Auxiliary material for paper GB002508 Origin of the deep Bering Sea nitrate deficit: Constraints from the nitrogen and oxygen isotopic composition of water column nitrate and benthic nitrate fluxes. Moritz F. Lehmann, Geochemistry and Geodynamics Research Center (GEOTOP-UQAM-McGill), University of Quebec at Montreal, Montreal, Quebec, Canada, Daniel M. Sigman,Department of Geosciences, Princeton University, Princeton, New Jersey, USA, Daniel C. McCorkle,Woods Hole Oceanographic Institution, Woods Hole, Massachusetts, USA, Brigitte G. Brunelle,Department of Geosciences, Princeton University, Princeton, New Jersey, USA, Sharon Hoffmann,Woods Hole Oceanographic Institution, Woods Hole, Massachusetts, USA, Markus Kienast,Department of Oceanography, Dalhousie University, Halifax, Nova Scotia, Canada, Greg Cane,Department of Geosciences, Princeton University, Princeton, New Jersey, USA, and Jaclyn Clement, Department of Oceanography, Naval Postgraduate School, Monterey, California, USA Global Biogeochemical Cycles, vol. 19, GB4005, doi:10.1029/2005GB002508, 2005 Lehmann, M. F., D. M. Sigman, D. C. McCorkle, B. G. Brunelle, S. Hoffmann, M. Kienast, G. Cane, and J. Clement (2005), Origin of the deep Bering Sea nitrate deficit: Constraints from the nitrogen and oxygen isotopic composition of water column nitrate and benthic nitrate fluxes, Global Biogeochem. Cycles, 19, GB4005, doi:10.1029/2005GB002508. This table shows the calculation scheme used to predict the radiocarbon content (D14C) of dissolved inorganic carbon (DIC) in the Bering Sea water column. The calculations assume that Bering Sea deep water (Healy 02-02 hydrocast 30) is "aged" water of the same density from the Subarctic North Pacific Ocean (SANP) (WOCE line P13N, station 19), with no diapycnal mixing and no dense water formation in the Bering Sea. The calculation accounts for increases in DIC due to organic matter oxidation (estimated from the change in oxygen concentration) and increases in DIC due to carbonate dissolution (estimated from the changes in alkalinity, corrected for the phosphate increase), and for the radiocarbon content of these respiration and dissolution DIC inputs. The difference between the predicted D14C of SANP water after respiration and dissolution, and the observed D14C of Bering Sea water of the same density, is converted to an apparent age difference between Bering Sea deep water and its presumed source in the SANP. These differences average 50 +/- 41 years. 1) density (sigma-0, kg/m^3) of the nine layers for which calculations were made. 2) pressure (dbar) of each layer at HLY02-02, HC30, Bering Sea 3) in situ temperature (C) at HLY02-02, HC30, Bering Sea 4) salinity (psu) at HLY02-02, HC30, Bering Sea 5) pressure (dbar) at WOCE P13N station 19, SANP 6) in situ temperature (C) at WOCE P13N station 19, SANP 7) salinity (psu) at WOCE P13N station 19, SANP 8) dissolved inorganic carbon (DIC, micromoles/kg) at WOCE P13N station 20, SANP (no DIC data were obtained at WOCE P13N station 19) 9) radiocarbon content (D14C, o/oo) at WOCE P13N station 19, SANP 10) oxygen content (micromol/kg) at WOCE P13N station 19, SANP (initial) 11) oxygen content (micromol/kg) at HLY02-02, HC30, Bering Sea (final) 12) oxygen difference (micromol/kg) between Bering Sea and SANP 13) assumed CO2 release: O2 consumption ratio during respiration ( = 106:170) 14) predicted increase in DIC due to respiration (micromol/kg) 15) assumed D14C of respiration-derived DIC ( = -50 o/oo) 16) alkalinity (microequiv/kg) at WOCE P13N station 20, SANP (initial) 17) alkalinity (microequiv/kg) at HLY02-02, HC30, Bering Sea (final) 18) observed alkalinity difference between Bering Sea and SANP (microequiv/kg) 19) phosphate (micromol/kg) at WOCE P13N station 20, SANP (initial) 20) phosphate (micromol/kg) at HLY02-02, HC30, Bering Sea (final) 21) phosphate difference between Bering Sea and SANP (micromol/kg) 22) assumed alkalinity : phosphate release ratio during respiration ( = -18) 23) phosphate correction (microequiv/kg) to the observed alkalinity change 24) assumed DIC:alkalinity release ratio during carbonate dissolution ( = 0.5) 25) predicted increase in DIC due to dissolution (micromol/kg) 26) assumed D14C of dissolution-derived DIC ( = -50 o/oo) 27) predicted final (Bering Sea) DIC (micromol/kg), SANP + respiration + dissolution 28) predicted final (Bering Sea) D14C (o/oo) of DIC, SANP + respiration + dissolution 29) predicted final (Bering Sea) D14C expressed as fraction modern 30) predicted final (Bering Sea) D14C expressed as an apparent age (yr) 31) observed final (Bering Sea, HC30) DIC (micromol/kg) 32) observed final (Bering Sea, HC30) D14C of DIC (o/oo) 33) observed final (Bering Sea, HC30) D14C expressed as fraction modern 34) predicted final (Bering Sea, HC30) D14C expressed as an apparent age (yr) 35) difference between observed and predicted Bering Sea D14C values (o/oo) 36) difference between observed and predicted Bering Sea apparent ages (yr) 37) average of the nine apparent age differences in the 1 to 4 km depth range 38) standard deviation of the nine apparent age differences in the 1 to 4 km depth range