37 ka以来日本海沉积物有机质碳和氮稳定同位素变化及其古海洋学意义

doi:10.13745/j.esf.sf.2022.1.6

地学前缘 ›› 2022, Vol. 29 ›› Issue (4): 123-135.DOI: 10.13745/j.esf.sf.2022.1.6

• 深海生物地球化学过程 • 上一篇下一篇

37 ka以来日本海沉积物有机质碳和氮稳定同位素变化及其古海洋学意义

邹建军¹^,²(), 宗娴¹, 朱爱美¹, 豆汝席¹, 林锦辉¹, 冯旭光¹, 董智¹, Sergey A. GORBARENKO³, 郑立伟⁴, 石学法¹^,²^,^*()

1.自然资源部第一海洋研究所海洋地质与成矿作用重点实验室, 山东青岛 266061
2.青岛海洋科学与技术试点国家实验室海洋地质过程与环境功能实验室, 山东青岛 266237
3.俄罗斯科学院远东分院太平洋海洋研究所, 俄罗斯符拉迪沃斯托克 690041
4.海南大学南海海洋资源利用国家重点实验室, 海南海口 570000

收稿日期:2021-09-30 修回日期:2021-11-10 出版日期:2022-07-25 发布日期:2022-07-28
通讯作者: 石学法
作者简介:邹建军(1979—),男,博士,研究员,主要从事中高纬海洋沉积和古环境研究。E-mail: zoujianjun@fio.org.cn
基金资助:
国家自然科学基金项目(41876065);国家自然科学基金项目(41420104005);国家自然科学基金委山东海洋科学中心项目(U1606401);泰山学者攀登计划(TSPD20181216)

Stable carbon and nitrogen isotope variations in sedimentary organic matter in the Sea of Japan since 37 ka: Paleoceanographic implications

ZOU Jianjun¹^,²(), ZONG Xian¹, ZHU Aimei¹, DOU Ruxi¹, LIN Jinhui¹, FENG Xuguang¹, DONG Zhi¹, Sergey A. GORBARENKO³, ZHENG Liwei⁴, SHI Xuefa¹^,²^,^*()

1. Key Laboratory of Marine Geology and Metallogeny, First Institute of Oceanography, Ministry of Natural Resources, Qingdao 266061, China
2. Laboratory for Marine Geology, Pilot National Oceanography Laboratory for Marine Science and Technology(Qingdao), Qingdao 266237, China
3. V.I. Il’ichev Pacific Oceanological Institute, Far East Branch of the Russian Academy of Sciences, Vladivostok 690041, Russia
4. State Key Laboratory of Marine Resource Utilization in South China Sea, Hainan University, Haikou 570000, China

Received:2021-09-30 Revised:2021-11-10 Online:2022-07-25 Published:2022-07-28
Contact: SHI Xuefa

摘要/Abstract

摘要：

海洋沉积物有机质碳氮稳定同位素(δ¹³C、δ¹⁵N)广泛用于有机质来源示踪、古生产力和古海洋环境重建。日本海沉积物δ¹³C和δ¹⁵N值一个显著特征是在末次冰盛期(LGM)同步负偏,但是对这一现象产生的原因以及他们的演化过程的认识仍然存在明显不足。在本研究中,我们详细调查了37 ka以来日本海中部LV53-23-1岩心沉积物δ¹³C和δ¹⁵N演化历史。结果显示,沉积物δ¹³C和δ¹⁵N分别介于-26.3‰至-22.5‰和1.6‰至6.1‰,低值出现在LGM(26.5~17 ka)暗色层状泥发育时期,指示较强的陆源输入贡献。在Heinrich冰阶1时期(17~14.5 ka),δ¹³C和δ¹⁵N快速正偏,表明日本海海洋环境发生了明显的转换,对应于对马海峡淹没及对马暖流入侵。14.5 ka之后,沉积物δ¹⁵N值恢复到5‰,与开阔大洋海水硝酸盐的δ¹⁵N值近似。我们采用二端员混合模型粗略地估算了有机质来源的相对贡献。LGM时期陆源有机质贡献介于65%至80%,14.5 ka以后海源有机质贡献介于60%至80%。除了增加的陆源有机质贡献以外,LGM时期沉积物δ¹⁵N亏损还涉及如下过程:(1)较高的含Fe沙尘供给提高日本海表层海洋生物固氮效率;(2)缺氧环境盛行减弱成岩作用对沉积物δ¹⁵N影响。37 ka以来,日本海沉积物δ¹³C和δ¹⁵N变化与有机质来源、营养盐的供给、表层生产力和沉积物氧化还原条件相关,实际受海平面和全球气候制约。

关键词: 碳氮稳定同位素, 沉积物有机质来源, 海平面, 末次冰期, 日本海

Abstract:

Stable carbon and nitrogen isotopes in sedimentary organic matter (δ¹³C and δ¹⁵N) have been widely used in the organic matter source tracing and reconstruction of paleoproductivity and paleoenvironment. A pronounced feature of sedimentary δ¹³C and δ¹⁵N in the Sea of Japan is their synchronous negative excursions during the Last Glacial Maximum (LGM), yet the causes and mechanisms of this phenomenon are poorly understood. In this study, we investigated the evolutionary history of sedimentary δ¹³C and δ¹⁵N since 37 ka in core LV53-23-1 retrieved from the Oki Ridge of the central Sea of Japan. According to the results, sedimentary δ¹³C and δ¹⁵N ranged from 26.3‰ to 22.5‰ and 1.6‰ to 6.1‰, respectively, with the lower values coinciding with the deposition of dark laminated mud during the LGM (26.5-17 ka), indicating an increased contribution of terrestrial organic matter. Both δ¹³C and δ¹⁵N showed positive excursions during Heinrich Statidal 1 (17-14.5 ka), indicating distinct oceanic environmental changes in the Sea of Japan, which corresponds to the Tsushima Strait flooding and the Tsushima Warm Current invasion into the Sea of Japan at that time. After 14.5 ka sedimentary δ¹⁵N reached ~5‰, comparable to the average δ¹⁵N of nitrate in seawater. We estimated the relative contributions of organic sources using a binary mixing model. The contribution of terrigenous organic matter ranged between 65% to 80% in the LGM, while marine source contributed between 60% to 80% since 14.5 ka. Besides, sedimentary δ¹⁵N depletion during the LGM can be caused by (1) improved nitrogen fixation in the surface water of the Sea of Japan due to higher dust-borne Fe supply, and (2) decreased effects of early diagenesis on sedimentary δ¹⁵N due to prevailing suboxic or anoxic environment. Taken together, the variations of sedimentary δ¹³C and δ¹⁵N in the Sea of Japan since 37 ka are controlled by eustatic sea level and global climate changes, which modulate the organic source, nutrient supply, primary productivity, and redox conditions in water column and sediment.

Key words: stable carbon and nitrogen isotopes, sedimentary organic matter sources, sea level, last glacial period, Sea of Japan

中图分类号:

P736.4

邹建军, 宗娴, 朱爱美, 豆汝席, 林锦辉, 冯旭光, 董智, Sergey A. GORBARENKO, 郑立伟, 石学法. 37 ka以来日本海沉积物有机质碳和氮稳定同位素变化及其古海洋学意义[J]. 地学前缘, 2022, 29(4): 123-135.

ZOU Jianjun, ZONG Xian, ZHU Aimei, DOU Ruxi, LIN Jinhui, FENG Xuguang, DONG Zhi, Sergey A. GORBARENKO, ZHENG Liwei, SHI Xuefa. Stable carbon and nitrogen isotope variations in sedimentary organic matter in the Sea of Japan since 37 ka: Paleoceanographic implications[J]. Earth Science Frontiers, 2022, 29(4): 123-135.

图/表 10

图1 研究站位和日本海内及周围海域表层环流示意图 a,b,c,d,e和f分别代表岩心(+)KCES1、96EBP4、ODP797、KT92-13P5、GH99-1246和GH99-1239。白色×代表沉积物捕获器站位。带箭头实线代指表层流系。图中缩写如下:SPF—亚极地锋带,LC—利曼寒流,TsWC—对马暖流,YSWC—黄海暖流,YSCC—黄海沿岸流,CDW—长江冲淡水,ZFCC—浙闽沿岸流,TwWC—台湾暖流,KC—黑潮。▲处为研究站位。

Fig.1 Location of the study area and surface circulation in and around the Sea of Japan

表1 LV53-23-1岩心的年龄控制点

Table 1 Age control points of core LV53-23-1

层位 /cm	测试材料和地层标志层	AMS ¹⁴C 年龄/a	日历年龄/ka	沉积速率 /(cm·ka^-1)
31	TL1		11.40
40	N.pachyderma+G.bulloides	12 000±50	13.32	4.69
60	N.pachyderma s.+G.bulloides	15 200±45	17.58	4.69
80	N.pachyderma sin	19 100±85	22.18	4.35
110	N.pachyderma sin	23 500±140	26.91	6.34
128-131	A-Tn		29.40	7.24
158	N.pachyderma+G.bulloides	29 300±270	32.80	7.94
208	N.pachyderma+G.bulloides	34 200±200	38.33	9.04

图2 LV53-23-1岩心沉积物有机质时间序列剖面 a—TOC;b—TN;c—TOC/TN(质量分数比);d—CaCO3;e—δ13C;f—δ15N。灰色垂直条带代指不同的气候时期。浅蓝色垂直条带代指火山灰层A-Tn。图2c中虚线指示TOC/TN比值为10。图2f中虚线指δ15N=5‰,横轴上部为沉积岩性图。H-LD—全新世-晚冰消期,HS1—Heinrich冰阶1事件,LGM—末次冰盛期。

Fig.2 Temporal profiles of sedimentary organic proxies of core LV53-23-1

图3 TOC-TN(a), TOC-平均粒径[47](b), TOC-绿素[25](c)相关散点图

Fig.3 Scatter plots of (a) TOC vs. TN, (b) TOC vs. mean grain size (adapted from [47]), and (c) TOC vs. chlorin (adapted from [25])

图4 δ15N-δ13C (a), δ15N-绿素[25](b), δ13C-TOC/TN (c)相关散点图

Fig.4 Scatter plots of (a) δ15N vs. δ13C, δ15N vs. chlorin (adapted from [25]), and (c) δ13C vs. TOC/TN

图5 LV53-23-1岩心沉积物有机质δ13C和δ15N与沉积物捕获器[51-52](a)和其他沉积岩心[7-8,39](b)比较

Fig.5 Comparisons of temporal profiles between sedimentary organic matter δ13C, δ15N in core LV53-23-1 and in (a) sediment trap (adapted from [51-52]) or (b) in other cores (adapted from [7,8,39])

图6 沉积物有机质TOC/TN-δ13C(a)和δ15N-δ13C(b)来源判别图

Fig.6 Discrimination plots for sedimentary organic sources. (a) TOC/TN vs. δ13C. (b) δ15N vs. δ13C.

图7 与LV53-23-1岩心其代用指标记录比较 a—δ15N;b—δ13C;c—δ18 OPF[25];d—Mo/Mn;e—U/Th[48];f—绿素含量[25];g—磁化率[25];h—TOC。垂直条带指示意义同图2。

Fig.7 Comparisons of temporal profiles between sedimentary organic matter δ13C, δ15N and other sedimentary proxies of core LV53-23-1

图8 与其他气候环境代用指标记录比较 a—海平面[68];b—中国东部石笋δ18O[69],指示东亚夏季风强度;c—中国黄土平均粒径[73],指示东亚冬季风强度;d—浮游有孔虫壳体δ18O[23,25,70-71],指示表层海水盐度;e—粉砂平均粒径[74]指示西风路径/强度;f—Zr/Sc比值[21]指示对马暖流动力;g—长链烷烃含量[6]指示陆源有机质相对丰度;h—Mo/Mn比值[48],指示底层水缺氧程度;i,j—沉积物δ13C和δ15N。

Fig.8 Comparisons of temporal profiles between sedimentary organic matter δ13C, δ15N and climate and environmental proxies

图9 末次盛冰期(a)和14.5 ka以来(b)日本海海洋环境演化示意图

Fig.9 A Schematic illustration of the environmental evolutions in the Sea of Japan during the Last Glacial Maximum (a) and since 14.5 ka (b)

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37 ka以来日本海沉积物有机质碳和氮稳定同位素变化及其古海洋学意义

Stable carbon and nitrogen isotope variations in sedimentary organic matter in the Sea of Japan since 37 ka: Paleoceanographic implications

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