10
K. M. G. Mostofa et al.
at 0 m and 48–90 μM C at 90–2600 m in June 2001), 16–77 % in Western North
Pacific (85–117 μM C at 0 m and 66–73 μM C at 150 m), 0–194 % in Atlantic
Ocean (50–97 μM C at <100 m and 33–59 μM C at >1000 m), 0–165 % in
Pacific Ocean (40–90 μM C at <100 m and 34–45 μM C at >1000 m), 28–121 %
in Indian Ocean and Arabian Sea (55–95 μM C at <100 m and 43 μM C at
>1000 m), 0–121 in Antarctic Ocean (38–75 μM C at <100 m and 34–60 μM C
at >1000 m), as well as 0–118 % in Arctic Ocean (34–107 μM C at <100 m and
49–54 μM C at >1000 m) (Mostofa et al. 2005a, 2009a; Fu et al. 2010; Ogawa
and Tanoue 2003; Ogawa and Ogura 1992; Wilkinson et al. 1997; Mitra et al.
2000; Yoshioka et al. 2002a; Hayakawa et al. 2003, 2004; Annual Report 2004;
Bade 2004; Sugiyama et al. 2004).
The contribution of extracellular release of photosynthetically-derived DOM
varies from 5 to 70 % in natural waters (Lancelot 1979; Fogg 1983; Connolly
et al. 1992). The autochthonous production is significantly higher in oceans with
a high water temperature (WT) than in those with a low water temperature, particularly in the Arctic Ocean. The key contributors to autochthonous DOM in
natural waters as well as in sediment pore waters are considered to be phytoplankton or algal biomass, bacteria, coral, coral reef, submerged aquatic vegetation, krill (shrimp-like marine crustaceans), seagrass, and marsh- and mangrove
forest (Mostofa et al. 2009a, b; Zhang et al. 2009; Li et al. 2011; McKnight et al.
1991, 1993, 1994, 2001; Tanoue et al. 1995, 1996; Fukuda et al. 1998; Nelson et
al. 1998, 2004; Tanoue 2000; Kahru and Mitchell 2001; Ogawa et al. 2001; Hata
et al. 2002; Rochelle-Newall and Fisher 2002a, b; Burdige et al. 2004; Cammack
et al. 2004; Steinberg et al. 2004; Wild et al. 2004; Yamashita and Tanoue 2004;
Biers et al. 2007; Chen et al. 2007; Vantrepotte et al. 2007; Wada et al. 2007;
Wang et al. 2007; Hanamachi et al. 2008; Henderson et al. 2008; Tanaka et al.
2008; Tzortziou et al. 2008; Ortega-Retuerta et al. 2009; Tranvik et al. 2009).
These studies demonstrate that autochthonous DOM is produced from POM by
several processes such as photoinduced and microbial respiration (or assimilation),
zooplankton grazing, bacterial release and uptake, viral interactions, and complex
microbial processes in sediment pore waters.
3.2.1 Respiration or Assimilation of Algae or Phytoplankton
Species and Bacteria
Algae or phytoplankton biomass and bacteria can release new DOM in natural waters by two key processes: first, photoinduced respiration or assimilation
of algae or phytoplankton biomass and bacteria, which can produce new DOM
(Mostofa et al. 2005a, 2009b, 2011; Rochelle-Newall and Fisher 2002a; Varela
et al. 2003; Aoki et al. 2008; Biddanda and Benner 1997; Hulatt et al. 2009).
Second, microbial respiration or assimilation of algae or phytoplankton and bacteria, which can release the new DOM in natural waters (Mostofa et al. 2009a, b,
2011; Parlanti et al. 2000; Zhang et al. 2009; Fu et al. 2010; McKnight et al. 1991,
1994, 2001; Nelson et al. 2004; Rochelle-Newall and Fisher 2002a; Cammack
K. M. G. Mostofa et al.
at 0 m and 48–90 μM C at 90–2600 m in June 2001), 16–77 % in Western North
Pacific (85–117 μM C at 0 m and 66–73 μM C at 150 m), 0–194 % in Atlantic
Ocean (50–97 μM C at <100 m and 33–59 μM C at >1000 m), 0–165 % in
Pacific Ocean (40–90 μM C at <100 m and 34–45 μM C at >1000 m), 28–121 %
in Indian Ocean and Arabian Sea (55–95 μM C at <100 m and 43 μM C at
>1000 m), 0–121 in Antarctic Ocean (38–75 μM C at <100 m and 34–60 μM C
at >1000 m), as well as 0–118 % in Arctic Ocean (34–107 μM C at <100 m and
49–54 μM C at >1000 m) (Mostofa et al. 2005a, 2009a; Fu et al. 2010; Ogawa
and Tanoue 2003; Ogawa and Ogura 1992; Wilkinson et al. 1997; Mitra et al.
2000; Yoshioka et al. 2002a; Hayakawa et al. 2003, 2004; Annual Report 2004;
Bade 2004; Sugiyama et al. 2004).
The contribution of extracellular release of photosynthetically-derived DOM
varies from 5 to 70 % in natural waters (Lancelot 1979; Fogg 1983; Connolly
et al. 1992). The autochthonous production is significantly higher in oceans with
a high water temperature (WT) than in those with a low water temperature, particularly in the Arctic Ocean. The key contributors to autochthonous DOM in
natural waters as well as in sediment pore waters are considered to be phytoplankton or algal biomass, bacteria, coral, coral reef, submerged aquatic vegetation, krill (shrimp-like marine crustaceans), seagrass, and marsh- and mangrove
forest (Mostofa et al. 2009a, b; Zhang et al. 2009; Li et al. 2011; McKnight et al.
1991, 1993, 1994, 2001; Tanoue et al. 1995, 1996; Fukuda et al. 1998; Nelson et
al. 1998, 2004; Tanoue 2000; Kahru and Mitchell 2001; Ogawa et al. 2001; Hata
et al. 2002; Rochelle-Newall and Fisher 2002a, b; Burdige et al. 2004; Cammack
et al. 2004; Steinberg et al. 2004; Wild et al. 2004; Yamashita and Tanoue 2004;
Biers et al. 2007; Chen et al. 2007; Vantrepotte et al. 2007; Wada et al. 2007;
Wang et al. 2007; Hanamachi et al. 2008; Henderson et al. 2008; Tanaka et al.
2008; Tzortziou et al. 2008; Ortega-Retuerta et al. 2009; Tranvik et al. 2009).
These studies demonstrate that autochthonous DOM is produced from POM by
several processes such as photoinduced and microbial respiration (or assimilation),
zooplankton grazing, bacterial release and uptake, viral interactions, and complex
microbial processes in sediment pore waters.
3.2.1 Respiration or Assimilation of Algae or Phytoplankton
Species and Bacteria
Algae or phytoplankton biomass and bacteria can release new DOM in natural waters by two key processes: first, photoinduced respiration or assimilation
of algae or phytoplankton biomass and bacteria, which can produce new DOM
(Mostofa et al. 2005a, 2009b, 2011; Rochelle-Newall and Fisher 2002a; Varela
et al. 2003; Aoki et al. 2008; Biddanda and Benner 1997; Hulatt et al. 2009).
Second, microbial respiration or assimilation of algae or phytoplankton and bacteria, which can release the new DOM in natural waters (Mostofa et al. 2009a, b,
2011; Parlanti et al. 2000; Zhang et al. 2009; Fu et al. 2010; McKnight et al. 1991,
1994, 2001; Nelson et al. 2004; Rochelle-Newall and Fisher 2002a; Cammack