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1.
本文根据反射地震、折射地震、磁力等资料，结合周边地质，探讨冲绳海槽南段基底组成。在海槽周边的东海陆架盆地、台湾褶皱带和琉球岛弧褶皱带，均出露不同程度变质的晚古生代、中生代和早第三纪地层。多道反射地震表明，海槽南段沉积盖层由上第三系和第四系组成，声学基底由下第三系及更老地层构成。邻近海槽的折射地震揭示，除第四系-中新统速度层之外，还存在纵波速度分别为4．7～5．3km／s和6．3km／s的下第三系和中生界速度层。磁异常分析和正反演拟合计算结果表明，海槽磁性基底主要由变质岩系构成，次为燕山期中酸性岩浆岩和喜山期中基性岩浆岩，磁性基底大部分相当声学基底。综合分析表明，海槽南段基底主要由不同程度变质的下第三系、中生界和上古生界构成；在海槽某些构造部位，已有喜山期基性岩浆岩形成。  相似文献   

2.
冲绳海槽南段基底组成分析   总被引：9，自引：3，他引：6  
根据反射地震、折射地震和磁力等资料,结合周边地质,探讨冲绳海槽南段基底组成。在海槽周边的东海陆架盆地、台湾褶皱带和琉球岛弧褶皱带,发育不同程度变质的晚古生代、中生代和早第三纪地层。多道反射地震表明,海槽南段沉积盖层由上第三系和第四系组成,声学基底由下第三系及更老地层构成。邻近海槽南段的折射地震揭示,除第四系．中新统速度层之外,还存在纵波速度分别为4．7—5．3km／s和6．3km／s的下第三系和中生界速度层。磁力异常分析和正反演拟合计算结果表明,海槽磁性基底主要由变质岩系构成,次为燕山期中酸性岩浆岩和喜山期中基性岩浆岩,磁性基底大部分相当声学基底。综合分析表明,海槽南段基底主要由不同程度变质的下第三系、中生界和上古生界构成;在海槽某些构造部位,已有喜山期基性岩浆岩形成。  相似文献   

3.
东海莫霍面起伏与地壳减薄特征初步分析   总被引：3，自引：0，他引：3  
收集、整理大量由地震剖面提供的沉积层厚度资料,得到东海沉积层等厚图。对完全布格重力异常进行沉积层重力效应改正后,得到剩余重力异常,利用地震资料揭示的莫霍面深度值来约束界面反演得到东海莫霍面埋深。结果表明,东海陆架盆地莫霍面深度在25～28 km之间平缓变化,地壳厚度为14～26 km,西厚东薄;冲绳海槽盆地莫霍面深度为16～26 km,地壳厚度为12～22 km,北厚南薄。东海陆架盆地东部与冲绳海槽盆地南部地壳减薄明显,拉张因子分别达到2.6和3。初步分析认为冲绳海槽地壳以过渡壳为主,并未形成洋壳。  相似文献   

4.
区域性大断裂(东海盆地西缘断裂)以东的磁性基底深度一般为7—10公里,并向断裂方向加深。推测基底以上的地层可能有数公里至近10公里弱磁性的、已固结或浅变质的前中新世岩层存在。 区域性大断裂以西区域,可能存在两个磁性层,即一个为中生代岩浆侵入体和近地表浅层覆盖的火山岩层;另一个磁性层则位于更深处。两个磁性层之间可能包含中生界中早期及前中生界的巨厚弱磁性变质岩系。 在两条与海岸近于平行的基底深拗陷带之间是一条基底相对隆起带,是深断裂岩浆活动的产物。 三条带的延伸,向北可能终止于东福山北东东向断裂带,向南则可能与福建省海岸平行至少延至台湾海峡南端。  相似文献   

5.
利用东海及邻域最新的磁力异常数据,分析东海的磁场特征,并利用该磁力数据计算东海的磁性基底界面,分析解释磁性界面的特征及地质特征。研究表明,从陆区、陆架盆地到冲绳海槽中部,磁力异常呈正负相间变化,最大值出现在福建沿海地区;磁性基底深度在4～11km之间变化。从冲绳海槽中部到琉球群岛,磁异常从正磁异常变为负磁异常;磁性基底深度为7～12km之间变化。从琉球弧前盆地到琉球海沟,磁力异常为正负相间变化,中部磁异常为负值,两侧异常为正值;磁性基底深度为7.5～11km之间变化。  相似文献   

6.
南冲绳海槽及其邻域的基底断裂构造   总被引：1，自引：1，他引：0  
林长松 《海洋学报》1999,21(1):61-70
EW、NEE和NE向基底断裂沿主构造线方向展布,多属张性断裂.基底大断裂宏观上形成和控制了各主构造带的基本构造格架和各具特色的地质构造发育.它们的形成与弧后地慢流上涌和岛弧的旋张掀斜运动而出现的海槽张裂运动密切相关.NW、NNW和NW向基底断裂多属张扭性平移断层.它们对主构造带分割断错,形成和控制了次一级构造区块各具特色的地球物理和地质构造特征.宫古断裂带长期活动,作用十分强烈.它们的形成是由于受来自菲律宾海方向的水平应力作用,地壳作破坏性应力调整的结果.  相似文献   

7.
南海中部地震反射波特征及其地质解释   总被引：8，自引：2，他引：6  
刘建华 《海洋学报》2000,22(6):73-80
20世纪70年代以来,在南海中部海区开展了各种地震调查,为研究盖层和基底发育、断裂和岩浆活动、海盆成生演化提供了重要依据。在对南海中部海区4112km48道反射地震资料解释的基础上,识别出了T1,T2,T4,T6,Tg等五个反射界面;识别出了I～V五套地震反射层组,推测时代分别为上新世-第四纪、中新世晚期、中新世早-中期、渐新世和前渐新世。层组I～Ⅱ全区广布。在陆坡、岛坡区,层组Ⅲ以下层组主要见于断陷中;在深海盆,层组Ⅲ分布仍较广,除了在深海盆北段见到层组Ⅳ外,在西南次海盆剖面两缘也见到该层组。在东部次海盆剖面中还不同程度见到了双程反射时间为8.4～8.7s的莫霍面反射,埋深为10～12km,地壳厚度为6～8km.西南次海盆水深和新生界基底埋深均比深海盆北段除外的东部次海盆深,分别为4000-4300和5200～5500m.根据年龄和基底深度关系经验公式,计算西南次海盆基底年龄为距今51～39Ma.地震反射层组解释和年龄一基底深度关系计算表明,西南次海盆形成并非晚于东部次海盆,而是同时或早于东部次海盆。  相似文献   

8.
长昌凹陷位于琼东南盆地深水区,向东通过西沙海槽与南海西北次海盆相通,其近东西向的展布形态明显异于深水区其他凹陷的NE-NEE向形态,为了弄清其地壳结构,从而更好地分析凹陷的结构和演化机制,这里根据深反射地震资料、VSP资料和最新重力资料对长昌凹陷的地壳结构进行了综合地球物理模拟.结果显示:长昌凹陷北侧地壳厚度为22～24 km,南侧地壳厚度约20～22 km,从两侧向长昌凹陷中央地壳厚度逐渐减薄,最薄处只有2.8 km;莫霍面深度与沉积基底呈镜像关系,沉积基底最深的地方莫霍面深度最浅,最浅深度距海平面13.8 km;凹陷中央东部存在一层厚约4 km的下地壳高速层,该层在地震剖面和层速度剖面上均可识别.  相似文献   

9.
湄公盆地的形成是南海北部陆缘地壳发生伸展作用的结果。其构造演化上总体可以分为基底形成、裂谷初期及其裂谷期、热沉降阶段Ⅰ和热沉降阶段Ⅱ共4个阶段;盆地基底中发育大量断裂构造,从断裂的走向来看可以分为4组:NE、NEE、NW和NWW走向;盆地的地温梯度值为32℃/km;发育中中新世和大约5Ma前后两次玄武质火山活动。湄公盆地基底由晚中生代侵入岩、火山岩和变质沉积岩组成,基底之上从始新统一直到第四系均有发育。盆地古近纪期间的沉积作用处于开阔海的状态,沉积物主要通过湄公河供给,沉积物厚度较大;中中新世期间,以河流-湖相浊积岩-滨、浅湖相-三角洲沉积体系为主,沉积物厚度较大,主体超过2000m,沉积中心——白虎油田附近沉积厚度超过4000m;晚中新世-第四纪期间,以海相沉积体系为主,沉积物厚度明显减薄,主体在1500m左右,最大沉积厚度为3000m。  相似文献   

10.
本文利用南通幅区域地质调查的重磁异常数据,在重磁异常特征分析的基础上,采用一维频谱分析法对南黄海进行磁性基底反演。结果表明:南黄海属于扬子块体向海域的延伸,具有元古代结晶基底和古生代褶皱基底的双基底结构,其磁性基底深度在2—10km之间变化,是褶皱基底与磁性层最小埋深的结合,在坳陷和隆起上表现不同。通过利用综合地质和地球物理综合方法,对南黄海区域的四大构造单元华北—狼林地块、扬子—京畿地块、华南—岭南地块、东海大陆架进行重磁异常变化特征和磁性基底特征分析,为研究区断裂等区域构造特征解释提供了依据。  相似文献   

11.
黄海含油气盆地区域地质与大地构造环境   总被引：25，自引：4，他引：25  
概述了黄海含油气盆地的区域地质背景和大地构造环境，对盆地内的油气勘探现状和远景进行了简要的评价。  相似文献   

12.
南海区域岩石圈的壳-幔耦合关系和纵向演化   总被引：11，自引：2，他引：11  
南海区域岩石圈由地壳层和上地幔固结层两部分组成。具典型大洋型地壳结构的南海海盆区莫霍面深度为９～１３ｋｍ,并向四周经陆坡、陆架至陆区逐渐加深;陆缘区莫霍面一般为１５～２８ｋｍ,局部区段深达３０～３２ｋｍ,总体呈与水深变化反相关的梯度带;东南沿海莫霍面深约２８～３０ｋｍ,往西北方向逐渐增厚,最大逾３６ｋｍ。南海区域上地幔天然地震面波速度结构明显存在横向分块和纵向分层特征。岩石圈底界深度变化与地幔速度变化正相关;地幔岩石圈厚度与地壳厚度呈互补性变化,莫霍面和岩石圈底界呈立交桥式结构,具有陆区厚壳薄幔—洋区薄壳厚幔的岩石圈壳－幔耦合模式。南海区域白垩纪末以来的岩石圈演化主要表现为陆缘裂离—海底扩张—区域沉降的过程,现存的壳－幔耦合模式显然为岩石圈纵向演化产物,其过程大致可分为白垩纪末至中始新世的陆缘裂离、中始新世晚期至中新世早期的海底扩张和中新世晚期以来的区域沉降等三个阶段。  相似文献   

13.
Four uniformly spaced regional gravity traverses and the available seismic data across the western continental margin of India, starting from the western Indian shield extending into the deep oceanic areas of the eastern Arabian Sea, have been utilized to delineate the lithospheric structure. The seismically constrained gravity models along these four traverses suggest that the crustal structure below the northern part of the margin within the Deccan Volcanic Province (DVP) is significantly different from the margin outside the DVP. The lithosphere thickness, in general, varies from 110–120 km in the central and southern part of the margin to as much as 85–90 km below the Deccan Plateau and Cambay rift basin in the north. The Eastern basin is characterised by thinned rift stage continental crust which extends as far as Laxmi basin in the north and the Laccadive ridge in the south. At the ocean–continent transition (OCT), crustal density differences between the Laxmi ridge and the Laxmi basin are not sufficient to distinguish continental as against an oceanic crust through gravity modeling. However, 5-6 km thick oceanic crust below the Laxmi basin is a consistent gravity option. Significantly, the models indicate the presence of a high density layer of 3.0 g/cm3 in the lower crust in almost whole of the northern part of the region between the Laxmi ridge and the pericontinental northwest shield region in the DVP, and also below Laccadive ridge in the southern part. The Laxmi ridge is underlain by continental crust upto a depth of 11 km and a thick high density material (3.0 g/cm3) between 11–26 km. The Pratap ridge is indicated as a shallow basement high in the upper part of the crust formed during rifting. The 15 –17 km thick oceanic crust below Laccadive ridge is seen further thickened by high density underplated material down to Moho depths of 24–25 km which indicate formation of the ridge along Reunion hotspot trace.  相似文献   

14.
Gravity studies over the continental margin of the central west coast of India show a sediment thickness of 2–3 km on the shelf associated with deeper horst and graben structures, of 6 km in the shelf margin basin, and about 1 km in the deep sea. The upward trend in free-air gravity anomaly toward the deep sea region is interpreted as crustal thinning. Model studies indicate a 25-km-thick crust in the shelf region and a minimum of 18 km in the more offshore region. An abrupt magnetic signature change suggests differential basement depths in the shelf region. Major faulting in the region is confirmed in water depths of approximately 100–200 m.  相似文献   

15.
Magnetic zoning and seismic structure of the South China Sea ocean basin   总被引：2，自引：0，他引：2  
We made a systematic investigation on major structures and tectonic units in the South China Sea basin based on a large magnetic and seismic data set. For enhanced magnetic data interpretation, we carried out various data reduction procedures, including upward continuation, reduction to the pole, 3D analytic signal and power spectrum analyses, and magnetic depth estimation. Magnetic data suggest that the South China Sea basin can be divided into five magnetic zones, each with a unique magnetic pattern. Zone A corresponds roughly to the area between Taiwan Island and a relict transform fault, zone B is roughly a circular feature between the relict transform fault and the northwest sub-basin, and zones C, D, and E are the northwest sub-basin, the east sub-basin, and the southwest sub-basin, respectively. This complexity in basement magnetization suggests that the South China Sea evolved from multiple stages of opening under different tectonic settings. Magnetic reduction also fosters improved interpretation on continental margin structures, such as Mesozoic and Cenozoic sedimentary basins and the offshore south China magnetic anomaly. We also present, for the first time, interpretations of three new 2D reflection seismic traverses, which are of ~2,000 km in total length and across all five magnetic zones. Integration of magnetic and seismic data enables us to gain a better 3D mapping on the basin structures. It is shown that the transition from the southwest sub-basin to the east sub-basin is characterized by a major ridge formed probably along a pre-existing fracture zone, and by a group of primarily west-dipping faults forming an exact magnetic boundary between zones D and E. The northwest sub-basin has the deepest basement among the three main sub-basins (i.e., the northwest sub-basin, the southwest sub-basin, and the east sub-basin). Our seismic data also reveal a strongly faulted continent–ocean transition zone of about 100 km wide, which may become wider and dominated with magmatism or transit to an oceanic crust further to the northeast.  相似文献   

16.
In 2001 and 2002, Australia acquired an integrated geophysical data set over the deep-water continental margin of East Antarctica from west of Enderby Land to offshore from Prydz Bay. The data include approximately 7700 km of high-quality, deep-seismic data with coincident gravity, magnetic and bathymetry data, and 37 non-reversed refraction stations using expendable sonobuoys. Integration of these data with similar quality data recorded by Japan in 1999 allows a new regional interpretation of this sector of the Antarctic margin. This part of the Antarctic continental margin formed during the breakup of the eastern margin of India and East Antarctica, which culminated with the onset of seafloor spreading in the Valanginian. The geology of the Antarctic margin and the adjacent oceanic crust can be divided into distinct east and west sectors by an interpreted crustal boundary at approximately 58° E. Across this boundary, the continent–ocean boundary (COB), defined as the inboard edge of unequivocal oceanic crust, steps outboard from west to east by about 100 km. Structure in the sector west of 58° E is largely controlled by the mixed rift-transform setting. The edge of the onshore Archaean–Proterozoic Napier Complex is downfaulted oceanwards near the shelf edge by at least 6 km and these rocks are interpreted to underlie a rift basin beneath the continental slope. The thickness of rift and pre-rift rocks cannot be accurately determined with the available data, but they appear to be relatively thin. The margin is overlain by a blanket of post-rift sedimentary rocks that are up to 6 km thick beneath the lower continental slope. The COB in this sector is interpreted from the seismic reflection data and potential field modelling to coincide with the base of a basement depression at 8.0–8.5 s two-way time, approximately 170 km oceanwards of the shelf-edge bounding fault system. Oceanic crust in this sector is highly variable in character, from rugged with a relief of more than 1 km over distances of 10–20 km, to rugose with low-amplitude relief set on a long-wavelength undulating basement. The crustal velocity profile appears unusual, with velocities of 7.6–7.95 km s−1 being recorded at several stations at a depth that gives a thickness of crust of only 4 km. If these velocities are from mantle, then the thin crust may be due to the presence of fracture zones. Alternatively, the velocities may be coming from a lower crust that has been heavily altered by the intrusion of mantle rocks. The sector east of 58° E has formed in a normal rifted margin setting, with complexities in the east from the underlying structure of the N–S trending Palaeozoic Lambert Graben. The Napier Complex is downfaulted to depths of 8–10 km beneath the upper continental slope, and the margin rift basin is more than 300 km wide. As in the western sector, the rift-stage rocks are probably relatively thin. This part of the margin is blanketed by post-rift sediments that are up to about 8 km thick. The interpreted COB in the eastern sector is the most prominent boundary in deep water, and typically coincides with a prominent oceanwards step-up in the basement level of up to 1 km. As in the west, the interpretation of this boundary is supported by potential field modelling. The oceanic crust adjacent to the COB in this sector has a highly distinctive character, commonly with (1) a smooth upper surface underlain by short, seaward-dipping flows; (2) a transparent upper crustal layer; (3) a lower crust dominated by dipping high-amplitude reflections that probably reflect intruded or altered shears; (4) a strong reflection Moho, confirmed by seismic refraction modelling; and (5) prominent landward-dipping upper mantle reflections on several adjacent lines. A similar style of oceanic crust is also found in contemporaneous ocean basins that developed between Greater India and Australia–Antarctica west of Bruce Rise on the Antarctic margin, and along the Cuvier margin of northwest Australia.  相似文献   

17.
To reveal the basement-involved faults and deep structures of the West Philippine Basin (WPB), the gravitational responses caused by these faults are observed and analyzed based on the latest spherical gravity model: WGM2012 Model. By mapping the free-air and Bouguer gravity anomalies, several main faults and some other linear structures are located and observed in the WPB. Then, by conducting a 2D discrete multi-scale wavelet decomposition, the Bouguer anomalies are decomposed into the first- to eighth-order detail and approximation fields (the first- to eighth-order Details and Approximations). The first- to third-order Details reflect detailed and localized geological information of the crust at different depths, and of which the higher-order reflects gravity field of the deeper depth. The first- to fourth-order Approximations represent the regional gravity fields at different depths of the crust, respectively. The fourth-order Approximation represents the regional gravity fluctuation caused by the density inhomogeneity of Moho interface. Therefore, taking the fourth-order Approximation as input, and adopting Parker-Oldenburg interactive inversion, We calculated the depth of Moho interface in the WPB. Results show that the Moho interface depth in the WPB ranges approximately from 8 to 12 km, indicating that there is typical oceanic crust in the basin. In the Urdaneta Plateau and the Benham Rise, the Moho interface depths are about 14 and 16 km, respectively, which provides a piece of evidence to support that the Banham Rise could be a transitional crust caused by a large igneous province. The second-order vertical derivative and the horizontal derivatives in direction 0° and 90° are computed based on the data of the third-order Detail, and most of the basement-involved faults and structures in the WPB, such as the Central Basin Fault Zone, the Gagua Ridge, the Luzon-Okinawa Fault Zone, and the Mindanao Fault Zone are interpreted by the gravity derivatives.  相似文献   

18.
This paper presents actuality of investigation and study of the crustal structure characters of East China Sea at home and abroad. Based on lots of investigation and study achievements and the difference of the crustal velocity structure from west to east, the East China Sea is divided into three parts - East China Sea shelf zone, Okinawa Trough zone and Ryukyu arc-trench zone. The East China Sea shelf zone mostly has three velocity layers, i.e., the sediment blanket layer （the velocity is 5.8-5.9 km/s）, the basement layer （the velocity is 6.0-6.3 km/s）, and the lower crustal layer （the velocity is 6.8-7.6 km/s）. So the East China Sea shelf zone belongs to the typical continental crust. The Okinawa Trough zone is located at the transitional belt between the continental crust and the oceanic crust. It still has the structural characters of the continental crust, and no formation of the oceanic crust, but the crust of the central trough has become to thinning down. The Ryukyu arc-trench zone belongs to the transitional type crust as a whole, but the ocean side of the trench already belongs to the oceanic crust. And the northwest Philippine Basin to the east of the Ryukyu Trench absolutely belongs to the typical oceanic crust.  相似文献   

19.
The Omo basin in south western Ethiopia at the Kenyan boundary is a northern extension of the trans- boundary Turkana rift. It is an Early Pliocene north-south trending depression bounded on either side by normal faulting. The Omo river flows in the middle of the basin and empties itself at its southern end into Lake Turkana.The structural pattern of the Omo basin is determined from 2D and 3D analyses of the gravity field. The basin is an asymmetric half-graben formed by and localized within the NS/NNE trending Early Pliocene normal faults. It is built up on the older NW trending structures that were reactivated and affected the recent NS faults. Automatic depth determination techniques and 3D inversion are used to estimate depth to the basement and determine the sedimentary thickness. The results indicate over 4 km thick sediments were deposited over the graben.The Omo basin lies within the East African Rift system and appears to connect the generally NW trending oil-rich Muglad-Melut basins of south Sudan and the highly prospective and similarly trending Anza graben of Kenya. The Omo basin contains thick sequence of sediments and appears to be a promising future site of intensive hydrocarbon exploration.  相似文献   

20.
About 16,000 km of multichannel seismic (MCS), gravity and magnetic data and 28 sonobuoys were acquired in the Riiser-Larsen Sea Basin and across the Gunnerus and Astrid Ridges, to study their crustal structure. The study area has contrasting basement morphologies and crustal thicknesses. The crust ranges in thickness from about 35 km under the Riiser-Larsen Sea shelf, 26–28 km under the Gunnerus Ridge, 12–17 km under the Astrid Ridge, and 9.5–10 km under the deep-water basin. A 50-km-wide block with increased density and magnetization is modeled from potential field data in the upper crust of the inshore zone and is interpreted as associated with emplacement of mafic intrusions into the continental margin of the southern Riiser-Larsen Sea. In addition to previously mapped seafloor spreading magnetic anomalies in the western Riiser-Larsen Sea, a linear succession from M2 to M16 is identified in the eastern Riiser-Larsen Sea. In the southwestern Riiser-Larsen Sea, a symmetric succession from M24B to 24n with the central anomaly M23 is recognized. This succession is obliquely truncated by younger lineation M22–M22n. It is proposed that seafloor spreading stopped at about M23 time and reoriented to the M22 opening direction. The seismic stratigraphy model of the Riiser-Larsen Sea includes five reflecting horizons that bound six seismic units. Ages of seismic units are determined from onlap geometry to magnetically dated oceanic basement and from tracing horizons to other parts of the southern Indian Ocean. The seaward edge of stretched and attenuated continental crust in the southern Riiser-Larsen Sea and the landward edge of unequivocal oceanic crust are mapped based on structural and geophysical characteristics. In the eastern Riiser-Larsen Sea the boundary between oceanic and stretched continental crust is better defined and is interpreted as a strike-slip fault lying along a sheared margin.  相似文献   

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