Chlorophylls and their Degradation in Nature
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1 Introduction Phytoplankton are responsible for approximately 40–50 % of the total primary production on Earth. They contribute to controlling the total CO2 concentration and pH of the ocean, which together with physical processes (e.g. solar energy input, sea–air heat exchanges, upwelling of subsurface waters and mixed layer thickness) dictates the air-to-sea CO2 gas exchanges (Longhurst et al. 1995; Field et al. 1998; Takahashi et al. 2002; Falkowski et al. 2004). The global net primary production from phytoplankton is 45–50 Gt C year−1, whilst from land plants K. M. G. Mostofa (*) · C. Q. Liu State Key Laboratory of Environmental Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences, Guiyang 550002, China e-mail: [email protected] X. L Pan Xinjiang Key Laboratory of Water Cycle and Utilization in Arid Zone, Xinjiang Institute of Ecology and Geography, Chinese Academy of Sciences, Urumqi 830011, People Republic of China D. Vione Dipartimento di Chimica, University of Turin,-I 10125 Turin, Italy Centro Interdipartimentale NatRisk, I-10095 Grugliasco, (TO), Italy K. Hayakawa Lake Biwa Environmental Research Institute, Shiga Prefecture, Ohtsu 520-0806, Japan T. Yoshioka Field Science Education and Research Center, Kyoto University, Kitashirakawa Oiwake-cho, Sakyo-ku, Kyoto 606-8502, Japan G. G. Komissarov Semenov Institute of Chemical Physics, Russian Academy of Sciences, Moscow 117977, Russia
K. M. G. Mostofa et al. (eds.), Photobiogeochemistry of Organic Matter, Environmental Science and Engineering, DOI: 10.1007/978-3-642-32223-5_8, © Springer-Verlag Berlin Heidelberg 2013
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it is of 45–68 Gt C year−1 and from coastal vegetation it is of 1.9 Gt C year−1 (Longhurst et al. 1995; Box 2004; Haberl et al. 2007). Since the development of techniques for Chl a detection in water in the decade of 1930 and 1940s (Harvey 1934, 1939), a number of research works has been published to develop analytical methodologies (Richards and Thompson 1952; Parsons and Strickland 1963; Jeffrey and Humphrey 1975), to elucidate Chl a origin (Fennel and Boss 2003; Letelier et al. 2004; Huisman et al. 2006) and to understand its photoinduced degradation into various pheopigments (Welschmeyer and Lorenzen 1985; Barlow et al. 1993; Stephens et al. 1997). An additional issue is the production of autochthonous DOM by photoinduced degradation of Chl a or phytoplankton biomass, under both photoinduced and microbial (bacterial) metabolism/assimilation/respiration (Kirchman et al. 1991, 1995; Tranvik 1993; Nelson et al. 1998, 2004; Hart et al. 2000; Parlanti et al. 2000; Carrillo et al. 2002; Rochelle-Newall and Fisher 2002; Nieto-Cid et al. 2006; Mostofa et al. 2009; Zhang et al. 2009). The spatial variability of the net primary productivity over the globe is substantially high, varying from about 1,000 g C m−2 for evergreen tropical rain forests to less than 30 g C m−2 for deserts (Scurlock et al. 1999). On the other hand, chlorophyll a (Chl a) concentrations vary from 0.0 to 2,080 μg L−1 in
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