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Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth
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| Zeitschriftentitel: | Climate of the Past |
|---|---|
| Personen und Körperschaften: | , , , |
| In: | Climate of the Past, 7, 2011, 1, S. 17-25 |
| Format: | E-Article |
| Sprache: | Englisch |
| veröffentlicht: |
Copernicus GmbH
|
| Schlagwörter: |
| author_facet |
Hu, Y. Yang, J. Ding, F. Peltier, W. R. Hu, Y. Yang, J. Ding, F. Peltier, W. R. |
|---|---|
| author |
Hu, Y. Yang, J. Ding, F. Peltier, W. R. |
| spellingShingle |
Hu, Y. Yang, J. Ding, F. Peltier, W. R. Climate of the Past Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth Paleontology Stratigraphy Global and Planetary Change |
| author_sort |
hu, y. |
| spelling |
Hu, Y. Yang, J. Ding, F. Peltier, W. R. 1814-9332 Copernicus GmbH Paleontology Stratigraphy Global and Planetary Change http://dx.doi.org/10.5194/cp-7-17-2011 <jats:p>Abstract. One of the critical issues of the Snowball Earth hypothesis is the CO2 threshold for triggering the deglaciation. Using Community Atmospheric Model version 3.0 (CAM3), we study the problem for the CO2 threshold. Our simulations show large differences from previous results (e.g. Pierrehumbert, 2004, 2005; Le Hir et al., 2007). At 0.2 bars of CO2, the January maximum near-surface temperature is about 268 K, about 13 K higher than that in Pierrehumbert (2004, 2005), but lower than the value of 270 K for 0.1 bar of CO2 in Le Hir et al. (2007). It is found that the difference of simulation results is mainly due to model sensitivity of greenhouse effect and longwave cloud forcing to increasing CO2. At 0.2 bars of CO2, CAM3 yields 117 Wm−2 of clear-sky greenhouse effect and 32 Wm−2 of longwave cloud forcing, versus only about 77 Wm−2 and 10.5 Wm−2 in Pierrehumbert (2004, 2005), respectively. CAM3 has comparable clear-sky greenhouse effect to that in Le Hir et al. (2007), but lower longwave cloud forcing. CAM3 also produces much stronger Hadley cells than that in Pierrehumbert (2005). Effects of pressure broadening and collision-induced absorption are also studied using a radiative-convective model and CAM3. Both effects substantially increase surface temperature and thus lower the CO2 threshold. The radiative-convective model yields a CO2 threshold of about 0.21 bars with surface albedo of 0.663. Without considering the effects of pressure broadening and collision-induced absorption, CAM3 yields an approximate CO2 threshold of about 1.0 bar for surface albedo of about 0.6. However, the threshold is lowered to 0.38 bars as both effects are considered. </jats:p> Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth Climate of the Past |
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| title |
Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_unstemmed |
Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_full |
Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_fullStr |
Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_full_unstemmed |
Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_short |
Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_sort |
model-dependence of the co<sub>2</sub> threshold for melting the hard snowball earth |
| topic |
Paleontology Stratigraphy Global and Planetary Change |
| url |
http://dx.doi.org/10.5194/cp-7-17-2011 |
| publishDate |
2011 |
| physical |
17-25 |
| description |
<jats:p>Abstract. One of the critical issues of the Snowball Earth hypothesis is the CO2 threshold for triggering the deglaciation. Using Community Atmospheric Model version 3.0 (CAM3), we study the problem for the CO2 threshold. Our simulations show large differences from previous results (e.g. Pierrehumbert, 2004, 2005; Le Hir et al., 2007). At 0.2 bars of CO2, the January maximum near-surface temperature is about 268 K, about 13 K higher than that in Pierrehumbert (2004, 2005), but lower than the value of 270 K for 0.1 bar of CO2 in Le Hir et al. (2007). It is found that the difference of simulation results is mainly due to model sensitivity of greenhouse effect and longwave cloud forcing to increasing CO2. At 0.2 bars of CO2, CAM3 yields 117 Wm−2 of clear-sky greenhouse effect and 32 Wm−2 of longwave cloud forcing, versus only about 77 Wm−2 and 10.5 Wm−2 in Pierrehumbert (2004, 2005), respectively. CAM3 has comparable clear-sky greenhouse effect to that in Le Hir et al. (2007), but lower longwave cloud forcing. CAM3 also produces much stronger Hadley cells than that in Pierrehumbert (2005). Effects of pressure broadening and collision-induced absorption are also studied using a radiative-convective model and CAM3. Both effects substantially increase surface temperature and thus lower the CO2 threshold. The radiative-convective model yields a CO2 threshold of about 0.21 bars with surface albedo of 0.663. Without considering the effects of pressure broadening and collision-induced absorption, CAM3 yields an approximate CO2 threshold of about 1.0 bar for surface albedo of about 0.6. However, the threshold is lowered to 0.38 bars as both effects are considered.
</jats:p> |
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| description | <jats:p>Abstract. One of the critical issues of the Snowball Earth hypothesis is the CO2 threshold for triggering the deglaciation. Using Community Atmospheric Model version 3.0 (CAM3), we study the problem for the CO2 threshold. Our simulations show large differences from previous results (e.g. Pierrehumbert, 2004, 2005; Le Hir et al., 2007). At 0.2 bars of CO2, the January maximum near-surface temperature is about 268 K, about 13 K higher than that in Pierrehumbert (2004, 2005), but lower than the value of 270 K for 0.1 bar of CO2 in Le Hir et al. (2007). It is found that the difference of simulation results is mainly due to model sensitivity of greenhouse effect and longwave cloud forcing to increasing CO2. At 0.2 bars of CO2, CAM3 yields 117 Wm−2 of clear-sky greenhouse effect and 32 Wm−2 of longwave cloud forcing, versus only about 77 Wm−2 and 10.5 Wm−2 in Pierrehumbert (2004, 2005), respectively. CAM3 has comparable clear-sky greenhouse effect to that in Le Hir et al. (2007), but lower longwave cloud forcing. CAM3 also produces much stronger Hadley cells than that in Pierrehumbert (2005). Effects of pressure broadening and collision-induced absorption are also studied using a radiative-convective model and CAM3. Both effects substantially increase surface temperature and thus lower the CO2 threshold. The radiative-convective model yields a CO2 threshold of about 0.21 bars with surface albedo of 0.663. Without considering the effects of pressure broadening and collision-induced absorption, CAM3 yields an approximate CO2 threshold of about 1.0 bar for surface albedo of about 0.6. However, the threshold is lowered to 0.38 bars as both effects are considered. </jats:p> |
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| spelling | Hu, Y. Yang, J. Ding, F. Peltier, W. R. 1814-9332 Copernicus GmbH Paleontology Stratigraphy Global and Planetary Change http://dx.doi.org/10.5194/cp-7-17-2011 <jats:p>Abstract. One of the critical issues of the Snowball Earth hypothesis is the CO2 threshold for triggering the deglaciation. Using Community Atmospheric Model version 3.0 (CAM3), we study the problem for the CO2 threshold. Our simulations show large differences from previous results (e.g. Pierrehumbert, 2004, 2005; Le Hir et al., 2007). At 0.2 bars of CO2, the January maximum near-surface temperature is about 268 K, about 13 K higher than that in Pierrehumbert (2004, 2005), but lower than the value of 270 K for 0.1 bar of CO2 in Le Hir et al. (2007). It is found that the difference of simulation results is mainly due to model sensitivity of greenhouse effect and longwave cloud forcing to increasing CO2. At 0.2 bars of CO2, CAM3 yields 117 Wm−2 of clear-sky greenhouse effect and 32 Wm−2 of longwave cloud forcing, versus only about 77 Wm−2 and 10.5 Wm−2 in Pierrehumbert (2004, 2005), respectively. CAM3 has comparable clear-sky greenhouse effect to that in Le Hir et al. (2007), but lower longwave cloud forcing. CAM3 also produces much stronger Hadley cells than that in Pierrehumbert (2005). Effects of pressure broadening and collision-induced absorption are also studied using a radiative-convective model and CAM3. Both effects substantially increase surface temperature and thus lower the CO2 threshold. The radiative-convective model yields a CO2 threshold of about 0.21 bars with surface albedo of 0.663. Without considering the effects of pressure broadening and collision-induced absorption, CAM3 yields an approximate CO2 threshold of about 1.0 bar for surface albedo of about 0.6. However, the threshold is lowered to 0.38 bars as both effects are considered. </jats:p> Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth Climate of the Past |
| spellingShingle | Hu, Y., Yang, J., Ding, F., Peltier, W. R., Climate of the Past, Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth, Paleontology, Stratigraphy, Global and Planetary Change |
| title | Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_full | Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_fullStr | Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_full_unstemmed | Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_short | Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| title_sort | model-dependence of the co<sub>2</sub> threshold for melting the hard snowball earth |
| title_unstemmed | Model-dependence of the CO<sub>2</sub> threshold for melting the hard Snowball Earth |
| topic | Paleontology, Stratigraphy, Global and Planetary Change |
| url | http://dx.doi.org/10.5194/cp-7-17-2011 |