长江口−东海内陆架早期成岩过程及影响因素

汲雨; 赵彬; 李康; 韩露露; 陈霖; 姚鹏

doi:10.12284/hyxb2023127

长江口−东海内陆架早期成岩过程及影响因素

doi: 10.12284/hyxb2023127

汲雨^{1, 2,},
赵彬^{1, 3},
李康^{1, 2},
韩露露^{1, 2},
陈霖^{1, 2},
姚鹏^{1, 3, ,}

1.
中国海洋大学海洋化学理论与工程技术教育部重点实验室，山东青岛 266100
2.
中国海洋大学化学化工学院，山东青岛 266100
3.
崂山实验室海洋生态与环境科学功能实验室，山东青岛 266237

基金项目: 国家自然科学基金（42076034，42006041）

详细信息

作者简介:
汲雨（1997-），女，山东省菏泽市人，主要从事海洋有机生物地球化学研究。E-mail：425613278@qq.com

通讯作者:
姚鹏（1977-），男，山东省菏泽市人，教授，主要从事海洋有机生物地球化学研究。E-mail：yaopeng@ouc.edu.cn

中图分类号: P736.21⁺3
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出版历程
- 收稿日期: 2022-12-04
- 修回日期: 2023-03-14
- 网络出版日期: 2023-04-28
- 刊出日期: 2023-08-31

Early diagenetic processes and influencing factors of the Changjiang River Estuary and East China Sea inner-shelf

Ji Yu^{1, 2
,},
Zhao Bin^{1, 3},
Li Kang^{1, 2},
Han Lulu^{1, 2},
Chen Lin^{1, 2},
Yao Peng^{1, 3
, ,}

1.
Key Laboratory of Marine Chemistry Theory and Technology, Ministry of Education, Ocean University of China, Qingdao 266100, China
2.
College of Chemistry and Chemical Engineering, Ocean University of China, Qingdao 266100, China
3.
Laboratory for Marine Ecology and Environmental Science, Laoshan Laboratory, Qingdao 266237, China

摘要

摘要: 边缘海沉积物中的早期成岩作用是影响碳循环和埋藏的重要过程，目前对早期成岩过程及其影响因素的了解还不够深入。于2018年8月在长江口−东海内陆架采集了短柱状沉积物，对间隙水中溶解无机碳（DIC）、溶解无机氮（DIN）、二价铁（${\rm{Fe}}^{2+}$）、二价锰（${\rm{ Mn}}^{2+}$）和硫酸根（${\rm{SO}}^{2-}_4$）离子等参数进行了分析，并结合表层沉积物中粒度、比表面积、有机碳及稳定碳同位素组成和底层水环境参数，研究了不同沉积环境下沉积物中的早期成岩过程及其影响因素。结果表明，长江口−东海内陆架泥质区沉积物间隙水中DIC和${{\rm {NH}}_4^+} $的浓度随着深度的增加逐渐增大，且在其中心站位有较高的DIC、${{\rm {NH}}_4^+} $产生通量（分别为4.03 mmol/（m²·d）和0.57 mmol/（m²·d））和${{\rm {SO}}_4^{2-}} $消耗通量（−4.56 mmol/（m²·d）），沉积物扰动深度为20～40 cm，自长江口向浙闽沿岸逐渐降低；而在砂质区，各溶质在剖面上均无明显变化，且通量较小（DIC: 0.60 mmol/（m²·d）；${{\rm {NH}}_4^+} $：−0.03 mmol/（m²·d）；${{\rm {SO}}_4^{2-}} $：−1.05 mmol/（m²·d）），沉积物不存在扰动。扰动层厚度与沉积物间隙水中DIC和${{\rm {NH}}_4^+} $等溶质通量呈正相关，表明沉积物的物理扰动是影响泥质区沉积有机碳再矿化的重要因素。综合上述结果，发现沉积有机碳在泥质区扰动层的降解方式以铁锰还原作用为主，扰动层以下以硫酸盐还原作用为主，而在砂质区的降解主要靠耗氧呼吸作用。本研究丰富了长江口及邻近海域沉积动力过程对早期成岩作用影响的认识，有助于深入理解大河河口及邻近海域有机碳的循环和埋藏。
- 长江口 /
- 沉积物间隙水 /
- 早期成岩过程 /
- 沉积物扰动 /
- 通量 /
- 有机碳降解
Abstract: Early diagenesis in marginal sea sediments is an important process that affects carbon cycling and burial. Early diagenetic processes and influencing factors, however, remains poorly constrained. Dissolved inorganic carbon (DIC), dissolved inorganic nitrogen (DIN), Fe²⁺, Mn²⁺, sulfate and other parameters in sediment porewaters of five short cores collected in August 2018 from the Changjiang River Estuary and East China Sea inner-shelf were analyzed. In combination with grain size composition, specific surface area, organic carbon concentrations and stable carbon isotopic composition in surface sediments and bottom water parameters, the early diagenetic processes and influencing factors in sediments under different sedimentary regimes were studied. Concentrations of DIC and ${{\rm {NH}}_4^+} $ in sediment porewaters in the mud area gradually increase with depth, and relatively high production fluxes of DIC and ${{\rm {NH}}_4^+} $ (4.03 mmol/(m²·d) and 0.57 mmol/(m²·d), respectively) and consumption fluxes of ${{\rm {SO}}_4^{2-}} $ (−4.56 mmol/(m²·d)) are observed at the center of the mud area, while in the sandy area, there are no obvious variations of these solutes, and the fluxes are lower compared with those in muddy sediments. According to the vertical distributions of these solutes in the sediment porewaters, the sediment disturbance depth in the mud area varies at 20−40 cm, and gradually decreases from the Changjiang River Estuary mud area to the Zhe-Min coast mud area, whereas in the sandy area, no sediment disturbance is found. The thickness of sediment disturbed layer is positively correlated with solute fluxes (e.g., DIC and ${{\rm {NH}}_4^+} $) in sediment porewaters, indicating that the physical reworking of sediments is an important factor affecting the remineralization of sedimentary organic carbon in the mud area. In general, the main decomposition pathway of the sedimentary organic carbon in the disturbed layer of the mud area is iron/manganese reduction, and below the disturbed layer the main pathway is the sulfate reduction, while in the sandy area, the main degradation pathway is aerobic respiration. This study enriches the understanding of the impact of sedimentary dynamic processes on early diagenesis in the Changjiang River Estuary and adjacent sea areas, and contributes to better understand the cycling and burial of organic carbon in the large-river estuary and adjacent sea areas.
- Changjiang River Estuary /
- sediment porewater /
- early diagenetic process /
- sediment rework /
- flux /
- organic carbon decomposition

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图 1 长江口−东海内陆架及邻近海域采样站位点信息（橙黄色色块代表东部边缘海泥质区）

Fig. 1 Information of sampling stations in the Changjiang River Estuary and East China Sea inner-shelf （the orange color block represents the mud area of the eastern marginal sea）

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图 2 长江口−东海内陆架沉积物间隙水中 DIC（a−e），$ {{\rm {NH}}_4^+} $（a−e），$ {{\rm {SO}}_4^{2-}} $（a−e），${\rm{NO}}_3^-$（f−j），$ {{\rm {NO}}_2^-}$（f−j），Fe²⁺（k−o）和Mn²⁺（k−o）的浓度剖面

图中虚线为扰动层和非扰动层的分界线

Fig. 2 Concentration profile of DIC (a−e), $ {{\rm {NH}}_4^+} $ (a−e), $ {{\rm {SO}}_4^{2-}} $ (a−e), ${{\rm {NO}}_3^-}$ (f−j), $ {{\rm {NO}}_2^-} $ (f−j), Fe²⁺ (k−o) and Mn²⁺ (k−o) in sediment porewater of the Changjiang River Estuary and East China Sea inner-shelf

The dotted line in the figure is the boundary between the reworked layer and the unreworked layer

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图 3 长江口−东海内陆架沉积物间隙水中DIC（a）、$ {{\rm {NH}}_4^+} $（b）、${{\rm {SO}}_4^{2-}} $（c）的通量分布

图中红色站位为本研究站位，灰色站位重新计算于参考文献[19]

Fig. 3 Fluxes distribution of DIC (a), $ {{\rm {NH}}_4^+} $ (b) and ${{\rm {SO}}_4^{2-}} $ (c) in sediment porewater of the Changjiang RiverEstuary and East China Sea inner-shelf

The red station in the figure is the station of this study, and the gray station is recalculated in the reference [19]

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图 4 长江口−东海内陆架基本理化参数对DIC、$ {{\rm {NH}}_4^+} $、${{\rm {SO}}_4^{2-}} $ 通量的 RDA

Fig. 4 RDA of DIC, $ {{\rm {NH}}_4^+} $ and ${{\rm {SO}}_4^{2-}} $ fluxes from basic physical and chemical parameters in the Changjiang River Estuary and East China Sea inner-shelf

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图 5 长江口−东海内陆架沉积物间隙水扰动层与非扰动层中${{\rm {NH}}_4^+} $（a）、${{\rm {SO}}_4^{2-}} $（b）浓度与DIC浓度的关系

Fig. 5 Relationship between concentrations of ${{\rm {NH}}_4^+} $ (a), ${{\rm {SO}}_4^{2-}} $ (b) and DIC in the reworked and unreworked layers of sediment porewater in the Changjiang River Estuary and East China Sea inner-shelf

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图 6 长江口−东海内陆架沉积物间隙水扰动层厚度与 DIC（a）、$ {{\rm {NH}}_4^+} $（b）、${{\rm {SO}}_4^{2-}} $（c）通量的关系以及 δ¹³C 与 ${{\rm {SO}}_4^{2-}} $ 通量（d）的关系

Fig. 6 The relationship between the thickness of sediment porewater reworked layer and DIC (a), $ {{\rm {NH}}_4^+} $ (b) and ${{\rm {SO}}_4^{2-}} $ (c) fluxes and relationship between δ¹³C and ${{\rm {SO}}_4^{2-}} $ fluxes (d) in the Changjiang River Estuary and East China Sea inner-shelf

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表 1 长江口−东海内陆架底层水和表层沉积物的基本理化参数

Tab. 1 Basic physical and chemical parameters of bottom water and surface sediment in the Changjiang River Estuary and East China Sea inner-shelf

站位	水深/m	底层水温/°C	底层水盐度	底层DO含量/（mg·L⁻¹）	TOC含量/%	δ¹³C值/‰	孔隙度	SSA/（m²·g⁻¹）	中值粒径/μm	（TOC/SSA） /（mg·m⁻²）
A6−3	13.7	25.4	28.0	5.18	0.69	−22.96	0.81	16.63	7.3	0.41
C2	18.3	27.3	29.4	6.75	0.68	−22.86	0.70	17.33	7.3	0.39
F2	26.4	25.2	34.0	1.58	0.54	−22.23	0.76	15.79	8.9	0.34
H2	26.2	26.4	34.1	3.14	0.61	−22.09	0.73	16.68	6.6	0.37
A6−7	47.0	21.1	30.1	3.19	0.29	−21.75	0.59	3.90	102	0.74

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表 2 长江口−东海内陆架沉积物间隙水中溶质的产生/消耗通量（正值代表产生，负值代表消耗）

Tab. 2 Production/consumption fluxes of solute in sediment porewater of the Changjiang River Estuary and East China Sea inner-shelf (positive value represents generation, negative value represents consumption)

站位	产生/消耗通量/（mmol·m⁻²·d⁻¹）
站位	DIC	$ {{\rm {NH}}_4^+} $	$ {{\rm {SO}}_4^{2-}} $	Fe²⁺	Mn²⁺
A6−3	4.03	0.57	−4.56	0.01	−0.03
C2	0.74	0.14	−1.14	0.02	−0.01
F2	3.23	0.29	−2.19	0	−0.01
H2	0.45	0.06	−1.04	0	0
A6−7	0.60	−0.03	−1.05	0	0

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表 3 世界典型河口和海洋环境沉积物间隙水中 DIC、$\bf{{ {NH}}_4^+}$、${\bf{{{{SO}}_4^{2-}} }}$的产生和消耗通量（单位：mmol/(m²·d)）

Tab. 3 Fluxes of DIC, $ {{\bf {NH}}_4^+}$, ${{\bf {SO}}_4^{2-}}$ in sediment porewater of typical estuaries and marine environment sediments in the world (unit: mmol/(m²·d) )

区域	DIC	$ {{\rm {NH}}_4^+} $	${{\rm {SO}}_4^{2-}} $	使用方法	参考文献
长江口	0.45～4.03	0.03～0.57	−1.04～−4.56	PROFILE模型	本研究
长江口	0.08～7.59	0.02～0.54	−0.03～−10.86	PROFILE模型	文献[19]（重新计算）
黄河口	2.18～16.55	0.01～1.37	−12.91～−31.64	PROFILE模型	文献[46]
东海泥质区	2.94～11.7	0.56～2.78	−5.78～−16.2	沉积物培养实验	文献[19]
南黄海泥质区	2.36～3.13	0.42～0.62	−2.26～−2.60	沉积物培养实验	文献[19]
巴布亚新几内亚湾	10～42	−	−	沉积物培养实验	文献[47]
亚马孙−圭亚那移动泥带	19～127	−	−	沉积物培养实验	文献[9]
亚马孙河口	1.79～42.57	0.03～2.94	−	沉积物培养实验	文献[48]
法属圭亚那	20～235	−	−	沉积物培养实验	文献[12]
刚果河口	1.13～4.08	0.11～0.37	−	Fick第一定律	文献[49]
波罗的海深水	0.01～3.33	0～0.38	−	Fick第一定律	文献[50]
波罗的海	2.3～43.5	−	−	沉积物培养实验	文献[51]
格但斯克盆地	−	0.29～2.95	−	Fick第一定律	文献[52]
格但斯克盆地	−	0.21～3.43	−	沉积物培养实验	文献[52]
墨西哥湾	3.4～82	0～7.2	−	沉积物培养实验	文献[53]
毛里塔尼亚	5.64～20.06	−	−	沉积物培养实验	文献[54]
新斯科舍浅海	14.74～151.53	−4.07～9.24	−	沉积物培养实验	文献[55]
亚得里亚海	0.50～8.76	0.04～1.62	−	Fick第一定律	文献[56]
亚得里亚海	2.2～173	0.16～1.61	−	沉积物培养实验	文献[56]
新不列颠海沟	0.10～0.60	−	−	Fick第一定律	文献[57]
拉普捷夫海	0.08～0.19	−	−	稳态下的一般反应−输运方程	文献[58]
阿鲁海	0.6～38.4	0.01～4.2	−	沉积物培养实验	文献[59]
注：“−”代表未检测。

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参考文献(63)

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