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2 (2) where q is the number of atmospheric sampling stations. In practice, it is convenient to reference all concentrations in the sum of squares to the value at the South Pole, and then solve for the values of α by using singular value decomposition [W. H. Press, B. R. Flannery, S. A. Teukolsky, W. T. Vetterling, Numerical Recipes (Cambridge Univ. Press, New York, 1992)] with a mass conservation constraint [G. H. Golub and C. F. V. Loan, Matrix Computations (Johns Hopkins Univ. Press, Baltimore, 1990)] that requires the terrestrial biosphere to balance all the other sources minus sinks.
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-1) occurs in the tropics and Southern Hemisphere (Table 1), where the spatiotemporal coverage of measurements used in T97 and tracer data used for model evaluation is very uneven. The recent completion of the World Ocean Circulation Experiment will greatly improve the coverage.
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2 sources that are difficult for the coarse resolution models to simulate in sufficient detail. Sable Island was excluded because it appears that the data may have a positive bias (K. Higuchi, personal communication). The following procedures were followed in calculating annual averages of model simulations for comparison with observations, (i) Sampling of models at coastal stations was moved out to sea by one grid cell in order to avoid inadvertent terrestrial contamination resulting from the coarse resolution of the atmospheric general circulation models (GCMs). (ii) All other sampling was done at the nearest grid cell to the station. (iii) Four stations were sampled by wind sectors in order to match as closely as possible the way that the actual sampling is done: Cape Grim, Tasmania (180° to 270°); Cape Meares, Oregon (210° to 330°); Key Biscayne, Florida (30° to 160°); and Mace Head, Ireland (210° to 300°).
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2 difference to about 90 μatm, or a 4.5 times increase of the gas exchange coefficient [which is already about twice as large as other commonly used estimates (17)], or some combination of the two. Tans et al. discussed this issue in their study (2). An independent constraint on the North Atlantic sink is the anthropogenic carbon inventory estimate obtained from analysis of observations of dissolved inorganic carbon [N. Gruber, J. L. Sarmiento, T. F. Stocker, Global Biogeochem. Cycles 10, 809 (1996)]. This estimate is almost identical to the OBM simulations (which agree with T97 in the North Atlantic).
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There was little impact on the estimates when the terrestrial uptake was assumed to be proportional to the heterotrophic respiration in the CASA model (19), which has very different temporal patterns from the NPP. In another case, the terrestrial uptake was assumed to be invariable with season and to be uniform within each of five regions (separate boreal and temperate regions in Eurasia-North Africa and North America, and the rest of land surfaces combined). The estimates of total terrestrial uptake for North America and for Eurasia-North Africa were well constrained and remained essentially unchanged from those shown in Table 2 (averaged over the four cases) even with this radical assumption.
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This research was carried out as part of the Carbon Modeling Consortium (CMC), which is supported by the Office of Global Programs and Geophysical Fluid Dynamics Laboratory of the NOAA. We acknowledge support from the Department of Energy. Stimulating discussions with our colleagues in the CMC and elsewhere is gratefully acknowledged, with particular appreciation to P. Bakwin, D. Baker, and M. Bender. L. Bruhwiler, R. Hemler, H. Levy, and W. Moxim provided advice on the GCTM and SKYHI simulations, T. Hughes helped access the OBM results, and C. Field provided the CASA simulation results.
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