ライフサイエンスコーパス: stratospheric

1 Unraveling the ultimate source of stratospheric (16)O(13)C(18)O enrichments may impose add

2 large and unexpected meridional variation in stratospheric (16)O(13)C(18)O, observed as proportions i

3 stratospheric ozone, estimates of the future stratospheric abundance of ozone-depleting gases were ma

4 Remarkable perturbations in the stratospheric abundances of chlorine species and ozone w

5 ade has seen broad exploratory research into stratospheric aerosol (SA) geoengineering, motivated by

6 ong-term influence of pyroCb activity on the stratospheric aerosol budget.

7 ta imply a negative radiative forcing due to stratospheric aerosol changes over this period of about

8 We propose a method for stratospheric aerosol climate modification that uses a s

9 idely known solar geoengineering proposal is stratospheric aerosol injection (SAI), which has impacts

10 asurements demonstrate that the "background" stratospheric aerosol layer is persistently variable rat

11 We show that half of the global stratospheric aerosol optical depth following the Kasato

12 On average, 30% of the global stratospheric aerosol optical depth originated in the LM

13 e, we present measurements of perchlorate in stratospheric aerosol particles and confirm that the str

14 Single-particle analyses of stratospheric aerosol show that about half of the partic

15 Nabro volcano and satellite observations of stratospheric aerosol that they attribute to troposphere

16 ve notable eruptions and associate each with stratospheric aerosol veils.

17 CVs in promoting the impacts of wildfires on stratospheric aerosols and chemistry.

18 The observed stratospheric aerosols and gases are fully explained by

19 nsitive marker of climate change; impacts on stratospheric aerosols and O(3) chemistry, which need to

20 he most abundant species in tropospheric and stratospheric aerosols due to high levels of atmospheric

21 Stratospheric aerosols from large tropical explosive vol

22 Several independent data sets show that stratospheric aerosols have increased in abundance since

23 Although stratospheric aerosols primarily consisted of sulfuric a

24 The mean age A of stratospheric air determined from CO2 data is approximat

25 ical tropopause and transport ozone rich dry stratospheric air into the tropics.

26 l N2O isotopomers might be useful tracers of stratospheric air parcel motion.

27 Injected BC warms the local stratospheric air, consequently perturbing transport and

28 resembles model predictions more closely in stratospheric air.

29 imate pollutant concentrations from proposed stratospheric aircraft by 25 to 100 percent.

30 a conserved tracer analogous to exhaust from stratospheric aircraft.

31 oxidation together with a strengthened lower-stratospheric and a weakened upper-stratospheric circula

32 the 13 June Nabro eruption plume was clearly stratospheric and contained both volcanic gases and aero

33 ated J values that are sufficient to explain stratospheric and mesospheric sulfur dioxide (SO2) conce

34 the tropical tropopause layer, and in polar stratospheric and noctilucent clouds.

35 which in turn are central reactants in many stratospheric and tropospheric chemical processes.

36 e constants for key reactions of interest in stratospheric and tropospheric chemistry.

37 Stratospheric and tropospheric difluorodichloromethane (

38 r, which may allow for a distinction between stratospheric and tropospheric influences at remote East

39 wave propagation, and thereby affecting both stratospheric and tropospheric NAM-annularity.

40 hemistry, e.g., as greenhouse gases, destroy stratospheric and tropospheric ozone, and control the at

41 B can also have a significant impact on both stratospheric and tropospheric ozone, and discuss the pr

42 surface O(3) due to the presence of abundant stratospheric and upper tropospheric O(3).

43 e-depleting substances are declining and the stratospheric Antarctic ozone layer is recovering.

44 Kelut eruption in 2014, stratospheric ash-rich aerosols were observed for months

45 sing observations to derive a time-series of stratospheric biomass burning aerosol optical depths ori

46 heric emissions, where we compare zonal-mean stratospheric brightness temperatures at planetographic

47 ubstances (VSLBr) are an important source of stratospheric bromine, an effective ozone destruction ca

48 Measurements of stratospheric carbon dioxide (CO2) and nitrous oxide (N2

49 following the eruption, and perturbations to stratospheric chemical composition resulting from the in

50 ations, and of the impact of volcanic ash on stratospheric chemistry and radiation.

51 including an interactive parameterization of stratospheric chemistry show how upper stratospheric ozo

52 , the CCMVal models have a fully interactive stratospheric chemistry.

53 cies (BrOx) contributing to tropospheric and stratospheric chemistry.

54 Remote-sensing data have revealed a peak in stratospheric chlorine after 1996, then a decrease of cl

55 As a consequence, stratospheric chlorine levels are declining and ozone is

56 rted here is a theoretical study of possible stratospheric chlorine reservoir species including isome

57 level, in hydrogen chloride (HCl), the main stratospheric chlorine reservoir, starting around 2007 i

58 and elevates the astrophysical importance of stratospheric chondritic porous interplanetary dust part

59 The lower stratospheric circulation and sea-surface temperature ap

60 ned lower-stratospheric and a weakened upper-stratospheric circulation inferred by this analysis.

61 autumn conditions of sea-ice concentration, stratospheric circulation, and sea-surface temperature.

62 that large variations in the strength of the stratospheric circulation, appearing first above approxi

63 on created by rising smoke plumes alters the stratospheric circulation, redistributing ozone and the

64 the large-scale upward motion of the global stratospheric circulation.

65 ng of satellite radiances provides a view of stratospheric climate change during the period 1979-2005

66 r the pronounced changes in tropospheric and stratospheric climate observed during the past few decad

67 s will act as the nucleation sites for polar stratospheric cloud ice and, after sedimentation into th

68 action of hydrogen chloride (HCl) with polar stratospheric cloud ice particles is essential for under

69 Polar stratospheric cloud lifetimes required for Arctic denitr

70 ons, acid rain, radiative balance, and polar stratospheric cloud nucleation.

71 due to uptake and/or sedimentation in polar stratospheric cloud particles.

72 eater surface area than typical Arctic polar stratospheric clouds (PSCs).

73 ld winters favourable for formation of polar stratospheric clouds (PSCs).

74 chlorine (Cl) activation occurs on the polar stratospheric clouds (PSCs; liquid and solid particles c

75 NO3-water particles, representative of polar stratospheric clouds, consists of an ice core surrounded

76 erature-dependent isotopic exchange on polar stratospheric clouds.

77 The stratospheric CO(2) oxygen isotope budget is thought to

78 We report observations of stratospheric CO2 that reveal surprisingly large anomalo

79 ossil bones and teeth, which all derive from stratospheric CO2.

80 loss during spring (up to 4.2% of the total stratospheric column).

81 cations for tropospheric oxidizing capacity, stratospheric composition and ozone chemistry.

82 contrast, the photostability of SO(3) under stratospheric conditions suggests that its removal effic

83 imately three times faster than under normal stratospheric conditions.

84 We quantify the stratospheric contribution to MSU channel 2 temperatures

85 om the influence of tropospheric forcing and stratospheric control, many studies have addressed the p

86 or tropospheric warming (8 to 15 y) than for stratospheric cooling (1 to 3 y).

87 ld have been feasible to detect human-caused stratospheric cooling by 1894, only 34 y after the assum

88 xperienced enhanced tropospheric warming and stratospheric cooling in the 15 to 45 degrees latitude b

89 This would cause stratospheric cooling, enhancement of the heterogeneous

90 reveal multidecadal tropospheric warming and stratospheric cooling, punctuated by short-term volcanic

91 Lower stratospheric cooling-primarily caused by ozone depletio

92 tained global-scale tropospheric warming and stratospheric cooling.

93 e active as greenhouse gases or as agents of stratospheric depletion.

94 ts 7.8-microm methane and 12.2-microm ethane stratospheric emissions, where we compare zonal-mean str

95 These stratospheric events also precede shifts in the probabil

96 pic approach documents several high-latitude stratospheric events that are not bipolar, but climatica

97 d sulfuric acids into stable salts to enable stratospheric geoengineering while reducing or reversing

98 This eclipse was the source of three stratospheric gravity waves.

99 rne analysis techniques for the detection of stratospheric gravity waves.

100 Here we show that the D/H ratio of stratospheric H2 develops enrichments greater than 440 p

101 (3)Br and CH(3)Cl, and thereby contribute to stratospheric halogen load.

102 Our observations suggest that these stratospheric harbingers may be used as a predictor of t

103 Through increases in stratospheric humidity, warming may also cause evaporati

104 e records from an array of ice cores suggest stratospheric injection of 14 +/- 2 Tg S associated with

105 las (Indonesia) is the source of the largest stratospheric injection of volcanic gases in the Common

106 (4-9) parts per trillion] [corrected] to the stratospheric input at the tropical tropopause.

107 alculations leads to an improvement in tropo-stratospheric interactions compared to simulations witho

108 n CO2 for CO2 biogeochemical cycle study and stratospheric intrusion flux at the surface are discusse

109 The linkage between La Nina and western US stratospheric intrusions can be exploited to provide a f

110 Evidence suggests deep stratospheric intrusions can elevate western US surface

111 We show more frequent late spring stratospheric intrusions when the polar jet meanders tow

112 0.1 parts per trillion by volume [pptv]) of stratospheric iodine injection, we use the Whole Atmosph

113 Organization, and are incompatible with zero stratospheric iodine injection.

114 We report measurements of stratospheric isotope fractionation in such a compound.

115 Lower and mid-stratospheric long-term trends are negative, and the tre

116 ell as resolving transport phenomena such as stratospheric mixing into the troposphere.

117 mission STS-66 have provided measurements of stratospheric mountain waves from space.

118 ulate the observed isotopic fractionation of stratospheric N2O.

119 ain the 15N/14N and 18O/16O fractionation of stratospheric nitrous oxide (N2O) and reconcile laborato

120 data indicate that present understanding of stratospheric nitrous oxide chemistry is incomplete.

121 ompatible with those determined for the main stratospheric nitrous oxide loss processes of photolysis

122 locity-resolved observations from the SOFIA (Stratospheric Observatory for Infrared Astronomy) legacy

123 intrusions brought dry and ozone rich air of stratospheric origin deep into the tropics.

124 Zonal mean stratospheric overturning circulation organizes the tran

125 f spatiotemporal variations in Earth's lower-stratospheric ozone (LSO) and temperature, which provide

126 ons of increased N(2)O abundance, leading to stratospheric ozone (O(3)) depletion, altered solar ultr

127 s the photochemical coupling between N2O and stratospheric ozone (O3), which can easily be decomposed

128 f increasing greenhouse gases and decreasing stratospheric ozone and is predicted to continue by the

129 y, and may be related to human influences on stratospheric ozone and/or atmospheric greenhouse gas co

130 o a significant decline from 2004 to 2007 in stratospheric ozone below an altitude of 45 km, with an

131 anges to high-latitude atmospheric dynamics, stratospheric ozone change, and tropical sea surface tem

132 on of stratospheric chemistry show how upper stratospheric ozone changes may amplify observed, 11-yea

133 ing (i.e. chlorine and bromine) compounds in stratospheric ozone chemistry and climate forcing is poo

134 sea ice, we show that including interactive stratospheric ozone chemistry in atmospheric model calcu

135 This suggests that stratospheric ozone chemistry is important for the under

136 terogeneous reactions that are important for stratospheric ozone chemistry under both background and

137 s, which individually impact global climate, stratospheric ozone concentration, or local photochemist

138 rctic, essentially complete removal of lower-stratospheric ozone currently results in an ozone hole e

139 that strong synergistic interactions between stratospheric ozone depletion and greenhouse warming are

140 Due to its significant contribution to stratospheric ozone depletion and its potent greenhouse

141 to be reduced by more realistic treatment of stratospheric ozone depletion and volcanic aerosol forci

142 ities of mid-UV radiation (UVB), a result of stratospheric ozone depletion during the austral spring,

143 t the entire atmosphere, resulting in severe stratospheric ozone depletion for several years.

144 s syndrome to increases in UV radiation from stratospheric ozone depletion needs to be completed.

145 and reduces their potential to contribute to stratospheric ozone depletion or global warming; HFCs do

146 pics-similar to those associated with modern stratospheric ozone depletion over Antarctica-plausibly

147 and summer can be explained as a response to stratospheric ozone depletion over Antarctica.

148 ric N(2)O concentrations have contributed to stratospheric ozone depletion(1) and climate change(2),

149 000 in six major categories (climate change, stratospheric ozone depletion, agricultural intensificat

150 trate the roles of methane, nitrogen oxides, stratospheric ozone depletion, and global warming drivin

151 models forced by greenhouse gases, aerosols, stratospheric ozone depletion, and volcanic eruptions an

152 + Liters) Neptune also has a lower impact in stratospheric ozone depletion, fine particulate matter f

153 ed as contributing to the warming, including stratospheric ozone depletion, local sea-ice loss, an in

154 ride (CH3Cl), compounds that are involved in stratospheric ozone depletion, originate from both natur

155 e to the potential contributions of CH3Br to stratospheric ozone depletion, technologies for the capt

156 powerful greenhouse gas and a major cause of stratospheric ozone depletion, yet its sources and sinks

157 ributors to the anthropogenic enhancement of stratospheric ozone depletion.

158 nt to previously unrecognized mechanisms for stratospheric ozone depletion.

159 d chlorine, respectively, which can catalyze stratospheric ozone depletion.

160 loride (CH(3)Cl) significantly contribute to stratospheric ozone depletion.

161 radiation indicate that the eruptions led to stratospheric ozone depletion.

162 romethane (CH3Cl) plays an important role in stratospheric ozone destruction, but many uncertainties

163 N(2)O), a greenhouse gas that contributes to stratospheric ozone destruction.

164 e gas that contributes to climate change and stratospheric ozone destruction.

165 Polar stratospheric ozone has decreased since the 1970s due to

166 eloped a method for diagnosing the amount of stratospheric ozone in these UT parcels using the compac

167 on precipitation and severe depletion of the stratospheric ozone layer in the Northern Hemisphere.

168 Accordingly, the stratospheric ozone layer is expected to recover.

169 The recovery of the stratospheric ozone layer relies on the continued declin

170 The threat N2O poses to the stratospheric ozone layer, coupled with the uncertain fu

171 source of odd-hydrogen radicals, destroy the stratospheric ozone layer, such that Earth's surface rec

172 The recognition that CFCs destroy the stratospheric ozone layer, with consequent enormous cons

173 known remaining anthropogenic threat to the stratospheric ozone layer.

174 2005 in the USA, because it can deplete the stratospheric ozone layer.

175 e by the Montreal Protocol in protecting the stratospheric ozone layer.

176 unted for when studying the evolution of the stratospheric ozone layer.

177 known to affect ENSO strength by modulating stratospheric ozone levels (OEI = 6 and (17)O = 3.3 per

178 ), and third and fourth quartile mean annual stratospheric ozone levels but increased with second, th

179 x, clear sky and issued ultraviolet indices, stratospheric ozone levels, and outdoor air temperature

180 , contributing, on average, 10% of the lower stratospheric ozone loss during spring (up to 4.2% of th

181 n dominate (~73%) the halogen-mediated lower stratospheric ozone loss during summer and early fall, w

182 , controlled substances due to their role in stratospheric ozone loss, also occur as dissolved contam

183 le the 1991 eruption of Pinatubo resulted in stratospheric ozone loss, it was due to heterogeneous ch

184 on and destruction, photooxidant cycling and stratospheric ozone loss.

185 ntemporary cities to calculate the impact on stratospheric ozone of a regional nuclear war between de

186 upon the same reaction network that reduces stratospheric ozone over the Arctic.

187 of the Montreal Protocol and the associated stratospheric ozone recovery might therefore manifest, o

188 redicting radiative forcing due to Antarctic stratospheric ozone recovery requires detecting changes

189 Furthermore, we demonstrate that stratospheric ozone recovery, resulting from the Montrea

190 This usage carries potential for stratospheric ozone reduction due to Br atom catalysis,

191 ll force SAM into its positive phase even if stratospheric ozone returns to normal levels, so that cl

192 ugh a photochemical reaction network linking stratospheric ozone to carbon dioxide and to oxygen.

193 at simulated changes in solar irradiance and stratospheric ozone was used to investigate the response

194 h this, models project a gradual increase in stratospheric ozone with the Antarctic ozone hole expect

195 orocarbons (CFCs) contribute to depletion of stratospheric ozone, CFC-containing metered-dose inhaler

196 To assess the effect of this trend on stratospheric ozone, estimates of the future stratospher

197 measures of compounds' abilities to deplete stratospheric ozone, have been a key regulatory componen

198 t may have coincided with a dramatic drop in stratospheric ozone, possibly due to a global temperatur

199 , augments the greenhouse effect, diminishes stratospheric ozone, promotes smog, contaminates drinkin

200 ve a key role in regulating tropospheric and stratospheric ozone, while some hHNPs bioaccumulate and

201 mical reactions-specifically those producing stratospheric ozone-and providing the major source of he

202 Implicated as a stratospheric ozone-depleting compound, methyl bromide (

203 t to the regulation of both tropospheric and stratospheric ozone.

204 ce in the Archean, prior to the formation of stratospheric ozone.

205 esterlies, largely in response to changes in stratospheric ozone.

206 e through radiative warming and depletion of stratospheric ozone.

207 for most of the anthropogenic destruction of stratospheric ozone.

208 gas that also plays a role in the cycling of stratospheric ozone.

209 se gases, tropospheric sulfate aerosols, and stratospheric ozone.

210 long-lived greenhouse gas that also destroys stratospheric ozone.

211 o periodic enhanced UV-B due to depletion of stratospheric ozone.

212 tent greenhouse gas (GHG) that also depletes stratospheric ozone.

213 The sodium/iron ratio in these stratospheric particles is higher and the magnesium/iron

214 ydrospheric isotope exchange with water, and stratospheric photochemistry.

215 ulations, which did not adequately represent stratospheric plume rise.

216 he OWBCs substantially weaken the wintertime stratospheric polar vortex by enhancing the upward plane

217 mbers of 1 and 2, subsequently weakening the stratospheric polar vortex in mid-winter (January-Februa

218 nd of plausible CMIP trajectories, while the stratospheric polar vortex shows robust strengthening, b

219 can be traced to recent trends in the lower stratospheric polar vortex, which are due largely to pho

220 sit the momentum transported, disturbing the stratospheric polar vortex, which can lead to a breakdow

221 Therefore, an accurate representation of stratospheric processes in climate models is necessary t

222 culation, determining boundary conditions to stratospheric processes, which in turn influence troposp

223 Stratospheric profiles of SF(5)CF(3) suggest that it is

224 hemistry and auroral chemistry dominates the stratospheric radiative heating at middle and high latit

225 The Dome C stratospheric reconstruction provides independent valida

226 Two mechanisms, the top-down stratospheric response of ozone to fluctuations of short

227 s and our ability to test simulations of the stratospheric response to emissions of greenhouse gases

228 summer 1831 CE and immediately prior to the stratospheric S fallout.

229 An unusually cold Arctic stratospheric season occurred in 2011, raising the quest

230 simpler isotopic distillation model reveal a stratospheric signature in the (17)O-excess record at Vo

231 Thus, although no stratospheric source needs to be invoked, the data indic

232 be produced from a combination of different stratospheric sources (sulfur dioxide and carbonyl sulfi

233 Results include the detection of two new stratospheric species, the methyl radical and diacetylen

234 composed of ethane and forms as a result of stratospheric subsidence and the particularly cool condi

235 Stratospheric subsidence at the edges of the disturbance

236 spheric field measurements and models of the stratospheric sulfate aerosol layer led to the suggestio

237 tropical eruption, requires revision of the stratospheric sulfate injection mass that is used for pa

238 Moreover, we will show height-resolved stratospheric sulfur dioxide and volcanic aerosol enhanc

239 About 10% of stratospheric sulfuric acid particles larger than 120 nm

240 e next few decades could cause up to half of stratospheric sulfuric acid particles to contain metals

241 cecraft reentries can be clearly measured in stratospheric sulfuric acid particles.

242 For changes in lower stratospheric temperature between 1979 and 2011, S/N rat

243 llite-based measurements of tropospheric and stratospheric temperature change.

244 i-correlation between tropospheric and lower stratospheric temperature is confirmed-the lower stratos

245 n 1860 had not been global, and high-quality stratospheric temperature measurements existed for North

246 into question our understanding of observed stratospheric temperature trends and our ability to test

247 fferences are unclear, model biases in lower stratospheric temperature trends are likely to be reduce

248 The spatial distribution of tropospheric and stratospheric temperature trends for 1979 to 2005 was ex

249 In contrast, global stratospheric temperature trends have much higher signal

250 ozone depletion through decreasing the lower stratospheric temperature.

251 Higher stratospheric temperatures accelerate catalytic reaction

252 A new data set of middle- and upper-stratospheric temperatures based on reprocessing of sate

253 Stratospheric temperatures on Saturn imply a strong deca

254 la: see text], computed for tropospheric and stratospheric temperatures over 1979 to 2018.

255 Anomalously high lower stratospheric temperatures were recorded for 4 months at

256 e weak because the instrument partly records stratospheric temperatures whose large cooling trend off

257 or quasi-liquid layer, at the ice surface at stratospheric temperatures.

258 ures using MSU channel 4, which records only stratospheric temperatures.

259 nhancing ozone loss rates at relatively warm stratospheric temperatures.

260 or the response of tropospheric oxidants and stratospheric thermal and mass balance.

261 lar vortex show correlations with long-lived stratospheric tracer and bulk isotope abundances opposit

262 dynamical variability will also affect other stratospheric tracers and needs to be accounted for when

263 concentrations were analyzed to investigate stratospheric transport rates.

264 th the Kuwae volcano, and likely not a large stratospheric tropical eruption, requires revision of th

265 ipses, from which we derive a time series of stratospheric turbidity.

266 Stratospheric volcanic aerosols reflect sunlight, which

267 ratures are sensitive to regional changes in stratospheric volcanic and tropospheric mineral aerosols

268 However, identification of stratospheric volcanic eruptions in the geological recor

269 on about 445 million years ago suggests that stratospheric volcanic eruptions may have contributed to

270 High quality records of stratospheric volcanic eruptions, required to model past

271 ere we present a new 2600-year chronology of stratospheric volcanic events using an independent appro

272 climate, but how climate change affects the stratospheric volcanic sulfate aerosol lifecycle and rad

273 overed in ice core sulphate originating from stratospheric volcanism.

274 Subsequently, the polar stratospheric vortex weakened significantly, resulting i

275 e ozone profiles retrieved during the Sudden Stratospheric Warming (SSW) event registered in Spring 2

276 he winter polar stratosphere known as Sudden Stratospheric Warming (SSW) events are well recognized f

277 Ultraviolet irradiance modulates stratospheric warming and ozone production, and influenc

278 In contrast, global-mean radiative forcing, stratospheric warming and surface cooling from infrequen

279 mission and transport are impacted by sudden stratospheric warmings (SSWs), which establish a negativ

280 Extreme polar vortex events known as sudden stratospheric warmings can influence surface winter weat

281 ger time scales, and may help to explain why stratospheric water vapor appears to have been increasin

282 Stratospheric water vapor concentrations decreased by ab

283 Even the low stratospheric water vapor content provides an important

284 Hence, lowermost stratospheric water vapor exerts a first order effect on

285 ric temperature, implying the existence of a stratospheric water vapor feedback.

286 s from analysis of observations showing that stratospheric water vapor increases with tropospheric te

287 These findings show that stratospheric water vapor is an important driver of deca

288 More limited data suggest that stratospheric water vapor probably increased between 198

289 We show here that stratospheric water vapor variations play an important r

290 tionation imprints the isotopic signature of stratospheric water vapor, which may allow for a distinc

291 (+0.03 +/- 0.01 watts per square metre) and stratospheric water vapour (+0.011 +/- 0.001 watts per s

292 er Boulder, Colorado, USA shows increases in stratospheric water vapour concentrations that cannot be

293 Stratospheric water vapour is a powerful greenhouse gas.

294 hydrogen interacts with methane, ozone, and stratospheric water vapour, leading to an indirect 100-y

295 s feature lower-level stretched vortices and stratospheric wave reflection.

296 from poor vertical resolution and Jupiter's stratospheric wind velocities have not yet been determin

297 asi-biennial oscillation (QBO) of equatorial stratospheric winds and the amplitude of the Madden-Juli

298 hm and is robust to the natural diversity in stratospheric winds.

299 tion in this region is a critical control of stratospheric WV.

300 l vertically over great distances, modifying stratospheric zonal jets, exciting wave activity and tur