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1 o periodic enhanced UV-B due to depletion of stratospheric ozone.
2 tent greenhouse gas (GHG) that also depletes stratospheric ozone.
3 t to the regulation of both tropospheric and stratospheric ozone.
4 ce in the Archean, prior to the formation of stratospheric ozone.
5 esterlies, largely in response to changes in stratospheric ozone.
6 e through radiative warming and depletion of stratospheric ozone.
7 for most of the anthropogenic destruction of stratospheric ozone.
8 gas that also plays a role in the cycling of stratospheric ozone.
9 se gases, tropospheric sulfate aerosols, and stratospheric ozone.
10 long-lived greenhouse gas that also destroys stratospheric ozone.
11 f increasing greenhouse gases and decreasing stratospheric ozone and is predicted to continue by the
12 y, and may be related to human influences on stratospheric ozone and/or atmospheric greenhouse gas co
13 mical reactions-specifically those producing stratospheric ozone-and providing the major source of he
14 o a significant decline from 2004 to 2007 in stratospheric ozone below an altitude of 45 km, with an
15 orocarbons (CFCs) contribute to depletion of stratospheric ozone, CFC-containing metered-dose inhaler
16 anges to high-latitude atmospheric dynamics, stratospheric ozone change, and tropical sea surface tem
17 on of stratospheric chemistry show how upper stratospheric ozone changes may amplify observed, 11-yea
18 ing (i.e. chlorine and bromine) compounds in stratospheric ozone chemistry and climate forcing is poo
19  sea ice, we show that including interactive stratospheric ozone chemistry in atmospheric model calcu
20                           This suggests that stratospheric ozone chemistry is important for the under
21 terogeneous reactions that are important for stratospheric ozone chemistry under both background and
22 s, which individually impact global climate, stratospheric ozone concentration, or local photochemist
23 rctic, essentially complete removal of lower-stratospheric ozone currently results in an ozone hole e
24                              Implicated as a stratospheric ozone-depleting compound, methyl bromide (
25 that strong synergistic interactions between stratospheric ozone depletion and greenhouse warming are
26       Due to its significant contribution to stratospheric ozone depletion and its potent greenhouse
27 to be reduced by more realistic treatment of stratospheric ozone depletion and volcanic aerosol forci
28 ities of mid-UV radiation (UVB), a result of stratospheric ozone depletion during the austral spring,
29 t the entire atmosphere, resulting in severe stratospheric ozone depletion for several years.
30       The main halogen gases responsible for stratospheric ozone depletion have been regulated under
31 s syndrome to increases in UV radiation from stratospheric ozone depletion needs to be completed.
32 and reduces their potential to contribute to stratospheric ozone depletion or global warming; HFCs do
33 pics-similar to those associated with modern stratospheric ozone depletion over Antarctica-plausibly
34 and summer can be explained as a response to stratospheric ozone depletion over Antarctica.
35 ric N(2)O concentrations have contributed to stratospheric ozone depletion(1) and climate change(2),
36 000 in six major categories (climate change, stratospheric ozone depletion, agricultural intensificat
37 trate the roles of methane, nitrogen oxides, stratospheric ozone depletion, and global warming drivin
38 models forced by greenhouse gases, aerosols, stratospheric ozone depletion, and volcanic eruptions an
39 + Liters) Neptune also has a lower impact in stratospheric ozone depletion, fine particulate matter f
40 ed as contributing to the warming, including stratospheric ozone depletion, local sea-ice loss, an in
41 ride (CH3Cl), compounds that are involved in stratospheric ozone depletion, originate from both natur
42 e to the potential contributions of CH3Br to stratospheric ozone depletion, technologies for the capt
43 tial impacts of the unaccounted emissions on stratospheric ozone depletion, with implications for the
44 powerful greenhouse gas and a major cause of stratospheric ozone depletion, yet its sources and sinks
45 radiation indicate that the eruptions led to stratospheric ozone depletion.
46 ributors to the anthropogenic enhancement of stratospheric ozone depletion.
47 nt to previously unrecognized mechanisms for stratospheric ozone depletion.
48 d chlorine, respectively, which can catalyze stratospheric ozone depletion.
49 loride (CH(3)Cl) significantly contribute to stratospheric ozone depletion.
50                                          The stratospheric ozone destruction caused by 0.77 pptv of i
51 romethane (CH3Cl) plays an important role in stratospheric ozone destruction, but many uncertainties
52 N(2)O), a greenhouse gas that contributes to stratospheric ozone destruction.
53 e gas that contributes to climate change and stratospheric ozone destruction.
54        To assess the effect of this trend on stratospheric ozone, estimates of the future stratospher
55                                        Polar stratospheric ozone has decreased since the 1970s due to
56  measures of compounds' abilities to deplete stratospheric ozone, have been a key regulatory componen
57 eloped a method for diagnosing the amount of stratospheric ozone in these UT parcels using the compac
58         The catalytic depletion of Antarctic stratospheric ozone is linked to anthropogenic emissions
59 osphere, causing reductions in extratropical stratospheric ozone lasting for about a year.
60 on precipitation and severe depletion of the stratospheric ozone layer in the Northern Hemisphere.
61                             Accordingly, the stratospheric ozone layer is expected to recover.
62 through the Montreal Protocol means that the stratospheric ozone layer is recovering(1) and that cons
63                          The recovery of the stratospheric ozone layer relies on the continued declin
64 f sustained, would delay the recovery of the stratospheric ozone layer(1-12).
65                  The threat N2O poses to the stratospheric ozone layer, coupled with the uncertain fu
66 source of odd-hydrogen radicals, destroy the stratospheric ozone layer, such that Earth's surface rec
67        The recognition that CFCs destroy the stratospheric ozone layer, with consequent enormous cons
68 echanisms initiated by wildfires thinned the stratospheric ozone layer.
69 e and bromine, thus potentially damaging the stratospheric ozone layer.
70 unted for when studying the evolution of the stratospheric ozone layer.
71  known remaining anthropogenic threat to the stratospheric ozone layer.
72  2005 in the USA, because it can deplete the stratospheric ozone layer.
73 e by the Montreal Protocol in protecting the stratospheric ozone layer.
74  known to affect ENSO strength by modulating stratospheric ozone levels (OEI = 6 and (17)O = 3.3 per
75 ), and third and fourth quartile mean annual stratospheric ozone levels but increased with second, th
76                                              Stratospheric ozone levels have slightly recovered.
77 x, clear sky and issued ultraviolet indices, stratospheric ozone levels, and outdoor air temperature
78 , contributing, on average, 10% of the lower stratospheric ozone loss during spring (up to 4.2% of th
79 n dominate (~73%) the halogen-mediated lower stratospheric ozone loss during summer and early fall, w
80 he relative contribution of iodine to future stratospheric ozone loss is likely to increase as anthro
81 , controlled substances due to their role in stratospheric ozone loss, also occur as dissolved contam
82 le the 1991 eruption of Pinatubo resulted in stratospheric ozone loss, it was due to heterogeneous ch
83 on and destruction, photooxidant cycling and stratospheric ozone loss.
84 ng from the regulated ODSs, with the avoided stratospheric ozone losses playing no role.
85 f spatiotemporal variations in Earth's lower-stratospheric ozone (LSO) and temperature, which provide
86 ons of increased N(2)O abundance, leading to stratospheric ozone (O(3)) depletion, altered solar ultr
87 s the photochemical coupling between N2O and stratospheric ozone (O3), which can easily be decomposed
88 ntemporary cities to calculate the impact on stratospheric ozone of a regional nuclear war between de
89  upon the same reaction network that reduces stratospheric ozone over the Arctic.
90 ly-driven dynamical response to the observed stratospheric ozone perturbation and find a significant
91                                              Stratospheric ozone plays a crucial role in life and eco
92 t may have coincided with a dramatic drop in stratospheric ozone, possibly due to a global temperatur
93 , augments the greenhouse effect, diminishes stratospheric ozone, promotes smog, contaminates drinkin
94  uncertain due to the confounding effects of stratospheric ozone recovery and climate change on ocean
95  of the Montreal Protocol and the associated stratospheric ozone recovery might therefore manifest, o
96 redicting radiative forcing due to Antarctic stratospheric ozone recovery requires detecting changes
97             Furthermore, we demonstrate that stratospheric ozone recovery, resulting from the Montrea
98             This usage carries potential for stratospheric ozone reduction due to Br atom catalysis,
99 ll force SAM into its positive phase even if stratospheric ozone returns to normal levels, so that cl
100 ugh a photochemical reaction network linking stratospheric ozone to carbon dioxide and to oxygen.
101 tarctic Plateau to be as an archive for past stratospheric ozone trends.
102 at simulated changes in solar irradiance and stratospheric ozone was used to investigate the response
103 ve a key role in regulating tropospheric and stratospheric ozone, while some hHNPs bioaccumulate and
104 h this, models project a gradual increase in stratospheric ozone with the Antarctic ozone hole expect

 
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