Xuanliang Ji, Fei Chai, Peng Xiu, Guimei Liu. Long-term trend of oceanic surface carbon in the Northwest Pacific from 1958 to 2017[J]. Acta Oceanologica Sinica. doi: 10.1007/s13131-021-1953-5
Citation:
Xuanliang Ji, Fei Chai, Peng Xiu, Guimei Liu. Long-term trend of oceanic surface carbon in the Northwest Pacific from 1958 to 2017[J]. Acta Oceanologica Sinica. doi: 10.1007/s13131-021-1953-5
Xuanliang Ji, Fei Chai, Peng Xiu, Guimei Liu. Long-term trend of oceanic surface carbon in the Northwest Pacific from 1958 to 2017[J]. Acta Oceanologica Sinica. doi: 10.1007/s13131-021-1953-5
Citation:
Xuanliang Ji, Fei Chai, Peng Xiu, Guimei Liu. Long-term trend of oceanic surface carbon in the Northwest Pacific from 1958 to 2017[J]. Acta Oceanologica Sinica. doi: 10.1007/s13131-021-1953-5
Key Laboratory of Research on Marine Hazards Forecasting, National Marine Environmental Forecasting Center, Ministry of Natural Resources, Beijing 100081, China
2.
State Key Laboratory of Satellite Ocean Environment Dynamics, Second Institute of Oceanography, Ministry of Natural Resources, Hangzhou 310012, China
3.
School of Marine Sciences, University of Maine, Orono 04469, ME, United States
4.
State Key Laboratory of Tropical Oceanography, South China Sea Institute of Oceanology, Chinese Academy of Sciences, Guangzhou 510301, China
Funds:
The National Key Research and Development Program of China under contract No. 2016YFC1401605); Southern Marine Science and Engineering Guangdong Laboratory (Zhuhai) under contract No. SML2020SP008; the Open Fund of Marine Telemetry Technology Innovation Center of the Ministry of Natural Resources; the National Natural Science Foundation of China under contract No. 41730536.
Contrasting decrease and increase trends of sea surface temperature (SST) have been documented in the western Subarctic (WSA) and the rest of the Northwest Pacific (NWP) from 1958 to 2017, respectively. Consequently, more (less) total carbon dioxide (TCO2) due to ocean cooling (warming) is transported to the surface, which leads to increase (decrease) of oceanic surface partial pressure of carbon dioxide (pCO2). With the combined influence of the rising atmospheric carbon dioxide (CO2) level and changing ocean conditions, a prominent increase in oceanic surface pCO2 occurred with different rates of increase in summer and winter in the NWP. The oceanic surface pCO2 is mainly controlled by the variation of TCO2 at the interdecadal timescale and by SST at the seasonal timescale. Our results also indicate that increasing SST tends to strengthen the capability of ocean in absorbing anthropogenic CO2 in the NWP, while ocean’s uptaking ability is weakened in the cooling area of the WSA.
Figure 1. Areas used for temporal analysis: a. modeled annual-mean temperature (°C), and b. modeled annual-mean oceanic surface pCO2 (μatm, 1 μatm=0.101 Pa).
Figure 2. Atmospheric CO2 set in Case 1 and Case 2. Black line: Case 1; Red line: Case 2. 1 μatm=0.101 Pa.
Figure 3. Comparison the model simulations and satellite observations. a. Sea surface temperature (SST), black line is modeled results, red line is satellite results. b. Oceanic surface pCO2, black curve line is modeled results, green dot is observed results. Black line is the variation trend line from model, green line is the variation trend line from observation. 1 μatm=0.101 Pa.
Figure 4. Decades variation of oceanic surface pCO2. Modeled oceanic surface pCO2 (top), and observations of pCO2 from the SOCAT database (bottom). a, e: 1990s decade; b, f: 2000s decade; c, g: 2010s decade. 1 μatm=0.101 Pa.
Figure 5. Seasonal climatology of oceanic surface pCO2 from model. a. Winter (DJF, December–February); b. spring (MAM, March–May); c. summer (JJA, June–August); d. autumn (SON, September–November). 1 μatm=0.101 Pa.
Figure 6. Spatial distributions of long-term trend rate of change. a. for SST, b. for TCO2 under Case 1, c. for oceanic surface pCO2 under Case 1, d. for TCO2 under Case 2, and e. for oceanic surface pCO2 under Case 2, 1 μatm=0.101 Pa).
Figure 7. Spatial distributions of the long-term trend rate of change. a. for pCO2, b. for pCO2-SST (same distribution under Case 1 and Case 2), c. for pCO2-TCO2 under Case 1, and d. for pCO2-TCO2 under Case 2. 1μatm=0.101 Pa.