ライフサイエンスコーパス: radiative forcing

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

2 ncy in dry deposition alters modeled CCN and radiative forcing.

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

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

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

6 ning the tropical climate response to global radiative forcing.

7 e uncertainty in anthropogenic aerosol-cloud radiative forcing.

8 ncern because of the contribution to climate radiative forcing.

9 challenging to estimate its contribution to radiative forcing.

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

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

12 and the potential for positive feedbacks on radiative forcing.

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

14 little effect on greenhouse gas emissions or radiative forcing.

15 deployment significantly increases long-term radiative forcing.

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

17 erosol-mixing states while calculating their radiative forcing.

18 nities for rapid mitigation of anthropogenic radiative forcing.

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

20 a substantial role in climate change through radiative forcing.

21 y of tropical Pacific convection to external radiative forcing.

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

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

24 ins are particularly sensitive to changes in radiative forcing.

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

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

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

28 e a potentially significant effect on global radiative forcing.

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

30 gest uncertainty in estimating anthropogenic radiative forcing.

31 the most uncertain components of the global radiative forcing.

32 tly missing in model calculations of aerosol radiative forcing.

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

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

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

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

37 formation and therefore cloud properties and radiative forcing.

38 fferences in the factors producing increased radiative forcing.

39 nstrain atmospheric CH4 levels and attendant radiative forcing.

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

41 eater increases for RCPs describing stronger radiative forcings.

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

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

44 ate and land use change decreases the direct radiative forcing (-0.38 W m(-2)) by 6.3% and the indire

45 ing (-0.38 W m(-2)) by 6.3% and the indirect radiative forcing (-1.68 W m(-2)) by 3.5% due to the siz

46 s (-52%) reduce the annual mean contrail net radiative forcing (-44%), adding to climate gains from r

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

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

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

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

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

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

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

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

55 iodine emissions have implications for ozone radiative forcing and possibly new particle formation ne

56 ion of clouds and their properties including radiative forcing and precipitation, yet the sources and

57 tion in pristine atmospheres, altering cloud radiative forcing and precipitation.

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

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

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

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

62 orous particles like dust could impact cloud radiative forcing and, thus, the climate via ice cloud f

63 contrail age, coverage, optical properties, radiative forcing, and energy forcing (EF) from individu

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

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

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

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

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

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

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

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

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

73 Overall, the total radiative forcing associated with anthropogenic aerosols

74 Radiative forcing associated with reduction in atmospher

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

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

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

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

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

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

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

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

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

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

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

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

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

88 sum of the total aerosol direct and indirect radiative forcing by 12.5%.

89 ther proposals suggest masking the increased radiative forcing by an increase in particles and/or clo

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

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

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

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

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

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

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

97 Radiative forcing by increasing deposition of industrial

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

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

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

101 at mangrove F(CH4) could offset the negative radiative forcing caused by CO(2) uptake by 52% and 24%

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

103 a systematic shift, being comparable to the radiative forcing change from preindustrial to present,

104 ls to show that in a CO(2)-enriched climate, radiative forcing changes drive annual precipitation inc

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

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

107 equatorial Pacific than expected from simple radiative forcing considerations.

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

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

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

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

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

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

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

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

116 The corresponding negative radiative forcing due to aerosol cloud interactions (RF[

117 ncentrations of PM(2.5) and ozone and direct radiative forcing due to aerosols and ozone.

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

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

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

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

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

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

124 r source of uncertainty in estimating global radiative forcing due to the complex nature of the aeros

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

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

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

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

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

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

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

132 methane, resulting in positive and negative radiative forcing effects, respectively.

133 ts to Arctic warming represents about 10% of radiative forcing effects.

134 The radiative forcing efficiencies of many individual emissi

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

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

137 (roughly 3/4) of the total aerosol indirect radiative forcing estimate.

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

139 the largest source of uncertainty in global radiative forcing estimates, hampering our understanding

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

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

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

143 o different processes: a rapid adjustment to radiative forcing, followed by a slower response to surf

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

145 antiago, and southern Chile; respective mean radiative forcings for the winter months were 2.8, 1.4,

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

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

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

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

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

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

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

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

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

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

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

157 Earth system modeling suggests that radiative forcing from this massive, high-latitude erupt

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

159 Effective radiative forcing has substantially increased since 2021

160 sed surface albedo, which yielded a positive radiative forcing (i.e., warming).

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

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

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

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

165 he past two decades, with enhanced post-fire radiative forcing in 2018 causing earlier melt and snow

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

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

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

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

170 Particle emissions affect radiative forcing in the atmosphere.

171 bonaceous aerosols play an important role in radiative forcing in the remote and climate-sensitive Ti

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

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

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

175 ios, with stronger drying as the strength of radiative forcing increases.

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

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

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

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

180 the high-latitudes' response to increases in radiative forcing is much larger than elsewhere in the w

181 We argue that the latter, even if the radiative forcing is negligible, should more appropriate

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

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

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

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

186 ensitivity of this region to slow changes in radiative forcing is thus strongly mediated by internal

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

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

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

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

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

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

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

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

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

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

197 ities < 0.2 m/s, and causes a direct aerosol radiative forcing of +0.15 W/m(2).

198 tration by ~10 % and causes a direct aerosol radiative forcing of -0.10 W/m(2).

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

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

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

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

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

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

205 Indirect radiative forcing of atmospheric aerosols by modificatio

206 amely, the ocean carbon buffer capacity, the radiative forcing of carbon dioxide and the carbon inven

207 bon (BrC) is an important contributor to the radiative forcing of climate by organic aerosols.

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

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

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

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

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

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

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

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

216 ound effects on air quality, visibility, and radiative forcing of climate.

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

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

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

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

221 Given assumptions concerning the radiative forcing of greenhouse gases, ice sheets and mi

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

223 Radiative forcing of methane (CH4) is significantly high

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

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

226 air quality, atmospheric deposition and the radiative forcing of sulfate aerosols.

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

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

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

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

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

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

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

234 We also estimate that the radiative forcing of tropospheric O(3) since 1850 AD is

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

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

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

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

239 However, radiative forcing on Jupiter has traditionally been attr

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

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

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

243 diation, moisture and wind (e.g. topography, radiative forcing or cold-air pooling).

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

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

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

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

248 age; and its absorption character may add to radiative forcing processes in the atmosphere.

249 Effective radiative forcing quantifies the effect of such anthropo

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

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

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

253 rnal decadal variability under anthropogenic radiative forcing remain largely unexplored.

254 Consequently, the uncertainty in aerosol radiative forcing remains one of the largest in the Asse

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

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

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

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

259 All three components exert a positive radiative forcing (RF) and lead to climate warming of si

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

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

262 nalytical model is developed to estimate the radiative forcing (RF) using a novel model form and an i

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

264 Converted to radiative forcing (RF), we estimated that fires generate

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

266 In a high radiative forcing scenario, such decreases in economic a

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

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

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

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

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

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

273 logenetic diversity associated with a higher radiative forcing signature.

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

275 een 8 cm(-3) and 24 cm(-3) By extension, the radiative forcing since 1850 from aerosol-cloud interact

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

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

278 ula: see text]) is one of the most uncertain radiative forcing terms as reported in the 5th Assessmen

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

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

281 Masked radiative forcing thereby offers an explanation for the

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

283 Cumulative radiative forcing through 2100 would be reduced by only

284 reveals a much greater sensitivity of cloud radiative forcing to CCN than previously reported, which

285 over recent decades and their corresponding radiative forcing to the climate system remain poorly un

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

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

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

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

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

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

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

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

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

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

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

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

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

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

300 O(2) + HONO) decrease air quality and impact radiative forcing, yet the factors responsible for their