The Western North Pacific

Nozaki Y, Horibe Y, Tsubota H (1981) The water column distributions of thorium isotopes in the western North Pacific. Earth Planet Sci Lett 54 (2) 203-216... 

Neff U, Bollhofer A, Frank N, Mangini A (1999) Explaining discrepant depth profiles of " U/ U and °Thexc in Mn-crasts. Geochim Cosmochim Acta 63(15) 2211-2218 Nozaki Y, Cochran JK, Turekian KK, Keller G (1977) Radiocarbon and °Pb distribution in submersible-taken deep-sea cores from Project Famous. Earth Planet Sci Lett 34 167-173 Nozaki Y, Horibe Y, Tsubota H (1981) The water coluirm distributions of thorium isotopes in the western North Pacific. EarthPlanet Sci Lett 54 203-216... 

Hirose K, Sugimura Y. 1987. Thorium isotopes in the surface air of the western north Pacific Ocean. J Environ Radioact 5 459-475. 

Tanabe, S., Tanaka, H., Tatsukawa, R., 1984. Polychlorobiphenyls, DDT, and hex-achlorocyclohexahe isomers in the western North Pacific ecosystem. Arch. Environ. Contam. Toxicol. 13, 731-738. 

Tsunogai, S., Shinagawa, T. and Kurata, T. (1985) Deposition of anthropogenic sulfate and Pb-210 in the western North Pacific area. Geochem. J., 19, 77-90. 

Nozaki, Y. and Tsunogai, S. (1976) 226Ra, 210Pb and 210Po disequilibria in the Western North Pacific. Earth Planet. Sci. Letts, 32, 313-321. 

Betzer P.R., Byrne R.H., Acker J.G., Lewis C.S., Jolley R.R. and Feely R.A. (1986) Biogenic input to the oceanic carbonate system Mass fluxes of pteropods and foraminifera in tropical, temperate, and sub-arctic regions of the western North Pacific, (manuscript). 

Yang GP, Tsunogai S (2005) Biogeochemistry of dimethylsulfide (DMS) and dimethylsulfoniopropionate (DMSP) in the surface microlayer of the western North Pacific. Deep-Sea Res Part I 52 553-567... 

Pacific Ocean revealed that N2O in the suboxic zone was enriched in relative to N2O in the atmosphere whereas N2O was slightly depleted in relative to atmospheric N2O (Yoshida et al., 1984). This in line with the argumentation that N2O in suboxic waters is consumed during denitrification and that N2O is formed during nitrification in oxic waters. Surprisingly, Yoshida et al. (1989), found N-enriched N2O in the oxic waters of the upper 2000 m of the western North Pacific and concluded that N2O is mainly produced by denitrification. A conclusion which seems to be counterintuitive, because denitrification in oxic waters should be negligible. 

Concentrations of N2 in non-denitrifying waters are generally close to the equibbrium concentrations. For example, dissolved N2 concentrations in the upper 200m of the western North Pacific Ocean and eastern Okhotsk Sea were in the range from 500 to 650 pmol kg (i.e. 1-4.3% supersaturated) (Nakayama et al.. 

Toyoda, S., Yoshida, N., Miwa, T., Matsui, Y., Yamagishi, H., Tsunogai, U., Nojiri, Y., and Tsurushima, N. (2002). Production mechanism and global budget of N20 inferred from its isotopomers in the western North Pacific. Geophys. Res. Lett. 29(3), 10.1029/2001GL014311. 

Figure 3.5 (A) The relative distribution of amino acids in total DOM (Lee and Bada, 1975 Henrichs and Williams, 1985 Hubberten et al., 1994), HMWDOM (McCarthy et al., 1996), phytoplankton, and bacteria (both from Cowie and Hedges, 1992).The data of Lee and Bada are a special case because not all the amino acids shown in this figure were quantified (see text for explanation). (B) The relative distribution on amino acids in total DOM, isolated from a variety of sites in the western North Pacific Ocean (data from Yamashita andTanoue (2003). S and D represent surface and deep DOM samples, respectively. Distributions in HMWDOM are shown for comparison (McCarthy et al., 1996).

Miyazaki, T., Wada, E., and Hattori, A. (1975). Nitrite production from ammonia and nitrate in the euphoric layer of the western North Pacific Ocean. Marine Science Communications 1, 381-394. 

As an alternative to partial assimilatory NOs reduction by phytoplankton, oxidation of NH4+ by Bacteria and Archaea (the first step in the 2-step process of nitrification) can produce N02 as an intermediate product. Nitrifying bacteria were first isolated from the marine environment by Watson (1965) and are now known to be ubiquitous in the global ocean. Wada and Hattori (1971) used a sensitive chemical assay to measure changes in N02 in incubated samples, to conclude that NH4+ was the major source of N02 in the PNM in the central North Pacific Ocean. Miyazaki et al. (1973, 1975), using a N tracer method, found that, in Sagami Bay and in the western North Pacific, NH4+ and NOs were both important sources ofN02. ... 

Kaeriyama, H., and Ikeda, T. (2004). Metabolism and chemical composition of mesopelagic ostracods in the western North Pacific Ocean. ICES J. Mar. Sci. 61, 535—541. 

Figure 3 Vertical profiles of dissolved silver in the North Atlantic (O) (composite of two stations 54.5° N, 48.5° W, and 52.7° N, 35° W data from Rivera-Duarte et al., 1999) and the western North Pacific ( ) (40° N, 145° W data from Zhang et al, 2001).

Matsunaga S.. M. Mochida, T. Saito and K. Kawamura In situ measurement of isoprene in the marine air and surface seawater from the western North Pacific, Atmos. Environ. 36 (2002) 6051-6057. 

Blank, M., Leinen, M. and Prospero J.M., 1985. Major Asian aeolian inputs indicated by the mineralogy of aerosols and sediments in the western North Pacific. Nature, 314 84-86. 

Ogura, N., 1970a. The relation between dissolved organic carbon and apparent oxygen utilization in the Western North Pacific. Deep-Sea Res., 17 221—231. 

Figure 3 The vertical profiles of dissolved (< 0.04 pm) REEs in the western North Pacific (CM-22 ), and the Southern Ocean (PA-41 O) from Alibo and Nozaki, unpublished. The North Atlantic profile data based on dissolved (<0.4pm) REEs (SS- 8 ) from Sholkovitz and Schneider (1991) and acid-soluble total concentrations for monoisotopic REEs (DBB- 86/1 ) from De Baar et al. (1983) and yttrium (TPG-7/8 A) from Alibo et al. (1999).

Figure 4 The PAAS-normalized (A) and the NPDW-normalized (B) patterns of dissolved REEs in the western North Pacific (Alibo...

Figure 2 The surface distribution of (A) aluminum, (B) gallium, and (C) zirconium and hafnium from coastal to open ocean regions in the North Pacific and western North Atlantic. Note the scale changes between oceans. In all panels, the coastal locations are plotted at the outside edges, with more oceanic locations in towards the middle. The data for Al and Ga in the eastern North Pacific are from 28°N 155°W to 36°N 123°W (Orians and Bruland, 1986, 1988b). For the Atlantic, the Ga data are from 37°N 75°W to 36°N 73°W (Orians and Bruland, 1988b), and the Al data are from Rhode Island, across the Gulf Stream, into the Sargasso Sea, then down toward the Caribbean (Measures et al, 1984, stations 0-1206). For Zr and FIf the western North Pacific data are from 38°N 146°E to 16°N 169°W, and in the eastern North Pacific from 50°N 145°W to 49°N 126°W (McKelvey and Orians, 1993 McKelvey, 1994).

Figure 4 Depth profiles of (A) dissolved gallium in the central North Pacific (solid symbols 28°N 155°W Orians and Bruland, 1988) and in the western North Atlantic (open symbols 32°N 64°W Shiller, 1998), and (B) dissolved indium in the western North Pacific (solid symbols 34°N 142°E Amakawa eta ., 1996) and in the eastern North Atlantic (open symbols 26° N, 37°W Alibo etat., 1999).

Figure 7 Depth profiles of (A) niobium and (B) tantalum in the western North Pacific (45°N 165°E Sohrin ef a/., 1998).

Watanabe Y, Yamaguchi A, Ishida H, et al. (2006) Lethality of increasing CO2 levels on deep-sea copepods in the western North Pacific. Journal of Oceanography 62 185-196. 

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