大别山南缘的构造变形研究
|
摘要
本文所研究的区域为大别造山带南缘浠水-马垅地区。该地区出露的岩片可分为铁冶岩片、麻桥岩片与飞虎山岩片。对三大岩片进行野外的观测、岩石显微构造、有限应变及温压分析。得出该地区的构造几何模型为管状。铁冶岩片处于管状模型的中心,能干性较强;麻桥岩片与飞虎山岩片组成管状模型的外壁。岩体中有长英质脉体充填。通过对大别造山带南缘构造带马垅地区所采岩石进行了岩石的有限应变测量测得应变椭圆的轴率Rs=1.5-2.0(所测矿物为长石),也指示该构造带岩石发生塑性变形。大别造山带南缘地质体中物质的运移方式为北西-南东方向,且为南东向北西运移。研究区西南缘发育断层殷店-马垅断层为右行走滑断层。经分析该地区的地质体变形受北西-南东向拉应力的影响,该方向的应力为印支期扬子板块向华北板块斜向挤压而产生的分量,并叠加太平洋板块向东亚板块碰撞在北西-南东方向水平分量而产生的合力。大别山南缘构造带上的片麻岩中的锆石用LA-ICP-MS法进行U-Pb测年。大别山南缘构造带马垅地区花岗片麻岩的原岩年龄为837±22Ma、MSWD=3.0,与前人在大别山南缘构造带所得年龄相一致,为多期构造活动后保留的元古宙扬子克拉通的原岩。所得年龄点集中分布下交点附近的不一致线上,所得年龄属于三叠纪印支期,其207Pb/206Pb的加权平均年龄分别为222±31Ma,MSWD=81,该年龄为扬子板块相对于秦岭-大别造山带的陆内俯冲的时间。飞虎山岩片年龄在谐和线下方,与谐和线的下交点年龄为151±79Ma,记录该地区燕山期构造活动的时间,是超高压变质岩折返的时代。
This paper studied the regions in the southern edge of the Dabie orogenic belt Xishui– Malong area. The rocks exposed in this region can be divided into Tie Ye group, Ma Qiao group and Feihu Shan group. The observations of rock micro-structure, finite strain and temperature and pressure analysis are carried out on these three groups. This paper get the region's tectonic geometry model tube. Tie Ye group in the center of tubular model, capable of strong; Ma Qiao group and Fei Hushan group are model composed of tubular outer wall. There are rock felsic veins filling. The experiment of rock finite strain has made on the Ma Qiao region, the shouthern edge of Dabie orogenic belt, measured the strain ellipse axial rate Rs=1.5-2.0, this result also indicates that the tectonic belt rocks plastic deformation occurs. Southwestern edge of the study area developed fault yindian - Ma Long fault is strike-slip fault. The analysis of the geology of the area deformation of the North West - South East, the impact of the tensile stress, the stress of the direction of the Yangtze plate to the North China plate oblique compression plate arising from the weight and superimposed the Pacific Plate to the East Asia plate collision in the North West - South East to the horizontal component of force generated. Zircon U-Pb dating used for gneiss of Tectonic belt in the southern edge of the Dabie Mountains. The southern edge of the Dabie Mountains belt Malong granitic gneiss area of the original rock age of 837±22Ma, MSWD = 3.0, with the former southern edge of the belt in the Dabie Mountains of age obtained is consistent for the multi-phase tectonic activity remaining after the Proterozoic period Yangtze craton of the original rock. The distribution of proceeds under the age spots near the intersection of the inconsistencies in line, derived from belonging to the Triassic age, Indo-China period, the weighted average of its 207Pb/206Pb age were 222±31Ma, MSWD = 81, the age of the Yangtze plate relative to the Qinling - Dabie orogenic belt intracontinental subduction of time. The age of Fei Hushan group harmonic line below the line under the intersection with the concordia age of 151±79Ma, record Yanshan period tectonic activity in the area, is the era of returned ultra-high pressure metamorphic rocks.
This paper studied the regions in the southern edge of the Dabie orogenic belt Xishui– Malong area. The rocks exposed in this region can be divided into Tie Ye group, Ma Qiao group and Feihu Shan group. The observations of rock micro-structure, finite strain and temperature and pressure analysis are carried out on these three groups. This paper get the region's tectonic geometry model tube. Tie Ye group in the center of tubular model, capable of strong; Ma Qiao group and Fei Hushan group are model composed of tubular outer wall. There are rock felsic veins filling. The experiment of rock finite strain has made on the Ma Qiao region, the shouthern edge of Dabie orogenic belt, measured the strain ellipse axial rate Rs=1.5-2.0, this result also indicates that the tectonic belt rocks plastic deformation occurs. Southwestern edge of the study area developed fault yindian - Ma Long fault is strike-slip fault. The analysis of the geology of the area deformation of the North West - South East, the impact of the tensile stress, the stress of the direction of the Yangtze plate to the North China plate oblique compression plate arising from the weight and superimposed the Pacific Plate to the East Asia plate collision in the North West - South East to the horizontal component of force generated. Zircon U-Pb dating used for gneiss of Tectonic belt in the southern edge of the Dabie Mountains. The southern edge of the Dabie Mountains belt Malong granitic gneiss area of the original rock age of 837±22Ma, MSWD = 3.0, with the former southern edge of the belt in the Dabie Mountains of age obtained is consistent for the multi-phase tectonic activity remaining after the Proterozoic period Yangtze craton of the original rock. The distribution of proceeds under the age spots near the intersection of the inconsistencies in line, derived from belonging to the Triassic age, Indo-China period, the weighted average of its 207Pb/206Pb age were 222±31Ma, MSWD = 81, the age of the Yangtze plate relative to the Qinling - Dabie orogenic belt intracontinental subduction of time. The age of Fei Hushan group harmonic line below the line under the intersection with the concordia age of 151±79Ma, record Yanshan period tectonic activity in the area, is the era of returned ultra-high pressure metamorphic rocks.
引文
[1]杨坤光,马昌前,许长海,杨巍然.北淮阳构造带与大别造山带的差异性隆升[J].中国科学,1999,29(2):97-103.
[2]杨坤光,马昌前,杨巍然.北淮阳马畈加里东岩体的研究及其地质意义[J].地球科学,1998,23(3):236-241.
[3]宋鸿林.变质核杂岩研究进展、基本特征及成因探讨[J].地学前缘,1995,2(1-2):103-111.
[4]张泽明,游振东,韩郁菁,桑隆康.大别-苏鲁榴辉岩带的岩石学、变质作用过程及成因研究[J].1995,69(4):306-325.
[5]杨坤光,姚淑梅,马昌前.大别地区花岗岩体石英c轴组构分析及其意义[J].地质科技情报,1999,18(1):29-32.
[6]陈晶,王清晨.大别山北部密棱岩中石英的高温应变[J].地质科学,1995,30(4):432-435.
[7]杨坤光,马昌前,简平,杨巍然.大别山北缘两次俯冲(碰撞)的岩石学和构造学证据[J].中国科学,2000,30(4):364-372.
[8]董树文,王小凤,黄德志.大别山超高压变质带内浅变质岩片的发现及意义[J].科学通报,1996,41(9):815-820.
[9]徐树桐,董树文,周海渊,陈冠宝.大别山东段(安徽)大别杂岩中的断层构造岩和推复构造[J].科学通报,1984,(5):298-300.
[10]徐树桐,苏文,刘贻灿,江来利.大别山东段高压变质岩中的金刚石[J].科学通报,1991,(17):1318-1321.
[11]水汀,薛虎.大别山东南麓韧性剪切构造带[J].中国地质科学院南京地质矿产研究所所刊,1989,10(1):52-63.
[12]王国灿,杨巍然.大别山核部罗田穹隆形成的构造及年代学证据[J].地球科学,1996,21(5):524-528.
[13]董树文,孙先知,张勇,黄德志,王刚,戴世坤,于邦存.大别山碰撞造山带基本结构[J].科学通报,1993,38(6):542-545.
[14]杨森楠,吴鉴,杨学忠,陆中旦.大别山前寒武纪构造演化[J].地球科学,1983,(3):81-91.
[15]徐树桐,江来利,刘贻灿,张勇.大别山(安徽部分)的构造格局和演化过程[J].地质学报,1992,66(1):1-14.
[16]翟明国,从柏林,陈晶,王清晨.大别山区变质岩中蓝晶石的几种退变质反应及其所指示的动力学过程[J].岩石学报,1995,11(3):257-272.
[17]陈江峰,董树文,邓衍尧,陈移之.大别造山带钾氩年龄的解释——差异上升的地块[J].地质论评,1993,39(1):17-22.
[18]王国灿,杨巍然.大别造山带中新生代隆升作用的时空格局[J].地球科学,1998,23(5):461-467.
[19]杨坤光,马昌前,许长海,杨巍然.东大别山北缘姚河岩体与边部糜棱岩带的研究及其地质意义[J].地震地质,1998,20(4):305-311.
[20]颜怀学,金福全,吴培基,陆光森,张廷秀,王道轩,崔可锐.关于中国南北板块在北淮阳地区界限的探讨[J].石油与天然气地质,1988,9(2):125-132.
[21]刘早学,李金平.麻城——团风剪切带的基本特征及形成时代初探[J].湖北地质,1993,7(1):38-44.
[22]徐磊,吴永生.磨子潭——晓天断裂(晓天至佛子岭间)的构造分析[J].地震地质,1984,6(4):45-53.
[23]杨志坚.试论桐柏——大别山地质构造演化特征[J].地质学报,1982,(2):123-135.
[24]郝杰,刘小汉.桐柏——大别碰撞造山带大型推覆-滑脱构造及其演化[J].地质科学,1988,(1):1-10.
[25]金维浚,宋鸿林,马文璞.桐柏——大别山西段的伸展构造[J].地质科学,1997,32(2):156-164.
[26]刘德良,李秀新.皖中地区深层构造分析[J].地质科学,1984,(1):42-50.
[27]许志琴.扬子板块北缘的大型深层滑脱构造及动力学分析[J].中国区域地质,1987,(4):289-300.
[28]杨巍然,王豪.中国板块构造概况[J].地球科学,1991,16(5):505-513.
[29]许志琴,卢一伦,汤耀庆.中国的脊梁——秦岭山链的形成、聚合、碰撞及陆内俯冲[J].中国地质科学院院报,1990,(20):130-132.
[30]黄汲清.中国区域地质的特征[J].地质学报,1954,34(3):217-144.
[31]向必伟,朱光,王勇生,谢成龙,胡召齐.糜棱岩化过程中矿物变形温度计[J].地球科学进展,2007,22(2):126-133.
[32]宋传中,牛漫兰,王道轩,刘国生,霍立新.岩石有限应变与造山带构造块体变形要素的估算[J].合肥工业大学学报,2005,28(9):1141-1145.
[33]江来利,吴维平,储东如.大别造山带东段扬子陆块和华北陆块间缝合带的位置[J].中国地质大学学报,2005,30(3):264-274.
[34]刘富,周汉文.大别造山带大陆深俯冲和折返过程中壳—幔相互作用信息[J].地质科技情报,2005,24(1):14-18.
[35]王云斌,梁明宏,霍勤知,魏振伟.利用变形花岗岩体中的长石矿物进行有限应变测量初探[J].西北地质,2004,37(1):19-24.
[36]邓乾忠,彭练红,陈林.襄樊——广济断裂构造地质特征及发展演化[J],资源环境与工程.2004,18:18-21.
[37]江来利,吴维平,储东如,刘贻灿,张勇.大别山北部碰撞后伸展-逆冲推覆构造[J].科学通报,2003,48(14):1557-1563.
[38]董云鹏,张国伟,姚安平,赵霞.襄樊—广济断裂西段三里岗—三阳构造混杂岩带构造变形与演化[J].地质科学,2003,38(4):425—436.
[39]王世锋,刘瑞珣.显微构造中应变标志物及应变测量[J].高校地质学报,2002,8(1):62-67.
[40]王清晨,林伟.大别山碰撞造山带的地球动力学[J].地学前缘,2002,9(4):257-265.
[41]周永胜,何昌荣.地壳岩石变形行为的转变及其温压条件[J].地震地质,2000,22(2):167-178.
[42]魏春景,陈斌,张翠光,陈晶.大别地区的变质作用及与碰撞造山过程的关系[J].地质力学学报,2000,6(3):35-38.
[43]江来利,刘贻灿,吴维平,苏文.大别山超高压变质岩的变形历史及折返过程[J].SCIENTIA GEOLOGICA SINICA,1999,34(4):432-441.
[44]刘源骏.大别山罗田“走滑剪切带”发现的意义——与美国弗朗西斯科群对比后对几个问题的思考[J].湖北地矿,1999,13(2):1-11.
[45]潘国强,赵连泽,夏木林.大别山碰撞造山带的构造模型及其地质演化[J].中国区域地质,1997,16(1):43-50.
[46]梁鼎新,辜骏如,郭福生,林银山.大别造山带的构造演化[J],华东地质学院学报.1995,18(2):135-142.
[47]刘迅.大别地块东南缘逆冲滑脱构造体系及其对金矿的控制作用[J].大地构造与成矿学,1994,18(2):127-137.
[48]董树文,孙先如,张勇,黄德志,王刚,戴世坤,于邦存.大别山碰撞造山带基本结构[J].科学通报,1993,38(6):542-545.
[49]王义天.大别碰撞造山带中生代的走滑断层作用[M].中国科学院地质与地球物理研究,1999.
[50]郑亚东,常志忠.岩石有限应变测量及韧性剪切带[M].地质出版社,1985.
[51]胡玲.显微构造地质学概论.地质出版社,1998.
[52]林文姣,杨文强.大别山南麓典型岩体磁组构学研究的地质意义[J].地质科技情报,2006,25(4):52-54.
[53]刘贻灿,李曙光.大别山下地壳岩石及其深俯冲[J].岩石学报,2005,21(4):1060-1066.
[54] Okay A I, Xu S T, Sengor A M C. Coesite from the Dabie Shan eclogites, central China[J]. Eur J Mineral,1989,1:595-598
[55] Wang X M, Liou J G, Mao H K. Coesite-bearing from the Dabie Mountains in central China[J]. Geology, 1989,17:1085-1088
[56] Xu S T, Okay A I, Ji S Y, et al. Diamond from the Dabie Shan metamorphicrocks and its implication for tectonic setting[J]. Science,1992,256:80-82
[57] Ames L, Zhou GZ and Xiong BC. Geochronology and isotopic character of ultrahigh-pressure metamorphism with implications for collision of the Sino-Korean and Yangtze cratons,central China[J],Tectonics,1996,15(2):472-489
[58] Rowley D B, Xue F, Tucker R D et al. Ages of ultra pressure metamorphic and protolith orthgenisses from the eastern Dabie Shan:U/Pb zircon geochronology[J].EarthPlant.Sci.Lett.1997,151:191-203
[59] Chen D, Isachsen C, Zhi X et al. Zircon U-Pb ages for gneiss from Qianshan,Anhui[J]. Chinese Sciences Bulletin, 2000.45(8):764-767
[60] Chen N, You Z, Suo S et al.1996.The U-Pb zircon ages of acid granulite and deformed granite from Dabie[J]. Chinese Sciences Bulletin,41(11):1009-1012(in chinese)
[61] Cheng Y, Liu D, William IS et al.2000.SHRIMP U-Pb dating of zircons of a dark-colored eclogite and a garnet-bearing gneissic-granitic rock from bixiling, Eastern Dabie Area[J]. Acta Geologica Sinica, 74(3):193-205(in chinese)
[62] Jian P, Liu D, Yang W et al.2000. Zircon mico ion-probe dating of Caledonian ecologite from Xiongdian weatern Dabie[J]. Chinese Science Bulletin, 45(19):2090-2093(in chinese)
[63]李曙光,李惠民,陈移之等.大别-苏鲁地体超高压变质年代学-Ⅱ,锆石U-Pb同位素体系[J].中国科学(D). 1997,27(3):200-206.
[64]陈道公,E Deloule,夏群科.北大别片麻岩中锆石U-Pb年龄离子探针初步测定[J].岩石学报,2000,16(2):199-202
[65]陈道公,Etienme Deloule,夏群科等.大别山双河超高压柳辉岩中变质锆石:离子探针和微区结构研究[J].岩石学报,2002,18(3):369-377
[66]江来利,吴维平,刘贻灿等.大别山南部宿松杂岩的U-Pb锆石和Ar-Ar角闪石年龄及其地质意义[J].岩石学报.2003,19(3):497-505
[67]陈道公,E Deloule,倪涛.大别地体新店柳辉岩变质锆石U-Pb年龄和氧同位素研究[J].中国科学D辑.2005,35(8):691-699
[68]吴元保,唐俊,张少兵等.北大别两期混合岩化作用:SHRIMP锆石U-Pb年龄证据[J].科学通报.2007,52(8):938-944
[69]钱存超.大别造山带南缘构造几何学特征与形成演化[M].博士论文.2006
[70]湖北省地质局.区域地质调查报告[M].1974.
[71]《大别山超高压变质作用与碰撞造山动力学》编写组.大别山超高压变质作用与碰撞造山动力学[M].北京:科学出版社,2005:210.
[72]徐树桐,刘贻灿,江来利,等.大别山造山带的构造几何学和运动学[M].合肥:中国科学技术大学出版社,2002:133
[73]高天山,李惠民,汤加富,等.大别造山带南缘浅粒岩的锆石U-Pb年龄及其地质意义[J].中国地质.2002,29(3):301-304
[74]薛怀民,刘敦一,董树文,等.湖北蕲春花岗岩类锆石SHRIMP年龄:大别山造山带内弱变质-未变质晋宁期花岗岩类的发现[J].地质学报.2004,78(1):81-88
[75]Ludwig K R.ISOPLOT:A plotting and regression program for radiogenic-isotope data[M]. U S Geological Survey Open-File Report,1991,39
[76]Gao S, Rudnick R L, Yuan H L, et al. Recycling lower continental crust in the North China craton[J].Nature,2004,432:892-897
[77]Yuan H L, Gao S, Liu X M, et al. Accurate U-Pb age and trace element determinations of zircon by laser ablation inductively coupled plasma mass spectrometry[J]. Geostandard and Geoanalytical Research,2004,28:353-370
[78]Rubatto D,Gebauer G,Compagnoni R.Dating of eclogite-facies zircons:the age of Alpine metamorphism in the Sesia-Lanzo Zone(Western Alps) [J]. Earth and Planetary Science Letters.1999.167.141-158
[79]Lee J, Williams I, Ellis D. Pb,U and Th diffusion in nature zircon[J], Nature, 1997, 390(13):159-162
[80]宋传中,张国伟,任升莲,等.秦岭—大别造山带中几条重要构造带的特征及其意义[J],西北大学学报(自然科学版),2009,39(3)
[2]杨坤光,马昌前,杨巍然.北淮阳马畈加里东岩体的研究及其地质意义[J].地球科学,1998,23(3):236-241.
[3]宋鸿林.变质核杂岩研究进展、基本特征及成因探讨[J].地学前缘,1995,2(1-2):103-111.
[4]张泽明,游振东,韩郁菁,桑隆康.大别-苏鲁榴辉岩带的岩石学、变质作用过程及成因研究[J].1995,69(4):306-325.
[5]杨坤光,姚淑梅,马昌前.大别地区花岗岩体石英c轴组构分析及其意义[J].地质科技情报,1999,18(1):29-32.
[6]陈晶,王清晨.大别山北部密棱岩中石英的高温应变[J].地质科学,1995,30(4):432-435.
[7]杨坤光,马昌前,简平,杨巍然.大别山北缘两次俯冲(碰撞)的岩石学和构造学证据[J].中国科学,2000,30(4):364-372.
[8]董树文,王小凤,黄德志.大别山超高压变质带内浅变质岩片的发现及意义[J].科学通报,1996,41(9):815-820.
[9]徐树桐,董树文,周海渊,陈冠宝.大别山东段(安徽)大别杂岩中的断层构造岩和推复构造[J].科学通报,1984,(5):298-300.
[10]徐树桐,苏文,刘贻灿,江来利.大别山东段高压变质岩中的金刚石[J].科学通报,1991,(17):1318-1321.
[11]水汀,薛虎.大别山东南麓韧性剪切构造带[J].中国地质科学院南京地质矿产研究所所刊,1989,10(1):52-63.
[12]王国灿,杨巍然.大别山核部罗田穹隆形成的构造及年代学证据[J].地球科学,1996,21(5):524-528.
[13]董树文,孙先知,张勇,黄德志,王刚,戴世坤,于邦存.大别山碰撞造山带基本结构[J].科学通报,1993,38(6):542-545.
[14]杨森楠,吴鉴,杨学忠,陆中旦.大别山前寒武纪构造演化[J].地球科学,1983,(3):81-91.
[15]徐树桐,江来利,刘贻灿,张勇.大别山(安徽部分)的构造格局和演化过程[J].地质学报,1992,66(1):1-14.
[16]翟明国,从柏林,陈晶,王清晨.大别山区变质岩中蓝晶石的几种退变质反应及其所指示的动力学过程[J].岩石学报,1995,11(3):257-272.
[17]陈江峰,董树文,邓衍尧,陈移之.大别造山带钾氩年龄的解释——差异上升的地块[J].地质论评,1993,39(1):17-22.
[18]王国灿,杨巍然.大别造山带中新生代隆升作用的时空格局[J].地球科学,1998,23(5):461-467.
[19]杨坤光,马昌前,许长海,杨巍然.东大别山北缘姚河岩体与边部糜棱岩带的研究及其地质意义[J].地震地质,1998,20(4):305-311.
[20]颜怀学,金福全,吴培基,陆光森,张廷秀,王道轩,崔可锐.关于中国南北板块在北淮阳地区界限的探讨[J].石油与天然气地质,1988,9(2):125-132.
[21]刘早学,李金平.麻城——团风剪切带的基本特征及形成时代初探[J].湖北地质,1993,7(1):38-44.
[22]徐磊,吴永生.磨子潭——晓天断裂(晓天至佛子岭间)的构造分析[J].地震地质,1984,6(4):45-53.
[23]杨志坚.试论桐柏——大别山地质构造演化特征[J].地质学报,1982,(2):123-135.
[24]郝杰,刘小汉.桐柏——大别碰撞造山带大型推覆-滑脱构造及其演化[J].地质科学,1988,(1):1-10.
[25]金维浚,宋鸿林,马文璞.桐柏——大别山西段的伸展构造[J].地质科学,1997,32(2):156-164.
[26]刘德良,李秀新.皖中地区深层构造分析[J].地质科学,1984,(1):42-50.
[27]许志琴.扬子板块北缘的大型深层滑脱构造及动力学分析[J].中国区域地质,1987,(4):289-300.
[28]杨巍然,王豪.中国板块构造概况[J].地球科学,1991,16(5):505-513.
[29]许志琴,卢一伦,汤耀庆.中国的脊梁——秦岭山链的形成、聚合、碰撞及陆内俯冲[J].中国地质科学院院报,1990,(20):130-132.
[30]黄汲清.中国区域地质的特征[J].地质学报,1954,34(3):217-144.
[31]向必伟,朱光,王勇生,谢成龙,胡召齐.糜棱岩化过程中矿物变形温度计[J].地球科学进展,2007,22(2):126-133.
[32]宋传中,牛漫兰,王道轩,刘国生,霍立新.岩石有限应变与造山带构造块体变形要素的估算[J].合肥工业大学学报,2005,28(9):1141-1145.
[33]江来利,吴维平,储东如.大别造山带东段扬子陆块和华北陆块间缝合带的位置[J].中国地质大学学报,2005,30(3):264-274.
[34]刘富,周汉文.大别造山带大陆深俯冲和折返过程中壳—幔相互作用信息[J].地质科技情报,2005,24(1):14-18.
[35]王云斌,梁明宏,霍勤知,魏振伟.利用变形花岗岩体中的长石矿物进行有限应变测量初探[J].西北地质,2004,37(1):19-24.
[36]邓乾忠,彭练红,陈林.襄樊——广济断裂构造地质特征及发展演化[J],资源环境与工程.2004,18:18-21.
[37]江来利,吴维平,储东如,刘贻灿,张勇.大别山北部碰撞后伸展-逆冲推覆构造[J].科学通报,2003,48(14):1557-1563.
[38]董云鹏,张国伟,姚安平,赵霞.襄樊—广济断裂西段三里岗—三阳构造混杂岩带构造变形与演化[J].地质科学,2003,38(4):425—436.
[39]王世锋,刘瑞珣.显微构造中应变标志物及应变测量[J].高校地质学报,2002,8(1):62-67.
[40]王清晨,林伟.大别山碰撞造山带的地球动力学[J].地学前缘,2002,9(4):257-265.
[41]周永胜,何昌荣.地壳岩石变形行为的转变及其温压条件[J].地震地质,2000,22(2):167-178.
[42]魏春景,陈斌,张翠光,陈晶.大别地区的变质作用及与碰撞造山过程的关系[J].地质力学学报,2000,6(3):35-38.
[43]江来利,刘贻灿,吴维平,苏文.大别山超高压变质岩的变形历史及折返过程[J].SCIENTIA GEOLOGICA SINICA,1999,34(4):432-441.
[44]刘源骏.大别山罗田“走滑剪切带”发现的意义——与美国弗朗西斯科群对比后对几个问题的思考[J].湖北地矿,1999,13(2):1-11.
[45]潘国强,赵连泽,夏木林.大别山碰撞造山带的构造模型及其地质演化[J].中国区域地质,1997,16(1):43-50.
[46]梁鼎新,辜骏如,郭福生,林银山.大别造山带的构造演化[J],华东地质学院学报.1995,18(2):135-142.
[47]刘迅.大别地块东南缘逆冲滑脱构造体系及其对金矿的控制作用[J].大地构造与成矿学,1994,18(2):127-137.
[48]董树文,孙先如,张勇,黄德志,王刚,戴世坤,于邦存.大别山碰撞造山带基本结构[J].科学通报,1993,38(6):542-545.
[49]王义天.大别碰撞造山带中生代的走滑断层作用[M].中国科学院地质与地球物理研究,1999.
[50]郑亚东,常志忠.岩石有限应变测量及韧性剪切带[M].地质出版社,1985.
[51]胡玲.显微构造地质学概论.地质出版社,1998.
[52]林文姣,杨文强.大别山南麓典型岩体磁组构学研究的地质意义[J].地质科技情报,2006,25(4):52-54.
[53]刘贻灿,李曙光.大别山下地壳岩石及其深俯冲[J].岩石学报,2005,21(4):1060-1066.
[54] Okay A I, Xu S T, Sengor A M C. Coesite from the Dabie Shan eclogites, central China[J]. Eur J Mineral,1989,1:595-598
[55] Wang X M, Liou J G, Mao H K. Coesite-bearing from the Dabie Mountains in central China[J]. Geology, 1989,17:1085-1088
[56] Xu S T, Okay A I, Ji S Y, et al. Diamond from the Dabie Shan metamorphicrocks and its implication for tectonic setting[J]. Science,1992,256:80-82
[57] Ames L, Zhou GZ and Xiong BC. Geochronology and isotopic character of ultrahigh-pressure metamorphism with implications for collision of the Sino-Korean and Yangtze cratons,central China[J],Tectonics,1996,15(2):472-489
[58] Rowley D B, Xue F, Tucker R D et al. Ages of ultra pressure metamorphic and protolith orthgenisses from the eastern Dabie Shan:U/Pb zircon geochronology[J].EarthPlant.Sci.Lett.1997,151:191-203
[59] Chen D, Isachsen C, Zhi X et al. Zircon U-Pb ages for gneiss from Qianshan,Anhui[J]. Chinese Sciences Bulletin, 2000.45(8):764-767
[60] Chen N, You Z, Suo S et al.1996.The U-Pb zircon ages of acid granulite and deformed granite from Dabie[J]. Chinese Sciences Bulletin,41(11):1009-1012(in chinese)
[61] Cheng Y, Liu D, William IS et al.2000.SHRIMP U-Pb dating of zircons of a dark-colored eclogite and a garnet-bearing gneissic-granitic rock from bixiling, Eastern Dabie Area[J]. Acta Geologica Sinica, 74(3):193-205(in chinese)
[62] Jian P, Liu D, Yang W et al.2000. Zircon mico ion-probe dating of Caledonian ecologite from Xiongdian weatern Dabie[J]. Chinese Science Bulletin, 45(19):2090-2093(in chinese)
[63]李曙光,李惠民,陈移之等.大别-苏鲁地体超高压变质年代学-Ⅱ,锆石U-Pb同位素体系[J].中国科学(D). 1997,27(3):200-206.
[64]陈道公,E Deloule,夏群科.北大别片麻岩中锆石U-Pb年龄离子探针初步测定[J].岩石学报,2000,16(2):199-202
[65]陈道公,Etienme Deloule,夏群科等.大别山双河超高压柳辉岩中变质锆石:离子探针和微区结构研究[J].岩石学报,2002,18(3):369-377
[66]江来利,吴维平,刘贻灿等.大别山南部宿松杂岩的U-Pb锆石和Ar-Ar角闪石年龄及其地质意义[J].岩石学报.2003,19(3):497-505
[67]陈道公,E Deloule,倪涛.大别地体新店柳辉岩变质锆石U-Pb年龄和氧同位素研究[J].中国科学D辑.2005,35(8):691-699
[68]吴元保,唐俊,张少兵等.北大别两期混合岩化作用:SHRIMP锆石U-Pb年龄证据[J].科学通报.2007,52(8):938-944
[69]钱存超.大别造山带南缘构造几何学特征与形成演化[M].博士论文.2006
[70]湖北省地质局.区域地质调查报告[M].1974.
[71]《大别山超高压变质作用与碰撞造山动力学》编写组.大别山超高压变质作用与碰撞造山动力学[M].北京:科学出版社,2005:210.
[72]徐树桐,刘贻灿,江来利,等.大别山造山带的构造几何学和运动学[M].合肥:中国科学技术大学出版社,2002:133
[73]高天山,李惠民,汤加富,等.大别造山带南缘浅粒岩的锆石U-Pb年龄及其地质意义[J].中国地质.2002,29(3):301-304
[74]薛怀民,刘敦一,董树文,等.湖北蕲春花岗岩类锆石SHRIMP年龄:大别山造山带内弱变质-未变质晋宁期花岗岩类的发现[J].地质学报.2004,78(1):81-88
[75]Ludwig K R.ISOPLOT:A plotting and regression program for radiogenic-isotope data[M]. U S Geological Survey Open-File Report,1991,39
[76]Gao S, Rudnick R L, Yuan H L, et al. Recycling lower continental crust in the North China craton[J].Nature,2004,432:892-897
[77]Yuan H L, Gao S, Liu X M, et al. Accurate U-Pb age and trace element determinations of zircon by laser ablation inductively coupled plasma mass spectrometry[J]. Geostandard and Geoanalytical Research,2004,28:353-370
[78]Rubatto D,Gebauer G,Compagnoni R.Dating of eclogite-facies zircons:the age of Alpine metamorphism in the Sesia-Lanzo Zone(Western Alps) [J]. Earth and Planetary Science Letters.1999.167.141-158
[79]Lee J, Williams I, Ellis D. Pb,U and Th diffusion in nature zircon[J], Nature, 1997, 390(13):159-162
[80]宋传中,张国伟,任升莲,等.秦岭—大别造山带中几条重要构造带的特征及其意义[J],西北大学学报(自然科学版),2009,39(3)