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Article(id=1200732560268579513, tenantId=1146029695717560320, journalId=1149651085930835976, issueId=1200732559459087132, articleNumber=null, orderNo=null, doi=10.12284/hyxb2024107, pmid=null, cstr=null, oa=null, hot=null, price=null, onlineType=0, articleFormat=0, articleType=null, articleTypeStr=research-article, receivedDate=1716998400000, receivedDateStr=2024-05-30, revisedDate=1725206400000, revisedDateStr=2024-09-02, acceptedDate=null, acceptedDateStr=null, onlineDate=1764206550900, onlineDateStr=2025-11-27, pubDate=1735574400000, pubDateStr=2024-12-31, doiRegisterDate=null, doiRegisterDateStr=null, onlineIssueDate=1764206550900, onlineIssueDateStr=2025-11-27, onlineJustAcceptDate=null, onlineJustAcceptDateStr=null, onlineFirstDate=null, onlineFirstDateStr=null, sourceXml=null, magXml=null, createTime=1764206550900, creator=13701087609, updateTime=1764206550900, updator=13701087609, issue=Issue{id=1200732559459087132, tenantId=1146029695717560320, journalId=1149651085930835976, year='2024', volume='46', issue='12', pageStart='1', pageEnd='134', issueExtLink='null', onlineDate='null', pubDate='null', beforeIssueId=null, nextIssueId=null, price=null, status=1, issueComplete=0, articleOrder=1, issueType=-1, specialIssue=null, createTime=1764206550707, creator=13701087609, updateTime=1764206656941, updator=13701087609, preIssue=null, nextIssue=null, ext={EN=IssueExt(id=1200733005095489798, tenantId=1146029695717560320, journalId=1149651085930835976, issueId=1200732559459087132, language=EN, specialIssueTitle=, coverIllustrator=null, specialIssueEditor=, specialIssueAbout=), CN=IssueExt(id=1200733005095489799, tenantId=1146029695717560320, journalId=1149651085930835976, issueId=1200732559459087132, language=CN, specialIssueTitle=, coverIllustrator=null, specialIssueEditor=, specialIssueAbout=)}, issueFiles=null}, startPage=1, endPage=12, ext={EN=ArticleExt(id=1200732560578958011, articleId=1200732560268579513, tenantId=1146029695717560320, journalId=1149651085930835976, language=EN, title=Variations in temperature and salinity along the MOSAiC drift trajectory and their influencing factors, columnId=1194652705852465724, journalTitle=Haiyang Xuebao, columnName=Article, runingTitle=null, highlight=null, articleAbstract=

Rapid changes in the Arctic environment significantly impact the characteristics of water masses in the Arctic Ocean, potentially affecting the ocean’s physical and biogeochemical processes. This study utilizes the latest MOSAiC observation data (from October 2019 to August 2020) and high-resolution reanalysis data (GLORYS12V1) to analyze the variations in temperature and salinity of water masses across the Eurasian Basin along the MOSAiC drift trajectory, and to explore the influence of the Atlantic inflow on these variations. The results show that: (1) Both temperature and salinity within the upper 100 m layer along the drift trajectory exhibit an overall pattern of initially increasing and then decreasing from the Amundsen Basin to the Nansen Basin. The spatial variation in salinity is greatest within the 0−20 m layer, with highly saline surface water (S >34) present in Nansen Basin. In contrast, the variation in temperature is greatest at the 100 m layer, with the depth of 0℃ isothermal less than 100 m in parts of the Nansen Basin. Although GLORYS12V1 simulates the higher temperature in the upper Nansen Basin, it reasonably captures the main features of horizontal and vertical variations in temperature and salinity along the drift trajectory. (2) The warm and saline Atlantic water generally flows anticlockwise in the Eurasian Basin, with its depth gradually deepening during transport, which predominantly determines the overall variations in temperature and salinity in intermedia and upper layers in the Eurasian Basin. The high salinity of surface water in the Nansen Basin is due to the drift trajectory involved into the regions influenced by deep winter convection in northern Svalbard. Strong wind events play a limited role in the distributional differences of temperature and salinity along the drift trajectory. (3) In the western Nansen Basin, the GLORYS12V1 reanalysis exhibits a northward deviation in the simulated horizontal extent of Atlantic Water, which results in an over estimation of temperature compared to in-situ observations. To improve the accuracy of the GLORYS12V1 simulated results, refining the setting of Atlantic inflow flux at the open boundary is suggested.

, correspAuthors=Xiaofan Luo, authorNote=null, correspAuthorsNote=null, copyrightStatement=Haiyang Xuebao, copyrightOwner=null, extLink=null, articleAbsUrl=null, sourceXml=null, magXml=null, pdfUrl=null, pdf=null, pdfFileSize=null, pdfExtLink=null, richHtmlUrl=null, mobilePdfUrl=null, reviewReport=null, pdfFirstPage=null, abstractGraph=null, abstractGraphContent=null, abstractVideo=null, citation=null, cebUrl=null, magXmlContent=null, mapNumber=null, authorCompany=null, fund=null, authors=null, authorsList=Hanzheng Wang, Xiaofan Luo, Wei Zhao, Hao Wei), CN=ArticleExt(id=1200732563775017689, articleId=1200732560268579513, tenantId=1146029695717560320, journalId=1149651085930835976, language=CN, title=MOSAiC漂流路径上的温盐变化特征及影响因素, columnId=1149698756456657529, journalTitle=海洋学报, columnName=论文, runingTitle=null, highlight=null, articleAbstract=

随着北极环境快速变化，北冰洋水团的分布特征也在发生改变，潜在地影响了海洋内部的物理和生物地球化学过程。本文使用最新的持续近1 a的MOSAiC海洋观测数据和高分辨率GLORYS12V1再分析数据分析了MOSAiC跨欧亚海盆漂流路径上水团温度和盐度的变化特征，并探究了大西洋水入流对路径水团温盐变化的影响。结果表明：（1）沿漂流路径海洋上100 m层的温盐自阿蒙森海盆至南森海盆呈现先升高后降低的变化特征，其中盐度在0～20 m层的空间差异最大，在南森海盆出现盐度大于34的高盐水；温度在100 m层空间差异最大，0℃等温线深度在南森海盆部分海区达到100 m以浅；虽然GLORYS12V1在南森海盆对上层温度模拟偏高，但其整体上抓住了漂流路径上温盐水平和垂向的主要变化特征，模拟水平较好。（2）高温高盐的大西洋水在欧亚海盆总体呈现为逆时针的流环，且输运过程中其深度逐渐加深，决定了中上层海洋温盐水平和垂向分布的整体差异；南森海盆表层20 m的高盐特征是由于漂流路径进入斯瓦尔巴群岛北部冬季深对流的势力范围，而大风事件对漂流路径上层温盐分布差异的作用有限。（3）在南森海盆西部100 m层，GLORYS12V1模拟的大西洋水水平扩展范围偏北，造成了该处模拟温度偏高的现象，分析认为改进边界大西洋入流通量的设置或可提升再分析数据精度。

, correspAuthors=罗晓凡, authorNote=null, correspAuthorsNote=
*罗晓凡，副教授，从事极地海洋生态动力学模拟研究。E-mail：
, copyrightStatement=版权所有©《海洋学报》编辑部 2024
王瀚正，罗晓凡，赵伟，等. MOSAiC漂流路径上的温盐变化特征及影响因素[J]. 海洋学报，2024，46(12)：1–12Wang Hanzheng，Luo Xiaofan，Zhao Wei, et al. Variations in temperature and salinity along the MOSAiC drift trajectory and their influencing factors[J]. Haiyang Xuebao，2024, 46(12)：1–12
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王瀚正（2001—），女，山东省烟台市人，从事极地海洋−海冰−生态环境演变研究。E-mail：

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王瀚正（2001—），女，山东省烟台市人，从事极地海洋−海冰−生态环境演变研究。E-mail：

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王瀚正（2001—），女，山东省烟台市人，从事极地海洋−海冰−生态环境演变研究。E-mail：

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boundary of Atlantic Water (b) derived from GLORYS12V1 reanalysis, figureFileSmall=G9wiMONoJ9X9/OCZeWywZg==, figureFileBig=L/EsO+HXycGeF6zBlsGGRA==, tableContent=null), ArticleFig(id=1200812298777514017, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=CN, label=图7, caption=GLORYS12V1北冰洋大西洋扇区50～200 m平均流场（a）和大西洋水上边界深度（b）的再分析结果, figureFileSmall=G9wiMONoJ9X9/OCZeWywZg==, figureFileBig=L/EsO+HXycGeF6zBlsGGRA==, tableContent=null), ArticleFig(id=1200812298861400099, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=EN, label=Fig. 8, caption=Observed temperature at the 100 m layer from March to May 2020 during MOSAiC and temperature at 100 m layer (a), SSH and ocean current within the upper 100 m layer (b) averaged over March to May 2020 based on GLORYS12V1 reanalysis; temperature at 100 m layer observed by IAOOS 23 platform in western Nansen Basin (c); satellite-based SSH in September 2017 (d); panels (e) and (f) are respectively same as (a) and (b) but for September 2017, figureFileSmall=CBktjJzbOP8ukTn822xQnw==, figureFileBig=senmL4Mbny5U0DSj1F0jGg==, tableContent=null), ArticleFig(id=1200812298974646312, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=CN, label=图8, caption=MOSAiC 2020年3–5月100 m层的观测温度和GLORYS12V1 3–5月平均的100 m层温度（a）、SSH和100 m以上平均流场（b）；IAOOS 23平台在南森海盆西侧100 m层观测的温度（c）；2017年9月卫星观测SSH（d）；GLORYS12V1 2017年9月100 m层温度（e）、SSH和100 m以上平均流场（f）, figureFileSmall=CBktjJzbOP8ukTn822xQnw==, figureFileBig=senmL4Mbny5U0DSj1F0jGg==, tableContent=null), ArticleFig(id=1200812299045949483, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=EN, label=Table 1, caption=

Buoy deployment and recovery metadata

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编号起始时间纬度经度终止时间纬度经度持续时间/d
2019O12019.10.0584.92°N131.27°E2020.08.0578.59°N1.54°W305
2019O22019.10.0784.87°N135.76°E2019.11.1385.95°N120.14°E40
2019O32019.10.0785.05°N137.83°E2020.08.0378.63°N4.35°W301
2019O42019.10.0885.11°N136.28°E2020.08.1480.13°N8.53°W311
2019O52019.10.0985.05°N139.05°E2020.07.1281.32°N1.69°W278
2019O62019.10.1085.14°N133.23°E2020.08.1380.25°N7.49°W308
2019O72019.10.1184.74°N135.84°E2019.10.2585.32°N128.36°E15
2019O82019.10.1184.99°N134.50°E2019.10.2585.55°N126.32°E15
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浮标布放和回收信息

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编号起始时间纬度经度终止时间纬度经度持续时间/d
2019O12019.10.0584.92°N131.27°E2020.08.0578.59°N1.54°W305
2019O22019.10.0784.87°N135.76°E2019.11.1385.95°N120.14°E40
2019O32019.10.0785.05°N137.83°E2020.08.0378.63°N4.35°W301
2019O42019.10.0885.11°N136.28°E2020.08.1480.13°N8.53°W311
2019O52019.10.0985.05°N139.05°E2020.07.1281.32°N1.69°W278
2019O62019.10.1085.14°N133.23°E2020.08.1380.25°N7.49°W308
2019O72019.10.1184.74°N135.84°E2019.10.2585.32°N128.36°E15
2019O82019.10.1184.99°N134.50°E2019.10.2585.55°N126.32°E15
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Classification of water masses

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水团上边界下边界
极地表层水（PSW）海表上盐跃层或冷盐跃层上界
冷盐跃层（CHL）S = 33S = 34
下盐跃层（LHL）S = 34σ = 27.85 kg/m3
大西洋水（AW）θ = 0℃θ = 0℃
), ArticleFig(id=1200812299297607730, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=CN, label=表2, caption=

水团划分标准

, figureFileSmall=null, figureFileBig=null, tableContent=
水团上边界下边界
极地表层水（PSW）海表上盐跃层或冷盐跃层上界
冷盐跃层（CHL）S = 33S = 34
下盐跃层（LHL）S = 34σ = 27.85 kg/m3
大西洋水（AW）θ = 0℃θ = 0℃
), ArticleFig(id=1200812299406659637, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=EN, label=Table 3, caption=

Evaluation of the GLORYS12V1 reanalysis temperature and salinity

, figureFileSmall=null, figureFileBig=null, tableContent=
STDBiasRMSErCF
盐度1.160.630.990.760.88
温度0.820.460.860.481.55
), ArticleFig(id=1200812299486351415, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=CN, label=表3, caption=

GLORYS12V1再分析温盐结果的评估

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STDBiasRMSErCF
盐度1.160.630.990.760.88
温度0.820.460.860.481.55
), ArticleFig(id=1200812299570237498, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=EN, label=Table 4, caption=

Evaluation of the GLORYS12V1 reanalysis ocean current

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浮标U/（cm·s−1）V/（cm·s−1）流速/（cm·s−1）流向/（°）
F1-15观测−2.2814.9815.46296.7
GLORYS−3.549.7411.15308.6
CF1.221.171.120.64
M6观测0.41−0.472.96167.6
GLORYS3.38−1.726.00173.8
CF1.941.221.901.01
M1-1观测7.773.4810.6189.9
GLORYS10.612.5311.1879.8
CF0.710.740.720.57
Karasik观测−0.440.062.01209.8
GLORYS−2.902.093.82305.6
CF1.351.751.551.01
所有站位
集合		CF0.700.590.630.69
r0.640.590.570.50
), ArticleFig(id=1200812299721232446, tenantId=1146029695717560320, journalId=1149651085930835976, articleId=1200732560268579513, language=CN, label=表4, caption=

GLORYS12V1再分析海流结果的评估

, figureFileSmall=null, figureFileBig=null, tableContent=
浮标U/（cm·s−1）V/（cm·s−1）流速/（cm·s−1）流向/（°）
F1-15观测−2.2814.9815.46296.7
GLORYS−3.549.7411.15308.6
CF1.221.171.120.64
M6观测0.41−0.472.96167.6
GLORYS3.38−1.726.00173.8
CF1.941.221.901.01
M1-1观测7.773.4810.6189.9
GLORYS10.612.5311.1879.8
CF0.710.740.720.57
Karasik观测−0.440.062.01209.8
GLORYS−2.902.093.82305.6
CF1.351.751.551.01
所有站位
集合		CF0.700.590.630.69
r0.640.590.570.50
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MOSAiC漂流路径上的温盐变化特征及影响因素
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王瀚正 1 , 罗晓凡 1, * , 赵伟 1 , 魏皓 1
海洋学报 | 论文 2024,46(12): 1-12
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海洋学报 | 论文 2024, 46(12): 1-12
MOSAiC漂流路径上的温盐变化特征及影响因素
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王瀚正1 , 罗晓凡1, * , 赵伟1, 魏皓1
作者信息
  • 1.天津大学 海洋科学与技术学院，天津 300072

    • 王瀚正（2001—），女，山东省烟台市人，从事极地海洋−海冰−生态环境演变研究。E-mail：

通讯作者:

*罗晓凡，副教授，从事极地海洋生态动力学模拟研究。E-mail：
Variations in temperature and salinity along the MOSAiC drift trajectory and their influencing factors
Hanzheng Wang1 , Xiaofan Luo1, * , Wei Zhao1, Hao Wei1
Affiliations
  • 1. School of Marine Science and Technology, Tianjin University, Tianjin, 300072, China
出版时间: 2024-12-31 doi: 10.12284/hyxb2024107
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摘要
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随着北极环境快速变化，北冰洋水团的分布特征也在发生改变，潜在地影响了海洋内部的物理和生物地球化学过程。本文使用最新的持续近1 a的MOSAiC海洋观测数据和高分辨率GLORYS12V1再分析数据分析了MOSAiC跨欧亚海盆漂流路径上水团温度和盐度的变化特征，并探究了大西洋水入流对路径水团温盐变化的影响。结果表明：（1）沿漂流路径海洋上100 m层的温盐自阿蒙森海盆至南森海盆呈现先升高后降低的变化特征，其中盐度在0～20 m层的空间差异最大，在南森海盆出现盐度大于34的高盐水；温度在100 m层空间差异最大，0℃等温线深度在南森海盆部分海区达到100 m以浅；虽然GLORYS12V1在南森海盆对上层温度模拟偏高，但其整体上抓住了漂流路径上温盐水平和垂向的主要变化特征，模拟水平较好。（2）高温高盐的大西洋水在欧亚海盆总体呈现为逆时针的流环，且输运过程中其深度逐渐加深，决定了中上层海洋温盐水平和垂向分布的整体差异；南森海盆表层20 m的高盐特征是由于漂流路径进入斯瓦尔巴群岛北部冬季深对流的势力范围，而大风事件对漂流路径上层温盐分布差异的作用有限。（3）在南森海盆西部100 m层，GLORYS12V1模拟的大西洋水水平扩展范围偏北，造成了该处模拟温度偏高的现象，分析认为改进边界大西洋入流通量的设置或可提升再分析数据精度。

水团  /  MOSAiC  /  模式  /  大西洋水  /  北冰洋

Rapid changes in the Arctic environment significantly impact the characteristics of water masses in the Arctic Ocean, potentially affecting the ocean’s physical and biogeochemical processes. This study utilizes the latest MOSAiC observation data (from October 2019 to August 2020) and high-resolution reanalysis data (GLORYS12V1) to analyze the variations in temperature and salinity of water masses across the Eurasian Basin along the MOSAiC drift trajectory, and to explore the influence of the Atlantic inflow on these variations. The results show that: (1) Both temperature and salinity within the upper 100 m layer along the drift trajectory exhibit an overall pattern of initially increasing and then decreasing from the Amundsen Basin to the Nansen Basin. The spatial variation in salinity is greatest within the 0−20 m layer, with highly saline surface water (S >34) present in Nansen Basin. In contrast, the variation in temperature is greatest at the 100 m layer, with the depth of 0℃ isothermal less than 100 m in parts of the Nansen Basin. Although GLORYS12V1 simulates the higher temperature in the upper Nansen Basin, it reasonably captures the main features of horizontal and vertical variations in temperature and salinity along the drift trajectory. (2) The warm and saline Atlantic water generally flows anticlockwise in the Eurasian Basin, with its depth gradually deepening during transport, which predominantly determines the overall variations in temperature and salinity in intermedia and upper layers in the Eurasian Basin. The high salinity of surface water in the Nansen Basin is due to the drift trajectory involved into the regions influenced by deep winter convection in northern Svalbard. Strong wind events play a limited role in the distributional differences of temperature and salinity along the drift trajectory. (3) In the western Nansen Basin, the GLORYS12V1 reanalysis exhibits a northward deviation in the simulated horizontal extent of Atlantic Water, which results in an over estimation of temperature compared to in-situ observations. To improve the accuracy of the GLORYS12V1 simulated results, refining the setting of Atlantic inflow flux at the open boundary is suggested.

water mass  /  MOSAiC  /  model  /  Atlantic Water  /  the Arctic Ocean
王瀚正, 罗晓凡, 赵伟, 魏皓. MOSAiC漂流路径上的温盐变化特征及影响因素. 海洋学报, 2024 , 46 (12) : 1 -12 . DOI: 10.12284/hyxb2024107
Hanzheng Wang, Xiaofan Luo, Wei Zhao, Hao Wei. Variations in temperature and salinity along the MOSAiC drift trajectory and their influencing factors[J]. Haiyang Xuebao, 2024 , 46 (12) : 1 -12 . DOI: 10.12284/hyxb2024107
正文
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1 引言
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北极是全球气候变化最为显著的区域，大气增温速率已达1979年以来全球大气平均增温速率的4倍[1]。大气温度升高的背景下，北冰洋海冰面积快速缩减成为最引发关注的环境变化之一。据卫星观测数据显示，在1979–2021年间，北极海冰覆盖范围以（54300 ± 2700） km2/a的速度减小[2]。海冰融化会增加海洋的淡水输入，降低表层水的盐度、改变跃层强度，进而影响海洋内部的物质和能量交换过程[3–5]。
北冰洋大西洋扇区毗邻北大西洋，海区中心为阿蒙森海盆和南森海盆，分别位于加各尔海脊两侧（图1）。高温高盐的大西洋入流通过弗拉姆海峡和巴伦支海进入北冰洋，对大西洋扇区内部的水团结构和环流特征有着重要的影响。多年观测指出，自1990s起进入北冰洋的大西洋水核心温度异常升高且流量增强，水层上边界深度也出现变浅趋势[4, 6–9],。大西洋水暖异常和水层变浅，可能导致更多的热量被带到表面，进一步加剧海冰的减少。与此同时在大西洋水之上，盐跃层强度也在不断减弱[10]，进入2010s后，大西洋扇区的盐跃层已减弱至难以抑制热量向表层海冰传递的程度，造成表层海水升温、海冰加速融化，这一现象被称为北冰洋的“大西洋化”[4]。“大西洋化”代表着北冰洋正在向一个全新的气候状态转变，这会对海洋水团和环流、生态系统乃至整个生物地球化学循环过程都产生深刻影响。厘清大西洋扇区水团分布的主要特征及关键影响过程是认识这个新气候状态下海洋动力与生态系统的基础。
受海冰、低温和极夜等恶劣自然条件的限制，在北冰洋开展的调查研究相对较少。为了进一步认识气候变化背景下北极发生的改变，同时加深对北极大气−海洋−海冰相互作用和生物地球化学循环相关过程的理解，国际上发起了北极气候研究多学科漂流冰站观测计划（Multidisciplinary drifting Observatory for the Study of Arctic Climate，MOSAiC，https://mosaic-expedition.org/）。该计划由德国阿尔弗雷德•魏格纳研究所（Alfred Wegener Institute，AWI）主持，全球20多个国家参与组织，主要内容是将“极星号（Polarstern）”科考船固定在海冰上，沿着探险家弗里德约夫•南森在1893–1896年第一次北极漂流探险的路线随冰漂流，同时进行一系列大气、海洋、海冰和生态观测。从2019年9月至2020年8月，MOSAiC计划获得了珍贵的现场观测数据，可用来进一步认识北冰洋大西洋扇区海洋水文结构的更多细节特征。
MOSAiC的海洋数据主要通过温盐深仪（conductivity-temperature-depth，CTD）、声学多普勒流速剖面仪（Acoustic Doppler Current Profiler，ADCP）、浮标等多种观测系统获得[11]。目前，部分海洋温盐数据已初步处理完毕，对漂流路径上的温盐特征有了基本的认识[11–14]。然而，已有研究大多关注于垂向上不同水团的温盐特征，而对整个路径上温盐的变化以及影响温盐变化的过程讨论不足。因此，本文主要关注MOSAiC漂流路径上100 m层温盐变化的特征，并探究影响温盐变化的因素及其主控过程。除观测数据外，本文还结合了GLORYS12V1（Global Ocean Physics Reanalysis）再分析数据来分析影响温盐变化的过程，同时评估了GLORYS12V1在北冰洋大西洋扇区的模拟能力，期望为北冰洋海洋模式的发展提供参考意义。
2 数据与方法
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2.1 观测数据
2.1.1 MOSAiC浮标观测数据
MOSAiC浮标观测系统由8个盐度冰系浮标（Salinity Ice Tether，SIT）组成，编号为2019O1～2019O8[12]。每个浮标配置5个SBE37IMP MicroCAT CTD，分别位于10 m、20 m、50 m、75 m和100 m处，CTD采样频率为2 min 1次，数据传输频率为10 min 1次。处理后的温度、盐度精确度分别为0.002℃、0.01。浮标选址在距离主冰站“极星号”破冰船约40 km处，其漂流路径与主冰站平行，2020年3月之前观测集中在阿蒙森海盆内部，2020年3月跨过加各尔海脊进入南森海盆，在南森海盆进行了为期3个多月的观测，2020年7月到达弗拉姆海峡（图1b）。各浮标观测起止时间和经纬度位置见表1。由于漂流过程中存在海冰的破裂、碰撞，因此浮标2019O2、2019O5、2019O7和2019O8存在数据缺失。本文使用2019O1、2019O3、2019O4和2019O6浮标观测数据进行分析，分析时间段为2019年10月10日至2020年8月3日。
2.1.2 MOSAiC全水深数据
为获得温度、盐度等变量的区域变化，MOSAiC计划在主冰站上配置了一套标准SeaBird SBE911plus装置（简称“PS-CTD”），用于全水深的采样[11]，采样频率为1次/周，1～4航段（Leg1～4）的采样站位位置见图1a。已发布的各航段全水深温盐数据为每个航段所有观测的中值，表层为0 m，每层间隔5 m，最大深度为4 000 m（https://doi.org/10.1594/PANGAEA.936275）。
2.1.3 MOSAiC海表10 m风速
MOSAiC在主冰站附近还设置了气象塔（Meteorological tower）用于记录海冰表面以上2 m和10 m的低空大气特征，包括温度、湿度、气压、风速等[15]。本文主要在第4节使用海表10 m的风速数据进行讨论（https://doi.org/10.1594/PANGAEA.957760）。
2.1.4 IAOOS自主观测平台数据
除MOSAiC观测数据外，本文还使用了2017年IAOOS 23（the Ice Atmosphere Ocean Observing System）自主观测平台在欧亚海盆西部的观测数据[16]。IAOOS的自主平台为冰系漂流平台，其上装备一系列海洋、海冰和大气的观测装置进行物理和生物地球化学观测。IAOOS 23平台于2017年4月12日从北极点附近开始漂流，向西跨过欧亚海盆，于2018年1月到达弗拉姆海峡，漂流路径与MOSAiC相似。温盐观测深度范围为0～400 m，每层间隔0.5 m，本文主要使用其100 m层的温度观测数据在第4节展开讨论，其他数据信息详见Athanase等[16]。
2.1.5 卫星观测海表面高度（Sea Surface Height，SSH）数据
本文使用的SSH观测数据来自CMEMS（the Copernicus Marine Environment Monitoring Service）下SL-TAC（Sea Level Thematic Assembly Centre）Level 4高度计产品。该产品融合多个卫星高度计，提供了1993年以来逐日的观测结果（https://data.marine.copernicus.eu/product/SEALEVEL_GLO_PHY_CLIMATE_L4_MY_008_057/description），其全球水平网格分辨率为0.25° × 0.25°。
2.1.6 锚系浮标海流观测数据
本文使用4组锚系浮标的海流观测数据对GLORYS12V1再分析海流结果进行评估，包括：（1）2015年PS93.1航次在弗拉姆海峡东侧布置的浮标F1-15，数据来源于https://doi.pangaea.de/10.1594/PANGAEA.877960；（2）2013年NABOS（Nansen and Amundsen Basins Observational System）于拉普捷夫海和喀拉海北部陆坡布放的浮标M1-1和M6，数据来源及相关介绍详见https://uaf-iarc.org/NABOS/；以及（3）2015年PS94航次在阿蒙森海盆中部的浮标Karasik，数据来源于https://doi.pangaea.de/10.1594/PANGAEA.870849。其中，浮标F1-15分析时间段为2015年7–11月，观测深度20～240 m；浮标M1-1和M6分析时间段均为2014年9月至2015年8月，观测深度分别为0～260 m和0～60 m；浮标Karasik分析时间段为2015年9月至2016年8月，观测深度在20～300 m。各浮标观测频率为每60 min观测1次，均处理为逐日结果并在观测深度上平均；同样地，GLORYS12V1再分析海流也处理为与浮标观测时间相同的逐日结果，并在观测深度上平均。
2.2 GLORYS12V1再分析数据
GLORYS12V1是CMEMS的全球海洋再分析产品（https://data.marine.copernicus.eu/product/GLOBAL_MULTIYEAR_PHY_001_030/description），其海洋环流模式基于NEMO海洋模块构建，水平网格分辨率为（1/12）°，垂向分为50层。GLORYS12V1使用降阶卡尔曼滤波同化了温度、盐度、海冰等要素场，同时采用三维变分算法，以校正模型大尺度、缓慢演化的误差。用于同化的观测资料包括CMEMS沿轨卫星高度计的海平面高度异常、卫星传感器AVHRR的海表面温度、Ifremer/CERSAT的海冰密集度，以及CORA数据集中现场观测的温盐垂向剖面[17]。CORA的温盐数据覆盖1990‒2010年，在2000年后，尽管Argo浮标的使用确保了全球海洋中每个1° × 1°网格每年至少有1～2个观测剖面，但温盐观测密度的空间差异仍然较大，尤其在高纬海冰覆盖的海区取样密度较低[18]。GLORYS12V1数据集提供了自1993年以来海平面高度、温度、盐度、海流和海冰密集度等关键海洋状态量，能够准确捕捉到海洋、海冰、大尺度环流以及海盆间交换的年际变化信号，为气候变化的研究提供可靠的物理海洋状态，同时也可用于区域海洋的研究。
2.3 分析方法
2.3.1 统计量
为评估GLORYS12V1再分析数据的结果，本文使用标准差（STD）、偏差（Bias）、均方根误差（RMSE）、相关系数（r）和成本函数（Cost Function，CF）对MOSAiC观测站位上同期的再分析结果进行评估。其中，CF值是表征相较于观测值本身波动的再分析结果与观测值差异的统计量，CF＜1表示模拟非常好，1＜CF≤2表示模拟好，2＜CF≤3表示模拟合理，CF＞3表示模拟差[19]。主要计算公式如下，其中M为模拟值，O为观测值，i为观测站位，N为观测值个数，上标“—”指算术平均值。
$ {\mathrm{STD}}=\sqrt{{\sum }_{i=1}^{N}{({O}_{i}-\overline{O})}^{2}/(N-1)}， $
$ {\mathrm{Bias}}=\left|\overline{M}-\overline{O}\right|， $
$ {\mathrm{RMSE}}=\sqrt{{\sum }_{i=1}^{N}{({M}_{i}-{O}_{i})}^{2}/N}， $
$ {\mathrm{CF}}=\frac{1}{N}{\sum }_{i=1}^{N}\frac{\left|{M}_{i}-{O}_{i}\right|}{{\mathrm{STD}}\left(O\right)}. $
2.3.2 水团划分
北冰洋水团在垂向上大致可分为4个部分：（1）极地表层水（Polar Surface Water，PSW）位于海冰之下，50 m以上，水体混合均匀，温度接近冰点，盐度较低；（2）盐跃层（Halocline Layer）在极地表层水之下，以低温（−1℃）高盐为主要特征，海冰的形成和融化对其强弱有关键的影响；（3）高温（>0℃）高盐（约34.8）的大西洋水（Atlantic Water，AW）在海盆内位于150～900 m，主要通过弗拉姆海峡和巴伦支海分两路从北大西洋进入北冰洋，其热量在向上传递的过程中会受到盐跃层的阻隔；（4）深层水和底层水分布于各海盆深处，水团性质均一稳定，基本保持不变[20–23]。北冰洋温盐的垂向变化主要在大西洋水之上，温盐在深层具有均一性，因此本文主要聚焦于大西洋水及之上水团在MOSAiC漂流路径上的温盐变化特征。
在北冰洋，通常把温度大于0℃的水体定义为大西洋水。在大西洋水之上，盐跃层可分为3部分：上盐跃层（Upper Halocline Layer，UHL）、冷盐跃层（Cold Halocline Layer，CHL）和下盐跃层（Lower Halocline Layer，LHL）。上盐跃层主要源自于太平洋扇区，盐度较低，其在欧亚海盆的扩展范围年际差异大，主要受穿极流的位置影响[24–25]。下盐跃层是大西洋水从巴伦支海或斯瓦尔巴群岛北部流入北冰洋时冷却变淡形成的，在流动过程中被转化的大西洋水与冷淡水进一步混合形成冷盐跃层，二者的差异在于下盐跃层的盐度和温度比冷盐跃层高，更接近大西洋水[26–28]。以往通常把S = 34.3定义为下盐跃层底部[29]，但由于近年来欧亚海盆的“大西洋化”，盐跃层盐度增加，Bertosio等[30]指出以往在阿蒙森海盆对盐跃层底部的定义已不再适用，并通过比较NO参数（NO = 9 × [NO3] + [O2]）和温盐梯度提出了在阿蒙森海盆以27.85 kg/m3作为下盐跃层底部的方法。本文参考Bertosio等[30]的研究结果，使用的水团划分标准见表2，其中S代表盐度，θ为位温，σ为密度超量。
3 结果
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3.1 MOSAiC浮标观测的温盐变化特征
温盐点聚图划分了漂流路径上100 m层的主要水团，以及水团在不同海盆内温盐特征的差异（图2a）。表层水在阿蒙森海盆更冷更淡。温度最小值在阿蒙森海盆位于冷盐跃层之上，而在南森海盆出现在下盐跃层。此外，在上100 m层，南森海盆已出现大西洋水，而在阿蒙森海盆未观测到温度大于0℃的暖水。MOSAiC浮标观测到的水团温盐特征与早期观测结果[3]基本一致，表明近些年水团整体变化不大。
浮标观测显示，沿漂流路径表层（0～20 m）盐度的空间变化显著，整体上呈现先升高后降低的变化特征（图2b）。在阿蒙森海盆表层盐度较低，约为32，越过加各尔海脊时，盐度逐渐升高，至南森海盆表层盐度高于34，而漂流至弗拉姆海峡后，表层盐度又降低到32以下。在表层之下，盐度随深度升高，且沿漂流路径空间变化逐渐减小，至100 m层基本维持在34～34.4之间，空间变化最小。沿漂流路径表层（0～20 m）温度基本在冰点附近，在弗拉姆海峡处略有升高（图2c）。表层之下，温度随深度增加，且空间差异逐渐变大。阿蒙森海盆100 m以上均为温度小于−1℃的冷水，而在南森海盆100 m层观测到温度大于0℃的大西洋暖水。值得注意的是，2020年4–5月漂流至南森海盆西部时，观测到100 m以浅为混合均匀、温盐性质均一的高盐低温水。为进一步认识影响漂流路径上温盐变化的主要因素，后文使用GLORYS12V1再分析数据做更深入的探究。
3.2 GLORYS12V1在漂流路径上的再分析结果
与观测相比（图3a），虽然在阿蒙森海盆内GLORYS12V1 50～100 m层的盐度偏低，但其再现了表层（0～20 m）盐度沿漂流路径先显著升高后缓慢降低的变化特征，抓住了盐度空间分布的差异。100 m以浅再分析盐度的偏差为0.63，RMSE为0.99，r为0.76，CF为0.88（表3），表明盐度在整个漂流路径上的模拟水平很好。温度在南森海盆50～100 m层的再分析结果偏高（图3b），表现为在漂流路径上提早出现了大西洋水的暖水信号。尽管如此，GLORYS12V1合理刻画了漂流路径上表层（0～20 m）温度接近冰点的特征，同时抓住了50～100 m层温度的变化特征—即在阿蒙森海盆为小于‒1℃的冷水，而在南森海盆存在大西洋暖水。整个路径上100 m层再分析温度的偏差为0.46℃，CF为1.55，模拟水平较好。此外，GLORYS12V1也抓住了海盆内盐度随深度增加、在大西洋水层温度最大的垂向变化特征（图4），同时相比于阿蒙森海盆（Leg1～3），大西洋水在南森海盆（Leg4）的核心温度更高、水层更厚。总体上，GLORYS12V1的再分析结果虽然在量值上稍有偏差，但其能够合理再现漂流路径上主要的温盐变化特征，可以用于进一步的分析。
根据再分析结果，沿漂流路径温盐等值线表现为从阿蒙森海盆到南森海盆向上倾斜，加各尔海脊是两个海盆间的过渡，存在明显的锋面（图3）。混合层深度从拉普捷夫海北部向南森海盆逐渐加深，在南森海盆西部最深可达50 m，到弗拉姆海峡深度变浅，该变化趋势与MOSAiC ITP结果相一致[11]。在阿蒙森海盆，27.85 kg/m3等密线（即下盐跃层底部）的深度与0℃等温线相当，约250 m，该深度处盐度接近35，远大于34.3，从再分析结果说明了Bertosio等[30]将σ = 27.85 kg/m3视为下盐跃层底部的合理性。沿漂流路径，在南森海盆表层出现低温高盐水，其盐度值大于34，与浮标观测结果相吻合。盐跃层在南森海盆水团厚度较薄，位置较浅，下盐跃层底部深度小于200 m，而在阿蒙森海盆盐跃层深度可达250 m。此外，南森海盆存在显著的大西洋水暖水核，0℃等温线深度在部分区域达到100 m以浅，而阿蒙森海盆大西洋水深度大于200 m。
4 分析与讨论
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海冰主要通过结冰和融冰过程对表层温盐产生影响[31]。由于MOSAiC计划本身是冰站观测，在漂流路径上均有海冰覆盖，无明显的结冰和融冰过程，因此海冰不是导致上100 m层温盐变化的主要原因。
在局地过程中，大风事件会加强海水的垂向混合，破坏水体层结，使混合层加深，进而造成海洋内部热量向表层和大气的释放[32–33]，因此强风会对温盐的垂向分布产生扰动。通过分析，Rinke等[34]指出，MOSAiC期间较强的气旋主要出现在冬春季节，尤其是在2020年2–4月。本文对比了冬春季MOSAiC海表面10 m风速与上100 m层温盐的变化（图5）。冬春季节，海表平均风速分别为5.5 m/s和6.2 m/s，大风事件集中在2–4月，最大风速可达12 m/s。根据温盐垂向特征，MOSAiC漂流路径上混合层深度约为20～50 m，而大风经过时（图5中阴影）50 m以浅的温盐未观测到显著“扰动”迹象，可见风致混合作用有限，大风事件对漂流路径上温盐变化的影响并不显著。
欧亚海盆毗邻北大西洋，高温高盐的大西洋水进入北冰洋后位于中层（约150～900 m），是影响海洋上层温盐分布特征的重要因素，因此进一步探讨大西洋水的入流路径对欧亚海盆上层海洋水团温盐分布特征的影响。早期研究指出大西洋水主要通过弗拉姆海峡和巴伦支海进入北冰洋。弗拉姆海峡分支经过斯瓦尔巴群岛北部后作为边界流向东流动，在圣安娜海槽北部与巴伦支海分支汇合后继续沿陆坡流动，而后在拉普捷夫海北部分向两个方向，一部分经阿蒙森海盆返回弗拉姆海峡，另一部分则继续向加拿大海盆流动[27, 35–37]。在流动过程中，大西洋水主要通过湍流、冬季对流混合和双扩散过程与周围水体进行热盐交换[38–39]，其核心温度逐渐降低。在此，首先使用4组锚系浮标的海流数据评估了GLORYS12V1对大西洋扇区大尺度环流结构的刻画能力，浮标分别位于弗拉姆海峡东侧（F1-15）、喀拉海北部陆坡（M6）、拉普捷夫海北部陆坡（M1-1）和阿蒙森海盆（Karasik，图6），均为大西洋水逆时针输运的关键位置。对比观测期间的平均结果可知（表4），GLORYS12V1在各浮标处对流向的模拟准确，能够再现大西洋水从弗拉姆海峡向北进入北冰洋后沿陆坡向东的边界流，以及在阿蒙森海盆内返回弗拉姆海峡的西向流（与MOSAiC从阿蒙森海盆东部至弗拉姆海峡的漂流路径相一致），从而抓住了绕欧亚海盆的逆时针环流结构（图6），整体上观测与GLORYS12V1流向的CF值为0.69，模拟水平很好。同时，GLORYS12V1刻画出了在浮标F1-15和M1-1处海流流速大的特点，而在浮标M6和Karasik处模拟的流速偏高，各站位流速模拟的CF值均小于2，所有站位集合后的流速东分量（U）、北分量（V）的CF值小于1，相关系数r约0.6，表明GLORYS12V1能够准确模拟出流速在陆坡大、在海盆内部小的大尺度空间分布特征，可用于后续的分析。
根据GLORYS12V1再分析的大西洋入流结构（图7a），沿入流主轴，在弗拉姆海峡东部、巴伦支海和南森海盆陆坡处流速较大，到阿蒙森海盆内部流速变小，绕欧亚海盆形成逆时针流环，自弗拉姆海峡西部流出。与此同时，沿入流路径，大西洋水的上边界深度也在不断加深（图7b）。在斯瓦尔巴群岛北部，上边界深度小于50 m，到南森海盆东部上边界加深至100 m，而后在阿蒙森海盆内部，大西洋水上边界深度达到200 m，进入加拿大海盆内，大西洋水的位置继续加深，部分海区大于300 m。
大西洋水的输运路径及深度变化对上层海洋的温盐变化起着决定性作用。沿大西洋水输运路径，陆地径流的输入使表层盐度减小，水体层化加强，混合层深度变浅，同时大西洋水深度加深，高盐高温特征在上层不显著（图7b）。MOSAiC的漂流路径为从阿蒙森海盆流至南森海盆，而后到弗拉姆海峡西部，与大西洋水入流方向相反，故观测的上100 m层温盐呈现先显著升高而后降低的变化特征。2020年4–5月南森海盆表层观测到低温高盐水，虽然高盐体现出可能存在深处涌升现象，但低温水的特征又表明此处并不存在涌升。GLORYS12V1再分析结果指出此处的低温高盐水主要为斯瓦尔巴群岛北部表层水扩展。已有研究表明在斯瓦尔巴群岛北部，由于大西洋水深度较浅且水体层结弱，冬季对流深度远大于中央海盆，塑造了表层水的高盐特征[27, 29]（图7b黄色阴影），而MOSAiC的漂流路径恰好在4–5月进入到高盐水的影响范围，导致观测结果呈现表层高盐的特征。
2020年3月末，MOSAiC浮标从阿蒙森海盆漂流跨过加各尔海脊进入南森海盆。根据3.2节的比较结果，3月底至5月初在南森海盆西部100 m层观测到温度小于−1℃的低温水，而GLORYS12V1在同一位置的再分析结果却显示为温度大于0℃的大西洋水（图3b，图8a），再分析结果比观测高近2℃。GLORYS12V1 100 m层温度的空间分布显示（图8a），大西洋水入流进入北冰洋后，在南森海盆西部水平向北扩展，其北边界到达加各尔海脊。在空间上，GLORYS12V1的大西洋水范围覆盖了MOSAiC的漂流路径，使得在再分析场中浮标3月底就已经进入大西洋水的范围内，而实际的观测场在6月才出现大西洋暖水信号。与MOSAiC结果相同的是，2017年IAOOS在南森海盆西部100 m层的观测也显示为低温水团[16]（约−1℃，图8c）。与同期GLORYS12V1结果相对比（图8e），发现同样存在再分析比观测温度高的现象；同时，2017年GLORYS12V1的大西洋水水平范围也向北扩展至加各尔海脊处，使得再分析场中观测路径上的温度偏高。综合两个航次的对比结果，认为是GLORYS12V1在100 m层模拟的大西洋水扩展范围偏北导致了再分析结果与观测间的差异。
水团的分布通常与环流结构息息相关。在GLORYS12V1的结果中（图8b和f），SSH在加各尔海脊南侧以南森海盆西部为中心呈现中间低四周高的空间分布，根据地转平衡关系，该处环流方向为气旋式，这与大西洋水的水平扩展范围相一致。而在卫星观测中（图8d，由于MOSAiC观测期间3–5月海冰覆盖率高，该处使用2017年9月IAOOS的对比结果），虽然极点附近被海冰覆盖，但仍能对比出低SSH中心比再分析结果更靠近加各尔海脊，且核心位置偏东，而GLORYS12V1的低SSH中心偏南，更靠近大西洋水在弗拉姆海峡的入口，与观测的空间分布有所差异。
综上，MOSAiC和IAOOS的观测结果共同说明了GLORYS12V1在100 m层对大西洋水的扩展范围模拟偏北导致了再分析温度高于观测，而根据水团与环流的关系，这意味着GLORYS12V1的环流结构也未能完全抓住大西洋水的流动细节。尽管GLORYS12V1能够准确描述大西洋水大尺度环流的基本结构，但其对区域环流的细节刻画还有待提高，本文认为通过调整大西洋水入流通量或可提高再分析数据的模拟精度，从而使模拟结果得到进一步优化。
5 总结与展望
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本文使用最新的MOSAiC观测数据和高分辨率GLORYS12V1再分析数据分析了MOSAiC漂流路径上的温盐变化特征，并探究其影响因素。观测结果表明，漂流路径上100 m层的温盐变化总体上表现为自阿蒙森海盆至南森海盆先升高，接近弗拉姆海峡又略有降低。其中，盐度在0～20 m空间差异最大，南森海盆表层存在盐度大于34的高盐水，在100 m层无异质性；温度恰好相反，表层温度均接近冰点，100 m层空间差异最大，南森海盆部分区域0℃等温线在100 m以浅。在垂向上，南森海盆内大西洋水较阿蒙森海盆核心温度更高且水层更厚。对比GLORYS12V1，虽然在南森海盆的再分析温度偏高，但GLORYS12V1很好地再现了上100 m层温盐先升高后降低的主要特征，捕捉到了温盐水平和垂向的变化趋势。
在北冰洋欧亚海盆，大西洋水入流的环流结构和水层的深度变化是影响上层海洋水团温盐变化的主要过程。大西洋水从弗拉姆海峡和巴伦支海进入北冰洋，在欧亚海盆逆时针流动的过程深度逐渐加深，核心温度降低，从而导致了海洋中上层水体温盐在水平和垂向上分布的整体差异。在南森海盆西部，漂流路径进入斯瓦尔巴群岛北部的冬季深对流区，造成表层水的高盐特征，而大风事件造成的垂向混合作用有限。GLORYS12V1在南森海盆西部对大西洋水范围模拟偏北，导致了再分析结果与观测温度的差异，根据水团与环流间的相互影响关系，本文认为可以通过调整大西洋水的入流通量优化模型的再分析结果。
海洋水团的变化受环流结构变化的调控，归因于气候和环境变化，最终会影响海洋生物和生态系统。在气候变化背景下，来自北大西洋热量输入的正异常对北冰洋大西洋扇区的影响十分显著，如大西洋扇区东侧出现的“大西洋化”现象和亚北极海洋生物的向北迁移（Borealization）[40]。高纬度地区对这些新变化是如何响应的，其中仍有许多问题亟待解决。随着北极海冰减少和大西洋水的异常变化，未来需要更多的关注投入到北冰洋大西洋扇区的研究当中，同时也需要更高频密集的观测以及更精准的数值模式为相关研究提供支持。
基金
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  • 国家重点研发计划(2023YFC2809105)
  • 国家重点研发计划(2023YFC3107702)
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2024年第46卷第12期
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文章信息
doi: 10.12284/hyxb2024107
  • 接收时间：2024-05-30
  • 首发时间：2025-11-27
  • 出版时间：2024-12-31
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  • 收稿日期：2024-05-30
  • 修回日期：2024-09-02
基金
国家重点研发计划(2023YFC2809105)
国家重点研发计划(2023YFC3107702)
作者信息
    1.天津大学 海洋科学与技术学院，天津 300072

通讯作者:

*罗晓凡，副教授，从事极地海洋生态动力学模拟研究。E-mail：
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Family		 属数
Number of
genus		 种数
Number of
species		 占总种数比例
Percentage of
total species (%)		 属
Genus		 种数
Number of
species		 占总种数比例
Percentage of total
species (%)
鹅膏菌科Amanitaceae 2 11 5.26 鹅膏菌属 Amanita 10 4.78
小菇科 Mycenaceae 2 12 5.74 丝盖伞属 Inocybe 5 2.39
多孔菌科 Polyporaceae 8 14 6.70 蜡蘑属 Laccaria 5 2.39
红菇科 Russulaceae 3 23 11.00 小皮伞属 Marasmius 6 2.87
小菇属 Mycena 11 5.26
光柄菇属 Pluteus 5 2.39
红菇属 Russula 17 8.13
栓菌属 Trametes 5 2.39
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