Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3
The production, transportation, deposition, and dissolution of carbonate profoundly form part of the global carbon cycle and affect the amount and distribution of dissolved inorganic carbon (DIC) and alkalinity (ALK), which drive atmospheric CO2 changes during glacial/interglacial cycles. These proc...
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古地理学报(英文版)
2016
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Online Access: | https://hdl.handle.net/20.500.11897/446402 |
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Open Polar |
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Peking University Institutional Repository (PKU IR) |
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ftpekinguniv |
language |
English |
topic |
Carbonate dissolution Planktonic foraminifera MIS3 South China Sea Carbonate dissolution Planktonic foraminifera MIS3 South China Sea |
spellingShingle |
Carbonate dissolution Planktonic foraminifera MIS3 South China Sea Carbonate dissolution Planktonic foraminifera MIS3 South China Sea Na Wang Bao-Qi Huang He Li Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 |
topic_facet |
Carbonate dissolution Planktonic foraminifera MIS3 South China Sea Carbonate dissolution Planktonic foraminifera MIS3 South China Sea |
description |
The production, transportation, deposition, and dissolution of carbonate profoundly form part of the global carbon cycle and affect the amount and distribution of dissolved inorganic carbon (DIC) and alkalinity (ALK), which drive atmospheric CO2 changes during glacial/interglacial cycles. These processes may provide significant clues for better understanding of the mechanisms that control the global climate system. In this study, we calculate and analyze the foraminiferal dissolution index (FDX) and the fragmentation ratios of planktonic foraminifera for the 60-25 ka B.P. time-span, based on samples from Core 17924 and ODP Site 1144 in the northeastern South China Sea (SCS), so as to reconstruct the deep-water car-bonate dissolution during Marine Isotope Stage 3 (MIS 3). Our analysis shows that the dissolution of carbonate increases gradually in Core 17924, whereas it remains stable at ODP Site 1144. This difference is caused by the deep-sea carbonate ion concentration﹙[CO32-]﹚that affected the dissolution in Core 17924 where the depth of 3440 m is below the saturation horizon. However, the depth of ODP Site 1144 is 2037 m, which is above the lysocline where the water is always saturated with calcium carbonate; the dissolution is therefore less dependent of chemical changes of the seawater. The combined effect of the productivity and the deep-water chemical evolution may decrease deep-water [CO32-] and accelerate car-bonate dissolution. The fall of the sea-level increased the input of DIC and ALK to the deep ocean and deepened the carbonate saturation depth, which caused an increase of the deep-water [CO32-]. The elevated [CO32-] partially neutralized the reduced [CO32-] contributed by remineralization of organic matter and slowdown of thermohaline. These consequently are the fundamental reasons for the difference in dissolution rate between these two sites. The production, transportation, deposition, and dissolution of carbonate profoundly form part of the global carbon cycle and affect the amount and distribution of dissolved inorganic carbon (DIC) and alkalinity (ALK), which drive atmospheric CO2 changes during glacial/interglacial cycles. These processes may provide significant clues for better understanding of the mechanisms that control the global climate system. In this study, we calculate and analyze the foraminiferal dissolution index (FDX) and the fragmentation ratios of planktonic foraminifera for the 60-25 ka B.P. time-span, based on samples from Core 17924 and ODP Site 1144 in the northeastern South China Sea (SCS), so as to reconstruct the deep-water car-bonate dissolution during Marine Isotope Stage 3 (MIS 3). Our analysis shows that the dissolution of carbonate increases gradually in Core 17924, whereas it remains stable at ODP Site 1144. This difference is caused by the deep-sea carbonate ion concentration﹙[CO32-]﹚that affected the dissolution in Core 17924 where the depth of 3440 m is below the saturation horizon. However, the depth of ODP Site 1144 is 2037 m, which is above the lysocline where the water is always saturated with calcium carbonate; the dissolution is therefore less dependent of chemical changes of the seawater. The combined effect of the productivity and the deep-water chemical evolution may decrease deep-water [CO32-] and accelerate car-bonate dissolution. The fall of the sea-level increased the input of DIC and ALK to the deep ocean and deepened the carbonate saturation depth, which caused an increase of the deep-water [CO32-]. The elevated [CO32-] partially neutralized the reduced [CO32-] contributed by remineralization of organic matter and slowdown of thermohaline. These consequently are the fundamental reasons for the difference in dissolution rate between these two sites. 1 100-107 5 |
author2 |
School of Earth and Space Sciences, Peking University, Beijing 100871, China |
format |
Journal/Newspaper |
author |
Na Wang Bao-Qi Huang He Li |
author_facet |
Na Wang Bao-Qi Huang He Li |
author_sort |
Na Wang |
title |
Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 |
title_short |
Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 |
title_full |
Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 |
title_fullStr |
Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 |
title_full_unstemmed |
Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 |
title_sort |
geochemistry and sedimentary environments deep-water carbonate dissolution in the northern south china sea during marine isotope stage 3 |
publisher |
古地理学报(英文版) |
publishDate |
2016 |
url |
https://hdl.handle.net/20.500.11897/446402 |
genre |
Planktonic foraminifera |
genre_facet |
Planktonic foraminifera |
op_source |
万方 http://d.g.wanfangdata.com.cn/Periodical_gdlxb-e201601005.aspx |
op_relation |
古地理学报(英文版).2016,5,(1),100-107. 1413411 2095-3836 http://hdl.handle.net/20.500.11897/446402 |
op_doi |
https://doi.org/20.500.11897/446402 |
_version_ |
1766169925992316928 |
spelling |
ftpekinguniv:oai:localhost:20.500.11897/446402 2023-05-15T18:00:43+02:00 Geochemistry and sedimentary environments Deep-water carbonate dissolution in the northern South China Sea during Marine Isotope Stage 3 Na Wang Bao-Qi Huang He Li School of Earth and Space Sciences, Peking University, Beijing 100871, China 2016 https://hdl.handle.net/20.500.11897/446402 en eng 古地理学报(英文版) 古地理学报(英文版).2016,5,(1),100-107. 1413411 2095-3836 http://hdl.handle.net/20.500.11897/446402 万方 http://d.g.wanfangdata.com.cn/Periodical_gdlxb-e201601005.aspx Carbonate dissolution Planktonic foraminifera MIS3 South China Sea Carbonate dissolution Planktonic foraminifera MIS3 South China Sea Journal 2016 ftpekinguniv https://doi.org/20.500.11897/446402 2021-08-01T10:55:48Z The production, transportation, deposition, and dissolution of carbonate profoundly form part of the global carbon cycle and affect the amount and distribution of dissolved inorganic carbon (DIC) and alkalinity (ALK), which drive atmospheric CO2 changes during glacial/interglacial cycles. These processes may provide significant clues for better understanding of the mechanisms that control the global climate system. In this study, we calculate and analyze the foraminiferal dissolution index (FDX) and the fragmentation ratios of planktonic foraminifera for the 60-25 ka B.P. time-span, based on samples from Core 17924 and ODP Site 1144 in the northeastern South China Sea (SCS), so as to reconstruct the deep-water car-bonate dissolution during Marine Isotope Stage 3 (MIS 3). Our analysis shows that the dissolution of carbonate increases gradually in Core 17924, whereas it remains stable at ODP Site 1144. This difference is caused by the deep-sea carbonate ion concentration﹙[CO32-]﹚that affected the dissolution in Core 17924 where the depth of 3440 m is below the saturation horizon. However, the depth of ODP Site 1144 is 2037 m, which is above the lysocline where the water is always saturated with calcium carbonate; the dissolution is therefore less dependent of chemical changes of the seawater. The combined effect of the productivity and the deep-water chemical evolution may decrease deep-water [CO32-] and accelerate car-bonate dissolution. The fall of the sea-level increased the input of DIC and ALK to the deep ocean and deepened the carbonate saturation depth, which caused an increase of the deep-water [CO32-]. The elevated [CO32-] partially neutralized the reduced [CO32-] contributed by remineralization of organic matter and slowdown of thermohaline. These consequently are the fundamental reasons for the difference in dissolution rate between these two sites. The production, transportation, deposition, and dissolution of carbonate profoundly form part of the global carbon cycle and affect the amount and distribution of dissolved inorganic carbon (DIC) and alkalinity (ALK), which drive atmospheric CO2 changes during glacial/interglacial cycles. These processes may provide significant clues for better understanding of the mechanisms that control the global climate system. In this study, we calculate and analyze the foraminiferal dissolution index (FDX) and the fragmentation ratios of planktonic foraminifera for the 60-25 ka B.P. time-span, based on samples from Core 17924 and ODP Site 1144 in the northeastern South China Sea (SCS), so as to reconstruct the deep-water car-bonate dissolution during Marine Isotope Stage 3 (MIS 3). Our analysis shows that the dissolution of carbonate increases gradually in Core 17924, whereas it remains stable at ODP Site 1144. This difference is caused by the deep-sea carbonate ion concentration﹙[CO32-]﹚that affected the dissolution in Core 17924 where the depth of 3440 m is below the saturation horizon. However, the depth of ODP Site 1144 is 2037 m, which is above the lysocline where the water is always saturated with calcium carbonate; the dissolution is therefore less dependent of chemical changes of the seawater. The combined effect of the productivity and the deep-water chemical evolution may decrease deep-water [CO32-] and accelerate car-bonate dissolution. The fall of the sea-level increased the input of DIC and ALK to the deep ocean and deepened the carbonate saturation depth, which caused an increase of the deep-water [CO32-]. The elevated [CO32-] partially neutralized the reduced [CO32-] contributed by remineralization of organic matter and slowdown of thermohaline. These consequently are the fundamental reasons for the difference in dissolution rate between these two sites. 1 100-107 5 Journal/Newspaper Planktonic foraminifera Peking University Institutional Repository (PKU IR) |