晚第四纪亚洲大陆边缘海有机碳埋藏演化研究进展

张斌; 于兆杰; 徐兆凯; 康晓莹; 郭向前; 杨逸飞; 万世明

晚第四纪亚洲大陆边缘海有机碳埋藏演化研究进展

张斌^{1, 2,},
于兆杰^1, ,,
徐兆凯¹,
康晓莹^{1, 2},
郭向前^{1, 2},
杨逸飞^{1, 2},
万世明¹

1.
中国科学院海洋研究所，山东青岛 266071
2.
中国科学院大学，北京 100049

基金项目: 国家自然科学基金（42376055和W2421051），山东省自然科学优秀青年基金（ZR2022YQ33），国家重点研发计划（2022YFF0800503）。

详细信息

作者简介:
张斌（1997—），男，博士研究生，主要从事海洋沉积与古环境研究。E-mail：Zhangbin191@mails.ucas.ac.cn

通讯作者:
于兆杰（1988—），男，研究员，主要从事海洋沉积与古环境研究。E-mail：yuzhaojie@qdio.ac.cn

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出版历程
- 收稿日期: 2025-04-17
- 修回日期: 2025-06-24
- 网络出版日期: 2025-07-10

Advances in the Study of Organic Carbon Burial Evolution in the Marginal Seas off the Asian Continent during the Late Quaternary

Zhang Bin^{1, 2
,},
Yu Zhaojie^{1
, ,},
Xu Zhaokai¹,
Kang Xiaoying^{1, 2},
Guo Xiangqian^{1, 2},
Yang Yifei^{1, 2},
Wan Shiming¹

1.
Institute of Oceanology, Chinese Academy of Sciences, Qingdao 266071, China
2.
University of Chinese Academy of Sciences, Beijing 100049, China

摘要

摘要: 亚洲大陆边缘海是全球最典型的“源—汇”体系之一，揭示其在第四纪气候变化背景下的有机碳埋藏过程对理解全球碳循环演化具有重要意义。本文系统综述了亚洲主要边缘海沉积物中有机碳的来源、埋藏通量变化及其驱动机制。研究结果表明，冰期各边缘海中普遍表现出有机碳含量升高、埋藏通量增加的特征，且多数区域的总有机碳（TOC）含量、有机质碳同位素组成（δ¹³C_org）以及TOC/总氮（TOC/TN）比值呈现出轨道时间尺度旋回特征。从成因机制来看，海平面变化调控着陆源物质入海过程与强度，季风系统影响流域侵蚀与水体结构，而洋流与缺氧区分布则共同制约着区域碳汇效率的差异性演化。典型站位的沉积记录显示，冰期陆源物质输入量的增加、最小含氧带的发展或沉积速率的升高往往有利于有机碳在海底的保存与埋藏；但在部分高纬度或者深水海域（如鄂霍茨克海和日本海），冰期时海洋生产力的下降则减弱海底有机碳的埋藏效率。此外，本文还基于δ¹³C_org与TOC/TN比值等指标的联合分析，进一步量化了不同来源有机质的混合特征与演化历史，并通过有机碳埋藏通量的估算结果揭示了不同海域碳汇能力对冰期—间冰期旋回的响应程度。尽管当前已经取得上述重要进展，但在端元构建、指标标准化与高分辨率时空重建等方面仍存不小的挑战。本文认为，未来应加强跨区域对比、机制耦合建模与高精度年代控制的协同研究。上述工作为理解亚洲边缘海碳汇演化过程及其在全球碳循环中的地质作用提供了基础支撑，并有助于科学地预测未来气候变化背景下海洋碳汇的演变趋势。
- 亚洲边缘海 /
- 陆源有机碳 /
- 海源有机碳 /
- 冰期-间冰期旋回 /
- 成因机制
Abstract: The Asian continental marginal seas are among the most representative “source-to-sink” coupled systems globally. Understanding their organic carbon (OC) burial processes under the context of Quaternary climate change is of great significance for unraveling the evolution of the global carbon cycle. This study provides a comprehensive review of the sources, burial flux variations, and driving mechanisms of OC in sediments from major Asian marginal seas. The results indicate that during glacial periods, most marginal seas exhibit increased OC content and burial fluxes. In many regions, total organic carbon (TOC) content, organic carbon isotopic composition (δ¹³C_org), and TOC/total nitrogen (TOC/TN) ratios display cyclic variations on orbital timescales. Mechanistically, sea-level changes regulate the process and intensity of terrigenous material delivery, monsoon systems influence watershed erosion and water column structure, while ocean currents and the distribution of oxygen minimum zones (OMZs) jointly control the spatial variability of carbon sink efficiency. Sedimentary records from representative sites suggest that increased terrigenous input, OMZ development, or higher sedimentation rates during glacials often enhance the preservation and burial of OC. However, in certain high-latitude or deep-water regions (e.g., the Sea of Okhotsk and the Japan Sea), reduced marine productivity during glacials may lower OC burial efficiency. Furthermore, this study employs combined proxies such as δ¹³C_org and TOC/TN ratios to quantify the mixing characteristics and evolutionary history of different OC sources, and estimates of OC burial fluxes reveal the differential responses of regional carbon sinks to glacial–interglacial cycles. Despite significant progress, challenges remain in end-member construction, proxy standardization, and high-resolution spatiotemporal reconstructions. Future research should focus on cross-regional comparisons, coupled mechanistic modeling, and refined chronological controls. These efforts will enhance our understanding of the evolution of carbon sinks in Asian marginal seas and their geological roles in the global carbon cycle, contributing to more accurate predictions of oceanic carbon sink dynamics under future climate change scenarios.
- Asian marginal seas /
- terrestrial organic carbon /
- marine organic carbon /
- glacial–interglacial cycles /
- driving mechanisms

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图 1 海洋有机碳埋藏演化示意图

Fig. 1 Schematic map of marine organic carbon burial evolution

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图 2 亚洲大陆边缘海地理概况及研究站位分布

ODP 722站位^[40]；IODP U1456站位^[9]；3104G站位^[41]；IODP U1445站位^[42]；NGHP01-19B站位^[43]；E87-30^[28]；IODP U1452站位^[44]；T93站位^[45]；MD05-2897站位^[46]；NS2020-05G站位^[38]；BIS-187-61站位^[47]；MD972142站位^[48]；ZHS-176站位^[49]；GHE24L站位^[50]；17937站位^[51]；TWS-1站位^[52]； MD06-3054站位^[33]；MD06-3052站位^[8]；39-A站位^[53]；A3站位^[54]；CHSC-15站位^[55]；W03站位^[56]；St10-PC站位^[57]；KCES-1站位^[58]；E09-08站位^[59]；LV53-23-1站位^[60]；MR0604-PC04站位^[61]；T00站位^[62]；PC3B站位^[63]；LV87-55-1站位^[64]；ODP 1143站位^[35]

Fig. 2 Geographical overview of the Asian continental margin sea and distribution of research stations

Site ODP 722^[40]；Site IODP U1456^[9]；Site 3104G^[41]；Site IODP U1445^[42]；Site NGHP01-19B^[43]；Site E87-30^[28]；Site IODP U1452^[44]；Site T93^[45]；Site MD05-2897^[46]；Site NS2020-05G^[38]；Site BIS-187-61^[47]；Site MD972142^[48]；Site ZHS-176^[49]；Site GHE24L^[50]；Site 17937^[51]；Site TWS-1^[52]； Site MD06-3054^[33]；Site MD06-3052^[8]；Site 39-A^[53]；Site A3^[54]；Site CHSC-15^[55]；Site W03^[56]；Site St10-PC^[57]；Site KCES-1^[58]；Site E09-08^[59]；Site LV53-23-1^[60]；Site MR0604-PC04^[61]；Site T00^[62]；Site PC3B^[63]；Site LV87-55-1^[64]；Site ODP 1143^[35]

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图 3 亚洲大陆边缘海典型站位（a）沉积物中TOC和TN含量间相关性以及（b）有机质来源判别图

MD06-3052站位数据^[72]；St10-PC站位数据^[57]；3104G站位数据^[41]；NS2020-05G站位数据^[38]；IODP U1456站位数据^[9，73]；NGHP01-19B站位数据^[43]；IODP U1452站位数据^[44]；TWS-1站位数据^[52]；CHE24L站位数据^[55]；MD06-3054站位数据^[33]；LV53-23-1站位数据^[60]；LV87-55-1站位数据^[6]

Fig. 3 Correlation between TOC and TN content in sediments at typical sites in the Asian continental margin Sea (a) and identification of organic matter sources (b)

Site MD06-3052^[72]；Site St10-PC^[57]；Site 3104G^[41]；Site NS2020-05G^[38]；Site IODP U1456^[9，73]；Site NGHP01-19B^[43]；Site IODP U1452^[44]；Site TWS-1^[52]；Site CHE24L^[55]；Site MD06-3054^[33]；Site LV53-23-1^[60]；Site LV87-55-1^[6]

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图 4 亚洲大陆边缘海典型站位MIS 6期以来有机碳组成指标剖面变化

（a）阿拉伯海IODP U1456站位沉积物TOC和TN含量变化^[9]；（b）孟加拉湾IODP U1452站位沉积物TOC和TN含量变化^[44]；（c）孟加拉湾IODP U1452站位沉积物TOC/ TN比值和δ¹³C_org值变化^[44]；（d）孟加拉湾NGHP01-19B站位沉积物TOC含量和δ¹³C_org值变化^[43]；（e）南海ODP 1143站位沉积物TOC/ TN比值和δ¹³C_org值变化^[35]；（f）菲律宾海MD06-3052站位沉积物TOC/TN比值和δ¹³C_org值变化^[72]；（g）菲律宾海MD06-3052站位沉积物TOC和TN含量变化^[72]（h）菲律宾海St10-PC站位沉积物TOC/ TN比值和δ¹³C_org值变化^[57]；（i）菲律宾海St10-PC站位沉积物TOC和TN含量变化^[57]；（j）东海CHSC-15站位沉积物陆源TOC和海源TOC含量变化^[55]；MIS（深海氧同位素阶段）1，3和5代表间冰期阶段，MIS 2，4和6代表冰期阶段。

Fig. 4 Changes of organic carbon component profile of typical stations in the Asian continental margin sea since MIS 6

(a) Changes in TOC and TN contents of sediments at Site U1456 in the Arabian Sea^[9]; (b) Changes in TOC and TN contents of sediments at Site U1452 in the Bay of Bengal^[44]; (c) Changes in the TOC/ TN ratio and δ¹³C_org value of sediments at Site U1452 in the Bay of Bengal^[44]; (d) Changes in sediment TOC content and δ¹³C_org value at Site NGHP01-19B in the Bay of Bengal^[43]; (e) Changes in the TOC/ TN ratio and δ¹³C_org value of sediments at Site ODP 1143 station in the South China Sea^[35]; (f) Changes in the TOC/TN ratio and δ¹³C_org value of sediments at Site MD06-3052 in the Philippine Sea^[72]; (g) Changes in TOC and TN contents of sediments at Site MD06-3052 in the Philippine Sea^[72]; (h) Changes in the TOC/ TN ratio and δ¹³C_org value of sediments at Site St10-PC in the Philippine Sea^[57]; (i) Changes in TOC and TN contents of sediments at Site St10-PC in the Philippine Sea^[57]; (j) Changes in the contents of terrestrial TOC and Marine TOC in sediments at Site CHSC-15 in the East China Sea^[55]; MIS (Marine Isotope Stages) 1, 3 and 5 represent the interglacial stages, and MIS 2, 4 and 6 represent the glacial stages.

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图 5 亚洲大陆边缘海典型站位32 ka以来有机碳组成指标剖面变化

（a）阿拉伯海3104G站位TOC和TN含量变化^[41]；（b）南海NS2020-05G站位沉积物TOC/TN比值和δ¹³C_org值变化^[38]；（c）菲律宾海MD06-3054站位沉积物TOC/TN比值和δ¹³C_org变化^[33]；（d）日本海LV53-23-1站位TOC和TN含量变化^[60]；（e）日本海LV53-23-1站位TOC/TN比值和δ¹³C_org变化^[60]；（f）鄂霍茨克海LV87-55-1站位TOC/TN比值和δ¹³C_org变化^[64]；（g）南海NS2020-05G和MD972142站位TOC含量变化^[38，48]；（h）南海GHE24L站位TOC/TN比值和δ¹³C_org变化^[50]；（i）南海GHE24L站位TOC和TN含量变化^[50]；（j）南海TWS-1站位TOC/TN比值和δ¹³C_org变化^[52]；（k）南海TWS-1站位TOC和TN含量变化^[52]；（l）南海17937站位TOC含量和TOC/TN比值变化^[51]；MIS（深海氧同位素阶段）1，3和5代表间冰期阶段，MIS 2，4和6代表冰期阶段。

Fig. 5 Changes of organic carbon component profile of typical stations in the Asian continental margin sea since 32 ka

(a) Changes in TOC and TN contents at Site 3104G in the Arabian Sea^[41]; (b) Changes in the TOC/TN ratio and δ¹³C_org value of sediments at Site NS2020-05G in the South China Sea^[38]; (c) Changes in the TOC/TN ratio and δ¹³C_org of sediments at Site MD06-3054 in the Philippine Sea^[33]; (d) Changes in TOC and TN contents at Site LV53-23-1 in the Sea of Japan^[60]; (e) Changes of TOC/TN ratio and δ¹³C_org at Site LV53-23-1 in the Sea of Japan^[60]; (f) Changes of TOC/TN ratio and δ¹³C_org at Site LV87-55-1 in the Sea of Okhorsk^[64]; (g) Changes in TOC content at Sites NS2020-05G and MD972142 in the South China Sea^{[38, 48]}; (h) Changes of TOC/TN ratio and δ¹³C_org at Site GHE24L in the South China Sea^[50]; (i) Changes in TOC and TN contents at Site GHE24L in the South China Sea^[50]; (j) Changes of TOC/TN ratio and δ¹³C_org at Site TWS-1 in the South China Sea^[52]; (k) Changes in TOC and TN contents at Site TWS-1 in the South China Sea^[52]; (1) Changes in TOC content and TOC/TN ratio at Site 17937 in the South China Sea^[51]; MIS (Marine Isotope Stages) 1, 3 and 5 represent the interglacial stages, and MIS 2, 4 and 6 represent the glacial stages.

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图 6 亚洲大陆边缘海典型站位不同来源有机碳贡献变化

（a）阿拉伯海U1456站位陆源和海源有机碳贡献比例变化^[73]；（b）孟加拉湾U1452站位陆源和海源有机碳贡献比例变化^[44]；（c）孟加拉湾NGHP01-19B站位陆源和海源有机碳贡献比例变化^[43]；（d）菲律宾海MD06-3502站位陆源和海源有机碳贡献比例变化^[72]；（e）菲律宾海St10-PC站位陆源和海源有机碳贡献比例变化^[57]；（f）东海CHSC-15站位陆源和海源有机碳贡献比例变化^[55]；（g）南海NS2020-05G站位陆源和海源有机碳贡献比例变化^[38]；（h）南海TWS-1站位陆源和海源有机碳贡献比例变化^[52]；（i）南海17937站位陆源和海源有机碳贡献比例变化^[51]；（j）菲律宾海MD06-3054站位陆源和海源有机碳贡献比例变化^[33]；（k）日本海LV52-23-1站位陆源和海源有机碳贡献比例变化^[60]；（l）鄂霍茨克海LV87-55-1站位陆源和海源有机碳贡献比例变化^[64]；MIS（深海氧同位素阶段）1，3和5代表间冰期阶段，MIS 2，4和6代表冰期阶段。

Fig. 6 Changes of organic carbon contributions from different sources at typical stations in the Asian continental margin sea

(a) Changes in the contribution ratios of land-based and Marine organic carbon at Site IODP U1456 in the Arabian Sea^[73]; (b) Changes in the contribution ratios of land-based and sea-based organic carbon at Site IODP U1452 in the Bay of Bengal^[44]; (c) Changes in the contribution ratios of land-based and Marine organic carbon at Site NGHP01-19B in the Bay of Bengal^[43]; (d) Changes in the contribution ratio of organic carbon from land and sea sources at Site MD06-3502 in the Philippine Sea^[72]; (e) Changes in the contribution ratios of land-based and Marine organic carbon at Site St10-PC in the Philippine Sea^[57]; (f) Changes in the contribution ratios of land-based and Marine organic carbon at Site CHSC-15 in the East China Sea^[55]; (g) Changes in the contribution ratio of land-based and Marine organic carbon at Site NS2020-05G in the South China Sea^[38]; (h) Changes in the contribution ratios of land-based and Marine organic carbon at Site TWS-1 in the South China Sea^[52]; (i) Changes in the contribution ratios of land-based and Marine organic carbon at Site 17937 in the South China Sea^[51]; (j) Changes in the contribution ratios of land-based and Marine organic carbon at Site MD06-3054 in the Philippine Sea^[33]; (k) Changes in the contribution ratios of land-based and Marine organic carbon at Site LV52-23-1 in the Sea of Japan^[60] (1) Changes in the contribution ratio of organic carbon from land and sea sources at Site LV87-55-1 in the Sea of Okhotsk^[64] MIS (Marine Isotope Stages) 1, 3 and 5 represent the interglacial stages, and MIS 2, 4 and 6 represent the glacial stages.

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图 7 亚洲大陆边缘海有机碳埋藏演化模式图

Fig. 7 The evolution model of organic carbon burial in the marginal seas of the Asian continent

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表 1 亚洲大陆边缘海典型站位有机碳研究进展

Tab. 1 Research progress of organic carbon at typical stations in the Asian continental margin sea

区域	站位号	站位地理位置	站位水深/ m	年代框架模式	时间尺度/ ka	研究指标	有机碳演化特征	有机碳指标变化的潜在影响因素	参考文献
鄂霍茨克海	MR0604-PC04	鄂霍茨克海南部	1215	磁化率及颜色反射率与氧同位素地层调谐	0-28	TOC，TOC/TN，δ¹⁵N，生物标志物	全新世含量高，末次冰期含量低	水体分层，海冰融水，反硝化作用	[61]
	T00	鄂霍茨克海中部	975	放射虫特征种含量与氧同位地层调谐	0-450	TOC，TOC/TN	冰期含量低，间冰期含量高	海冰变化，陆源输入，水体分层，海平面	[62]
	PC3B	鄂霍茨克海中部	1048	氧同位素地层调谐	0-500	TOC，TN,TOC/TN	冰期含量低，间冰期含量高	海冰变化，水体混合	[63]
	LV87-55-1	鄂霍茨克海北部	1400	有孔虫AMS ¹⁴C 测年、火山灰年代学	0-30	TOC，TN，TOC/TN，δ¹³C，δ¹⁵N，有机碳来源	早全新世含量高，末次冰期含量低	冻土融化，海平面，河流输入	[64]
日本海	LV53-23-1	日本海中部	1282	有孔虫AMS ¹⁴C 测年、火山灰年代学	0-37	TOC，TN,TOC/TN，δ¹³C，δ¹⁵N，有机碳来源	冰期陆源有机碳相对贡献更高	对马暖流强弱，营养盐及生产力变化，水体含氧量	[60]
	KCES-1	日本海南部	1463.8	有孔虫AMS ¹⁴C 测年、火山灰年代学	0-50	TOC	MIS1期TOC含量高	/	[58]
	E09-08	日本海南部	1259	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-500	TOC，TOC/TN，δ¹³C，δ¹⁵N，生物标志物	MIS 2，10，12期δ¹³C, δ¹⁵N低，TOC/TN高	海平面变化，陆源有机质输入变化，反硝化作用	[59]
黄海	W03	黄海北部	54.5	有孔虫AMS ¹⁴C 测年	0-10	TOC，TN，TOC/TN，δ¹³C，生物标志物，有机碳来源	全新世早期TOC含量逐渐增加，中晚期保持平稳	ENSO变率，东亚冬季风，沿岸洋流，陆源输入	[56]
	26个表层站位	黄海南部	/	/	/	TOC，TN，TOC/TN，δ¹³C，有机碳来源贡献	/	陆源输入、生产力、洋流	[74]
东海	A3	东海西部	25	210Pb和贝壳AMS ¹⁴C 测年	0-0.7	TOC，TOC/TN，,δ¹³C，生物标志物	1950年前长江河口沉积陆源有机碳低1950年后升高	ENSO变率，东亚冬季风，大河上游降水状况	[54]
	CSHC-15	东海东部	940	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-200	TOC, TN, TOC/TN, δ¹³C, δ¹⁵N,有机碳来源	冰期陆源有机质贡献增加间冰期海源贡献增加	海平，黑潮，东亚季风，生产力，NPIW等	[55]
	39-A	东海南部	45	有孔虫AMS ¹⁴C 测年	0-3	TOC，TN，TOC/TN，δ¹³C，生物标志物	1400yr以来，陆源TOC含量与埋藏效率增加	东亚冬季风强度，沿岸流强度	[53]
南海	SH08	南海北部	1327	有孔虫AMS ¹⁴C 测年	0-26	TOC，TN，TOC/TN，δ¹³C，生物标志物，有机碳来源	LGM和冰消期TOC含量较高，全新世则较低	海平面，东亚冬季风强度	[75]
	TWS-1	南海北部	1186	有孔虫AMS ¹⁴C 测年	0-23	TOC，TN，TOC/TN，δ¹³C，有机碳来源，有机碳MAR	陆源有机碳通量在末次冰消期早期和中全新世呈峰值	海平面，东亚冬季风强度	[52]
	GHE24L	南海北部	1387	有孔虫AMS ¹⁴C 测年	0-21	TOC，TN，TOC/TN，δ¹³C，有机碳MAR	LGM阶段TOC含量和MAR较高，全新世较低	海平面，海洋生产力，黑潮强度	[50]
	ZHS-176	南海北部	1383	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-25	TOC，δ¹³C，有机碳来源	MIS2期TOC含量较高，全新世有机碳含量较低	海平面，东亚冬季风强度，上升流强度，生产力	[49]
	BIS-187-61	南海西南部	2226	氧同位素地层调谐	0-140	TOC，TOC/TN，有机碳MAR	TOC含量和物质堆积速率在MIS 2,4和6期增加	海平面，东亚冬季风强度，上升流强度，生产力	[47]
	MD972142	南海东部	1557	氧同位素地层调谐	0-900	TOC，生物标志物	冰期TOC含量较高，间冰期TOC含量较低	海平面，东亚冬季风强度，生产力	[48]
	NS2020-05G	南海南部	1737	有孔虫AMS ¹⁴C 测年	0-30	TOC，TOC/TN，δ¹³C，生物标志物	LGM期间陆源和海源有机碳保存效率较高作为碳汇	沉积速率，底层水氧化还原状况	[38]
	MD05- 2897	南海南部	1658	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-500	TOC，有机碳物质堆积速率	TOC含量和堆积速率在间冰期较高，冰期略低	东亚夏季风，生产力	[46]
菲律宾海	MD06- 3502	菲律宾海西部	732	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-156	TOC，TN，TOC/TN，δ¹³C，有机碳来源，有机碳MAR	TOC含量和物质堆积速率呈现冰期高而间冰期低	海平面，陆架松散沉积物的物理剥蚀过程	[72]
	MD06-3504	菲律宾海西部	2057	有孔虫AMS ¹⁴C 测年	0-28	TOC，TN，TOC/TN，δ¹³C	末次冰期有机碳以陆源为主，全新世以海源为主	海平面	[33]
	St10-PC	菲律宾海北部	2670	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-380	TOC，TN，TOC/TN，δ¹³C，有机碳MAR	TOC含量和MAR在冰期增加	洋流活动，底层水氧化还原状况，	[57]
泰国湾	T93	泰国湾西南部	59	有孔虫AMS ¹⁴C 测年	0-14	TOC，TN，TOC/TN，δ¹³C，有机碳来源，有机碳MAR	末次冰消期以来随着海平面上升陆源有机碳占比下降	海平面，东亚夏季风	[45]
孟加拉湾	NGHP01-19B	孟加拉湾北部	1422	有孔虫AMS ¹⁴C 测年、氧同位素地层调谐	0-110	TOC，TN，TOC/TN，δ¹³C，δ¹⁵N，有机碳MAR	TOC含量呈现冰期高而间冰期低的特征	陆源输入，水体分层，印度季风	[43]
	U1452	孟加拉湾南部	3671	氧同位素地层调谐	0-190	TOC，TN，TOC/TN，δ¹³C	TOC含量呈现冰期高而间冰期低的特征	陆源输入，印度季风	[44]
	U1445	孟加拉湾北部	2513	磁性地层学和生物地层学	0-2300	TOC，TN，,TOC/TN，δ¹³C	2.3Ma以来有机碳贡献从海源向陆源转变	陆源输入，印度季风	[42]
阿拉伯海	U1456	阿拉伯海东部	3640	磁性地层学和生物地层学	0-700	TOC，TN，TOC/TN，δ¹³C，有机碳来源，有机碳MAR	TOC含量和有机碳MAR呈现冰期高而间冰期特征	陆源输入，喜马拉雅-青藏高原高地物理剥蚀	[73]
	3104G	阿拉伯海东部	1680	有孔虫AMS 14C 测年	0-40	TOC，TN，δ¹³C，有机碳MAR	LGM有机碳MAR显著增加	沉积速率	[41]
	722	阿拉伯海西部	2027.8	磁性地层学和生物地层学	0-700	有机碳MAR	冰期有机碳MAR显著增加	陆源输入	[40]

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