Sentences with phrase «annual mean radiative»
(Top left) Global annual mean radiative influences (W m — 2) of LGM climate change agents, generally feedbacks in glacial - interglacial cycles, but also specified in most Atmosphere - Ocean General Circulation Model (AOGCM) simulations for the LGM.
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Tsushima, Y., A. Abe - Ouchi, and S. Manabe, 2005: Radiative damping of annual variation in global mean surface temperature: Comparison between observed and simulated feedback.
To contribute to an understanding of the underlying causes of these changes we compile various environmental records (and model - based interpretations of some of them) in order to calculate the direct effect of various processes on Earth's radiative budget and, thus, on global annual mean surface temperature over the last 800,000 years.
The importance of orbital variations, of the greenhouse gases CO2, CH4 and N2O, of the albedo of land ice sheets, annual mean snow cover, sea ice area and vegetation, and of the radiative perturbation of mineral dust in the atmosphere are investigated.
Abstract:» The sensitivity of global climate with respect to forcing is generally described in terms of the global climate feedback — the global radiative response per degree of global annual mean surface temperature change.
Therefore, the total annual and global mean radiative forcing during the LGM is likely to have been approximately — 8 W m — 2 relative to 1750, with large seasonal and geographical variations and significant uncertainties (see Section 6.4.1).
Abstract:» The sensitivity of global climate with respect to forcing is generally described in terms of the global climate feedback — the global radiative response per degree of global annual mean surface temperature change.
The term «climate sensitivity» refers to the steady - state increase in the global annual mean surface air temperature associated with a given global mean radiative forcing.
Figure 7.18 Annual mean top of the atmosphere radiative forcing due to aerosol — radiation interactions (RFari, in W m — 2) due to different anthropogenic aerosol types, for the 1750 — 2010 period.
«A multiple linear regression analysis of global annual mean near - surface air temperature (1900 — 2012) using the known radiative forcing and the El Niño — Southern Oscillation index as explanatory variables account for 89 % of the observed temperature variance.
The global annual mean top of the atmosphere DMS aerosol all sky radiative forcing is − 2.03 W / m2, whereas, over the southern oceans during SH summer, the mean DMS aerosol radiative forcing reaches − 9.32 W / m2.»
The climate sensitivity parameter (units: °C (W m - 2)-1) refers to the equilibrium change in the annual mean global surface temperature following a unit change in radiative forcing.
However, it should be noted that all of these studies suggest the majority of the global annual mean direct radiative forcing due to sulphate occurs in cloud - free regions.
ECS is the increase in the global annual mean surface temperature caused by an instantaneous doubling of the atmospheric concentration of CO2 relative to the pre-industrial level after the model relaxes to radiative equilibrium, while the TCR is the temperature increase averaged over 20 years centered on the time of doubling at a 1 % per year compounded increase.
The spatial distribution of the forcings is similar in the studies showing strongest radiative forcings over industrial regions of the Northern Hemisphere although the ratio of the annual mean Northern Hemisphere / Southern Hemisphere radiative forcing varies from 2.0 (Graf et al., 1997) to 6.9 (Myhre et al., 1998c)(see Section 6.14.2 for further details).
Global - annual mean adjusted radiative forcing at the top of the atmosphere is, in general, a reliable metric relating the effects of various climate perturbations to global mean surface temperature change as computed in general circulation models (GCMs).
Therefore, the total annual and global mean radiative forcing during the LGM is likely to have been approximately — 8 W m — 2 relative to 1750, with large seasonal and geographical variations and significant uncertainties (see Section 6.4.1).
The annual mean forcing from these cloud systems is in the range of — 45 to — 55 W m — 2 and effectively these cloud systems are shielding both the northern and the southern polar regions from intense radiative heating.