148
K. M. G. Mostofa et al.
Zika et al. 1985a, b; Moffett and Zika 1987a; Palenic and Morel 1988; Cooper
and Lean 1989; Johnson et al. 1989; Sakugawa et al. 2000, 2006; Mostofa and
Sakugawa 2009; Gerringa et al. 2004; Obernosterer et al. 2001; Fujiwara et al.
1993; Moore et al. 1993; Sikorsky and Zika 1993a, b; Sarthou et al. 1997; Richard
et al. 2007; Petasne and Zika 1997; Lobanov et al. 2008; Sakugawa et al. 1995;
Cooper and Lean 1992; Moffett and Zika 1983; Szymczak and Waite 1991; Resing
et al. 1993; Miller and Kester 1994; Amouroux and Donard 1995; Fujiwara et al.
1995; Kieber and Heltz 1995; Herut et al. 1998; Cooper et al. 2000; Akane et al.
2004, 2005; Avery et al. 2005; Croot et al. 2005; Miller et al. 2005; O’Sullivan et
al. 2005; Olasehinde et al. 2008; Boehm et al. 2009; Clark et al. 2010a, b; Rusak
et al. 2010). H 2 O 2 concentrations in surface freshwater are 6–68 nM in upstream
rivers and 9–501 nM in rivers in Japan, 1300–3200 nM in rivers and 700–1300 nM
in reservoirs in Russia, 88–320 nM in rivers in the USA, and 10–1300 nM in
several lakes in USA and Canada (Table 1). H 2 O 2 concentrations in surface seawater are 11–440 nM in estuaries in USA and Japan, 0–496 nM in coastal Bay
and coastal seawaters in Japan, 25–360 nM in Amazon and Orinoco River plume,
3–1700 nM in Chesapeake Bay, 22–256 nM in Bay of Biscay (Atlantic Ocean),
124–275 nM in Biscayne Bay and Gulf Stream, <200 nM in Port Aransas seawater, <150 nM in Florida west coast, 8–50 nM in Peru upwelling area (Coastal
and offshore), 8–100 nM in the Mediterranean (Israeli coastal waters) and the
Red Sea (Gulf of Aqaba), 20–80 nM in Baltic Sea (German Coastal waters),
15–110 nM in Great Barrier Reef seawater (Australia), 120–280 nM in Gulf of
Mexico, 50–420 nM in Caribbean Sea, 95–175 nM in Sargasso Sea and Western
Mediterranean, 16–220 nM in Atlantic Ocean, and 5–25 nM in Southern Ocean in
Antarctic regions (Table 1). H 2 O 2 concentrations are remarkably higher in Russian
rivers and reservoir (700–3200 nM) than in other rivers (6–501 nM) and lakes
(10–1300 nM) in the freshwater environments. High concentrations (0–420 nM)
are commonly observed in estuaries, bays and coastal seawaters, and an exceptionally high concentration (1700 nM) was detected in Cheasapeake Bay. H 2 O 2 concentrations are apparently lowest in the Southern Ocean, Antactic (5–25 nM). On
the other hand, the occurrence of ROOH compounds is not often studied in natural
waters (Table 1). ROOH concentrations are 9–73 nM in upstreams, 0–200 nM in
rivers, 32–389 nM in coastal seawaters, and 1–6 nM in the eastern Atlantic Ocean
(Table 1).
1.7 Production Rates and Sources of H 2 O 2
Production rates of H 2 O 2 are greatly variable among upstreams (245–903 nM h −1 ),
groundwater (0–4800 nM h −1 ), rivers (390–7400 nM h −1 ), lakes (81–2400 nM h −1 ),
coastal waters (4536–35640 nM h −1 ), and seawaters (0–161 nM h −1 ) (Table 2)
(Mostofa and Sakugawa 2009; Obernosterer et al. 2001; Scully et al. 1996; Richard
et al. 2007; Miller and Kester 1994; Cooper et al. 1988; Moffett and Zafiriou 1993;
Yocis et al. 2000; Clark et al. 2009; Mostofa KMG and Sakugawa H, unpublished;
K. M. G. Mostofa et al.
Zika et al. 1985a, b; Moffett and Zika 1987a; Palenic and Morel 1988; Cooper
and Lean 1989; Johnson et al. 1989; Sakugawa et al. 2000, 2006; Mostofa and
Sakugawa 2009; Gerringa et al. 2004; Obernosterer et al. 2001; Fujiwara et al.
1993; Moore et al. 1993; Sikorsky and Zika 1993a, b; Sarthou et al. 1997; Richard
et al. 2007; Petasne and Zika 1997; Lobanov et al. 2008; Sakugawa et al. 1995;
Cooper and Lean 1992; Moffett and Zika 1983; Szymczak and Waite 1991; Resing
et al. 1993; Miller and Kester 1994; Amouroux and Donard 1995; Fujiwara et al.
1995; Kieber and Heltz 1995; Herut et al. 1998; Cooper et al. 2000; Akane et al.
2004, 2005; Avery et al. 2005; Croot et al. 2005; Miller et al. 2005; O’Sullivan et
al. 2005; Olasehinde et al. 2008; Boehm et al. 2009; Clark et al. 2010a, b; Rusak
et al. 2010). H 2 O 2 concentrations in surface freshwater are 6–68 nM in upstream
rivers and 9–501 nM in rivers in Japan, 1300–3200 nM in rivers and 700–1300 nM
in reservoirs in Russia, 88–320 nM in rivers in the USA, and 10–1300 nM in
several lakes in USA and Canada (Table 1). H 2 O 2 concentrations in surface seawater are 11–440 nM in estuaries in USA and Japan, 0–496 nM in coastal Bay
and coastal seawaters in Japan, 25–360 nM in Amazon and Orinoco River plume,
3–1700 nM in Chesapeake Bay, 22–256 nM in Bay of Biscay (Atlantic Ocean),
124–275 nM in Biscayne Bay and Gulf Stream, <200 nM in Port Aransas seawater, <150 nM in Florida west coast, 8–50 nM in Peru upwelling area (Coastal
and offshore), 8–100 nM in the Mediterranean (Israeli coastal waters) and the
Red Sea (Gulf of Aqaba), 20–80 nM in Baltic Sea (German Coastal waters),
15–110 nM in Great Barrier Reef seawater (Australia), 120–280 nM in Gulf of
Mexico, 50–420 nM in Caribbean Sea, 95–175 nM in Sargasso Sea and Western
Mediterranean, 16–220 nM in Atlantic Ocean, and 5–25 nM in Southern Ocean in
Antarctic regions (Table 1). H 2 O 2 concentrations are remarkably higher in Russian
rivers and reservoir (700–3200 nM) than in other rivers (6–501 nM) and lakes
(10–1300 nM) in the freshwater environments. High concentrations (0–420 nM)
are commonly observed in estuaries, bays and coastal seawaters, and an exceptionally high concentration (1700 nM) was detected in Cheasapeake Bay. H 2 O 2 concentrations are apparently lowest in the Southern Ocean, Antactic (5–25 nM). On
the other hand, the occurrence of ROOH compounds is not often studied in natural
waters (Table 1). ROOH concentrations are 9–73 nM in upstreams, 0–200 nM in
rivers, 32–389 nM in coastal seawaters, and 1–6 nM in the eastern Atlantic Ocean
(Table 1).
1.7 Production Rates and Sources of H 2 O 2
Production rates of H 2 O 2 are greatly variable among upstreams (245–903 nM h −1 ),
groundwater (0–4800 nM h −1 ), rivers (390–7400 nM h −1 ), lakes (81–2400 nM h −1 ),
coastal waters (4536–35640 nM h −1 ), and seawaters (0–161 nM h −1 ) (Table 2)
(Mostofa and Sakugawa 2009; Obernosterer et al. 2001; Scully et al. 1996; Richard
et al. 2007; Miller and Kester 1994; Cooper et al. 1988; Moffett and Zafiriou 1993;
Yocis et al. 2000; Clark et al. 2009; Mostofa KMG and Sakugawa H, unpublished;