Global Carbon Sinks and Their Variability Inferred from Atmospheric O
            <sub>2</sub>
            and δ
            <sup>13</sup>
            C

Battle, Mark; Bender, Michael L.; Tans, Pieter P.; White, James W. C.; Ellis, J. T.; Conway, T. J.; Francey, R. J.

doi:10.1126/science.287.5462.2467

Cited by 483 publications

(472 citation statements)

References 21 publications

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“…We also add a constraint on the global oceanic uptake of 2.0 ± 1.2 GtC yr À1 (for each year of the whole period), based on O 2 /N 2 data [Battle et al, 2000]. Finally, we do not model explicitly year-to-year changes in the atmospheric transport over 1980-1998.…”

Section: Appendix A: Atmospheric Inverse Set-upsmentioning

confidence: 99%

“…[4] Top-down studies used atmospheric observations of CO 2 [Keeling et al, 1995], CO 2 and d 13 C [Keeling et al, 1996;Francey et al, 1995;Joos et al, 1999], and O 2 :N 2 , 13 C, and CO 2 [Battle et al, 2000] to apportion the global IAV signal between land and oceans, with conflicting results. Some of the differences, particularly those involving d 13 C, can be attributed to differences in d 13 C data sets linked to the difficulty in maintaining an accurate 13 C calibration.…”

Section: Introductionmentioning

confidence: 99%

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Multiple constraints on regional CO₂ flux variations over land and oceans

Peylin

Bousquet

Quéré

et al. 2005

Global Biogeochemical Cycles

172

177

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[1] To increase our understanding of the carbon cycle, we compare regional estimates of CO 2 flux variability for 1980-1998 from atmospheric CO 2 inversions and from process-based models of the land (SLAVE and LPJ) and ocean (OPA and MIT). Over the land, the phase and amplitude of the different estimates agree well, especially at continental scale. Flux variations are predominantly controlled by El Niño events, with the exception of the post-Pinatubo period of the early 1990s. Differences between the two land models result mainly from the response of heterotrophic respiration to precipitation and temperature. The ''Lloyd and Taylor'' formulation of LPJ [Lloyd and Taylor, 1994] agrees better with the inverse estimates. Over the ocean, inversion and model results agree only in the equatorial Pacific and partly in the austral ocean. In the austral ocean, an increased CO 2 sink is present in the inversion and OPA model, and results from increased stratification of the ocean. In the northern oceans, the inversions estimate large flux variations in line with time-series observations of the subtropical Atlantic, but not supported by the two model estimates, thus suggesting that the CO 2 variability from high-latitude oceans needs further investigation.

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Section: Appendix A: Atmospheric Inverse Set-upsmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Multiple constraints on regional CO₂ flux variations over land and oceans

Peylin

Bousquet

Quéré

et al. 2005

Global Biogeochemical Cycles

172

177

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“…Measurements of variations in atmospheric oxygen have provided a wealth of insights into the global carbon cycle [Keeling and Shertz, 1992;Keeling et al, 1993Keeling et al, , 1996Bender et al, 1996;Battle et al, 2000]. This is because atmospheric oxygen is in many respects a mirror of atmospheric CO2, caused by the tight link between 02 and CO2 that occurs during the photosynthesis by land plants and the subsequent respiration and remineralization of terrestrial organic matter [Severinghaus, 1995].…”

Section: Introductionmentioning

confidence: 99%

Air‐sea flux of oxygen estimated from bulk data: Implications For the marine and atmospheric oxygen cycles

Gruber¹,

Gloor

Fan³

et al. 2001

Global Biogeochemical Cycles

104

170

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Abstract. We estimate the annual net air-sea fluxes of oxygen for 13 regions on the basis of a steady state inverse modeling technique that is independent of air-sea gas exchange parameterizations. The inverted data consist of the observed oceanic oxygen concentration after a correction has been applied to account for biological cycling. We find that the tropical oceans (13øS-13øN) emit •212 Tmol 02 yr -•, which is compensated by uptake of 148 Tmol yr -• in the Northern Hemisphere (>13øN) and by uptake of 65 Tmol yr -• in the Southern Hemisphere (<13øS). These results imply that the dominant feature of oxygen transport in the combined oceanatmosphere system is the existence of a closed circulation cell in each hemisphere. These two cells consist of 02 uptake by the ocean in the middle and high latitudes of both hemispheres and transport in the ocean toward the tropics, where 02 is lost to the atmosphere and transported in the atmosphere back toward the poles. We find an asymmetry in the two cells involving 02 uptake in the temperate regions of the Northern Hemisphere versus loss of 02 in the temperate regions of the Southern Hemisphere. There is an additional asymmetry between the Atlantic basin, which has a net southward transport at all latitudes north of 36øS, in agreement with independent transport estimates, versus the Indian and Pacific Oceans, which have a strong equatorward transport everywhere. We find that these inverse estimates are relatively insensitive to details in the inversion scheme but are sensitive to biases in the ocean general circulation model that provides the linkage between surface fluxes and ocean interior concentrations. Forward simulations of 02 in an atmospheric tracer transport model using our inversely estimated oxygen fluxes as a boundary condition agree reasonably well with observations of atmospheric potential oxygen (APe m 02 + ce2). Our results indicate that the north-south asymmetry in the strength of the two hemispheric cells coupled with a strong asymmetry in fossil fuel emissions can explain much of the observed interhemispheric gradient in APe. Therefore it might not be necessary to invoke the existence of a large southward interhemispheric transport of e2 in the ocean, such as proposed by Stephens et al. [1998]. However, we find that uncertainties in the modeled APe distribution stemming from seasonal atmospheric rectification effects and the limited APe data coverage prevent the currently available APe data from providing strong constraints on the magnitude of interhemispheric transport. Stephens et al. [1998] recently proposed a new tracer combination, atmospheric potential oxygen (APO • 02 + CO2), that removes the terrestrial influence from the atmospheric 02 signal, including most of the signal from the burning of fossil fuels. Variations in APO therefore reflect mainly the air-sea exchange of oxygen and, to a smaller degree, also the air-sea exchange of CO2, N2, and a residual signal from the burning of fossil fuels. Annual mean observations of APO from 10 station...

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“…Future climate depends largely on the evolution of atmospheric CO 2 levels. As one of the major CO 2 reservoirs, the ocean has mitigated this rising CO 2 by taking up nearly one-third of anthropogenic CO 2 emissions at a rate of about 1.5-2.0 Pg C yr 21 [Battle et al, 2000;Sarmiento et al, 2000;Keeling and Garcia, 2002;Takahashi et al, 2002;Gurney et al, 2004;Sabine et al, 2004a;Gruber et al, 2009]. As a consequence, oceanic uptake of anthropogenic CO 2 can lead to ocean acidification, which reduces ocean pH value, lowers calcium carbonate saturation state, changes seawater chemical speciation, and further alters ocean biogeochemical cycle [Doney et al, 2009a].…”

Section: Introductionmentioning

confidence: 99%

Variability of oceanic carbon cycle in the North Pacific from seasonal to decadal scales

Xiu

Chai

2014

JGR Oceans

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Variability of upper-ocean carbon cycle in the North Pacific during 1958-2010 period is investigated using a physical-biogeochemical model. Comparisons with in situ data from five different oceanographic environments in the South China Sea, Monterey Bay, North Pacific gyre, northwestern Pacific, and Gulf of Alaska indicate that the model usually captures observed seasonal and interannual variability in both sea surface pCO 2 and sea-air CO 2 flux. Seasonal variability of pCO 2 and CO 2 flux in the North Pacific follows the change in sea surface temperature (SST) closely with high and low values in summer and winter, respectively. Total CO 2 modifies pCO 2 seasonal pattern in an opposite manner with respect to SST, and surface wind speed modifies the magnitude of CO 2 flux variations. On interannual and decadal time scales, sea surface pCO 2 is primarily controlled by anthropogenic CO 2 , followed by modulations by the El Niño-Southern Oscillation and the Pacific Decadal Oscillation (PDO), while sea-air CO 2 flux is significantly regulated by the PDO and the North Pacific Gyre Oscillation (NPGO). We show that anthropogenic CO 2 tends to amplify the influence on CO 2 flux from the PDO but to damp the influence from the NPGO.

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Global Carbon Sinks and Their Variability Inferred from Atmospheric O ₂ and δ ¹³ C

Cited by 483 publications

References 21 publications

Multiple constraints on regional CO₂ flux variations over land and oceans

Multiple constraints on regional CO₂ flux variations over land and oceans

Air‐sea flux of oxygen estimated from bulk data: Implications For the marine and atmospheric oxygen cycles

Variability of oceanic carbon cycle in the North Pacific from seasonal to decadal scales

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Global Carbon Sinks and Their Variability Inferred from Atmospheric O 2 and δ 13 C

Cited by 483 publications

References 21 publications

Multiple constraints on regional CO2 flux variations over land and oceans

Multiple constraints on regional CO2 flux variations over land and oceans

Air‐sea flux of oxygen estimated from bulk data: Implications For the marine and atmospheric oxygen cycles

Variability of oceanic carbon cycle in the North Pacific from seasonal to decadal scales

Contact Info

Product

Resources

About

Global Carbon Sinks and Their Variability Inferred from Atmospheric O ₂ and δ ¹³ C

Multiple constraints on regional CO₂ flux variations over land and oceans

Multiple constraints on regional CO₂ flux variations over land and oceans