Development of Carbonate Platform and Its Response to Cenozoic Tectonic in Reed Bank Area, the South China Sea
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摘要: 为了探索碳酸盐台地在海盆演化过程中的作用，对南海南部礼乐滩区域碳酸盐台地的发育及其与新生代构造沉降特征的相关性进行研究.对多道地震数据的分析表明：在研究区广泛发育包括碳酸盐台地和生物礁在内的碳酸盐沉积，其发育时间主要集中在晚渐新世至早中新世期间，在中中新世后开始退积和淹没.通过对穿越礼乐滩区的两条NW-SE向测线NH973-2和DPS93-2的构造沉降反演，进行沉降量、沉降速率计算和构造分析.结果表明：沉降速率及沉降量随不同时期的构造活动而发生变化，可分为缓慢沉降期(古新世-早渐新世，张裂阶段)、隆升剥蚀期(晚渐新世-早中新世，漂移阶段)、加速沉降期(早中新世末期，后漂移阶段1)、强烈沉降期(中新世，后漂移阶段2)和稳定沉降期(晚中新世至今，后漂移阶段3)5个发育期.碳酸盐台地的发育期和南海海盆的漂移阶段相对应，构造沉降的分析表明该期间具有构造抬升作用，其与相对上升的海平面结合有利于碳酸盐沉积的发育.在南海扩张期间主地幔对流的控制下，南部陆缘区礼乐地块和礼乐滩盆地之间较大的地壳厚度差异会导致侧向上地温梯度的差异，从而形成礼乐滩盆地之下的次生对流.该次生对流控制了研究区在晚渐新世至早中新世期间的隆升剥蚀作用.Abstract: In order to research the role of carbonate platform in the evolution of basin, the development of the carbonate platform and its correlation with the Cenozoic tectonic subsidence characteristics in the Reed Bank area in the southern South China Sea are explored in this study. The rate and amount of tectonic subsidence, and the tectonics are analyzed on the basis of two multi-channel seismic profiles across the Reed Bank area in NW-SE direction. Detailed seismic interpretations prove the occurrence of a wide distributed carbonate platform developed between the Late Oligocene to Early Miocene, which was submerged after the Middle Miocene. Reconstruction of the tectonic subsidence history shows that the tectonic subsidence was controlled by the tectonic activities in different periods, and could be divided into 5 episodes: the slow subsidence episode (Paleocene to Early Oligocene, rifting stage), the uplift and erosion episode (Late Oligocene to Early Miocene, drifting stage), the accelerating subsidence episode(the latest Early Miocene, post-drift stage 1), the intensive subsidence episode(Miocene, post-drift stage 2), and the steady subsidence episode (Late Miocene to present, post-rift stage 3). The development stage of the carbonate platform was consistent with the drifting stage of the South China Sea, during which the tectonic subsidence analysis suggests an uplift and erosion characteristics. This stable shallow water environment was favorable to the development of carbonates. During the drifting stage, large-scale mantle under the oceanic basin and the lateral temperature gradients under the continental margin might have triggered a secondary mantle convection under the rifted Reed Bank basin, resulting in the uplift and erosion activities in this stage, and the wide-development of carbonate platform.
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Key words:
- the South China Sea /
- Reed Bank area /
- carbonate platform /
- tectonics /
- secondary convection
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图 1 南海南部陆缘地貌特征和地震测线位置
黑线为研究区测线位置，红圈为钻井位置，黑色虚线为盆地边界，黄色虚线为洋陆边界
Fig. 1. Morphological features of the Reed Bank and the adjacent areas
图 2 礼乐滩区域新生代层序界面时代，岩性及主要构造事件
Fig. 2. The Cenozoic sequence boundaries, lithology and major tectonic events in Reed Bank area
图 3 南海南部穿越礼乐滩区域的两条NW-SE向多道地震测线地质解释(虚框为本文构造沉降研究所取的区域)
a.多道地震测线NH973-2地质解释；b.多道地震测线DPS93-2地质解释
Fig. 3. The interpretation of two multi-channel seismic profiles across the Reed Bank area in NW-SE direction in southern South China Sea
图 4 NH973-2测线选中区域原始地震剖面(a)和地质解释(b)
Fig. 4. Typical original seismic section (a) and its geological interpretation (b) of the seismic section of NH973-2
图 5 DPS93-2测线选中区域原始地震剖面(a)和地质解释(b)
Fig. 5. Typical original seismic section (a) and its geological interpretation (b) of the seismic section of DPS93-2
图 6 地震剖面中典型碳酸盐识别特征及Sampagita-1井岩性
a, b, c.NH973-2测线北部地层层序及碳酸盐识别特征；d.礼乐滩区Sampagita-1井岩性, 钻井数据来自Steuer et al.(2014)
Fig. 6. Typical identification of characteristics of carbonate in seismic section and the lithology of the well of Sampagita-1
图 7 研究区NH973-2(a)和DPS93-2(b)两条多道地震测线时深转换
a, b.沉降量和沉降速率计算相应的横坐标位置
Fig. 7. Time-depth conversions of the multi-channel seismic sections, NH973-2 (a) and DPS93-2 (b)
图 8 礼乐滩区域两条测线的构造沉降
a.NH973-2测线的沉降量和沉降速率; b.DPS93-2测线的沉降量和沉降速率; c.NH973-2测线和DPS93-2测线上所选取的8个点(①~⑧)的沉降速率和平均沉降速率柱状图
Fig. 8. Tectonic subsidence of two profiles in Reed Bank area
图 9 礼乐滩区域NH973-2(a)和DPS93-2(b)测线的构造沉降史曲线(斜率为平均沉降速率)
①构造沉降；②总沉降
Fig. 9. Tectonic subsidence curve of profile NH973-2 (a) and DPS93-2 (b) in Reed Bank area
表 1 古水深分布
Table 1. The distribution of paleo-water depth
反射界面 Tg T70 T60 T40 T32 T20 T0 地质时代(Ma) 65.0 32.0 19.0 15.3 10.5 5.5 0 古水深(m) 0 100.00 50.00 352.96 745.98 1 155.38 1 605.72 注：表中数据来自文献(丁巍伟等, 2011). 
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表 2 南海南部时速统计
Table 2. Time-speed statistics in southern South China Sea
TWT(s) Vn(km·s-1) TWT(s) Vn(km·s-1) TWT(s) Vn(km·s-1) TWT(s) Vn(km·s-1) 0.0 1 500 1.8 2 244 3.6 2 928 5.6 3 414 0.2 1 510 2.0 2 330 3.8 2 989 5.8 3 453 0.4 1 550 2.2 2 418 4.0 3 044 6.0 3 492 0.5 1 600 2.4 2 494 4.1 3 068 6.2 3 529 0.6 1 646 2.5 2 532 4.3 3 120 6.4 3 578 0.8 1 775 2.6 2 577 4.5 3 164 6.6 3 621 1.0 1 900 2.8 2 642 4.6 3 187 6.8 3 662 1.2 1 993 3.0 2 720 4.8 3 238 7.0 3 700 1.4 2 071 3.2 2 800 5.0 3 280 1.5 2 107 3.4 2 871 5.2 3 327 1.6 2 144 3.5 2 891 5.4 3 370
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表 3 各层岩性参数统计
Table 3. Statistics of lithologic parameters of each layer
反射层 各层岩性(%) 各层岩性参数 泥岩 砂岩 灰岩 rho_G(kg/m3) SurPor CC(m) T20~T0 48.4 28.5 23.1 2 698 0.61 0.000 49 T32~T20 36.6 25.9 37.5 2 698 0.62 0.000 52 T40~T32 29.9 9.6 60.5 2 707 0.66 0.000 61 T60~T40 18.2 18.8 63.0 2 701 0.65 0.000 59 T70~T60 18.2 13.3 68.5 2 704 0.66 0.000 62 Tg~T70 62.6 34.6 2.8 2 695 0.58 0.000 43 注：表中数据来自赵中贤等(2010)，其中，rho_G为岩性颗粒密度，SurPor为孔隙度，CC为压实常数.
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