ライフサイエンスコーパス: radiative forcing

1 ection of incoming solar radiation (negative radiative forcing).

2 e uncertainty in anthropogenic aerosol-cloud radiative forcing.

3 challenging to estimate its contribution to radiative forcing.

4 ls affect cloud cover, cloud top height, and radiative forcing.

5 do of the particle from negative to positive radiative forcing.

6 and the potential for positive feedbacks on radiative forcing.

7 modeling, and time-dependent calculation of radiative forcing.

8 little effect on greenhouse gas emissions or radiative forcing.

9 deployment significantly increases long-term radiative forcing.

10 sible for human health impacts and low-cloud radiative forcing.

11 erosol-mixing states while calculating their radiative forcing.

12 nities for rapid mitigation of anthropogenic radiative forcing.

13 al thermostat" response of ENSO to exogenous radiative forcing.

14 a substantial role in climate change through radiative forcing.

15 y of tropical Pacific convection to external radiative forcing.

16 ry) are responsible for most of the contrail radiative forcing.

17 a large fraction of the physical response to radiative forcing.

18 ins are particularly sensitive to changes in radiative forcing.

19 mine the impact of these indirect effects on radiative forcing.

20 of eastern boundary current regions to CO(2) radiative forcing.

21 o exogenous (both natural and anthropogenic) radiative forcing.

22 e a potentially significant effect on global radiative forcing.

23 cification of the time-varying human-induced radiative forcing.

24 ue to reductions in short-lived gases or net radiative forcing.

25 vely to understand the contribution of BB to radiative forcing.

26 e, thereby buffering human effects on global radiative forcing.

27 formation and therefore cloud properties and radiative forcing.

28 fferences in the factors producing increased radiative forcing.

29 nstrain atmospheric CH4 levels and attendant radiative forcing.

30 t has the potential to be a strong source of radiative forcing.

31 ning results from spatial structure in CO2's radiative forcing.

32 ransfer to suppress the cloud masking of the radiative forcing.

33 ntly larger than in other scenarios of lower radiative forcing.

34 ning the tropical climate response to global radiative forcing.

35 ion, and climate's response to anthropogenic radiative forcings.

36 nearly linear dependence on a wide range of radiative forcings.

37 eater increases for RCPs describing stronger radiative forcings.

38 t increases in human-induced greenhouse gas (radiative) forcing.

39 resulted from a combination of human-induced radiative forcing and an unusually large realization of

40 anic and atmospheric circulation patterns to radiative forcing and climate change to improve the skil

41 and may play an important role in planetary radiative forcing and climate.

42 ore likely to have larger impacts on aerosol radiative forcing and could serve as biomass burning tra

43 cles (UAVs) during the CARDEX (Cloud Aerosol Radiative Forcing and Dynamics Experiment) investigation

44 e changes would continue to overestimate the radiative forcing and global warming in coming decades i

45 oral and spatial scales and integrating both radiative forcing and internal variability in climate wi

46 with the global mean greenhouse gases(GHGs) radiative forcing and is attributable primarily to a str

47 fluenced by, among other factors, changes in radiative forcing and remote Pacific climate variability

48 s of emissions scenarios, not just the total radiative forcing and resultant warming level, must be c

49 hipping to determine the induced global-mean radiative forcing and temperature change.

50 rosols formed by nucleation of vapors affect radiative forcing and therefore climate.

51 atmospheric composition changes, historical radiative forcing, and forcing per unit of emission due

52 cts and their direct and indirect effects on radiative forcing, and hence on climate.

53 This reduces the associated anthropogenic radiative forcing, and hence the size of the warming.

54 ntury, then the associated large increase in radiative forcing, and how the Earth system would respon

55 he processes controlling cloud formation and radiative forcing, and links the biology at the ocean su

56 in both hemispheres, as well as to external radiative forcing, and that it may have a central role i

57 c sea surface temperature gradient, external radiative forcings, and the low-pass filtering character

58 btained from satellite observations of cloud radiative forcing are effective for identifying systemat

59 iple, a climate that is insensitive to gross radiative forcing as produced by doubling CO2 might stil

60 Radiative forcing associated with reduction in atmospher

61 ed ice-ocean-atmosphere system and a growing radiative forcing associated with rising concentrations

62 The topic of cloud radiative forcing associated with the atmospheric aeroso

63 A significant proportion of the direct radiative forcing associated with the rise in atmospheri

64 to slow global warming, until recently, the radiative forcing associated with volcanic aerosols in t

65 Here I simulate the radiative forcings associated with changes in surface al

66 simulate a mitigation policy that stabilizes radiative forcing at 4.5 W m(-2) (approximately 526 ppm

67 ty density functions obtained for the direct radiative forcing at the top of the atmosphere give a cl

68 nce 1750 corresponds to a global annual-mean radiative forcing at the tropopause of 1.82 +/- 0.19 W m

69 into question previous estimates of surface radiative forcing based on presumed global long-term inc

70 oval of atmospheric carbon dioxide decreases radiative forcing, but is largely compensated by slower

71 rns and mechanisms of nonlinear responses to radiative forcing, but their utility has been greatly li

72 e response of the Earth system to changes in radiative forcings, but also on how humankind responds t

73 increasing precipitation by 7% and net cloud radiative forcing by 1.0 W m(-2) at the top of the atmos

74 The effect of radiative forcing by anthropogenic aerosols is one of th

75 tion implicate a shift in the periodicity of radiative forcing by atmospheric carbon dioxide as the c

76 les should be measured or controlled and (2) radiative forcing by BrC aerosols could be overestimated

77 elevated early Paleogene temperatures, (ii) radiative forcing by carbon dioxide deviates significant

78 rm climate records, and indicate that a weak radiative forcing by carbon dioxide is highly unlikely o

79 overestimation of BC loadings and BC Direct Radiative Forcing by current models over North Pacific,

80 The degree to which this increase in radiative forcing by dust in snow has affected timing an

81 Radiative forcing by increasing deposition of industrial

82 We suggest that the resulting indirect radiative forcing by ozone effects on plants could contr

83 observations suggest a higher sensitivity of radiative forcing by trade cumuli to increases in cloud

84 ouse gases is usually quantified in terms of radiative forcing, calculated as the difference between

85 mate studies, we calculate the difference in radiative forcing caused by having a core-shell aerosol

86 ly dynamical responses of climate to natural radiative forcing changes involving El Nino and the Nort

87 ace energy balance, we isolate the impact of radiative forcing, climate feedback and ocean heat uptak

88 m(-2), which is much larger than some of the radiative forcings considered in the Intergovernmental P

89 sensitivity of Earth's climate to changes in radiative forcing could depend on the background climate

90 nd transparent way to compare the cumulative radiative forcing created by alternative technologies fu

91 On a cumulative radiative forcing (CRF) basis, the environmental improve

92 ensitivity of Earth's climate to an external radiative forcing depends critically on the response of

93 ustal dust in the atmosphere impacts Earth's radiative forcing directly by modifying the radiation bu

94 Global aerosol direct radiative forcing (DRF) is an important metric for asses

95 absorption of solar energy and hence direct radiative forcing (DRF), little is known regarding the i

96 arge temporal variability in the atmospheric radiative forcing due to aerosols over northern India.

97 ynamics, which will ultimately determine net radiative forcing due to permafrost thaw.

98 e quantify the future evolution of the total radiative forcing due to perpetual constant year 2000 em

99 On regional scales, direct radiative forcing due to smoke can be large and might in

100 The global-mean direct radiative forcing due to smoke from biomass burning worl

101 obal satellite aerosol data imply a negative radiative forcing due to stratospheric aerosol changes o

102 The direct radiative forcing due to this EC-rich factor was roughly

103 ibute more to global warming than the direct radiative forcing due to tropospheric ozone increases.

104 The net effect of all agents was to increase radiative forcing during the first year (34 +/- 31 Watts

105 hat Earth's climate sensitivity to CO2-based radiative forcing (Earth system sensitivity) was half as

106 -eq yr(-1) ), producing an overall positive radiative forcing effect of 2.4 +/- 0.3 kt CO2 -eq yr(-1

107 change to estimate GHG fluxes and associated radiative forcing effects for the whole wetland, and sep

108 Pbio factors using a forest growth model and radiative forcing effects with a time horizon of 100 yea

109 The radiative forcing efficiencies of many individual emissi

110 -cover-atmosphere feedbacks induced by CO(2) radiative forcing enhance the radiative effects of CO(2)

111 Simulations of glacier mass balances with radiative forcing-equivalent changes in atmospheric temp

112 from atmospheric heating measurements, soot radiative forcing estimates currently differ by a factor

113 BrC), adding uncertainties to global aerosol radiative forcing estimations.

114 The negative radiative forcing expected from this CO2 uptake is up to

115 el simulations run under the same historical radiative forcings fails to reproduce the observed regio

116 wind speed to estimate the clear-sky direct radiative forcing for 2002, incorporating measurements o

117 al gas can produce net climate damages (more radiative forcing) for decades.

118 A large positive component of this radiative forcing from aerosols is due to black carbon--

119 The reduction in radiative forcing from albedo alone is equivalent to a c

120 The magnitude of the direct radiative forcing from black carbon itself exceeds that

121 n of the new temperature reconstruction with radiative forcing from greenhouse gases estimates an Ear

122 ntury in simulations that stipulate that the radiative forcing from greenhouse gases increases by ove

123 systematically overestimate the response to radiative forcing from increasing greenhouse gas concent

124 st uncertain component of the overall global radiative forcing from preindustrial time.

125 a major (35-53%) contributor of atmospheric radiative forcing from the estuary, while N2O contribute

126 The simulations adopt the aerosol radiative forcing from the Indian Ocean experiment obser

127 is up to 231 times greater than the positive radiative forcing from the methane emissions.

128 ld be roughly 10-fold less than if that same radiative forcing had been produced using sulfate aeroso

129 of coal for electric power plants can reduce radiative forcing immediately, and reducing CH(4) losses

130 Methane has the second-largest global radiative forcing impact of anthropogenic greenhouse gas

131 pical regions to relatively small changes in radiative forcing, implying even greater probable respon

132 e to each country, which is applied to total radiative forcing in 2005 to determine the combined clim

133 implications for aerosol hygroscopicity and radiative forcing in areas with wildfire influence owing

134 response to CO2, defined by the response to radiative forcing in the absence of changes in sea surfa

135 their potential impacts in human health and radiative forcing in the air.

136 f summer temperatures to Holocene insolation radiative forcing in the Alaskan sub-Arctic, possibly be

137 Particle emissions affect radiative forcing in the atmosphere.

138 displays the climate impact, as expressed by radiative forcing in watts per meter squared, of individ

139 vised treatment indicates a global net cloud radiative forcing increase of approximately 1 W m(-2) fo

140 Inferred annual surface radiative forcings increased stepwise to 13-17 Wm(-2) be

141 uencing climatic conditions directly through radiative forcing, increasing carbon dioxide concentrati

142 ising from temperature observations, climate radiative forcings, internal variability and the model r

143 ngwave effect dominates and the net contrail radiative forcing is believed to be positive.

144 ing regions, such as the subtropics, the CO2 radiative forcing is larger because the atmosphere is dr

145 In particular, North Atlantic TC response to radiative forcing is poorly understood and creates the d

146 the intertropical convergence zone, the CO2 radiative forcing is reduced, or "masked," by deep-conve

147 of energy from the Earth's climate system if radiative forcing is reduced.

148 hese results suggest that present-day direct radiative forcing is stronger than present model estimat

149 a strongly nonlinear response of monsoons to radiative forcings is found in the seasonal onset of the

150 The gain factor of so-called "cloud radiative forcing" is then computed as the difference be

151 mitted by the Earth and atmosphere (positive radiative forcing) is partly compensated by their reflec

152 Given differences with current radiative forcing it remains uncertain if the Pacific wi

153 From studies of aerosol radiative forcing, it is known that black carbon can exi

154 Specifically, relative to CO(2) radiative forcing, land-cover-atmosphere feedbacks lead

155 osols for climate (expressed in terms of the radiative forcing metric or changes in global surface te

156 Others suggest that radiative forcing might also play a role.

157 on aerosols should be explicitly included in radiative forcing models.

158 remaining are due to imperfect knowledge of radiative forcing, natural climate variability, and erro

159 aerosols is estimated to be equivalent to a radiative forcing of -0.5 +/- 0.4 watts per square meter

160 A radiative forcing of -1 Wm(-2), for example, might be ac

161 tion cross section show SF(5)CF(3) to have a radiative forcing of 0.57 watt per square meter per part

162 ve concentration pathway with end-of-century radiative forcing of 8.5 W/m(2).

163 e limited but suggest an additional negative radiative forcing of about -0.1 watt per square meter fr

164 ize led to cloud brightening and global-mean radiative forcing of around -0.2 watts per square metre

165 Indirect radiative forcing of atmospheric aerosols by modificatio

166 ls is thought to contribute substantially to radiative forcing of climate change over the industrial

167 emissions to the atmosphere and so limit the radiative forcing of climate change.

168 est a larger role for biomass burning in the radiative forcing of climate in the remote TWP than is c

169 The largest uncertainty in the historical radiative forcing of climate is caused by the interactio

170 e of one of the largest uncertainties in the radiative forcing of climate over the industrial period.

171 effect that is consistent with concerns over radiative forcing of climate.

172 coverage of low clouds, yielding significant radiative forcing of climate.

173 ing radiation leads to a significant role in radiative forcing of climate.

174 he importance of ice-albedo feedbacks on the radiative forcing of climate.

175 the humid climate due to a stronger longwave radiative forcing of coarser aerosols.

176 for this purpose, which use the accumulated radiative forcing of each gas by a set time horizon to e

177 Tropospheric aerosols affect the radiative forcing of Earth's climate, but their variable

178 2) yr(-1) is required to offset the positive radiative forcing of increasing CH4 emissions until the

179 Radiative forcing of methane (CH4) is significantly high

180 Notably, the overall radiative forcing of open-water fluxes (3.5 +/- 0.3 kg C

181 n the SCM that account for nonlinearities in radiative forcing of ship-induced IAE.

182 We also show, using the SIM data, that solar radiative forcing of surface climate is out of phase wit

183 enhanced greenhouse-gas emissions add to the radiative forcing of terrestrial ecosystems, these emiss

184 anding for how such aerosols influence solar radiative forcing of the atmosphere.

185 gasoline or diesel vehicles leads to greater radiative forcing of the climate for 80 or 280 yr, respe

186 re thought to be important for anthropogenic radiative forcing of the climate, yet remain poorly unde

187 onstruction of the links between climate and radiative forcing of the Earth's surface temperatures.

188 can hardly be relevant as compared with the radiative forcing of the increase of greenhouse gases.

189 In addition to radiative forcing on climate, intensification of the Pac

190 standing of the resulting impact of aircraft radiative forcing on climate.

191 ing, and decreasing albedo exerts a positive radiative forcing on climate.

192 health, air quality, and direct and indirect radiative forcing on climate.

193 However, radiative forcing on Jupiter has traditionally been attr

194 ased into the atmosphere thus exert a direct radiative forcing on the climate system.

195 st crucial feedbacks results from changes in radiative forcing on the hydrological cycle, which influ

196 This is the largest radiative forcing, on a per molecule basis, of any gas f

197 l model to quantify the uncertainty in cloud radiative forcing over the industrial period caused by u

198 ously from wet to dry stable states as their radiative forcings pass a critical threshold, sometimes

199 ed CO2 as measured by the 20-year-integrated radiative forcing per unit of carbon input (the 20-year

200 al of all greenhouse gases in terms of their radiative forcing potential relative to carbon dioxide d

201 The spatial structure of the radiative forcing reduces the need for the atmosphere to

202 In cloudy regions with a radiative forcing relative to 1750, model results sugges

203 ains, Canada, and evaluate its impact on net radiative forcing relative to potential long-term net ca

204 ndary conditions, abrupt climate changes and radiative forcing remains uncertain, however.

205 rosol optical depth (AOD), clouds, and their radiative forcing requires regionally representative aer

206 atmosphere, with potential implications for radiative forcing, residence times and other aerosol cha

207 We quantify the radiative forcing (RF) and global-mean temperature respo

208 Direct radiative forcing (RF) due to aviation BC emissions is e

209 We quantify uncertainties in radiative forcing (RF) due to short-lived increases in O

210 e gases but also of air pollutants with high radiative forcing (RF), particularly black carbon (BC).

211 of the twenty-first century for the steepest radiative forcing scenario is about 15 per cent warmer (

212 es of future global warming across the major radiative forcing scenarios, in general.

213 tor of approximately two even under the same radiative forcing scenarios.

214 Future modeling of OA radiative forcing should consider the importance of both

215 The palsa site (intact permafrost and low radiative forcing signature) had a phylogenetically clus

216 The bog (thawing permafrost and low radiative forcing signature) had lower alpha diversity a

217 The fen (no underlying permafrost, high radiative forcing signature) had the highest alpha, beta

218 logenetic diversity associated with a higher radiative forcing signature.

219 ethane concentrations, causing a global-mean radiative forcing similar in size but opposite in sign t

220 These represent scenarios in which total radiative forcing stabilizes before 2100 (RCP 4.5) or co

221 Without the radiative forcing supplied by CO(2) and the other noncon

222 ally based evidence of clear-sky CO2 surface radiative forcing that is directly attributable to the i

223 rature change by prescribing, in addition to radiative forcing, the observed history of sea surface t

224 Masked radiative forcing thereby offers an explanation for the

225 assimilation and by prescribing the external radiative forcings, this system simulates the observed l

226 Cumulative radiative forcing through 2100 would be reduced by only

227 thane, held to be responsible for 18% of the radiative forcing, to the atmosphere.

228 black carbon (BC) and thus could increase BC radiative forcing unintentionally.

229 ogen fertilization, leading to a decrease in radiative forcing, up to about two-thirds of this amount

230 e shorter timescale and by variations in the radiative forcings used to drive models over the longer

231 rs (an increase of approximately 9 Wm(-2) of radiative forcing) was almost completely negated by a lo

232 quare meter of burned area), but to decrease radiative forcing when averaged over an 80-year fire cyc

233 emains roughly constant in response to CO(2)-radiative forcing, whereas relative humidity over land d

234 rface temperature, internal variability, and radiative forcing, which includes anthropogenic factors

235 enology led to contrasting anomalies of snow radiative forcing, which is dominated by De and accounts

236 e (CaCO3) aerosol particles might reduce net radiative forcing while simultaneously increasing column

237 Uncertainties in how radiative forcing will impact the tropical Pacific clima

238 on the hydrological cycle that only consider radiative forcing will therefore tend to underestimate f

239 magnitude and possibly the sign of the dust radiative forcing, with implications for numerical weath

240 These snowmelt season radiative forcings would have resulted in additional ann