ライフサイエンスコーパス: stratosphere

1 sions contribute to ozone destruction in the stratosphere.

2 trength of the meridional overturning of the stratosphere.

3 iabatic overturning mass flux throughout the stratosphere.

4 ne the penetration of the hot spots into the stratosphere.

5 easurements of infrared spectra of Jupiter's stratosphere.

6 latitudes in the upper troposphere and lower stratosphere.

7 e crystals and more water vapor entering the stratosphere.

8 al range of chemical ozone loss in the lower stratosphere.

9 is transported from the troposphere into the stratosphere.

10 were observed in the 1999/2000 Arctic winter stratosphere.

11 significant potential to denitrify the lower stratosphere.

12 ne and chlorine compounds in the terrestrial stratosphere.

13 and possibly more humid future Arctic lower stratosphere.

14 the photochemical haze (or smog) in Titan's stratosphere.

15 e existence of unidentified NOX sinks in the stratosphere.

16 CO2 data is approximately 5 years in the mid-stratosphere.

17 m supersonic aircraft could reach the middle stratosphere.

18 he Atlantic and Tethysian realms through the stratosphere.

19 reactions characteristic of the present-day stratosphere.

20 serves as a major transport pathway into the stratosphere.

21 Hg (RM) forms throughout the troposphere and stratosphere.

22 fy the total bromine loading injected to the stratosphere.

23 us chemical reactions in the troposphere and stratosphere.

24 in water vapour concentrations in the lower stratosphere.

25 are dynamically connected through the polar stratosphere.

26 posphere (9 to 14 kilometers) into the lower stratosphere.

27 may dominate the O(3) SC signal in the upper stratosphere.

28 osphere and between different regions of the stratosphere.

29 ia, India, and Indonesia to enter the global stratosphere.

30 upwelling cannot be the main source for the stratosphere.

31 .5 h, in comparison with 3-5 days in Earth's stratosphere.

32 ction of sulfate aerosol precursors into the stratosphere.

33 occurrence of processes native to planetary stratospheres.

34 tion characteristic of aerosols in planetary stratospheres.

35 Mountain waves also occurred throughout the stratosphere (15 to 45 kilometers) over a broad mountain

36 frequently affected the Northern Hemisphere stratosphere aerosol loadings, whereas the Southern Hemi

37 Wave activity in the stratosphere also appears analogous to that occurring on

38 circulation strength at upper levels of the stratosphere amounts to at least 100 %.

39 reached 1.95 +/- 0.05(1sigma) in the middle stratosphere and 2.22 +/- 0.07 in the Arctic vortex vers

40 tely 50 kilometers, descend to the lowermost stratosphere and are followed by anomalous tropospheric

41 sotope slopes between the laboratory and the stratosphere and between different regions of the strato

42 ormed within the eastward phase in the lower stratosphere and cannot be accounted for by the standard

43 ects 5 Tg yr(-1) of sulphur dioxide into the stratosphere and cross-comparing simulations from 5 clim

44 nsidered against the background of a cooling stratosphere and geo-engineering plans to increase sulph

45 stent circulation anomalies in the lowermost stratosphere and is greatest during boreal winter.

46 st particles (IDPs) collected in the Earth's stratosphere and meteorites are fragments of comets and

47 erestimate the observed cooling of the lower stratosphere and overestimate the warming of the troposp

48 t of the tropopause-the boundary between the stratosphere and troposphere-has increased by several hu

49 rtance of the dynamical coupling between the stratosphere and troposphere.

50 sions through the coupled chemistries of the stratosphere and troposphere.

51 s the dynamics of the mid- and high-latitude stratosphere and weather in the lower atmosphere.

52 -12b lacks a prominent thermal inversion (or stratosphere) and has very efficient day-night energy ci

53 ery different isotopic fractionations in the stratosphere, and (ii) laboratory photolysis experiments

54 use substantial ozone depletion in the lower stratosphere, and any increases in future abundances (e.

55 ars, transporting more aged air to the lower stratosphere, and characterized by a larger relative con

56 torms, low-latitude upper troposphere, polar stratosphere, and northern aurora.

57 The object exploded in the stratosphere, and the ensuing shock wave blasted the cit

58 ard and westward wind jets in the equatorial stratosphere (approximately 16 to 50 kilometers altitude

59 onal variability of temperatures in Saturn's stratosphere as a manifestation of a wave phenomenon sim

60 erosol that they attribute to troposphere to stratosphere ascent via the Asian monsoon.

61 chemistry is irreversible transport from the stratosphere, associated with deep intrusions.

62 ssion, providing a detection of an exoplanet stratosphere at 5sigma confidence.

63 iation of the N2:O2 dimer produce NOx in the stratosphere at a rate comparable to the oxidation of N2

64 present throughout the upper troposphere and stratosphere at both poles.

65 rine and bromine will reach a maximum in the stratosphere between 1997 and 1999 and will decline ther

66 ols by the impact and their injection in the stratosphere, blocking incoming solar radiation.

67 imentation of these large sizes in the lower stratosphere, but the nucleation process is not yet know

68 orange-brown smog, which is produced in the stratosphere by photochemical reactions following the di

69 /bromine free-radical chemistry of the lower stratosphere by shifting total available inorganic chlor

70 persistent ozone depletion is heating of the stratosphere by smoke, which strongly absorbs solar radi

71 burden of sulfate aerosols injected into the stratosphere by the eruption of Mount Pinatubo in 1991 c

72 that cause denitrification in a nonvolcanic stratosphere cannot efficiently form in a volcanic envir

73 ary contributions are through cooling of the stratosphere (caused by ozone) and warming of the tropos

74 ) (1997-1998)-induced changes in troposphere-stratosphere chemistry and dynamics.

75 se the significance of volcanic halogens for stratosphere chemistry and suggest that modelling of pas

76 In Titan's stratosphere, collisional stabilization of the initial C

77 that, at typical upper troposphere and lower stratosphere conditions, particles are formed by this nu

78 t tropospheric air enters the lower tropical stratosphere continuously, ascends, and is transported r

79 s, volcanogenic sulphate injections into the stratosphere cooled the NH preferentially, inducing a he

80 nt climate perturbation ends abruptly as the stratosphere cools and becomes supersaturated, causing r

81 Thus, hydration of the global stratosphere could be especially sensitive to changes of

82 It has been suggested that stratospheres could form in highly irradiated exoplanets

83 in decrease in the temperature of the Arctic stratosphere due to anthropogenic and/or natural effects

84 the midlatitude upper troposphere and lower stratosphere during PV intrusions.

85 c plume was injected directly into the lower stratosphere during the initial eruption well before rea

86 nd temperature that prevail in the Antarctic stratosphere during the period of maximum ozone (O3) dis

87 Air samples from the lower stratosphere exhibit 15N/14N and 18O/16O enrichment in n

88 The continuous injection of sulfur into the stratosphere has been suggested as a "geoengineering" sc

89 y ozone loss process in the cold polar lower stratosphere hinges on chlorine monoxide (ClO) and one o

90 y is well known for ozone destruction in the stratosphere, however reactive halogens also play an imp

91 methane into higher hydrocarbons in Titan's stratosphere implies a surface or subsurface methane res

92 mponent that extends from the surface to the stratosphere in middle and high latitudes of both hemisp

93 ective injection into the mid-latitude lower stratosphere in summer.

94 at projected for a colder future nonvolcanic stratosphere in the 2010 decade.

95 ) hydrolysis can be important in the Earth's stratosphere, in the heterogeneous formation of sulfuric

96 Climate models predict that the lower stratosphere is cooling as a result of greenhouse gas bu

97 component that resides in the mesosphere and stratosphere is not of chondritic composition.

98 er vapor and CO entering the global tropical stratosphere is transported over the Asian monsoon/Tibet

99 val mechanisms are slow, so that much of the stratosphere is ultimately heated by the localized smoke

100 Saturn's south polar stratosphere is warmer than predicted from simple radiat

101 ven if only 2% of these halogens reached the stratosphere, it would have resulted in strong global oz

102 ificant change in the chemistry of the lower stratosphere leading to a reduction potentially larger t

103 -lasting cold conditions in the Arctic lower stratosphere led to persistent enhancement in ozone-dest

104 ated with volcanic aerosols in the lowermost stratosphere (LMS) had not been considered.

105 of HCl with ozone found throughout the lower stratosphere (LS).

106 oduces hot spots in its upper atmosphere and stratosphere near its poles, and the temperature maps de

107 Transport of air from the troposphere to the stratosphere occurs primarily in the tropics, associated

108 the organic aerosol formation regions in the stratosphere of a Saturn's moon Titan.

109 oling and ozone depletion in the polar lower stratosphere of both hemispheres, coupled with an increa

110 The smoggy stratosphere of Saturn's largest moon, Titan, veils its

111 reservoir, starting around 2007 in the lower stratosphere of the Northern Hemisphere, in contrast wit

112 d the largest volcanic sulfur release to the stratosphere of the past 7,000 y.

113 reported for the ratio of CH3D to CH4 in the stratosphere of the saturnian moon Titan.

114 ribute HOLW structures to transport from the stratosphere or mid-latitude troposphere are inconsisten

115 ed large volumes of sulphur dioxide into the stratosphere; or (3) MIF-S in rocks was mostly created b

116 In the upper stratosphere, our record extends back to 1986 and shows

117 In the lower stratosphere, our water vapour record extends back to 19

118 the substantial cooling of the global lower stratosphere over 1979-2003 occurred in two pronounced s

119 nt of risk associated with ozone loss in the stratosphere over the central United States in summer ba

120 ow more water vapor to travel into the lower stratosphere over the TP, effectively short-circuiting t

121 er vapor convectively injected deep into the stratosphere over the United States can fundamentally ch

122 high resolution temperature structure in the stratosphere over the United States in summer that resol

123 of convective penetration of water into the stratosphere over the United States in summer using the

124 York City, compounds that either deplete the stratosphere ozone or have significant global warming po

125 rease in the abundance of water vapor in the stratosphere (plausibly by as much as approximately 1 pa

126 the Asian monsoon/TP region enters the lower stratosphere primarily over the TP, and it is then trans

127 While ozone in the stratosphere protects the earth from harmful ultraviolet

128 tablished here that connects humidity in the stratosphere, relative humidity near the tropical tropop

129 A previous claim for the presence of a stratosphere remains open to question, owing to the chal

130 wavelength-dependent radiative effects, the stratosphere remains sufficiently cold and dry to hamper

131 partitioning of bromine and the input to the stratosphere remains uncertain.

132 The early stratosphere should have been dry, thereby precluding th

133 eric CO2 were observed to propagate into the stratosphere, showing that tropospheric air enters the l

134 The Earth's equatorial stratosphere shows oscillations in which the east-west w

135 Ozone loss is amplified in a denitrified stratosphere, so the effects of falling temperatures in

136 circulation changes initially induced in the stratosphere subsequently penetrate into the troposphere

137 by the meridional overturning of mass in the stratosphere, the Brewer-Dobson circulation.

138 In the stratosphere, the major source of O((1)D) is O(3) photol

139 Injecting sulfate aerosol into the stratosphere, the most frequently analyzed proposal for

140 , but are rapidly photolysed above the lower stratosphere, the timescale for their removal is set mai

141 In the lower stratosphere, these two estimates agree, and at a potent

142 s from increases in water vapor entering the stratosphere through the tropical tropopause layer, with

143 etrated hundreds of kilometers into Saturn's stratosphere (to the 1-millibar region).

144 altered solar ultraviolet radiation, altered stratosphere-to-troposphere O(3) flux, increased troposp

145 erved in many UT air parcels, as a result of stratosphere-to-troposphere transport events.

146 The strength of stratosphere-to-troposphere transport is largely control

147 3/HOx in cold climates is driven by enhanced stratosphere-to-troposphere transport of O3, and that re

148 Stratosphere-troposphere exchange could be enhanced by t

149 ere we study volcanic aerosol changes in the stratosphere using lidar measurements from the NASA CALI

150 through the Asian monsoon, and deep into the stratosphere, using satellite observations of hydrogen c

151 h transport from the upper troposphere/lower stratosphere (UT/LS).

152 tion in the tropical upper troposphere/lower stratosphere via the Ozone El-Nino Southern Oscillations

153 At solar maximum, a warming of the summer stratosphere was found to strengthen easterly winds, whi

154 ere on a global scale, before they reach the stratosphere where they release chlorine atoms that caus

155 es about half of the bromine that enters the stratosphere, where it plays an important role in ozone

156 the D/H ratio of H2 produced from CH4 in the stratosphere, where production is isolated from the infl

157 The smoke-laden air rises to the upper stratosphere, where removal mechanisms are slow, so that

158 to study the irreversible transport from the stratosphere, where the triple oxygen isotopes of CO2 ar

159 l chlorine and bromine, respectively, to the stratosphere, where they catalyze the destruction of ozo

160 Conversely, if there is a stratosphere-where temperature increases with altitude-t

161 gases such as ozone and water vapour in the stratosphere - which affect surface climate - is influen

162 gnificant quantities of SO4 aerosol into the stratosphere, which are known to affect ENSO strength by

163 se regulate the humidity of air entering the stratosphere, which in turn has a strong influence on th

164 ozone loss and heating of the lower tropical stratosphere, which, in turn, would increase water vapor

165 The diurnal odd-nitrogen cycle in the stratosphere will be marked by a complex isotope signatu

166 se may typically allow entry of air into the stratosphere with as much as approximately 1.7 times the

167 ude air is entrained into the tropical lower stratosphere within about 13.5 months; transport is fast

168 Moreover, the radiative heating of the lower stratosphere would be roughly 10-fold less than if that