冲绳海槽宫古段中央地堑的形态与分布
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摘要
采用中国科学院海洋研究所“科学1号”调查船及国家海洋局“向阳红9号”调查船最近几年在冲绳海槽宫古段进行海底地形及反射地震调查所取得的数据,首次详细展示了冲绳海槽宫古段南北长约200km区域内中央地堑的形态及空间展布特征。本文给出的成果大大加深了关于冲绳海槽中央地堑各种变化的认识。指出,按照形态,中央地堑分为U型、V型和半地堑三种。其中大部分中央地堑为U型地堑。地堑的深度40～250m,宽度6～14km,长度17～33km。冲绳海槽宫古段的最大水深为2244.4m,位于中央地堑城阳段北端底部靠东的一侧(125°19.3′E,25°49.8′N)。本研究区的中央地堑可分为断续的9段,从东北向西南大致呈右旋雁行排列。但黄岛段相对于崂山段,城阳段相对于莱西段,李仓段相对于城阳段又稍微向西偏出,呈现为左旋雁行排列。地堑的走向一般为N60°E左右,相对于冲绳海槽的走向更偏向于东西方向,偏角在15°左右。各段中央地堑是被NW向断裂错开的。这些断裂在海底表现为明显的海底断崖地貌和陡沟地貌,在地震剖面上表现为明显的地层错位,其错位的幅度往往老地层比新地层要大。根据地震剖面分析,这些NW向的断裂应该是走滑性质的。本文展示的中央地堑在形态上和空间展布形式上都和扩张洋脊类似。莱西段和城阳段中央地堑之间重叠地堑,在形式上也类似于扩张洋脊的重叠扩张中心。从地堑深度较浅并发育重叠地堑来分析,冲绳海槽的扩张速率应当介于慢速扩张和中速扩张之间。本研究区莱西段、即墨段和平度段海底地形相对较高,中央地堑深度变浅,并发育重叠中央地堑,应该相当于快速扩张大洋中脊的轴高,可能是正在孕育岩浆活动的位置。目前我们所观测到的中央地堑的错断和有规律的排列说明海槽的主体演化过程已经在拉张盆地和断陷盆地的基础上上升到一个更高的阶段。本文根据中央地堑的展布形式、重叠中央地堑,及其两侧中央地堑中的海底山推测此区域海底扩张可能正在进行。
Based on geophysical data obtained by R/V “Science 1” of Institute of Oceanology, Chinese Academy of Sciences (IOCAS) and R/V “Xiangyanghong No.9” of State Oceanic Administration (SOA) in a 200 km long area of Okinawa Trough Miyoko Section recent years, we show the topography and distribution of central graben in great detail for the first time. Central graben within Miyoko Section is separated into 9 discontinuous segments by strike slip faults, from north to south namely Laoshan, Huangdao, Jiaonan, Jiaozhou, Pingdu, Jimo, Laixi, Chengyang and Licang Segment respectively, and shows a dextral echelon pattern in general. By cross shapes, three types of central graben can be distinguished, namely U type, V type and half graben. U type is the most common central graben among those found in our study area. The depth of central graben is from 40 m to 250 m, wide from 6 km to 14 km, length from 17 km to 33 km. The largest water depth of Miyoko Section is 2244.4 m, found at the east side of north end bottom of Chengyang Segment (125°19.3′E, 25°49.8′N). Within the dextral echelon pattern, Huangdao, Chengyang, Licang Segment moves to the west relatively to Laoshan, Laixi and Chengyang Segment respectively, showing a local sinistral echelon pattern. The striking direction of central graben is N60°E roughly, that is 15°more to the east comparing to the striking of the Okinawa Trough. There is 6 km long overlap distance between Laixi Segment and Chengyang Segments, simile with an overlap spreading center in the Mid-Ocean Ridge. The topography and distribution of central graben we show in this paper is simile with that of low spreading mid-ocean ridge, but the shallow graben depth and overlap graben indicate that they are simile with the fastest end of low spreading mid-ocean ridge. Based on the shallow central graben and high topography of Laixi, Jimo and Pingdu Segments and the development of overlap graben, we believe that those segment are simile with fast spreading axis high, and probably are places where magma is developing, and sea floor spreading is possibly on going along the central graben of Okinawa Trough.
Based on geophysical data obtained by R/V “Science 1” of Institute of Oceanology, Chinese Academy of Sciences (IOCAS) and R/V “Xiangyanghong No.9” of State Oceanic Administration (SOA) in a 200 km long area of Okinawa Trough Miyoko Section recent years, we show the topography and distribution of central graben in great detail for the first time. Central graben within Miyoko Section is separated into 9 discontinuous segments by strike slip faults, from north to south namely Laoshan, Huangdao, Jiaonan, Jiaozhou, Pingdu, Jimo, Laixi, Chengyang and Licang Segment respectively, and shows a dextral echelon pattern in general. By cross shapes, three types of central graben can be distinguished, namely U type, V type and half graben. U type is the most common central graben among those found in our study area. The depth of central graben is from 40 m to 250 m, wide from 6 km to 14 km, length from 17 km to 33 km. The largest water depth of Miyoko Section is 2244.4 m, found at the east side of north end bottom of Chengyang Segment (125°19.3′E, 25°49.8′N). Within the dextral echelon pattern, Huangdao, Chengyang, Licang Segment moves to the west relatively to Laoshan, Laixi and Chengyang Segment respectively, showing a local sinistral echelon pattern. The striking direction of central graben is N60°E roughly, that is 15°more to the east comparing to the striking of the Okinawa Trough. There is 6 km long overlap distance between Laixi Segment and Chengyang Segments, simile with an overlap spreading center in the Mid-Ocean Ridge. The topography and distribution of central graben we show in this paper is simile with that of low spreading mid-ocean ridge, but the shallow graben depth and overlap graben indicate that they are simile with the fastest end of low spreading mid-ocean ridge. Based on the shallow central graben and high topography of Laixi, Jimo and Pingdu Segments and the development of overlap graben, we believe that those segment are simile with fast spreading axis high, and probably are places where magma is developing, and sea floor spreading is possibly on going along the central graben of Okinawa Trough.
引文
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梁瑞才,吴金龙,刘保华,王勇.2001.冲绳海槽中段线性磁条带异常及其构造发育.海洋学报,23(2):69～78.
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LinJ.1992.ThesegmentedMid-AtlanticRidge.Oceanus,34:9～16.
MacdonaldKC,ScheirerDS,CarbotteSM.1991.Mid-oceanridges:discontinuites,segmentsandgiantcracks.Science,253:986～994.
PerramLJ,MacdonaldKC.1990.Aone-millionyearhistoryofthe11°45′NEastPacificRisediscontinuity.JournalofGeophysicalResearch,95:21363～21381.
SibuetJC,LetouzeyJ,BarbierF,CharvetJ,FoucherJP,HildeTWC,KimuraM,ChiaoLY,MarssetB,MullerC,StephanJF.1987.BackarcextensionintheOkinawaTrough.JournalofGeophysicalResearch,92:14041～14063.
SempereJC,PurdyGM,SchoutenH.1990.SegmentationoftheMid-AtlanticRidgebetween24°Nand30°40′N.Nature,334:427～431.
SpencerS,SmithDK,CannJR,LinJ,McallisterE.1979.Structureandstabilityofnon-transformdiscontinuitiesontheMid-AtlanticRidgebetween24°Nand30°N.MarineGeophysicalResearch,19:339～362.
ZierenbergRAKoskiRAMortonJLBouseRMShanksWC1993.Genesisofmassivesulfidedepositsonasediment-coveredspreadingcenter,EscanabaTrough,41°N,GordaRidge.EconomicGeology,88:2069～2098.
李乃胜.1990.冲绳海槽的地质构造属性.海洋与湖沼,19(4):437～358.
梁瑞才,吴金龙,刘保华,王勇.2001.冲绳海槽中段线性磁条带异常及其构造发育.海洋学报,23(2):69～78.
栾锡武.2006.热液活动和洋脊扩张速率的关系及其在冲绳海槽的应用.海洋地质与第四纪地质,26(2):156～165.
翟世奎,干晓群.1995.冲绳海槽海底热液活动区玄武岩的矿物学和岩石化学特征及其地质意义.海洋与湖沼,26(2):115～123.
BalluVS,HikdebrandJA,WebbSC.1998.SeafloorgravityevidenceforhydrothermalalterationofthesedimentsinMiddleValley,JuandeFucaRidge.MarineGeology,150:99～111.
HermanBM,AndersonRN,TruchanM.1978.ExtensionalTectonicsintheOkinawaTrough.A.A.P.G.Mem.,29:119～208.
JinXianglong,YuPuzhi.1987.StructureandTectonicEvolutionoftheOkinawaTrough.ScienticSinica,Seri31(5):614～623.
KimuraM,FurukawaM,IzawaE,IshikawaM,KuramotoS,SakaiH,UyedaS,MakrisJ.1991.ReportonDELP1988cruisesintheOkinawaTroughpart7.GeologicinvestigationofthecentralriftinthemiddletosouthernOkinawaTrough.Bull.EarthquakeResearch,Inst.Univ.Tokyo,66:179～209.
LeeCS,JrShorGG,BibeLD.1980.OkinawaTrough:Originofaback-arcbasin.MarineGeology,35:219～241.
LinJ.1992.ThesegmentedMid-AtlanticRidge.Oceanus,34:9～16.
MacdonaldKC,ScheirerDS,CarbotteSM.1991.Mid-oceanridges:discontinuites,segmentsandgiantcracks.Science,253:986～994.
PerramLJ,MacdonaldKC.1990.Aone-millionyearhistoryofthe11°45′NEastPacificRisediscontinuity.JournalofGeophysicalResearch,95:21363～21381.
SibuetJC,LetouzeyJ,BarbierF,CharvetJ,FoucherJP,HildeTWC,KimuraM,ChiaoLY,MarssetB,MullerC,StephanJF.1987.BackarcextensionintheOkinawaTrough.JournalofGeophysicalResearch,92:14041～14063.
SempereJC,PurdyGM,SchoutenH.1990.SegmentationoftheMid-AtlanticRidgebetween24°Nand30°40′N.Nature,334:427～431.
SpencerS,SmithDK,CannJR,LinJ,McallisterE.1979.Structureandstabilityofnon-transformdiscontinuitiesontheMid-AtlanticRidgebetween24°Nand30°N.MarineGeophysicalResearch,19:339～362.
ZierenbergRAKoskiRAMortonJLBouseRMShanksWC1993.Genesisofmassivesulfidedepositsonasediment-coveredspreadingcenter,EscanabaTrough,41°N,GordaRidge.EconomicGeology,88:2069～2098.
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