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

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

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

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

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

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

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

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

12 The observed stratospheric aerosols and gases are fully explained by

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

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

15 Stratospheric aerosols from large tropical explosive vol

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

17 Although stratospheric aerosols primarily consisted of sulfuric a

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

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

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

21 resembles model predictions more closely in stratospheric air.

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

23 a conserved tracer analogous to exhaust from stratospheric aircraft.

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

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

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

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

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

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

30 Stratospheric and tropospheric difluorodichloromethane (

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

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

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

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

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

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

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

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

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

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

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

42 The lower stratospheric circulation and sea-surface temperature ap

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

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

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

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

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

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

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

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

51 Polar stratospheric cloud lifetimes required for Arctic denitr

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

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

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

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

56 erature-dependent isotopic exchange on polar stratospheric clouds.

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

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

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

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

61 We quantify the stratospheric contribution to MSU channel 2 temperatures

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

63 This would cause stratospheric cooling, enhancement of the heterogeneous

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

65 tained global-scale tropospheric warming and stratospheric cooling.

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

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

68 These stratospheric events also precede shifts in the probabil

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

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

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

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

73 (4-9) parts per trillion] [corrected] to the stratospheric input at the tropical tropopause.

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

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

76 Evidence suggests deep stratospheric intrusions can elevate western US surface

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

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

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

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

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

82 ulate the observed isotopic fractionation of stratospheric N2O.

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

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

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

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

87 Zonal mean stratospheric overturning circulation organizes the tran

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

105 000 in six major categories (climate change, stratospheric ozone depletion, agricultural intensificat

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

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

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

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

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

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

112 ributors to the anthropogenic enhancement of stratospheric ozone depletion.

113 nt to previously unrecognized mechanisms for stratospheric ozone depletion.

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

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

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

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

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

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

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

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

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

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

124 known remaining anthropogenic threat to the stratospheric ozone layer.

125 2005 in the USA, because it can deplete the stratospheric ozone layer.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

145 e through radiative warming and depletion of stratospheric ozone.

146 for most of the anthropogenic destruction of stratospheric ozone.

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

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

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

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

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

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

153 ydrospheric isotope exchange with water, and stratospheric photochemistry.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

168 Stratospheric subsidence at the edges of the disturbance

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

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

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

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

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

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

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

176 ozone depletion through decreasing the lower stratospheric temperature.

177 Higher stratospheric temperatures accelerate catalytic reaction

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

179 Stratospheric temperatures on Saturn imply a strong deca

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

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

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

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

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

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

186 concentrations were analyzed to investigate stratospheric transport rates.

187 Stratospheric volcanic aerosols reflect sunlight, which

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

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

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

191 Stratospheric water vapor concentrations decreased by ab

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

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

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

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

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

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

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

199 Stratospheric water vapour is a powerful greenhouse gas.

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

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