158 Ma),滇东地区发生挤压之后伴随着一期应力松弛调整,伸展减压诱发地幔物质部分融熔,来自于深处的软流圈地幔的流体与岩石圈地幔发生交代作用,形成富集型地幔,交代富集的岩石圈地幔局部受热、部分熔融,发生上升侵位。

    通过对滇东南建水地区发现的煌斑岩进行地球化学、锆石U-Pb年代学分析结合区域构造变形特征,得出以下认识:

    (1)麦地村煌斑岩在岩石分类上属于碱性玄武岩系列,其锆石U-Pb年龄为(158.4±2.4) Ma,为晚侏罗世初期的产物,对应于华南东部的第一期构造热事件。

    (2)麦地村煌斑岩在形成过程中发生过源区低程度的部分熔融,经历了橄榄石、单斜辉石和斜长石等的分离结晶作用,在岩浆上升侵位过程中受到少量地壳物质的混染,并在地表发生过一定程度的热液蚀变作用。

    (3)麦地村煌斑岩富集轻稀土元素,相对亏损重稀土元素,大离子亲石元素富集程度不明显,高场强元素U、Ta、Pb等表现出一定程度富集,不具有Nb-Ta-Ti负异常的配分曲线,具有与洋岛玄武岩OIB相似的稀土及微量元素配分特征。地球化学特征表明该煌斑岩为伸展环境下板内碱性玄武岩。

    (4)研究区发育中生代时期的NNE构造,早期NNE向褶皱叠加有后期同方向正断层。早期褶皱轴面主体倾向SEE,表现为SEE-NWW挤压应力作用下的构造特征。后期断层倾向NWW、SEE两个方向,多为高角度正断层,表现出SEE-NWW向张应力作用下的特征。煌斑岩正是由于该区发生挤压之后伴随着一期应力松弛调整,伸展减压,伸展减压诱发地幔物质部分融熔,来自于深处的软流圈地幔的流体与岩石圈地幔发生交代作用,形成富集型地幔,交代富集的岩石圈地幔局部受热、部分熔融,发生上升侵位。煌斑岩的侵位时间即是滇东地区从挤压向伸展转换的起始时间。

    致谢: 本稿在成文过程中,中国地质大学(武汉)廖群安老师、续海金老师给予了指导性的建议,笔者在此表示衷心的感谢,感谢参与评审本稿的专家学者。
  • 图  1   云南建水岩浆岩分布图及构造背景图

    1-石炭纪火山岩;2-二叠纪火山岩;3-三叠纪火山岩;4-侏罗纪基性岩体;5-侏罗纪中酸性岩体;6-白垩纪中酸性岩体;7-麦地村煌斑岩;8-断层倾向玫瑰花图;9-南华系;10-泥盆-二叠系;11-石炭-二叠系;12-石炭-二叠系玄武岩;13-三叠-侏罗系;14-新近系-第四系;15-正断层;16-逆断层;17-角度不整合;18-向斜;19-背斜;20-剖面

    Figure  1.   The distribution of magmatic rocks and tectonic map of background in Jianshui, Yunnan Province

    1-Carboniferous volcanic rocks; 2-Permian volcanic rocks; 3-Triassic volcanic rocks; 4-Jurassic basic rock mass; 5-Jurassic intermediate-acid rock; 6-Cretaceous intermediate-acid rock; 7-Maidicun lamprophyre; 8-Rose diagram of fault dip; 9-Nanhuan; 10-Devonian-Permian; 11-Carboniferous-Permian; 12-Carboniferous-Permian basalt; 13-Triassic-Jurassic; 14-Neogene-Quaternary; 15-Normal fault; 16-Reverse fault; 17-Divergent unconformity; 18-Synclinal fold; 19-Anticlinal fold; 20-Section

    图  2   云南建水县曲溪蚂蚁新寨-利民乡实测构造地层剖面PM1(a),云南石屏县白石岩-他广村实测构造地层剖面PM2(b)

    1-灰岩;2-白云岩;3-泥岩;4-粉砂岩;5-粉砂质泥岩;6-石英砂岩;7-泥盆系;8-石炭系;9-二叠系;10-三叠系;11-上三叠统舍资组二段;12-侏罗系禄丰群一段

    Figure  2.   The measured structural stratigraphic section from Mayixinzai to Liminxing, Yunnan Province (PM1); the measured structural

    stratigraphic section from Baishiyan to Tagguangcun, Yunnan Province (PM2) 1-Limestone; 2-Dolomite; 3-Mudstone; 4-Siltstone; 5-Silty mudstone; 6-Quartz sandstone; 7-Devonian; 8-Carboniferous; 9-Permian; 10-Triassic; 11-Dhezi strata; 12-Lufeng strata

    图  3   与围岩接触处烘烤变形(镜头方向290°)

    D2q2-中泥盆统曲靖组二段

    Figure  3.   Deformation of baking of the contact with surrounding rocks (lens direction 290°)

    D2q2-Middle Devonian two stages of Qujing Formation

    图  4   辉石斑晶中残留的环带结构(正交光)

    Cc-方解石Ab-钠长石Aug-普通辉石

    Figure  4.   Residual girdle structure of pyroxene phenocryst (crossed nicols)

    Cc-Calcite Ab-Albite Aug-Augite

    图  5   麦地村煌斑岩部分锆石阴极发光图

    Figure  5.   Cathodoluminescence image of the zircons

    图  6   煌斑岩锆石的谐和年龄

    Figure  6.   Zircon concordia age for the lamprophyre

    图  7   Na2O+K2O-LOI图解

    Figure  7.   Na2O+K2O-LOI diagrams

    图  8   岩石Nb/Y-Zr/TiO2分类图解[28]

    Figure  8.   Zr/Ti-Nb/Y diagrams[28]

    图  9   球粒陨石标准化稀土配分图[29]及原始地幔标准化微量元素蛛网图[30]

    JXL-焦溪岭煌斑岩; MDC-麦地村煌斑岩; OIB-洋岛玄武岩; N-type MORB-正常洋脊玄武岩

    Figure  9.   Chondrite-normalized REE patterns[29] and primitive mantle-normalized trace element spider diagrams[30]

    JXL-Jiaoxiling lamprophyre; MDC-Maidicun lamprophyre; OIB-Ocean Island Basalts; N-type MORB-Normal type mid-oceanic ridges basalts

    图  10   麦地村煌斑岩La-La/Sm与La-La/Yb图解

    Figure  10.   La-La/Sm diagram and La-La/Yb diagram

    图  11   Zr/Nb-La/Nb图解、Th/Nb-Th/La图解[46]

    Figure  11.   Zr/Nb-La/Nb diagram, Th/Nb-Th/La diagram[46]

    图  12   构造环境判别图解[47-48]

    Figure  12.   Tectonic environment discrimination diagram[47-48]

    表  1   建水地区麦地村煌斑岩锆石LA-ICP-MS U-Pb测年分析结果表

    Table  1   LA-ICP-MS U-Pb zircon dating results of Maidicun lamprophyre from Jianshui area

    下载: 导出CSV

    表  2   建水县麦地村煌斑岩主量元素(%)、微量(10-6)元素测试结果

    Table  2   Major (%) and trace element (10-6) analytical results for Maidicun lamprophyre from Jianshui area

    下载: 导出CSV
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出版历程
  • 收稿日期:  2015-11-17
  • 修回日期:  2016-02-25
  • 网络出版日期:  2023-09-26
  • 刊出日期:  2016-12-24

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