黄海全新世浮游植物生产力和群落结构变化规律及控制机制
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摘要
黄海是西北太平洋非常重要的陆架边缘海，地处亚洲季风影响的区域，又受到黄海暖流及黑潮的作用，其生态环境具有明显的区域性特征。为揭示黄海全新世期间生态环境演变规律的控制机制，需要有长期的黄海生态环境演变资料，因此高分辨率的黄海全新世古环境记录非常重要。本论文利用南黄海中部泥质区同一纬度断面的三个沉积物岩心（YS01，ZY1，ZY2）的生物标志物指标，基于海源生物标志物含量可以反映浮游植物生产力，生物标志物比值可以反映浮游植物群落结构的前提，重建了南黄海全新世的浮游植物生产力和群落结构以及海水表层温度（SST），对黄海全新世生态环境的演变规律及控制机制进行探讨。
早全新世阶段（10.5-7ka），南黄海的生态环境主要受海平面变化的控制。在7ka之前的全新世低海平面阶段，生物标志物指标重建的浮游植物生产力以及颗石藻对浮游植物群落结构的贡献都很低。多个生物标志物指标都记录了9.6ka MWP-1C融水脉冲事件：在MWP-1C之前，海洋初级生产力较低，陆源有机质的相对贡献很高；在MWP-1C之后，海洋初级生产力升高，陆源有机质的相对贡献快速降低，但沉积有机质中陆源有机质仍占主导。早全新世低海平面阶段，研究站位更容易受到陆地径流量的影响。在夏季季风影响下，降雨引起的陆地径流使黄海处于低盐河口环境，不利于颗石藻生长。相比中晚全新世，早全新世时期颗石藻对浮游植物群落的贡献相对较低。
中晚全新世阶段（7-0ka），海平面趋于稳定，黄海暖流入侵黄海，黄海环流体系形成。黄海暖流的入侵对南黄海的生态环境产生很大影响，浮游植物生产力和群落结构对黄海暖流的强度以及路径的变化有直接响应，受控于黄海暖流的变化。总体上讲，浮游植物生产力水平在中晚全新世黄海环流体系形成后整体升高，陆源有机质对沉积有机质的贡献较早全新世降低。岩心ZY1及ZY2生物标志物含量结果显示，两岩心的总浮游植物生产力水平的变化趋势相似。从6ka至0ka，两岩心的总生产力都呈上升趋势，并且在3ka都有明显的转变，东亚冬季风是该阶段南黄海浮游植物生产力的控制因素。黄海环流体系形成后，自6ka以来增强的东亚冬季季风驱动会使黄海环流体系增强，且可以通过风尘输入为南黄海带来更多的营养盐，都有利于浮游植物初级生产力的提高。而位于最西侧更靠近黄海沿岸流的YS01岩心记录的生产力从6ka以来没有明显上升趋势，且此岩心附近海域浮游植物生产力平均水平高于另外两个岩心，表明该处浮游植物生产力除了受东亚冬季季风的控制，可能还受黄海陆架锋锋面上升流的影响。由于对高盐度环境的需求，颗石藻生产力变化同时受到黄海暖流强度及夏季季风降水引起的径流量强弱的影响。在黄海暖流影响的区域，黄海暖流影响增强，利于颗石藻生长，使得颗石藻对浮游植物群落结构的相对贡献增大。南黄海浮游植物生产力和群落结构在晚全新世（3ka）有明显改变，这可能与ENSO活动强度增大、频次增多的影响相关，但其作用机制尚未清楚，可能与大气及海洋环流的变化有关。
岩心ZY1及ZY2的长链烯酮含量及生物标志物比值（A/B）在中晚全新世的变化有一定的差异，两岩心指标的差值与黑潮强度指标的变化趋势比较一致，反映了黄海暖流主流轴中晚全新世的空间摆动。在黑潮增强阶段（6-4.2ka和1.7-0ka），黄海暖流主流轴向东摆动，对岩心ZY1影响较大，表现为颗石藻生产力及对其浮游植物群落结构的相对贡献更高。相反，在黑潮减弱阶段（4.2-1.7ka），黄海暖流主流轴向西摆动，对岩心ZY2影响更大，引起较高的颗石藻生产力及其对浮游植物群落结构相对较高的贡献。
岩心YS01的SST结果记录了南黄海全新世的气候演化的经历：早全新世阶段（9.6-7ka），主要受北半球太阳辐射的变化控制，呈大幅波动增温过程；中全新世阶段（7-2.8ka），从6.8ka黄海暖流入侵黄海维持高温到6ka后，SST整体降低，呈现低温震荡；晚全新世阶段（2.8-0ka），SST整体升高且呈小振幅波动。在黄海暖流入侵黄海后的中晚全新世，黄海暖流影响区域SST的变化受黄海暖流控制，并且对黑潮的变化有很好响应。
岩心YS01的SST记录反映出南黄海全新世存在几次明显的降温事件：0.3-0.5ka，1.2-1.6ka，2.7-3.1ka，4.2-4.5ka，5.5-5.9ka，6.9-7.2ka，8.1-8.5ka和9.2-9.5ka，并且SST记录中存在~532年变化周期，生物标志物比值A/B记录存在~1560年的变化周期，这与北大西洋、黑潮和陆地等全球环境指标记录的气候突变事件及周期循环有较好的一致性。说明南黄海在黄海暖流控制下，通过大气及海洋环流的变化对全球气候变化事件也有较好的响应。该岩心的SST记录表明南黄海的古环境演化在区域性海洋环境尤其是黄海暖流控制下对全球性气候变化的响应。
The Yellow Sea (YS) is an important marginal sea in the northwestern Pacific andits environment and ecology have changed significantly during the Holocene. Thechanges were driven by the interactions of the Yellow Sea Warm Current (YSWC),the East Asian Monsoon (EAM) and the Kuroshio Current (KC). In order to study theHolocene environmental and ecosystem variations in the YS, high-resolution recordswhich could provide materials for paleoclimatic and palaeoceanographic research arenecessary. This thesis carries out the multi-biomarkers in three sediment cores (YS01,ZY1, ZY2) drilled from the same latitude section in the South Yellow Sea (SYS)central mud area to reconstruct the past sea surface temperature (SST), phytoplanktonproductivity and community structure changes. The biomarker method is based on theassumptions that sedimentary biomarker contents reflect phytoplankton productivityand biomarker ratios reflect community structure.
During the early Holocene (10.5-7ka), the phytoplankton primary productivityand community structure changes in the SYS are mainly controlled by the sea-levelrising and display lower paleoproductivity and haptophyte contribution. The rapidsea-level rise event MWP-1C occurred in9.6ka was recorded in core YS01withincreased primary productivity and decreased terrestrial organic matter contribution.Reconstructed phytoplankton community structure variations may also be affected bythe East Asian Summer Monsoon (EASM) which could lead to the precipitationchanges. More runoff transported to the YS induced by stronger rainfall precipitationwould decrease the salinity, which would result in less haptophyte contribution. TheYS was in a low salinity estuarine environment stage during the early Holocene andhaptophytes contribute less compared with the Mid-late Holocene.
During the Mid-late Holocene (7-0ka), after the intrusion of the YSWC at about6.8ka, the SYS environment has been under the influence of the YSWC, andproductivity-community structure has been affected by the YSWC strength-pathwayvariations. Phytoplankton productivity is enhanced and contributes more comparedwith terrestrial organic matters after the formation of the YS circulation system. Thecontent values of the marine biomarkers in the core ZY1and ZY2are similar, andthey also reveal similar temporal trends. From6ka to3ka, the biomarker contents inthe two cores were relatively low with small oscillations, followed by a distinctincrease at about3ka which indicated productivity increased with stronger East AsianWinter Monsoon (EAWM). The circulation system in the YS are strengthened byincreased EAWM. In addition, a stronger EAWM could increase nutrient levels ineuphotic layer and increase dust input, all enhancing productivity. For core YS01which locates to the west of the other two cores, the marine biomarker contents ishigher and lack of an increasing trend. We presume that the productivity in thislocation could also be affected by the YS continental shelf front upwelling besides theEAWM. In areas influenced by the YSWC, an increase in haptophyte contributionwould be caused by stronger YSWC influence with the EASM precipitationmodulating. The abrupt increase of productivity values and haptophyte contributionduring the late Holocene (3ka) may be related to the occurrence of stronger and morefrequent ENSO, reflecting the onset and enhanced magnitude of modern ENSOsystem.
Some differences of the biomarker records between core ZY1and ZY2suggestspatial variations in responses to YSWC and KC forcing. When the KC wasintensified during the periods6-4.2ka and1.7-0ka, the YSWC extended eastward,exerting more influence on core ZY1. On the other hand, when the KC weakenedduring4.2-1.7ka, the YSWC extended westward, exerting more influence on the coreZY2.
The SST results in core YS01show that three periods of the regional climatechanges can be identified during the Holocene. During the early Holocene (9.6-7ka),it shifted from cold to warm with large amplitude under the control of Northern Hemisphere solar irradiance; the middle Holocene (7-2.8ka), the higher SST lasteduntil6ka and then decreased with oscillation; the late Holocene (2.8-0ka), theclimate was replaced by a warm stage with small fluctuations. The SST changes arecontrolled by the YSWC and in good response to the KC variations.
There are also eight cold events recorded in core YS01, which occurred at0.3-0.5ka,1.2-1.6ka,2.7-3.1ka,4.2-4.5ka,5.5-5.9ka,6.9-7.2ka,8.1-8.5ka and9.2-9.5kathrough the last9.6ka. The SST displays periodicity of~532yr during the last9.6kaand biomarker proxy A/B ratio displays periodicity of~1560yr after the YSWCintrusion. The cold events and the millennial scale climate cycle appear to correlatewell with records in the North Atlantic, the KC and other different regions of theworld, suggesting global climatic tele-connections. The SST records in core YS01indicate that the YS climate is affected by global and regional climate change.
早全新世阶段（10.5-7ka），南黄海的生态环境主要受海平面变化的控制。在7ka之前的全新世低海平面阶段，生物标志物指标重建的浮游植物生产力以及颗石藻对浮游植物群落结构的贡献都很低。多个生物标志物指标都记录了9.6ka MWP-1C融水脉冲事件：在MWP-1C之前，海洋初级生产力较低，陆源有机质的相对贡献很高；在MWP-1C之后，海洋初级生产力升高，陆源有机质的相对贡献快速降低，但沉积有机质中陆源有机质仍占主导。早全新世低海平面阶段，研究站位更容易受到陆地径流量的影响。在夏季季风影响下，降雨引起的陆地径流使黄海处于低盐河口环境，不利于颗石藻生长。相比中晚全新世，早全新世时期颗石藻对浮游植物群落的贡献相对较低。
中晚全新世阶段（7-0ka），海平面趋于稳定，黄海暖流入侵黄海，黄海环流体系形成。黄海暖流的入侵对南黄海的生态环境产生很大影响，浮游植物生产力和群落结构对黄海暖流的强度以及路径的变化有直接响应，受控于黄海暖流的变化。总体上讲，浮游植物生产力水平在中晚全新世黄海环流体系形成后整体升高，陆源有机质对沉积有机质的贡献较早全新世降低。岩心ZY1及ZY2生物标志物含量结果显示，两岩心的总浮游植物生产力水平的变化趋势相似。从6ka至0ka，两岩心的总生产力都呈上升趋势，并且在3ka都有明显的转变，东亚冬季风是该阶段南黄海浮游植物生产力的控制因素。黄海环流体系形成后，自6ka以来增强的东亚冬季季风驱动会使黄海环流体系增强，且可以通过风尘输入为南黄海带来更多的营养盐，都有利于浮游植物初级生产力的提高。而位于最西侧更靠近黄海沿岸流的YS01岩心记录的生产力从6ka以来没有明显上升趋势，且此岩心附近海域浮游植物生产力平均水平高于另外两个岩心，表明该处浮游植物生产力除了受东亚冬季季风的控制，可能还受黄海陆架锋锋面上升流的影响。由于对高盐度环境的需求，颗石藻生产力变化同时受到黄海暖流强度及夏季季风降水引起的径流量强弱的影响。在黄海暖流影响的区域，黄海暖流影响增强，利于颗石藻生长，使得颗石藻对浮游植物群落结构的相对贡献增大。南黄海浮游植物生产力和群落结构在晚全新世（3ka）有明显改变，这可能与ENSO活动强度增大、频次增多的影响相关，但其作用机制尚未清楚，可能与大气及海洋环流的变化有关。
岩心ZY1及ZY2的长链烯酮含量及生物标志物比值（A/B）在中晚全新世的变化有一定的差异，两岩心指标的差值与黑潮强度指标的变化趋势比较一致，反映了黄海暖流主流轴中晚全新世的空间摆动。在黑潮增强阶段（6-4.2ka和1.7-0ka），黄海暖流主流轴向东摆动，对岩心ZY1影响较大，表现为颗石藻生产力及对其浮游植物群落结构的相对贡献更高。相反，在黑潮减弱阶段（4.2-1.7ka），黄海暖流主流轴向西摆动，对岩心ZY2影响更大，引起较高的颗石藻生产力及其对浮游植物群落结构相对较高的贡献。
岩心YS01的SST结果记录了南黄海全新世的气候演化的经历：早全新世阶段（9.6-7ka），主要受北半球太阳辐射的变化控制，呈大幅波动增温过程；中全新世阶段（7-2.8ka），从6.8ka黄海暖流入侵黄海维持高温到6ka后，SST整体降低，呈现低温震荡；晚全新世阶段（2.8-0ka），SST整体升高且呈小振幅波动。在黄海暖流入侵黄海后的中晚全新世，黄海暖流影响区域SST的变化受黄海暖流控制，并且对黑潮的变化有很好响应。
岩心YS01的SST记录反映出南黄海全新世存在几次明显的降温事件：0.3-0.5ka，1.2-1.6ka，2.7-3.1ka，4.2-4.5ka，5.5-5.9ka，6.9-7.2ka，8.1-8.5ka和9.2-9.5ka，并且SST记录中存在~532年变化周期，生物标志物比值A/B记录存在~1560年的变化周期，这与北大西洋、黑潮和陆地等全球环境指标记录的气候突变事件及周期循环有较好的一致性。说明南黄海在黄海暖流控制下，通过大气及海洋环流的变化对全球气候变化事件也有较好的响应。该岩心的SST记录表明南黄海的古环境演化在区域性海洋环境尤其是黄海暖流控制下对全球性气候变化的响应。
The Yellow Sea (YS) is an important marginal sea in the northwestern Pacific andits environment and ecology have changed significantly during the Holocene. Thechanges were driven by the interactions of the Yellow Sea Warm Current (YSWC),the East Asian Monsoon (EAM) and the Kuroshio Current (KC). In order to study theHolocene environmental and ecosystem variations in the YS, high-resolution recordswhich could provide materials for paleoclimatic and palaeoceanographic research arenecessary. This thesis carries out the multi-biomarkers in three sediment cores (YS01,ZY1, ZY2) drilled from the same latitude section in the South Yellow Sea (SYS)central mud area to reconstruct the past sea surface temperature (SST), phytoplanktonproductivity and community structure changes. The biomarker method is based on theassumptions that sedimentary biomarker contents reflect phytoplankton productivityand biomarker ratios reflect community structure.
During the early Holocene (10.5-7ka), the phytoplankton primary productivityand community structure changes in the SYS are mainly controlled by the sea-levelrising and display lower paleoproductivity and haptophyte contribution. The rapidsea-level rise event MWP-1C occurred in9.6ka was recorded in core YS01withincreased primary productivity and decreased terrestrial organic matter contribution.Reconstructed phytoplankton community structure variations may also be affected bythe East Asian Summer Monsoon (EASM) which could lead to the precipitationchanges. More runoff transported to the YS induced by stronger rainfall precipitationwould decrease the salinity, which would result in less haptophyte contribution. TheYS was in a low salinity estuarine environment stage during the early Holocene andhaptophytes contribute less compared with the Mid-late Holocene.
During the Mid-late Holocene (7-0ka), after the intrusion of the YSWC at about6.8ka, the SYS environment has been under the influence of the YSWC, andproductivity-community structure has been affected by the YSWC strength-pathwayvariations. Phytoplankton productivity is enhanced and contributes more comparedwith terrestrial organic matters after the formation of the YS circulation system. Thecontent values of the marine biomarkers in the core ZY1and ZY2are similar, andthey also reveal similar temporal trends. From6ka to3ka, the biomarker contents inthe two cores were relatively low with small oscillations, followed by a distinctincrease at about3ka which indicated productivity increased with stronger East AsianWinter Monsoon (EAWM). The circulation system in the YS are strengthened byincreased EAWM. In addition, a stronger EAWM could increase nutrient levels ineuphotic layer and increase dust input, all enhancing productivity. For core YS01which locates to the west of the other two cores, the marine biomarker contents ishigher and lack of an increasing trend. We presume that the productivity in thislocation could also be affected by the YS continental shelf front upwelling besides theEAWM. In areas influenced by the YSWC, an increase in haptophyte contributionwould be caused by stronger YSWC influence with the EASM precipitationmodulating. The abrupt increase of productivity values and haptophyte contributionduring the late Holocene (3ka) may be related to the occurrence of stronger and morefrequent ENSO, reflecting the onset and enhanced magnitude of modern ENSOsystem.
Some differences of the biomarker records between core ZY1and ZY2suggestspatial variations in responses to YSWC and KC forcing. When the KC wasintensified during the periods6-4.2ka and1.7-0ka, the YSWC extended eastward,exerting more influence on core ZY1. On the other hand, when the KC weakenedduring4.2-1.7ka, the YSWC extended westward, exerting more influence on the coreZY2.
The SST results in core YS01show that three periods of the regional climatechanges can be identified during the Holocene. During the early Holocene (9.6-7ka),it shifted from cold to warm with large amplitude under the control of Northern Hemisphere solar irradiance; the middle Holocene (7-2.8ka), the higher SST lasteduntil6ka and then decreased with oscillation; the late Holocene (2.8-0ka), theclimate was replaced by a warm stage with small fluctuations. The SST changes arecontrolled by the YSWC and in good response to the KC variations.
There are also eight cold events recorded in core YS01, which occurred at0.3-0.5ka,1.2-1.6ka,2.7-3.1ka,4.2-4.5ka,5.5-5.9ka,6.9-7.2ka,8.1-8.5ka and9.2-9.5kathrough the last9.6ka. The SST displays periodicity of~532yr during the last9.6kaand biomarker proxy A/B ratio displays periodicity of~1560yr after the YSWCintrusion. The cold events and the millennial scale climate cycle appear to correlatewell with records in the North Atlantic, the KC and other different regions of theworld, suggesting global climatic tele-connections. The SST records in core YS01indicate that the YS climate is affected by global and regional climate change.
引文
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