南海北部琼东南盆地第四系陆架边缘轨迹迁移及深水沉积模式

doi:10.13745/j.esf.sf.2022.1.2

地学前缘 ›› 2022, Vol. 29 ›› Issue (4): 55-72.DOI: 10.13745/j.esf.sf.2022.1.2

南海北部琼东南盆地第四系陆架边缘轨迹迁移及深水沉积模式

马畅¹(), 葛家旺¹^,²^,^*(), 赵晓明¹^,², 廖晋³, 姚哲³, 朱继田³, 方小宇², 向柱¹

1.西南石油大学地球科学与技术学院, 四川成都 610500
2.南方海洋科学与工程广东省实验室(湛江), 广东湛江 524000
3.中海石油(中国)有限公司海南分公司, 海南海口 570100

收稿日期:2021-08-10 修回日期:2021-09-28 出版日期:2022-07-25 发布日期:2022-07-28
通讯作者: 葛家旺
作者简介:马畅(1997—),男,硕士研究生,主要从事沉积学方面研究工作。E-mail: swpumc@163.com
基金资助:
国家自然科学基金项目(42072183);国家自然科学基金项目(41902124);南方海洋科学与工程广东省实验室(湛江)资助项目“南海水合物富集规律及固态流化开采机理研究(一期)(ZJW-2019-03)

Quaternary Qiongdongnan Basin in South China Sea: Shelf-edge trajectory migration and deep-water depositional models

MA Chang¹(), GE Jiawang¹^,²^,^*(), ZHAO Xiaoming¹^,², LIAO Jin³, YAO Zhe³, ZHU Jitian³, FANG Xiaoyu², XIANG Zhu¹

1. School of Geoscience and Technology, Southwest Petroleum University, Chengdu 610500, China
2. Guangdong Laboratory of Southern Marine Science and Engineering-Zhanjiang, Zhanjiang 524000, China
3. Research Institute of Haikou Branch, CNOOC, Haikou 570100, China

Received:2021-08-10 Revised:2021-09-28 Online:2022-07-25 Published:2022-07-28
Contact: GE Jiawang

摘要/Abstract

摘要：

陆架边缘迁移轨迹综合受控于构造、物源、海平面和气候等多种因素,其迁移演化与深水沉积体系发育关系密切。陆架边缘迁移规律及沉积物输送体制与深水砂体预测是当前国际地学领域的热点议题。本文通过基于琼东南盆地新采集的高精度地震资料,定量表征了第四系陆架边缘轨迹,识别了低角度缓慢上升型、中等角度上升型和高角度急剧上升型等3类陆架边缘轨迹类型。2.4 Ma以来,陆架边缘轨迹时空演化可分为3个阶段且具有侧向差异性:2.4~1.9 Ma以低角度缓慢上升型为主,1.9~0.8 Ma西北部以低角度缓慢上升型为主,东北部则以中等角度上升型为主,0.8 Ma至今西北部以中等角度上升型为主,东北部以高角度急剧上升型为主。琼东南盆地第四系陆架边缘迁移轨迹研究表明:当陆架边缘轨迹角0°<α<4°时,陆坡区峡谷规模较小且下切浅,深海平原区发育多期大型海底扇沉积,块体搬运沉积(MTDs)较少;当4°<α<35°时,陆坡区峡谷规模有所增加,深海平原区海底扇沉积与块体搬运沉积均有出现;当35°<α<90°时,陆坡区峡谷发育较少但下切深,深水平原区沉积以大型块体搬运沉积为主,海底扇几乎不发育。琼东南盆地更新世以来气温不断下降,以及东亚冬季风的显著增强,物源供给增强加之海平面的下降进而导致了西北部陆架边缘表现为进积特征;研究区东北部的断裂活动频繁以及物源供给弱,导致了研究区东北部陆坡推进距离远远小于研究区西北部且发育多期次块体搬运沉积物。以上认识对南海北部陆架边缘体系及深水扇预测具有一定的理论意义。

关键词: 琼东南盆地, 第四系, 陆架边缘轨迹, 定量化表征, 深水沉积体系

Abstract:

The shelf-edge trajectory is comprehensively controlled by tectonics, sediment supply, sea level and climate, and its migration and evolution are closely related to the deep-water depositional systems. The shelf-edge clinoform stacking pattern, sediment-budget partition in deep-water areas and reservoir evaluations are current geoscience hot topics. Based on the newly acquired high-precision, high-density 2D seismic data of the Qiongdongnan Basin (QDNB), this paper quantitatively characterized the Quaternary shelf-edge trajectory and identified three trajectory types in QDNB: flat to slightly rising, moderately rising and steeply rising types. Since 2.4 Ma the temporal evolution of the shelf-edge trajectory in QDNB can be divided into three stages with lateral differences: 2.4-1.9 Ma, mainly the slightly rising type; 1.9-0.8 Ma, the slightly rising type in the western part and moderately rising type in the eastern part; 0.8 Ma-present, the moderately rising type in the western part and steeply rising type in the eastern part. The vertical migration of the shelf-edge trajectory is jointly controlled by the rise and fall of sea level caused by climate change and associated with sediment supply. The differences in tectonic activity and provenance supply lead to lateral variations of the shelf-edge trajectory and progradation or aggradation stacking patterns. According to the above studies, when the shelf-edge trajectory angle, α, is between 0° and 4°, the continental slope canyons are small-scaled and shallow mostly, with developments of multistage large-scale submarine fan deposits in the deep-water area but less mass-transport deposits (MTDs). When 4° <α< 35° the continental slope canyons increase in scale, with occurrences of both submarine fan deposits and MTDs. When 35°<α<90° a few but steep continental slope canyons are developed, along with developments of mainly large-scale MTDs in the deep-water plains, almost without submarine fan deposits. Since the Quaternary the temperature in QDNB continues to drop while the East Asian winter monsoon increases significantly, causing the sediment supply to increase; while decreasing sea level results in progradation at the northwestern shelf edge. In comparison, frequent fault activities and relatively low sediment supply at the northeastern shelf edge result in a much shorter slope advance distance and developments of multistage MTDs. Results of this study have theoretical significance for the predictions of continental shelf-edge system and deep-water deposition in QDNB and other basins.

Key words: Qiongdongnan Basin, Quaternary, shelf-edge trajectory, quantitative characterization, deep-water depositional system

中图分类号:

P736.21
P737

马畅, 葛家旺, 赵晓明, 廖晋, 姚哲, 朱继田, 方小宇, 向柱. 南海北部琼东南盆地第四系陆架边缘轨迹迁移及深水沉积模式[J]. 地学前缘, 2022, 29(4): 55-72.

MA Chang, GE Jiawang, ZHAO Xiaoming, LIAO Jin, YAO Zhe, ZHU Jitian, FANG Xiaoyu, XIANG Zhu. Quaternary Qiongdongnan Basin in South China Sea: Shelf-edge trajectory migration and deep-water depositional models[J]. Earth Science Frontiers, 2022, 29(4): 55-72.

图/表 16

图1 斜坡发育样式(a-c)与陆架边缘迁移轨迹样式(d-f)(改编自文献[4])

Fig.1 Slope development patterns (a-c) and shelf-edge trajectory migration patterns (d-f). Modified from [4].

表1 陆架边缘-深水体系沉积模式三端员类型及特征(据文献[4])

Table 1 List of the tri-factor combinations for various shelf-edge and deep-water depositional models. Modified after [4].

气候条件	物源供给	可容纳空间	沉积模式
寒冷干旱	低物源供给	低可容纳空间	陆坡发育砂岩、浊积岩,富含砂质的海底扇
		中可容纳空间	发育海底水道峡谷,泥质的斜坡和盆地平原
		高可容纳空间	深水区沉积大量泥质运输体系
	高物源供给	低可容纳空间	陆坡发育砂岩、浊积岩,富含砂质的海底扇
		中可容纳空间	发育浊积岩朵叶体、水道-天然堤复合体,三角洲前缘,高水位情况下的浊积扇朵叶-水道充填复合体的海底扇
		高可容纳空间	三角洲前缘和海侵形成的泥岩
温暖潮湿	低物源供给	低可容纳空间	陆坡发育厚层砂体,砂质盆底扇
	低物源供给	中可容纳空间	泥质陆坡、盆底扇平原
	高物源供给	低可容纳空间	分布面积广泛、厚度大、体积大的盆底扇,砂质河道充填
	高物源供给	中可容纳空间	砂泥交互的沉积体系,海底扇有浊积岩朵叶、水道充填,深水泥质沉积

图2 琼东南盆地构造划分及研究区位置图(引自文献[8])

Fig.2 Tectonic division in the Qiongdongnan Basin (QDNB) and the location of the study area. Adapted from [8].

图3 琼东南盆地新近纪—第四系地层综合柱状图(改编自[6,15])

Fig.3 Column diagram of the Neogene-Quaternary Qiongdongnan Basin. Modified from [6,15].

图4 琼东南盆地第四系层序界面特征(测线1和测线10位置见图2)

Fig.4 Sequence stratigraphic model of the Quaternary Qiongdongnan Basin showing the four sequence boundaries (see Fig.2 for survey line locations)

图5 斜坡地形及陆架边缘的形态特征和几何参数示意图

Fig.5 Slope topographic model illustrating the slope morphology (left) and geometric parameters for shelf edge (right)

图6 琼东南盆地第四系陆架边缘加积与进积距离交汇图(a)及各剖面陆架边缘轨迹角度统计图(b)

Fig.6 Scatter plots of shelf-edge accretion distance vs. progradation distance (a) and related shelf-edge trajectory angle statistics for the three stratigraphic sequences of the Quaternary Qiongdongnan Basin

图7 琼东南盆地第四系典型剖面陆架边缘轨迹迁移图(测线1和10见图2)

Fig.7 Sectional views of shelf-edge trajectory migrations on the profiles of survey lines 1 (a) and 10 (b) in the Quaternary Qiongdongnan Basin (survey line locations see Fig.2)

图8 琼东南盆地第四系陆架边缘加积距离统计图(a)及陆架边缘进积距离统计图(b)

Fig.8 Statistics of shelf-edge accretion (a) and progradation (b) distances for the three stratigraphic sequences of the Quaternary Qiongdongnan Basin

表2 琼东南盆地物源供给参数统计表

Table 2 Statistical table of sediment supply parameters for the Qiongdongnan Basin

测线	层位	A/m	P/m	R_a/ (m·Ma^-1)	R_p/ (m·Ma^-1)	F_c/ (m²·Ma^-1)
1	T27-T20	174.66	6 237.50	194.07	6 930.56	1 210.49
	T20-T14	243.34	11 362.50	243.34	11 362.50	2 764.95
	T14-T0	826.40	6 737.50	1 033.00	8 421.88	6 959.84
2	T27-T20	125.48	9 287.50	139.42	10 319.44	1 294.88
	T20-T14	354.60	8 712.50	354.60	8 712.50	3 089.45
	T14-T0	756.64	5 587.50	945.80	6 984.38	5 284.66
3	T27-T20	51.12	7 300.00	56.80	8 111.11	414.64
	T20-T14	369.52	10 650.00	369.52	10 650.00	3 935.39
	T14-T0	701.36	2 037.50	876.70	2 546.88	1 786.28
4	T27-T20	162.00	5 575.00	180.00	6 194.44	1 003.50
	T20-T14	293.84	9 212.50	293.84	9 212.50	2 707.00
	T14-T0	708.16	5 150.00	885.20	6 437.50	4 558.78
5	T27-T20	105.46	4 862.50	117.18	5 402.78	569.78
	T20-T14	105.36	8 362.50	105.36	8 362.50	881.07
	T14-T0	853.04	1 712.50	1 066.30	2 140.63	1 826.04
6	T27-T20	62.96	3 962.50	69.96	4 402.78	277.20
	T20-T14	199.40	4 175.00	199.40	4175.00	832.50
	T14-T0	988.44	1 587.50	1 235.55	1 984.38	1 961.44
7	T27-T20	58.68	3 600.00	65.20	4 000.00	234.72
	T20-T14	358.52	4 662.50	358.52	4 662.50	1 671.60
	T14-T0	768.80	1 225.00	961.00	1 531.25	1 177.23
8	T27-T20	263.76	2 850.00	293.07	3 166.67	835.24
	T20-T14	136.00	2 275.00	136.00	2 275.00	309.40
	T14-T0	751.48	2 675.00	939.35	3 343.75	2 512.76
9	T27-T20	79.52	4 812.50	88.36	5 347.22	425.21
	T20-T14	84.24	1 687.50	84.24	1 687.50	142.16
	T14-T0	768.48	1 187.5	960.60	1 484.38	1 140.71
10	T27-T20	95.64	2 387.50	106.27	2 652.78	253.71
	T20-T14	77.88	4 250.00	77.88	4 250.00	330.99
	T14-T0	768.04	25.00	960.05	31.25	24.00
11	T27-T20	95.32	3 387.50	105.91	3 763.89	358.77
	T20-T14	94.44	3 850.00	94.44	3 850.00	363.59
	T14-T0	762.44	987.50	953.05	1 234.38	941.14
12	T27-T20	123.28	612.50	136.98	680.56	83.90
	T20-T14	294.28	262.50	294.28	262.50	77.25
	T14-T0	647.92	150.00	809.90	187.50	121.49

表2 琼东南盆地物源供给参数统计表

Table 2 Statistical table of sediment supply parameters for the Qiongdongnan Basin

测线	层位	A/m	P/m	R_a/ (m·Ma^-1)	R_p/ (m·Ma^-1)	F_c/ (m²·Ma^-1)
1	T27-T20	174.66	6 237.50	194.07	6 930.56	1 210.49
	T20-T14	243.34	11 362.50	243.34	11 362.50	2 764.95
	T14-T0	826.40	6 737.50	1 033.00	8 421.88	6 959.84
2	T27-T20	125.48	9 287.50	139.42	10 319.44	1 294.88
	T20-T14	354.60	8 712.50	354.60	8 712.50	3 089.45
	T14-T0	756.64	5 587.50	945.80	6 984.38	5 284.66
3	T27-T20	51.12	7 300.00	56.80	8 111.11	414.64
	T20-T14	369.52	10 650.00	369.52	10 650.00	3 935.39
	T14-T0	701.36	2 037.50	876.70	2 546.88	1 786.28
4	T27-T20	162.00	5 575.00	180.00	6 194.44	1 003.50
	T20-T14	293.84	9 212.50	293.84	9 212.50	2 707.00
	T14-T0	708.16	5 150.00	885.20	6 437.50	4 558.78
5	T27-T20	105.46	4 862.50	117.18	5 402.78	569.78
	T20-T14	105.36	8 362.50	105.36	8 362.50	881.07
	T14-T0	853.04	1 712.50	1 066.30	2 140.63	1 826.04
6	T27-T20	62.96	3 962.50	69.96	4 402.78	277.20
	T20-T14	199.40	4 175.00	199.40	4175.00	832.50
	T14-T0	988.44	1 587.50	1 235.55	1 984.38	1 961.44
7	T27-T20	58.68	3 600.00	65.20	4 000.00	234.72
	T20-T14	358.52	4 662.50	358.52	4 662.50	1 671.60
	T14-T0	768.80	1 225.00	961.00	1 531.25	1 177.23
8	T27-T20	263.76	2 850.00	293.07	3 166.67	835.24
	T20-T14	136.00	2 275.00	136.00	2 275.00	309.40
	T14-T0	751.48	2 675.00	939.35	3 343.75	2 512.76
9	T27-T20	79.52	4 812.50	88.36	5 347.22	425.21
	T20-T14	84.24	1 687.50	84.24	1 687.50	142.16
	T14-T0	768.48	1 187.5	960.60	1 484.38	1 140.71
10	T27-T20	95.64	2 387.50	106.27	2 652.78	253.71
	T20-T14	77.88	4 250.00	77.88	4 250.00	330.99
	T14-T0	768.04	25.00	960.05	31.25	24.00
11	T27-T20	95.32	3 387.50	105.91	3 763.89	358.77
	T20-T14	94.44	3 850.00	94.44	3 850.00	363.59
	T14-T0	762.44	987.50	953.05	1 234.38	941.14
12	T27-T20	123.28	612.50	136.98	680.56	83.90
	T20-T14	294.28	262.50	294.28	262.50	77.25
	T14-T0	647.92	150.00	809.90	187.50	121.49

图9 琼东南盆地第四系陆架边缘加积速率(Ra)与进积速率(Rp)交汇图(a)及沉积物净通量(Fc)与进积速率(Rp)交汇图(b)

Fig.9 Scatter plots of shelf-edge accretion rate vs. progradation rate (a) and sediment net flux vs. progradation rate (b) in the eastern and western parts of the three stratigraphic sequences of the Quaternary Qiongdongnan Basin

图10 琼东南盆地2.4 Ma以来陆架边缘坡折线时空演化

Fig.10 Schematic diagram showing the temporo-spatial changes of shelf edge trajectories in the Qiongdongnan Basin since 2.4 Ma

图11 琼东南盆地第四系陆架边缘迁移轨迹控制因素(海平面变化据[20,37];物源供给据[30-31,34-35,44];构造沉降(以西北部为主)据[23-24];气候变化据[38,41⇓-43])

Fig.11 Factors controlling the shelf-edge trajectory in the Quaternary Qiongdongnan Basin. Data of sea level change from [20,37]; source supply from [30,31,34-35,44]; tectonic subsidence from [23-24]; climate change from [38,41⇓-43].

图12 琼东南盆地第四系典型剖面1原始剖面及沉积体系解释图(地震剖面1位置见图2)

Fig.12 Profile (top panel) and depositional interpretation (bottom panel) on the profile of survey line 1 in the Quaternary Qiongdongnan Basin (see Fig.2 for location of survey line 1)

图13 琼东南盆地第四系典型剖面6和10原始剖面及沉积体系解释图(地震剖面6和10位置见图2)

Fig.13 Depositional interpretations on the profiles of survey lines 6 (top panel) and 10 (bottom panel) in the Quaternary Qiongdongnan Basin (survey line locations shown in Fig.2)

图14 琼东南盆地第四系深水沉积对陆架边缘轨迹响应模式

Fig.14 Deepwater depositional mode in response to the shelf edge trajectory in Quaternary Qiongdongnan Basin

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南海北部琼东南盆地第四系陆架边缘轨迹迁移及深水沉积模式

Quaternary Qiongdongnan Basin in South China Sea: Shelf-edge trajectory migration and deep-water depositional models

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