西准噶尔山地四级夷平面的划分及构造地貌分区
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摘要
基于SRTM3-DEM数据,运用ArcGIS技术,采用空间分析、三维地表形态分析和剖面形态分析方法,结合野外调查,对克拉玛依盆地以西、塔城盆地以东的西准噶尔山地的地貌结构进行了初步研究,划分出4级夷平面,讨论了各级夷平面的特征,依据地表特征分析对研究区内的构造地貌区进行了划分。4级夷平面海拔高度分别是2 734~1 760m、1 520~1 200m、1 000~300m和800~660m。参考地表面三维统计得到的拐点(1 320m/1 270m),将1 270m以上地貌面分为2级夷平面:1 760m以上夷平面(Ⅰ)和1 520~1 200m夷平面(Ⅱ),地形起伏度均在500~200m以内。Ⅱ级夷平面可能发育于白垩纪至新近纪,山地剥蚀的后期与新近系昌吉河群相对比。1 000m以下分为两级剥蚀面,其中之一,剥蚀面高度1 000~660m,并一直延伸至300m高度,为一变形的山麓及山前剥夷面(Ⅲ)。该剥蚀面具有埋藏剥蚀面性质,形成于中更新世—晚更新世。另一级山间剥蚀面出现在860~660m高度上(Ⅳ),发育于晚更新世后期至全新世。4级夷平面代表了山地的4次稳定时期与其间的4次快速抬升,第Ⅲ级剥蚀面的变形记录了青藏高原晚第四纪隆升的远程效应。不同分区之间的构造地貌差异为区域构造分析提供了有价值的分区信息,构成区域构造分区中的一个重要因素。区域研究表明,西准噶尔山地的总体构造线方向呈NE向展布,其与东部的准噶尔盆地和西部塔城盆地及以西地区的NW向构造线方向明显不同,受控于数条NE向断裂的南部扎伊尔山地与北部吾尔喀什尔山地的盆-山间列的构造地貌组合构成了区域南、北之间的对比。依据DEM所做的地表特征分析,把研究区分为北部中山与盆地间列区(Ⅰ-1)、南部中低山区(Ⅰ-2)和东南部山缘及山前平原区(Ⅱ)3个构造地貌区。西准噶尔山地(Ⅰ区)属于天山—准噶尔—萨彦—贝加尔构造强变形带和地震活动带的一部分,这里虽未发生过强烈地震,但具备了发震的基本条件,且临近克拉玛依油气资源开发重地,建议进行必要的地震观测和地震预报。
By using spatial analysis,three dimensional surface analysis,profile shape analysis and the platform of Arc GIS based on SRTM3-DEM data,and combining with field geological survey,the geomorphologic structures of West Junggar Mountain between the western part of Karamay Basin and the eastern part of Tacheng Basin are studied;the planation surfaces are divided into four levels,and their structural geomorphologic features are discussed;and three subareas of structural geomorphology are divided.There are at least four levels of planation surfaces in the mountain,which appear on 2734-1760m,1520-1200m,1000-300mand 800-660mabove the sea level.Two planation surfaces,at over 1 760mabove the sea level(the levelⅠ)and at between 1520mand 1200mabove the sea level(the levelⅡ)respectively,were detected based on the inflection point obtained in three dimensional statistics for the ground surface(at 1320m/1270m above the sea level),and both undulations of them are of no more than 500-200m.The levelⅡ was shaped in the Cretaceous-Neogene Period,and the later period of denudation coincided with Changjihe Group shaped in the Neogene Period.There are two denudation planes under the inflection point.One of them exits in1000-660mand extends to 300mabove the sea level,and it is a deformed denudation plane existing at the foothill and the front of mountain(the levelⅢ),and it was shaped during the Middle Pleistocene to the Late Pleistocene and buried by the pluvial-alluvial deposits of the Late Pleistocene-Holocene Epoch.The other appears in 860-660mabove the sea level(the levelⅣ),it was shaped during the Late Pleistocene-Holocene Epoch as the pluvial-alluvial deposits of the Late Pleistocene Epoch have been whittled down.The above four level planations represent four stable periods and four rapid uplift periods among planations,but the deformation of levelⅢrecorded a response of the uplift of Qinghai-Tibet Plateau during the Late Quaternary Period.The structural geomorphologic difference in space provides some valuable information for the partition of regional tectonics,which composes one important factor for regional tectonic partition.The research of West Junggar Mountain shows that the direction of structural line lies as a whole on the direction of northeastsouthwest,which is different from the direction of northwest-southeast of Junggar Basin and Tacheng Basin and western part of it,and this makes a contrast between Zaire Mountain of the southern part controlled by several faults in the direction of northeast and the structural geomorphologic constitution of alternatingly distributed basins and mountains in Ur Kashi Mountain of the north part.Three structural geomorphologic subareas were divided according to the DEM ground surface features;they are northern subarea of the alternatingly distributed middle mountains and basins(Ⅰ-1),south subarea of middle-low mountains(Ⅰ-2),and south-eastern subarea of the mountain edges and the frontier plane of the mountain(Ⅱ).The West Junggar Mountain(Ⅰarea)belongs to a part of intense deformation zone of structure and seismic active zone of Tianshan-Junggar-Sayan-Baikal,although there has not been a violent earthquake in history,it possesses some basic conditions of seismic action in future,and it is close to the petro-gas development area in Karamay Basin, so essential seismic observation and seismic forecast is suggested.
By using spatial analysis,three dimensional surface analysis,profile shape analysis and the platform of Arc GIS based on SRTM3-DEM data,and combining with field geological survey,the geomorphologic structures of West Junggar Mountain between the western part of Karamay Basin and the eastern part of Tacheng Basin are studied;the planation surfaces are divided into four levels,and their structural geomorphologic features are discussed;and three subareas of structural geomorphology are divided.There are at least four levels of planation surfaces in the mountain,which appear on 2734-1760m,1520-1200m,1000-300mand 800-660mabove the sea level.Two planation surfaces,at over 1 760mabove the sea level(the levelⅠ)and at between 1520mand 1200mabove the sea level(the levelⅡ)respectively,were detected based on the inflection point obtained in three dimensional statistics for the ground surface(at 1320m/1270m above the sea level),and both undulations of them are of no more than 500-200m.The levelⅡ was shaped in the Cretaceous-Neogene Period,and the later period of denudation coincided with Changjihe Group shaped in the Neogene Period.There are two denudation planes under the inflection point.One of them exits in1000-660mand extends to 300mabove the sea level,and it is a deformed denudation plane existing at the foothill and the front of mountain(the levelⅢ),and it was shaped during the Middle Pleistocene to the Late Pleistocene and buried by the pluvial-alluvial deposits of the Late Pleistocene-Holocene Epoch.The other appears in 860-660mabove the sea level(the levelⅣ),it was shaped during the Late Pleistocene-Holocene Epoch as the pluvial-alluvial deposits of the Late Pleistocene Epoch have been whittled down.The above four level planations represent four stable periods and four rapid uplift periods among planations,but the deformation of levelⅢrecorded a response of the uplift of Qinghai-Tibet Plateau during the Late Quaternary Period.The structural geomorphologic difference in space provides some valuable information for the partition of regional tectonics,which composes one important factor for regional tectonic partition.The research of West Junggar Mountain shows that the direction of structural line lies as a whole on the direction of northeastsouthwest,which is different from the direction of northwest-southeast of Junggar Basin and Tacheng Basin and western part of it,and this makes a contrast between Zaire Mountain of the southern part controlled by several faults in the direction of northeast and the structural geomorphologic constitution of alternatingly distributed basins and mountains in Ur Kashi Mountain of the north part.Three structural geomorphologic subareas were divided according to the DEM ground surface features;they are northern subarea of the alternatingly distributed middle mountains and basins(Ⅰ-1),south subarea of middle-low mountains(Ⅰ-2),and south-eastern subarea of the mountain edges and the frontier plane of the mountain(Ⅱ).The West Junggar Mountain(Ⅰarea)belongs to a part of intense deformation zone of structure and seismic active zone of Tianshan-Junggar-Sayan-Baikal,although there has not been a violent earthquake in history,it possesses some basic conditions of seismic action in future,and it is close to the petro-gas development area in Karamay Basin, so essential seismic observation and seismic forecast is suggested.
引文
[1]杨巍然,王杰,梁晓.亚洲大地构造基本特征和演化规律[J].地学前缘,2012,19(5):1-17.
[2]王国灿,杨巍然.地质晚近时期山脉地区隆升及剥露作用研究[J].地学前缘,1998,5(1):151-156.
[3]潘保田,高红山,李吉均.关于夷平面的科学问题:兼论青藏高原夷平面[J].地理科学,2002,22(5):520-526.
[4]Fielding E J.Morphotectonic evolution of the Himalayas and Tibetan Plateau[M]∥Summerfield M A.Geomorphology and Global Tectonics.London:John Wiley&Sons Press Ltd.,2000:201-222.
[5]任纪舜.昆仑—秦岭造山系的几个问题[J].西北地质,2004,37(1):1-5.
[6]王树基.亚洲中部山地夷平面研究:以天山山系为例[M].北京:科学出版社,1998:1-152.
[7]Zhou S Z,Xu L B,Cui J X,et al.Geomorphologic evolution and environmental change in the Shaluli Mountain region during the Quaternary[J].Chinese Science Bulletin,2005,50(1):52-57.
[8]王宗秀,李涛.新疆博格达山链新生代再生造山机理:岩石圈内切层“开”“合”造山的典型代表[J].地质通报,2004,23(3):289-293.
[9]Zhao Z J,Fang X M,Li J J,et al.Paleomagnetic dating of the Jiuquan Gravel in the Hexi Corridor:Implication on midPleistocene uplift of the Qinghai-Tibetan Plateau[J].Chinese Science Bulletin,2001,46(23):2001-2005.
[10]陈宣华,李丽,尹安,等.东昆仑造山带多期隆升历史的地质热年代学证据[J].地质通报,2011,31(11):1647-1660.
[11]郭召杰,张志诚,吴朝东,等.中、新生代天山隆升过程及其与准噶尔、阿尔泰山比较研究[J].地质学报,2006,80(1):1-15.
[12]李传新,郭召杰.晚新生代天山北缘构造变形定量研究[J].地质科学,2011,46(3):709-722.
[13]李玮.准噶尔西北缘造山带中生代盆地形成机制及构造演化[D].北京:中国地质科学院地质研究所,2007.
[14]肖序常,罗照华.西昆仑及邻区岩石圈结构构造化:塔里木南—西昆仑多学科地学断面简要报道[J].地质通报,2002,21(2):63-68.
[15]高红山,潘保田,邬光剑,等.祁连山东段剥蚀面与青藏高原隆升[J].冰川冻土,2004,26(5):540-544.
[16]王岸,王国灿.构造地貌及其分析方法评述[J].地质科技情报,2005,24(4):7-20.
[17]杨景春,李有利.地貌学原理[M].北京:北京大学出版社,2001.
[18]李容全,邱维理.地文期与地文期研究[J].第四纪研究,2005(6):676-685.
[19]Ojany F F.Erosing and planation surface in Machakos-Kitui area of Kenya[J].GeoJournal,1978,2(4):289-294.
[20]任雪梅,陈忠,罗丽霞,等.夷平面研究综述[J].地理科学,2003,23(1):107-111.
[21]吴忱,张秀清,马永红.再论华北山地甸子梁期夷平面及早第三纪地文期[J].地理学与国土研究,1997,13(3):39-46.
[22]赵洪壮,李有利,杨景春,等.基于DEM数据的北天山地貌形态分析[J].地理科学,2009,29(3):445-449.
[23]杨昕,汤国安,刘学军,等.数字地形分析的理论、方法与应用[J].地理学报,2009,64(9):1058-1070.
[24]Kuhni A,Pfiffner O A.The relief of the Swiss Alps and adjacent areas and its relation to lithology and structure:Topographic analysis from a 250 m DEM[J].Geomorphology,2001(4):285-307.
[25]Dong W J,Tang M C.A numerical modeling study on the processes of uplift and planation of the Tibetan Plateau[J].Science in China:Series D,1997,40(3):246-250.
[26]洪顺英,申旭辉,荆凤,等.基于SRTM-DEM的阿尔泰山构造地貌特征分析[J].国土资源遥感,2007,73(3):62-66.
[27]朱永峰,王涛,徐新.新疆及邻区地质矿产研究进展[J].岩石学报,2007,23(8):1785-1789.
[28]肖序常,汤耀庆,李锦铁,等.古中亚复合巨型缝合带南缘构造演化[M].北京:北京科学技术出版社,1991.
[29]彭希龄.新疆新构造运动的表现和特点[J].成都理工学院学报,1998,25(2):169-181.
[30]柏美祥.新疆河谷阶地的年代[J].内陆地震,1998,12(1):13-19.
[31]冯锐,马宗晋,方剑,等.发展中的板块边界:天山—贝加尔活动构造带[J].地学前缘,2007,14(4):1-17.
[32]马宗晋,曲国胜,陈新发.准噶尔盆地深浅构造分析及油气展布规律[J].新疆石油地质,2008,29(4):411-414.
[33]吴孔友,查明,王绪龙,等.准噶尔盆地构造演化与动力学背景再认识[J].地球学报,2005,26(3):217-222.
[34]杨巍然,曾佐勋,李德威,等.板内地震过程的三层次构造模式[J].地学前缘,2009,16(1):206-217.
[2]王国灿,杨巍然.地质晚近时期山脉地区隆升及剥露作用研究[J].地学前缘,1998,5(1):151-156.
[3]潘保田,高红山,李吉均.关于夷平面的科学问题:兼论青藏高原夷平面[J].地理科学,2002,22(5):520-526.
[4]Fielding E J.Morphotectonic evolution of the Himalayas and Tibetan Plateau[M]∥Summerfield M A.Geomorphology and Global Tectonics.London:John Wiley&Sons Press Ltd.,2000:201-222.
[5]任纪舜.昆仑—秦岭造山系的几个问题[J].西北地质,2004,37(1):1-5.
[6]王树基.亚洲中部山地夷平面研究:以天山山系为例[M].北京:科学出版社,1998:1-152.
[7]Zhou S Z,Xu L B,Cui J X,et al.Geomorphologic evolution and environmental change in the Shaluli Mountain region during the Quaternary[J].Chinese Science Bulletin,2005,50(1):52-57.
[8]王宗秀,李涛.新疆博格达山链新生代再生造山机理:岩石圈内切层“开”“合”造山的典型代表[J].地质通报,2004,23(3):289-293.
[9]Zhao Z J,Fang X M,Li J J,et al.Paleomagnetic dating of the Jiuquan Gravel in the Hexi Corridor:Implication on midPleistocene uplift of the Qinghai-Tibetan Plateau[J].Chinese Science Bulletin,2001,46(23):2001-2005.
[10]陈宣华,李丽,尹安,等.东昆仑造山带多期隆升历史的地质热年代学证据[J].地质通报,2011,31(11):1647-1660.
[11]郭召杰,张志诚,吴朝东,等.中、新生代天山隆升过程及其与准噶尔、阿尔泰山比较研究[J].地质学报,2006,80(1):1-15.
[12]李传新,郭召杰.晚新生代天山北缘构造变形定量研究[J].地质科学,2011,46(3):709-722.
[13]李玮.准噶尔西北缘造山带中生代盆地形成机制及构造演化[D].北京:中国地质科学院地质研究所,2007.
[14]肖序常,罗照华.西昆仑及邻区岩石圈结构构造化:塔里木南—西昆仑多学科地学断面简要报道[J].地质通报,2002,21(2):63-68.
[15]高红山,潘保田,邬光剑,等.祁连山东段剥蚀面与青藏高原隆升[J].冰川冻土,2004,26(5):540-544.
[16]王岸,王国灿.构造地貌及其分析方法评述[J].地质科技情报,2005,24(4):7-20.
[17]杨景春,李有利.地貌学原理[M].北京:北京大学出版社,2001.
[18]李容全,邱维理.地文期与地文期研究[J].第四纪研究,2005(6):676-685.
[19]Ojany F F.Erosing and planation surface in Machakos-Kitui area of Kenya[J].GeoJournal,1978,2(4):289-294.
[20]任雪梅,陈忠,罗丽霞,等.夷平面研究综述[J].地理科学,2003,23(1):107-111.
[21]吴忱,张秀清,马永红.再论华北山地甸子梁期夷平面及早第三纪地文期[J].地理学与国土研究,1997,13(3):39-46.
[22]赵洪壮,李有利,杨景春,等.基于DEM数据的北天山地貌形态分析[J].地理科学,2009,29(3):445-449.
[23]杨昕,汤国安,刘学军,等.数字地形分析的理论、方法与应用[J].地理学报,2009,64(9):1058-1070.
[24]Kuhni A,Pfiffner O A.The relief of the Swiss Alps and adjacent areas and its relation to lithology and structure:Topographic analysis from a 250 m DEM[J].Geomorphology,2001(4):285-307.
[25]Dong W J,Tang M C.A numerical modeling study on the processes of uplift and planation of the Tibetan Plateau[J].Science in China:Series D,1997,40(3):246-250.
[26]洪顺英,申旭辉,荆凤,等.基于SRTM-DEM的阿尔泰山构造地貌特征分析[J].国土资源遥感,2007,73(3):62-66.
[27]朱永峰,王涛,徐新.新疆及邻区地质矿产研究进展[J].岩石学报,2007,23(8):1785-1789.
[28]肖序常,汤耀庆,李锦铁,等.古中亚复合巨型缝合带南缘构造演化[M].北京:北京科学技术出版社,1991.
[29]彭希龄.新疆新构造运动的表现和特点[J].成都理工学院学报,1998,25(2):169-181.
[30]柏美祥.新疆河谷阶地的年代[J].内陆地震,1998,12(1):13-19.
[31]冯锐,马宗晋,方剑,等.发展中的板块边界:天山—贝加尔活动构造带[J].地学前缘,2007,14(4):1-17.
[32]马宗晋,曲国胜,陈新发.准噶尔盆地深浅构造分析及油气展布规律[J].新疆石油地质,2008,29(4):411-414.
[33]吴孔友,查明,王绪龙,等.准噶尔盆地构造演化与动力学背景再认识[J].地球学报,2005,26(3):217-222.
[34]杨巍然,曾佐勋,李德威,等.板内地震过程的三层次构造模式[J].地学前缘,2009,16(1):206-217.
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