Variation of diffuse attenuation coefficient of downwelling irradiance in the Arctic Ocean
doi: 10.1007/s13131-014-0489-3
Variation of diffuse attenuation coefficient of downwelling irradiance in the Arctic Ocean
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摘要: The diffuse attenuation coefficient (Kd) for downwelling irradiance is calculated from solar irradiance data measured in the Arctic Ocean during 3rd and 4th Chinese National Arctic Research Expedition (CHINARE), including 18 stations and nine stations selected for irradiance profiles in sea water respectively. In this study, the variation of attenuation coefficient in the Arctic Ocean was studied, and the following results were obtained. First, the relationship between attenuation coefficient and chlorophyll concentration in the Arctic Ocean has the form of a power function. The best fit is at 443 nm, and its determination coefficient is more than 0.7. With increasing wavelength, the determination coefficient decreases abruptly. At 550 nm, it even reaches a value lower than 0.2. However, the exponent fitted is only half of that adapted in low-latitude ocean because of the lower chlorophyll-specific absorption in the Arctic Ocean. The upshot was that, in the case of the same chlorophyll concentration, the attenuation caused by phytoplankton chlorophyll in the Arctic Ocean is lower than in low-latitude ocean. Second, the spectral model, which exhibits the relationship of attenuation coefficients between 490 nm and other wavelength, was built and provided a new method to estimate the attenuation coefficient at other wavelength, if the attenuation coefficient at 490 nm was known. Third, the impact factors on attenuation coefficient, including sea ice and sea water mass, were discussed. The influence of sea ice on attenuation coefficient is indirect and is determined through the control of entering solar radiation. The linear relationship between averaging sea ice concentration (ASIC, from 158 Julian day to observation day) and the depth of maximum chlorophyll is fitted by a simple linear equation. In addition, the sea water mass, such as the ACW (Alaskan Coastal Water), directly affects the amount of chlorophyll through taking more nutrient, and results in the higher attenuation coefficient in the layer of 30-60 m. Consequently, the spectral model of diffuse attenuation coefficient, the relationship between attenuation coefficient and chlorophyll and the linear relationship between the ASIC and the depth of maximum chlorophyll, together provide probability for simulating the process of diffuse attenuation coefficient during summer in the Arctic Ocean.Abstract: The diffuse attenuation coefficient (Kd) for downwelling irradiance is calculated from solar irradiance data measured in the Arctic Ocean during 3rd and 4th Chinese National Arctic Research Expedition (CHINARE), including 18 stations and nine stations selected for irradiance profiles in sea water respectively. In this study, the variation of attenuation coefficient in the Arctic Ocean was studied, and the following results were obtained. First, the relationship between attenuation coefficient and chlorophyll concentration in the Arctic Ocean has the form of a power function. The best fit is at 443 nm, and its determination coefficient is more than 0.7. With increasing wavelength, the determination coefficient decreases abruptly. At 550 nm, it even reaches a value lower than 0.2. However, the exponent fitted is only half of that adapted in low-latitude ocean because of the lower chlorophyll-specific absorption in the Arctic Ocean. The upshot was that, in the case of the same chlorophyll concentration, the attenuation caused by phytoplankton chlorophyll in the Arctic Ocean is lower than in low-latitude ocean. Second, the spectral model, which exhibits the relationship of attenuation coefficients between 490 nm and other wavelength, was built and provided a new method to estimate the attenuation coefficient at other wavelength, if the attenuation coefficient at 490 nm was known. Third, the impact factors on attenuation coefficient, including sea ice and sea water mass, were discussed. The influence of sea ice on attenuation coefficient is indirect and is determined through the control of entering solar radiation. The linear relationship between averaging sea ice concentration (ASIC, from 158 Julian day to observation day) and the depth of maximum chlorophyll is fitted by a simple linear equation. In addition, the sea water mass, such as the ACW (Alaskan Coastal Water), directly affects the amount of chlorophyll through taking more nutrient, and results in the higher attenuation coefficient in the layer of 30-60 m. Consequently, the spectral model of diffuse attenuation coefficient, the relationship between attenuation coefficient and chlorophyll and the linear relationship between the ASIC and the depth of maximum chlorophyll, together provide probability for simulating the process of diffuse attenuation coefficient during summer in the Arctic Ocean.
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Arrigo K R, Perovich D K, Pickart R S, et al. 2012. Massive phytoplankton blooms under Arctic Sea ice. Science, 336(6087): 1408 Arrigo K R, Robinson D H, Worthen D L, et al. 1998. Bio-optical properties of the southern Ross Sea. J Geophys Res, 102(C10): 21683-21695 Austin R W, Petzold T J. 1981. The determination of the diffuse attenuation coefficient of sea water using the Coastal Zone Color Scanner. In: Gower J F R, ed. Oceanography from Space. New York: Springer US, 239-256 Chang G C, Dickey T D. 2004. Coastal ocean optical influences on solar transmission and radiant heating rate. J Geophys Res, 109: C01020 Chen M, Huang Yipu, Guo Laodong, et al. 2002. Biological productivity and carbon cycling in the Arctic Ocean. Chinese Science Bulletin, 17(12): 1037-1327 Cota G F, Harrison W G, Platt T, et al. 2003. Bio-optical properties of the Labrador Sea. J Geophys Res, 108(C7): 3228 Dickey Dommy D, Chang Grace C. 2001. Recent advances and future visions: temporal variability of optical and bio-optical properties of the ocean. Oceanography, 14(3): 15-29 Jerlov N G. 1976. Marine Optics. New York: Elsevier, 231 Kirk J T. 1994. Light and Photosynthesis in Aquatic Ecosystems. 2nd ed. New York: Cambridge University Press, 400 Lewis M R, Carr M, Feldman G, et al. 1990. Influence of penetrating solar radiation on the heat budget of the equatorial pacific ocean. Nature, 347: 543-545 Liu Zilin, Chen Jianfang, Liu YanLan, et al. 2008. The areal characteristics of chlorophylla in sediments and seawater in the surveyed srea, Arctic Ocean. Acta Sedimentologica Sinica, 26(6): 1035-1040 Manizza Manfredi, Le Que're Corinne, Watson A J, et al. 2005. Biooptical feedbacks among phytoplankton, upper ocean physics and sea-ice in a global model. Geophysical Research Letters, 32: L05603, doi: 10.1029/2004GL020778 Marra J, Langdon C, Knudson C A. 1995. Primary production, water column changes, and the demise of a Phaeocystis bloom at the Marine Light-Mixed Layers site (59°N, 21°W) in the northeast Atlantic Ocean. J Geophys Res, 100: 6633-6644 Matsuoka A, Huot Y, Koji Shimada, et al. 2007. Bio-optical characteristics of the western Arctic Ocean: implication for ocean color algorithms. Can J Remote Sensing, 33(6): 503-518 McClain C R, Arrigo K, Tai K S, et al. 1996. Observations and simulations of physical and biological processes at ocean weather station P, 1951-1980. J Geophys Res, 101: 3697-3713 Mitchell B G. 1992. Predictive bio-optical relationships for polar oceans and marginal ice zones. J Mar Syst, 3: 91-105 Mobley C D. 1994. Light and Water: Optical Properties of Water. Salt Lake City: Academic Press, 133 Morel Andre. 1988. Optical modeling of the upper ocean in relation to its biogenous matter content (Case I Waters). J Geophys Res, 93(C9): 10749-10768 Morel A, Antoine D. 1994. Heating rate within the upper ocean in relation to its bio-optical state. J PhysOceanogr, 24: 1652-1665 Morel A, Maritorena S. 2001. Bio-optical properties of oceanic waters: A reappraisal. J Geophys Res, 106(C4): 7163-7180 Mueller J L, Davis C, Arnone R, et al. 2002. Above water radiance and remote sensing reflectance measurement and analysis protocols. NASA Tech Memo, TM-2002-210004, 171-182 Pabi Sudeshna, van Dijken Gert L, Arrigo Kevin R. 2008. Primary production in the Arctic Ocean, 1998-2006. J Geophys Res, 113: C08005 Plat T, Rao Subba D V. 1975. Primary production of marine microphysics. In: Cooper J P, ed. Photosynthesis and Productivity in Different Environment. Cambridge: Cambridge University Press, 249-280 Sang H Lee, Terry E Whitledge. 2005. Primary and new production in the deep Canada Basin during summer 2002. Polar Biol, 28: 190-197 Sathyendranath S, Gouveia A D, Shetye A R, et al. 1991. Biological control of surface temperature in the Arabian Sea. Nature, 349: 54-56 Shi Jiuxin, Zhao Jinping, Jiao Yutian, et al. 2004. Pacific inflow and its links with abnormal variation in the Arctic Ocean. Chinese Journal of Polar Science (in Chinese), 16(3): 253-260 Smith R C, Baker K S. 1984. Analysis of ocean optical data. In: Blizard Marvin A, ed. Ocean Optics Ⅷ. Monterey, USA: SPIE, 119-126 Smith R C, Baker K S. 1986. The analysis of ocean optical data. In: Blizard Marvin A, ed. Ocean Optics Ⅷ. Orlando, USA: SPIE, 95-107 Siegel D A, Ohlmann J C, Washburn L, et al. 1995. Solar radiation, phytoplankton pigments and the radiant heating of the equatorial Pacific warm pool. J Geophys Res, 100: 4885-4891 Wang Jian, Cota Glenn F, Ruble David A. 2005. Absorptions and backscattering in the Beaufort and Chukchi Seas. J Geophys Res, 110: C04014 Wheeler P A. 1997. Preface: the 1994 Arctic Ocean Section. Deep-Sea Res Part II, 44(8): 1483-1485 Zhao Jinping, Wang Weibo. 2010. Calculation of photosynthetically available radiation using multispectral data in the Arctic. Chinese Journal of Polar Science, 21(2): 113-126 -
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