Skip to main content

Thank you for visiting nature.com. You are using a browser version with limited support for CSS. To obtain the best experience, we recommend you use a more up to date browser (or turn off compatibility mode in Internet Explorer). In the meantime, to ensure continued support, we are displaying the site without styles and JavaScript.

  • Article
  • Published:

Last glacial atmospheric CO2 decline due to widespread Pacific deep-water expansion

Nature Geoscience volume 13, pages 628–633 (2020)Cite this article

Subjects

Abstract

Ocean circulation critically affects the global climate and atmospheric carbon dioxide through redistribution of heat and carbon in the Earth system. Despite intensive research, the nature of past ocean circulation changes remains elusive. Here we present deep-water carbonate ion concentration reconstructions for widely distributed locations in the Atlantic Ocean, where low carbonate ion concentrations indicate carbon-rich waters. These data show a low-carbonate-ion water mass that extended northward up to about 20° S in the South Atlantic at 3–4 km depth during the Last Glacial Maximum. In combination with radiocarbon ages, neodymium isotopes and carbon isotopes, we conclude that this low-carbonate-ion signal reflects a widespread expansion of carbon-rich Pacific deep waters into the South Atlantic, revealing a glacial deep Atlantic circulation scheme different than commonly considered. Comparison of high-resolution carbonate ion records from different water depths in the South Atlantic indicates that this Pacific deep-water expansion developed from approximately 38,000 to 28,000 years ago. We infer that its associated carbon sequestration may have contributed critically to the contemporaneous decline in atmospheric carbon dioxide, thereby helping to initiate the glacial maximum.

This is a preview of subscription content, access via your institution

Access options

Buy this article

  • Purchase on Springer Link
  • Instant access to full article PDF
Buy now

Prices may be subject to local taxes which are calculated during checkout

Fig. 1: Comparison of εNd and 14C ages at 3.8 and 5 km water depths in the South Atlantic Ocean.
Fig. 2: Modern and LGM Atlantic meridional [CO32–] transects.
Fig. 3: [CO32–] versus δ13C and εNd.
Fig. 4: South Atlantic [CO32–] reconstructions at 3.8 and 5 km water depths compared with atmospheric CO2 during the last 60 ka.

Similar content being viewed by others

Data availability

We have chosen not to deposit the data at this time but declare that all data presented in this study are provided in the Supplementary Tables.

References

  1. Oppo, D. et al. Data constraints on glacial Atlantic water mass geometry and properties. Paleoceanogr. Paleoclimatol. 33, 1013–1034 (2018).

    Google Scholar 

  2. Lynch-Stieglitz, J. et al. Atlantic meridional overturning circulation during the Last Glacial Maximum. Science 316, 66–69 (2007).

    Google Scholar 

  3. Howe, J. N. W. et al. North Atlantic Deep Water production during the Last Glacial Maximum. Nat. Commun. 7, 11765 (2016).

    Google Scholar 

  4. Gebbie, G. How much did Glacial North Atlantic Water shoal? Paleoceanogr. Paleoclimatol. 29, 190–209 (2014).

    Google Scholar 

  5. Skinner, L., Fallon, S. J., Waelbroeck, C., Michel, E. & Barker, S. Ventilation of the deep Southern Ocean and deglacial CO2 rise. Science 328, 1147–1151 (2010).

    Google Scholar 

  6. Piotrowski, A. et al. Reconstructing deglacial North and South Atlantic deep water sourcing using foraminiferal Nd isotopes. Earth Planet. Sci. Lett. 357–358, 289–297 (2012).

    Google Scholar 

  7. Burke, A. et al. The glacial mid-depth radiocarbon bulge and its implications for the overturning circulation. Paleoceanogr. Paleoclimatol. 30, 1021–1039 (2015).

    Google Scholar 

  8. Robinson, L. F. & van de Flierdt, T. Southern Ocean evidence for reduced export of North Atlantic Deep Water during Heinrich event 1. Geology 37, 195–198 (2009).

    Google Scholar 

  9. Anderson, R. F. et al. Deep-sea oxygen depletion and ocean carbon sequestration during the last ice age. Glob. Biogeochem. Cycles 33, 301–317 (2019).

    Google Scholar 

  10. Jaccard, S. L. & Galbraith, E. D. Large climate-driven changes of oceanic oxygen concentrations during the last deglaciation. Nat. Geosci. 5, 151–156 (2012).

    Google Scholar 

  11. Key, R. M. et al. A global ocean carbon climatology: results from Global Data Analysis Project (GLODAP). Glob. Biogeochem. Cycles 18, GB4031 (2004).

    Google Scholar 

  12. Yu, J. et al. Sequestration of carbon in the deep Atlantic during the last glaciation. Nat. Geosci. 9, 319–324 (2016).

    Google Scholar 

  13. Burke, A. & Robinson, L. F. The Southern Ocean’s role in carbon exchange during the last deglaciation. Science 335, 557–561 (2012).

    Google Scholar 

  14. Skinner, L. C. et al. North Atlantic versus Southern Ocean contributions to a deglacial surge in deep ocean ventilation. Geology 41, 667–670 (2013).

    Google Scholar 

  15. Barker, S., Knorr, G., Vautravers, M., Diz, P. & Skinner, L. Extreme deepening of the Atlantic overturning circulation during deglaciation. Nat. Geosci. 3, 567–571 (2010).

    Google Scholar 

  16. Adkins, J. F., McIntyre, K. & Schrag, D. P. The salinity, temperature, and δ18O of the glacial deep ocean. Science 298, 1769–1773 (2002).

    Google Scholar 

  17. Yu, J. M. & Elderfield, H. Benthic foraminiferal B/Ca ratios reflect deep water carbonate saturation state. Earth Planet. Sci. Lett. 258, 73–86 (2007).

    Google Scholar 

  18. Yu, J. et al. Loss of carbon from the deep sea since the Last Glacial Maximum. Science 330, 1084–1087 (2010).

    Google Scholar 

  19. Marchitto, T. & Broeker, W. Deep water mass geometry in the glacial Atlantic Ocean: a review of constraints from the paleonutrient proxy Cd/Ca. Geochem. Geophys. Geosyst. 7, (2006).

  20. Yu, J. More efficient North Atlantic carbon pump during the Last Glacial Maximum. Nat. Commun. 10, 2170 (2019).

    Google Scholar 

  21. Chalk, T. B., Foster, G. L. & Wilson, P. A. Dynamic storage of glacial CO2 in the Atlantic Ocean revealed by boron [CO3 2−] and pH records. Earth Planet. Sci. Lett. 510, 1–11 (2019).

    Google Scholar 

  22. Broecker, W., Yu, J. & Putnam, A. E. Two contributors to the glacial CO2 decline. Earth Planet. Sci. Lett. 429, 191–196 (2015).

    Google Scholar 

  23. Yu, J. M., Elderfield, H. & Piotrowski, A. Seawater carbonate ion–δ13C systematics and application to glacial–interglacial North Atlantic Ocean circulation. Earth Planet. Sci. Lett. 271, 209–220 (2008).

    Google Scholar 

  24. Menviel, L. et al. Poorly ventilated deep ocean at the Last Glacial Maximum inferred from carbon isotopes: a data-model comparison study. Paleoceanogr. Paleoclimatol. 31, 2–17 (2017).

    Google Scholar 

  25. Muglia, J., Skinner, L. & Schmittner, A. Weak overturning circulation and high Southern Ocean nutrient utilization maximized glacial ocean carbon. Earth Planet. Sci. Lett. 496, 47–56 (2018).

    Google Scholar 

  26. Hodell, D. A., Charles, C. D. & Sierro, F. J. Late Pleistocene evolution of the ocean’s carbonate system. Earth Planet. Sci. Lett. 192, 109–124 (2001).

    Google Scholar 

  27. Gottschalk, J. et al. Past carbonate preservation events in the deep southeast Atlantic Ocean (Cape Basin) and their implications for Atlantic overturning dynamics and marine carbon cycling. Paleoceanogr. Paleoclimatol. 33, 643–663 (2018).

    Google Scholar 

  28. Gottschalk, J. et al. Abrupt changes in the southern extent of North Atlantic Deep Water during Dansgaard–Oeschger events. Nat. Geosci. 8, 950–954 (2015).

    Google Scholar 

  29. Zhao, N. et al. Glacial–interglacial Nd isotope variability of North Atlantic Deep Water modulated by North American ice sheet. Nat. Commun. 10, 5773 (2019).

    Google Scholar 

  30. Roberts, J. et al. Evolution of South Atlantic density and chemical stratification across the last deglaciation. Proc. Natl Acad. Sci. USA 113, 514–519 (2016).

    Google Scholar 

  31. Ferrari, R. et al. Antarctic sea ice control on ocean circulation in present and glacial climates. Proc. Natl Acad. Sci. USA 111, 8753–8758 (2014).

    Google Scholar 

  32. Adkins, J. F. The role of deep ocean circulation in setting glacial climates. Paleoceanogr. Paleoclimatol. 28, 539–561 (2013).

    Google Scholar 

  33. Talley, L. D. Closure of the global overturning circulation through the Indian, Pacific, and Southern oceans: schematics and transports. Oceanography 26, 80–97 (2013).

    Google Scholar 

  34. Matsumoto, K., Oba, T., Lynch-Stieglitz, J. & Yamamoto, H. Interior hydrography and circulation of the glacial Pacific Ocean. Q. Sci. Rev. 21, 1693–1704 (2002).

    Google Scholar 

  35. Hu, R., Piotrowski, A. M., Bostock, H. C., Crowhurst, S. & Rennie, V. Variability of neodymium isotopes associated with planktonic foraminifera in the Pacific Ocean during the Holocene and Last Glacial Maximum. Earth Planet. Sci. Lett. 447, 130–138 (2016).

    Google Scholar 

  36. Keigwin, L. D. North Pacific deep water formation during the latest glaciation. Nature 330, 362–364 (1987).

    Google Scholar 

  37. Anderson, D. M. & Archer, D. Glacial–interglacial stability of ocean pH inferred from foraminifer dissolution rates. Nature 416, 70–73 (2002).

    Google Scholar 

  38. Rae, J. W. B. et al. Deep water formation in the North Pacific and deglacial CO2 rise. Paleoceanogr. Paleoclimatol. 29, 645–667 (2014).

    Google Scholar 

  39. Umling, N. E. & Thunell, R. C. Mid-depth respired carbon storage and oxygenation of the eastern equatorial Pacific over the last 25,000 years. Q. Sci. Rev. 189, 43–56 (2018).

    Google Scholar 

  40. Doss, W. & Marchitto, T. M. Glacial deep ocean sequestration of CO2 driven by the eastern equatorial Pacific biologic pump. Earth Planet. Sci. Lett. 377, 43–54 (2013).

    Google Scholar 

  41. Kerr, J., Rickaby, R., Yu, J. M., Elderfield, H. & Sadekov, A. Y. The effect of ocean alkalinity and carbon transfer on deep-sea carbonate ion concentration during the past five glacial cycles. Earth Planet. Sci. Lett. 471, 42–53 (2017).

    Google Scholar 

  42. Yu, J. et al. Deep South Atlantic carbonate chemistry and increased interocean deep water exchange during last deglaciation. Q. Sci. Rev. 15, 80–89 (2014).

    Google Scholar 

  43. Galbraith, E. D. et al. Carbon dioxide release from the North Pacific abyss during the last deglaciation. Nature 449, 890–893 (2007).

    Google Scholar 

  44. Ronge, T. A. et al. Radiocarbon constraints on the extent and evolution of the South Pacific glacial carbon pool. Nat. Commun. 7, 11487 (2016).

    Google Scholar 

  45. Gottschalk, J. et al. Carbon isotope offsets between benthic foraminifer species of the genus Cibicides (Cibicidoides) in the glacial sub-Antarctic Atlantic. Paleoceanogr. Paleoclimatol. 31, 1583–1602 (2016).

    Google Scholar 

  46. Gottschalk, J. et al. Biological and physical controls in the Southern Ocean on past millennial-scale atmospheric CO2 changes. Nat. Commun. 7, 11539 (2016).

    Google Scholar 

  47. Basak, C. et al. Breakup of last glacial deep stratification in the South Pacific. Science 359, 900–904 (2018).

    Google Scholar 

  48. Jacobel, A. W., McManus, J. F., Anderson, R. F. & Winckler, G. Repeated storage of respired carbon in the equatorial Pacific Ocean over the last three glacial cycles. Nat. Commun. 8, 1727 (2017).

    Google Scholar 

  49. Bereiter, B. et al. Revision of the EPICA Dome C CO2 record from 800 to 600 kyr before present. Geophys. Res. Lett. 42, 542–549 (2015).

    Google Scholar 

  50. Schlitzer, R. Ocean Data View v.5.3.0 (Alfred Wegener Institute, 2006); https://odv.awi.de/

  51. Barker, S., Greaves, M. & Elderfield, H. A. A study of cleaning procedures used for foraminiferal Mg/Ca paleothermometry. Geochem. Geophys. Geosyst. 4, 8407 (2003).

    Google Scholar 

  52. Yu, J. M., Elderfield, H., Greaves, M. & Day, J. Preferential dissolution of benthic foraminiferal calcite during laboratory reductive cleaning. Geochem. Geophys. Geosyst. 8, Q06016 (2007).

    Google Scholar 

  53. Yu, J. M., Day, J., Greaves, M. & Elderfield, H. Determination of multiple element/calcium ratios in foraminiferal calcite by quadrupole ICP-MS. Geochem. Geophys. Geosyst. 6, Q08P01 (2005).

    Google Scholar 

  54. Feely, R. A. et al. Impact of anthropogenic CO2 on the CaCO3 system in the oceans. Science 305, 362–366 (2004).

    Google Scholar 

  55. Grant, K. M. et al. Rapid coupling between ice volume and polar temperature over the past 150,000 years. Nature 491, 744–747 (2012).

    Google Scholar 

  56. Mackensen, A., Hubberten, H.-W., Bickert, T., Fischer, G. & Fütterer, D. K. The δ13C in benthic foraminiferal tests of Fontbotia wuellerstorfi (Schwager) relative to the δ13C of dissolved inorganic carbon in Souther Ocean deep water: implications for glacial ocean circulation models. Paleoceanogr. Paleoclimatol. 8, 587–610 (1993).

    Google Scholar 

  57. Hodell, D. A., Venz, K. A., Charles, C. D. & Ninnemann, U. S. Pleistocene vertical carbon isotope and carbonate gradients in the South Atlantic sector of the Southern Ocean. Geochem. Geophys. Geosyst. 4, 1004 (2003).

    Google Scholar 

  58. Curry, W. B. & Oppo, D. Glacial water mass geometry and the distribution of δ13C of ∑CO2 in the western Altantic Ocean. Paleoceanogr. Paleoclimatol. 20, PA1017 (2005).

    Google Scholar 

  59. Lisiecki, L. E. & Raymo, M. E. A Pliocene–Pleistocene stack of 57 globally distributed benthic δ18O records. Paleoceanogr. Paleoclimatol. 20, PA1003 (2005).

    Google Scholar 

  60. Ninnemann, U. S. & Charles, C. D. Changes in the mode of Southern Ocean circulation over the last glacial cycle revealed by foraminiferal stable isotopic variability. Earth Planet. Sci. Lett. 201, 383–396 (2002).

    Google Scholar 

Download references

Acknowledgements

We thank P. Wang for the long-time service with foraminifera shell picking in the laboratory. This work is supported by NSFC41676026, ARC Discovery Projects (DP140101393, DP190100894) and Future Fellowship (FT140100993) to J.Y., Future Fellowship (FT180100606) and Discovery (DP180100048) to L.M., NSFC (41991322 and 41930864) to Z.D.J. and Australian Laureate Fellowship (FL120100050) to E.J.R. The contribution of J.F.M. was supported in part by the US-NSF. J.Y. was supported in part by the “111” Project (BP0719030) when visiting P. Cai at Xiamen University. G.M. acknowledges support from the University of Vigo’s programme to attract excellent research talent, and a generous start-up package. Core materials were provided by ODP/IODP/DSDP, LDEO (N. Anest), NOC (G. Rothwell, D. Thornalley and I. N. McCave), GEREGE (N. Thouveny) and WHOI (E. Roosen) core repositories.

Author information

Authors and Affiliations

  1. Research School of Earth Sciences, The Australian National University, Canberra, Australian Capital Territory, Australia

    J. Yu, E. J. Rohling & G. Marino

  2. State Key Laboratory of Loess and Quaternary Geology, Institute of Earth Environment, Chinese Academy of Sciences, Xi’an, China

    J. Yu, Z. D. Jin, X. Ma & F. Zhang

  3. Climate Change Research Centre, University of New South Wales, Sydney, New South Wales, Australia

    L. Menviel

  4. CAS Center for Excellence in Quaternary Science and Global Change, Xi’an, China

    Z. D. Jin & F. Zhang

  5. Open Studio for Oceanic–Continental Climate and Environment Changes, Qingdao National Laboratory for Marine Science and Technology, Qingdao, China

    Z. D. Jin

  6. Lamont–Doherty Earth Observatory, Columbia University, New York, NY, USA

    R. F. Anderson & J. F. McManus

  7. State Key Laboratory of Marine Geology, Tongji University, Shanghai, China

    Z. Jian

  8. Department of Earth Sciences, University of Cambridge, Cambridge, UK

    A. M. Piotrowski

  9. Ocean and Earth Science, National Oceanography Centre, University of Southampton, Southampton, UK

    E. J. Rohling

  10. Centro de Investigación Mariña, GEOMA, Palaeoclimatology Lab, Universidade de Vigo, Vigo, Spain

    G. Marino

Authors
  1. J. Yu
    View author publications

    You can also search for this author in PubMed Google Scholar

  2. L. Menviel
    View author publications

    You can also search for this author in PubMed Google Scholar

  3. Z. D. Jin
    View author publications

    You can also search for this author in PubMed Google Scholar

  4. R. F. Anderson
    View author publications

    You can also search for this author in PubMed Google Scholar

  5. Z. Jian
    View author publications

    You can also search for this author in PubMed Google Scholar

  6. A. M. Piotrowski
    View author publications

    You can also search for this author in PubMed Google Scholar

  7. X. Ma
    View author publications

    You can also search for this author in PubMed Google Scholar

  8. E. J. Rohling
    View author publications

    You can also search for this author in PubMed Google Scholar

  9. F. Zhang
    View author publications

    You can also search for this author in PubMed Google Scholar

  10. G. Marino
    View author publications

    You can also search for this author in PubMed Google Scholar

  11. J. F. McManus
    View author publications

    You can also search for this author in PubMed Google Scholar

Contributions

J.Y. designed the project and wrote the paper. Z.D.J. and F.Z. managed shell picking. A.M.P. and J.F.M. arranged samples. A.M.P. assisted seawater neodymium data compilation. X.M. plotted Fig. 2. All authors commented on the manuscript.

Corresponding author

Correspondence to J. Yu.

Ethics declarations

Competing interests

The authors declare no competing interests.

Additional information

Peer review information Primary Handling Editor: Rebecca Neely.

Publisher’s note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Extended data

Extended Data Fig. 1 New benthic B/Ca (red circles; unit: μmol/mol) against benthic δ18O (grey circles; unit: ‰) and the LR04 record59 (bold grey lines).

For MD96–2085 and RC11–86, G. inflata and G. sacculifer δ18O (crosses) are shown, after adjusted by +1.8‰ and +3‰, respectively. All benthic B/Ca shown are from this study. References for age models and δ18O are given in Supplementary Table 1.

Extended Data Fig. 2 New and published deep-water [CO32-] using benthic B/Ca along with qualitative proxies for 3–4 km cores from the South Atlantic.

For RC13–228, RC13–229, and TNO57–6, [CO32-] are from this study, and %CaCO3, >63 μm, and fragmentation are from ref. 26. MD07–3076 data are from ref. 28. Age models and δ18O references are given in Supplementary Table 1. All cores show lower deep-water [CO32-] during the LGM than the Holocene.

Extended Data Fig. 3 Deep-water [CO32-] based on benthic B/Ca along with qualitative [CO32-] proxies in core TNO57–21 from the abyssal depth (~5 km) in the South Atlantic.

Also shown are %CaCO3 for another two abyssal cores RC11–83 (41.6°S, 9.8°E, 4718m) and ODP 1089 (40.9°S, 9.9°E, 4621m). Data are from refs. 15,42,60. All cores suggest slightly higher [CO32-] at ~5 km in the South Atlantic during the LGM than the Holocene.

Extended Data Fig. 4 Endmembers for modern and LGM water masses.

#: Italic numbers are assumed values, and using other values would have little effect on mixing lines shown in Fig. 3, due to insensitivity of mixing curvature to DIC values (see Extended Data Fig. 6). *: This study; see Supplementary Tables 1 and 2 for cores used to define associated endmembers.

Extended Data Fig. 5 Meridional Pacific Ocean [CO32-] distribution.

a, [CO32-] transect. b, hydrographic sites11 used to generate a. Today, the core of PDW is located at ~1–2 km in the polar North Pacific with a [CO32-] of ~50 μmol/kg. The low [CO32-] signature can be traced in the Southern Ocean (~50°S) due to the southward transport (southward black arrows) of PDW at ~1–2 km33. During the LGM, the core of GPDW is thought to deepen to ~3 km (dashed half circle)34. Our study suggests that the southward transport (dashed arrows) of GPDW was more extensive. By the time when GPDW was transported to the Pacific sector of the Southern Ocean, its signals would be transported via ACC (circle with an inner dot; transport out of the page) to the South Atlantic Ocean. White circles indicate cores at 3–4 km from the equatorial Pacific Ocean shown in Fig. 3. These cores show lower [CO32-] than the abyssal South Atlantic waters (TNO57–21), indicating that GPDW likely had lower [CO32-] than GAABW.

Extended Data Fig. 6 Alternative scenarios that may contribute to interpretation of the LGM data.

a, as Fig. 3d, but only triple [Nd] of GNAIW. New mixing trend is shown by the blue region. b, as Fig. 3d, but only invoke various degrees of biological respiration (dashed horizontal arrows) associated with GPDW-GAABW-GNAIW mixtures. c, as Fig. 3d, but mixing (blue region) with an aged and hence lower [CO32-] (70 μmol/kg) GAABW. Note that these are just some examples that can potentially contribute to explaining the LGM data, and should not be treated as exhaustive. At present, uncertainties (for example, large endmember εNd ranges and largely unconstrained [Nd]) preclude quantification of mixing ratios and respiration effects and their relative importance. Nevertheless, the more radiogenic εNd at 3.8 km (Fig. 1) would require mixing with GPDW.

Extended Data Fig. 7 Mixing curvature to water-mass endmember DIC and Nd contents.

Effect of endmember DIC changes on (a) δ13C-[CO32-] and (b) εNd-[CO32-]. Relative to the reference cases (grey lines), DICGNAIW and DICGAABW are decreased and increased by 200 μmol/kg, respectively, to intentionally enlarge the DIC contrast between water masses. Effect of endmember [Nd] changes on (c) δ13C-[CO32-] and (d) εNd-[CO32-]. Endmember [Nd] are varied from 1/3 to 3× of the reference value for (c) GNAIW and (d) GAABW. To simplify the view, only GNIAW and GAABW are shown, and GNIAW εNd is only considered at −13.5. This figure suggests that mixing curvature is insensitive to endmember DIC changes, but sensitive to [Nd] changes.

Extended Data Fig. 8 Zonal distribution of [CO32-] in the Southern Ocean.

a, Seawater [CO32-] for three sectors of the Southern Ocean. b, Hydrographic sites (~50–60°S)11 used to generate a. In today’s Southern Ocean, [CO32-] is not zonally homogeneous. Instead, the low-[CO32-] PDW signature is seen in relatively restricted regions at ~1–2 km in the Pacific sector of the Southern Ocean. Via ACC, this signal would be transported to other sectors including the South Atlantic, although its influence is not very clearly seen due to strong vertical mixing that tends to erode any signal anomalies. Our study suggests that the influence of GDPW was more extensive and deeper (~3–4 km) in the Southern Ocean during the LGM. GPDW influence is recorded by [CO32-] and other proxies (for example, εNd and 14C) from the deep South Atlantic.

Extended Data Fig. 9 Scenarios for different GAABW δ13C values.

a, “Mackensen” effects that would affect both deep-water δ13C and [CO32-]. b, Habitat change that only affects deep-water δ13C. See “GAABW δ13C endmember” in Methods for details.

Extended Data Fig. 10 LGM-Holocene [CO32-] difference for cores from >3 km in the Atlantic.

sd: standard deviation.

Supplementary information

Supplementary Data 1.

Supplementary Tables 1–7.

Rights and permissions

Reprints and permissions

About this article

Check for updates. Verify currency and authenticity via CrossMark

Cite this article

Yu, J., Menviel, L., Jin, Z.D. et al. Last glacial atmospheric CO2 decline due to widespread Pacific deep-water expansion. Nat. Geosci. 13, 628–633 (2020). https://doi.org/10.1038/s41561-020-0610-5

Download citation

  • Received:

  • Accepted:

  • Published:

  • Issue Date:

  • DOI: https://doi.org/10.1038/s41561-020-0610-5

This article is cited by

Search

Advanced search

Quick links

Nature Briefing Microbiology

Sign up for the Nature Briefing: Microbiology newsletter — what matters in microbiology research, free to your inbox weekly.

Get the most important science stories of the day, free in your inbox. Sign up for Nature Briefing: Microbiology