International Journal of Current Research and Review
Research Article
DOI: 10.31782/IJCRR.2018.10108
IJCRR
Section: Life
sciences
Sci. Journal
Impact Factor
4.016
ICV: 71.54
Unusual Changes in Stratospheric Ozone
and Water Vapor Over Antarctica and its
Relation to Mesosphere Dynamics during
a Minor Sudden Stratosphere Warming
G. Venkata Chalapathi1, S. Eswaraiah2*, P. Vishnu Prasanth3,
Jaewook Lee2, K. Niranjan Kumar4, Yong Ha Kim2
Department of Physics, Govt. Degree college, Anantapur-515001, India; 2Department of Astronomy and Space Science, Chungnam National
University, Daejeon- 305-764, Korea; 3Department of Physics, Sree Vidyanikethan Engineering College, Tirupati- 517102, India; 4Atmosphere and
Ocean Research Institute (AORI), The University of Tokyo, Chiba, 277-8568, Japan.
1
ABSTRACT
Objective: Usually, the stratospheric ozone will show its significance in the variability of mesospheric tides in normal days over
the low-latitude region. But during sudden stratosphere warmings, the water vapor and ozone over the polar region will change
and shows some different effects on mesosphere tides. In the present study, we have provided the unusual changes in both
water vapor and ozone over Antarctica and their role in altering the mesospheric tides.
Method: Using MLS data in the stratosphere and Rothera (68oS, 68oW) MF radar observations in the mesosphere, the variability of Antarctica ozone and H2O during sudden stratospheric warming (SSW) winter 2010, and their influence on mesosphere
dynamics has presented. The unusual increment of ozone reduction is noticed and consequent enhancement in H2O and HNO3
is also observed during the warming period. Mesospheric tidal components (diurnal, semi-diurnal and terr-diurnal) have been
estimated using the hourly wind data from the MF radar.
Result: The unusual changes in H2O and Ozone were observed during the warming period the similar behavior was observed
in semi-diurnal tidal components during 2010 winter and their relation to ozone enhancement is discussed.
Conclusion: The observations indicate that the enhancement of H2O and HNO3 leads to produce the ozone during warming
period and hence the increment in ozone reduction is achieved over the polar region. Further, the enhancement of BrewerDobson mean circulation was clearly noticed through ozone transport during the warming period. The tidal enhancement after
the SSW could be due to the non-linear interaction between planetary waves and tides.
Key Words: Sudden Stratospheric Warming, Ozone and H2O variability, Mesospheric Tides, MF Radar
INTRODUCTION
It is well known that in the winter polar stratosphere, stratospheric sudden warming (SSW) occurs as a result of the
interactions between vertically propagating planetary waves
and the zonal winds (15). Ozone destruction occurs over
both the polar regions in local winter-spring. In the Antarctic, essentially complete removal of lower-stratospheric
ozone currently results in an ozone hole every year (14). In
the winter polar lower stratosphere, low temperatures induce
condensation of water vapor (H O) and nitric acid (HNO )
into polar stratospheric clouds (PSCs). Further, it is understood that PSCs along with cold aerosols provide surfaces
for heterogeneous conversion of chlorine from longer-lived
reservoir species, such as chlorine nitrate (ClONO ) and
hydrogen chloride (HCl), into reactive (ozone-destroying)
forms, with chlorine monoxide (ClO) predominant in daylight (20). In the Antarctic, enhanced ClO is usually present
for 4-5 months (through to the end of September) (19), leading to the destruction of most of the ozone in the polar vortex
between 14 and 20 km altitude.
Corresponding Author:
Dr. Sunkara Eswaraiah, Department of Astronomy and Space Science, Chungnam National University, Daejeon, Korea; Ph:+82-10-30690508;
E-mail: eswar.mst@gmail.com
ISSN: 2231-2196 (Print)
ISSN: 0975-5241 (Online)
Received: 20.02.2018
Revised: 22.03.2018
Int J Cur Res Rev | Vol 10 • Issue 10 • May 2018
Accepted: 25.04.2018
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Chalapathi et.al.: Variability of H2O and Ozone during minor SSW
Understanding the variabilities of H O and ozone in particular during the SSW events is important to understand
the variabilities of mesospheric tides, as the forcing of the
semi-diurnal tide, in particular, is mainly due to the absorption of ultraviolet radiation by ozone in the stratosphere and
mesosphere. Few studies have been established on the tidal
variabilities at high-latitudes in relation to the major SSW
events over NH hemisphere (2,12). Such studies over SH
hemisphere are sparse.
It is well established that ozone reduction takes place in the
polar region especially in Antarctica region and hence ozone
hole during winter. The chemistry of ozone formulation and
its reduction during normal year winters and during 2010
minor SSW period is well explained by de Latt et al. (5).
In their study, they identified that ozone reduction has been
enhanced during the 2010 winter period. In the present study,
we are going to explain how this ozone enhancement during
2010 winter will affect the tides in the MLT (Mesosphere
lower thermosphere) region. Such study was not done so
far, for the first time we are providing in detail study on the
variability of MLT tides during the minor event occurred in
2010.
Data
In the present study, we make use of stratospheric zonal
winds and temperatures obtained from ERA-Interim reanalysis datasets provided by the European Center for Mediumrange Weather Forecasts (ECMWF) (1) for the evaluation of
2010 minor SSW event. The water vapor and ozone profiles
are retrieved from Microwave Limb Sounder (MLS) and
mesosphere tides from Rother MF (Medium Frequency) radar.
Methodology
The ERA-Interim reanalysis provides the data between the
pressure levels 1000 and 1 hPa (~0-48 km) with a latitudinal
and longitudinal grid of 1.5 × 1.5 . We have utilized zonal
mean temperature and zonal winds at 10 hPa.
Earth Observing System (EOS) Microwave Limb Sounder,
hereafter called MLS, is one of the four instruments aboard
NASA’s Aura satellite, and it has a radiometer that retrieves
temperature from the bands near the O spectral line at 118
and 239 GHz. It measures the temperature from 316 to 0.001
hPa pressure levels with a track resolution of 230 km, which
includes the global coverage from 82 S to 82 N with ~ 15 orbits per day, providing ~30 samples daily for given latitude.
Details of the MLS and temperature validation are given in
Schwartz et al. (17). In the present study, we have used the
H O, HNO , temperature, and ozone (O ) profiles derived at
80 S.
To study the mesosphere dynamics during the 2010 minor
SSW period, we used a Rothera MF Radar (68 S, 68 W) wind
Int J Cur Res Rev | Vol 10 • Issue 10 • May 2018
measurements, which is a coherent, spaced-antenna system
and has been operated since 1997. The radar has a transmitting power of 25 kW at a frequency of 1.98 MHz and provides winds in the mesosphere at 4 km altitude resolution
every hour (11). The hourly wind profiles during 2010 have
been used in the present analysis.
RESULTS AND DISCUSSION
Evolution of 2010 SSW in SH
Fig. 1 depicts daily zonal mean temperature at 80 S (Fig.1a)
and zonal wind at 60 S (Fig.1b) obtained from ERA-Interim
reanalysis dataset for the year 2010 observed at 10 hPa. The
daily mean amplitude of PW of zonal wavenumber ( ) 1 and
2 at 10 hPa over 60 S is displayed in Fig.1c. The PW amplitudes of 1 and 2 were computed from the distribution of
geopotential heights along the constant latitude.
It is clear from the figure that during 2010 three episodic minor warming events occurred in early August (day 212), midSeptember (day 259) and in the end of October (day 300),
marked with dotted vertical lines. Though three episodic
warmings occurred in 2010, September (day 259) event was
the record one and influenced the mesosphere largely (6,7).
During 2010 the temperature indicates that the warming
lasted for more than eight days with temperature increases
of ~10-15K from the normal days and the second event (day
259) was the most noticeable. The zonal wind was weakened
by ~20-25 m/s in each episodic warming.
During 2010 minor SSW, the amplitude of PW ( 2) over 60
S was comparable to that of PW ( 1) during the first episodic
warming (Fig.1c) and later PW ( 1) is stronger than PW (
2). Further, the PW ( 1) amplitude during 2010 winter was
weaker than the 2002 major SSW, and hence the PW interaction with the mean flow may lead to only deceleration, not a
reversal, of zonal wind over 60 S at 10 hPa (Fig. 1b).
Reduction in ozone destruction: 2010 SSW
Figure 2 presents the daily mean variability of HNO , H O
and O for the 2010 minor SSW year and also other years at
different heights (~22, 32 and 68 hPa) derived from MLS
measurements at 80 S. H O is given in parts per billion (ppbv)
and ozone is given in parts per million (ppmv). Further, the
five-day running mean was functional in order to reduce
noise if any of the data and to obtain better clarity in comparison with different years. In the figure top panel shows the
HNO3, H2O variability at mid stratosphere ~22 hPa (25 km)
and corresponding ozone (Figs.2(a)-2(c)), lower two panels show the similar behavior at lower stratosphere ~32 hPa
(23.5 km) and ~68 hPa (19 km)). From the figure, it is clear
that the reduced photochemical ozone destruction is evident
in 2010 at 25 km, during mid-August and in early Septem-
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Chalapathi et.al.: Variability of H2O and Ozone during minor SSW
ber when the HNO and H O are moderately increased and it
could be due to an increase of stratopause temperatures during SSW. However, at lower stratosphere heights the process
is continuing and following as usual winter trend and not affected by SSW and hence photochemical ozone destruction
is unaffected.
Usually, during winter, a strong polar vortex forms over Antarctica and it inhibits the mixing of warm mid-latitude air and
enhances radiative cooling in absence of solar radiation. The
average minimum winter temperatures over Antarctica will
be~193K. If the temperature drops below~195 K, polar stratospheric clouds (PSCs) are formed in the Antarctica ozone
layer. The most common type of PSCs forms from nitric acid
(HNO ) and water (H O). The PSC formation will occur on an
average of 1-2 months in Arctic and 5-6 months in Antarctic
regions. Once formed, PSC particles will undergo vertical
transport to lower altitudes due to gravity, they trigger the
chemical reactions (denitrification and dehydration) in the
stratosphere and cause the highly reactive chlorine gas (ClO)
to be formed, which catalytically destroys ozone. As long
as temperatures remain sufficiently low, PSC formation will
continue and hence the ozone destruction. However, once
the sunlight increase due to season transition vortex warms,
the PSC will disappear slowly and halogen spices are deactivated and hence the ozone reproduction starts. Both H O
and HNO in the stratosphere will affect directly or indirectly
on ClO production in PSC reaction and reduce the amount
of ClO production and hence reduce the ozone destruction.
The clear mechanism for the reduction of photochemical
ozone destruction at 22 hPa is shown in Fig. 3. The figure
depicts five-day running mean MLS measurements of HNO
, O , H O and temperature as a function of time for the 2010
minor SSW year and other non-SSW years 2012,2013 at 22
hPa (~25 km), where the ozone reproduction is greater due
to SSW effect compared to other lower altitudes. Once temperatures drop below the PSC formation temperature around
the day 150 (~1 June), denitrification starts as evidenced by
the decrease in HNO3. However, full denitrification will be
reached within about 20 days. At the same time, the chlorine reservoir HCl is empty (18) due to chemical reactions
of HCl on PSC’s. Usually, dehydration starts about 20 days
later than denitrification as the pure ice formation temperatures are delayed by 20 days after PSC formation temperature. Due to decrease of solar isolation in August (~day225)
ozone is being destroyed slowly by halogens as ClO start
to increase around day 225. When ClO is abundant around
day’s 250-270 (mid-September), ozone destruction is maximum. During late winter /transition period starts (~day 270),
temperatures increases to above the PSC formation threshold level, PSCs starts to evaporate and the active halogens
are rapidly deactivated back into reservoir species like HCl.
The slow increase in HNO and H O starting around DOY
270 also shows that mixing is taking place. However, after
55
day300 (~late October – early November) ozone slowly increases again, mainly by mixing of
mid-latitude air. This behavior is very similar for all years
but different in SSW years (2010). In contrast, during 2010
SSW, the warming occurred during late August (day 212)
and mid-September (259) and lasted for about a week and
significantly affected the mesosphere and thermosphere (6).
However, in 2010 the chemical species and ozone are greatly
affected by the warmings that occurred in the occurred in
the stratosphere. For instance, during 2010 winter the first
warming was noticed on the day 212 and the temperature
was increased, even crossed the PSC threshold level and
hence HNO and H O suddenly raised and ClO decreases
which result in an increase of HCl on the day212. The net
photochemical chemical reactions result in increasing ozone
around the day 250, instead of reduction; showing that catalytic ozone depletion at 22 hPa in 2010 is not unusual. In
the following subsections, we will discuss, how these ozone
increase around the days 250-270 affects the MLT dynamics.
Sudden Stratospheric Warming-Ozone effects
on the mesospheric tides
Fig.4 depicts the daily variability of zonal diurnal, semi-diurnal and terr-diurnal tides measured by Rothera MF radar
during SH winter at 80 km. Fig. 4(a) shows the variability
of tides in 2010 SSW year. Fig. 4(b) shows the variability
of stratospheric ozone during 2010 SSW year and non-SSW
years 2012, 2013, respectively. It is clear from the figure
that the semi-diurnal tidal amplitude is increasing (~ 40 m/s)
during last 15 days of the October (day 285-300). Usually,
the tidal amplitudes are falling below 20 m/s in SH winter.
The role of stratospheric ozone in coupling the low-latitude
stratosphere and MLT region has been studied by Goncharenko, et al. (10). They suggested that the increase in the
ozone density at 2 hPa (~ 43.5 km) lasts ~35 days following
the SSW long after the downfall of PWs, causing enhancement in SDT amplitude. However, at the polar latitudes, the
mechanism is different. The meridional circulation forced
by PWs in the polar region during SSW leads to transport
of ozone from pole to equator (9,16), and thus increases the
peak ozone heating rate at ~ 43 km at low-latitudes, resulting
in the amplification of SDT in the MLT region (10,13).
As shown in Fig.4b, the ozone density at 22 hPa (the ozone
is usually generated at this altitude) is gradually increasing in
the winter from the day 200 onwards and attains maximum
value during warming day (259) and after that it extremely
deviates from the normal seasonal trend, except a small hike
around the day 300. The variation in ozone trend in 2010
winter could be due to the strong B-D circulation forced by
enriched PWs at polar region. The circulation transported the
ozone from SH to NH high latitudes as a consequence of
pole-pole circulation (Figure 1 of Butchart, 2014) or it could
be transported to low latitudes. Alternatively, the ozone could
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Chalapathi et.al.: Variability of H2O and Ozone during minor SSW
be downward transported to lower altitudes in SH itself. The
small upturn in the O density around the day 300 could be
due to the minor warming that occurred on the day 300 (6).
Since MLS satellite is located in a Sun-synchronous orbit,
the zonal mean values of O might have been aliased with
the migrating tides. Figure 5 indicates that even when ozone
density is lower than the usual value, the SDTs are enhanced
during the days 270-310. This may suggest that ozone alone
may not play a dominant role in the amplification of tides
over the Antarctic MLT region.
Further, we also verified the O anomaly during 2010 SSW
winter and 2012 non-SSW winter periods and presented in
Figure 5. It is clear from the figure (Fig.5a) that the ozone
density is high at tropical region at starting of winter at 43
km (2 hPa), where the tides will generate and as soon as
reaching peak warming day, the ozone is transported towards
NH high-latitude region and more ozone is ascertained at
60 N, it could be due to B-D circulation at the stratosphere
(Butchart, 2014, Figure 1). The B-D circulation at the stratosphere (~43 km) shown with a curved arrow in Fig.5(a) and
the ozone density is comparatively low at ~ 60 S. In a normal
year (Non-SSW) (Fig.5(b)) the circulation was not observed,
and the usual trend was apparent at 43 km. It states that the
strong mean circulation forced by enriched PWs at polar region, transported the ozone from SH to NH high latitudes
as a consequence of pole-pole circulation (Butchart,2014) or
it could be downward transported to lower altitudes at SH
itself.
So, we may conclude that the enhancement of SDT amplitudes at high-latitudes are due to different effect than those
observed at low latitudes (4,8,21). It tells that, the effect of
ozone and water vapor is less significant on the Antarctic
mesospheric tides. Thus, the above discussion suggests that
the enhancement in SDT amplitudes could be due to the
PWs-tidal interaction.
CONCLUSIONS
In the present communication, we described the variability of
Antarctica ozone and H O during the winter period of 2010
SSW year, and their influence on mesospheric tides. The tidal components (diurnal, semi-diurnal and terr-diurnal) in the
MLT region have been estimated using the hourly wind data
from both Rothera (68 S, 68 W) MF radar. The main findings
are summarized as follows;
1. In 2010, we noticed record minor stratosphere warming (SSW) in mid-September (day 259) using ERAinterim data analysis.
2. It is noticed that the stratosphere chemistry below
50hPa is not affected by SSW. The chemical species
ClO, H O, HNO plays a key role in destruction (ClO)
Int J Cur Res Rev | Vol 10 • Issue 10 • May 2018
and reconstruction (H O, HNO ) of ozone in the middle
and upper stratosphere.
3. Though the SSW occurs during the days 250-270, the
Ozone will not rise due to ozone destruction element
ClO element is abundant even when H O, HNO slowly
increasing (Fig.3). During the days 270-300 the ClO is
falling rapidly and H O and HNO increase shows the
vertical mixing and produces more ozone.
4. The unusual behavior was observed in semi-diurnal
tidal components during SSW year 2010. The Semidiurnal tidal enhancement is noticed during the days
270-310, irrespective of the day of peak warming occurred in 2010.
5. The reason why tidal amplitudes are enhancing during
the days 270-300, may be explained like this: Since
the ozone destruction between 20-25 km is reduced to
60% during SSW years compared to other years and
the recovery of ozone is fast between the days 270-300
due to downward transport of chemical species, rather
than horizontal mixing, and transport of humid rich air
(H O) and hence change in vertical propagating tides.
However, the effect could be low since the ozone density is less during the days 270-300.
The above discussion suggests that though the ozone destruction is reduced during SSW period, ozone alone cannot
affect the tidal enhancement, it may be due to planetary wave
(PW)-tidal interaction. To quantify this, issue the non-linear
interaction between tides-and PWs should be discussed.
ACKNOWLEDGEMENTS
We deeply appreciate the ERA-Interim and MLS team for
providing the data used in the present study. SE acknowledges for financial support by the Korea Polar Research Institute
(PE17020), Korea and Chungnam National University, Daejeon, Korea. Our sincere thanks to Prof. Dennis Riggin for
providing the Rothera MF radar data.
Authors acknowledge the immense help received from the
scholars whose articles are cited and included in references
of this manuscript. The authors are also grateful to authors /
editors / publishers of all those articles, journals and books
from where the literature for this article has been reviewed
and discussed.
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Figure 2: Daily mean variability of HNO , H O and Ozone (O)
in the stratosphere using MLS measurements during normal
years (2012, 2013) and comparison with minor warming event
year (2010) at 22 hPa (a-b), at 32 hPa (d-f), and at 68 hPa (gh). All profiles are at ~ 80 S.
Int J Cur Res Rev | Vol 10 • Issue 10 • May 2018
Chalapathi et.al.: Variability of H2O and Ozone during minor SSW
Figure 3: The five-day running mean MLS measurements
of H O, HNO , O and temperature at ~ 22hPa for the years
2010,2012 and 2013 during DOY 100-350. All profiles are at
~ 80 S.
Figure 5: Zonal mean ozone mass mixing ratio anomaly
(ppmv) profiles calculated from the south pole to north pole
at 2 hPa (~43 km) altitude for the SSW year 2010 (Top Panel)
and the non-SSW year 2012 (bottom panel). The vertical line
indicates the day of peak warming. The horizontal line indicates 60 latitude. Curved arrow in top panel shows the transport of ozone due to mean circulation.
Figure 4: (a)Variability of diurnal, semi-diurnal and terr-diurnal
zonal components measured by Rothera MF radar (68 S,68
W) during 2010 SH winter at 80 km, (b) daily mean variability
of Ozone (O ) in stratosphere using MLS measurements during Non-SSW years (2012,2013) and comparison with minor
warming event years (2010) at 22 hPa. All profiles are at ~ 80
S. Vertical lines indicate the day of peak warming.
Int J Cur Res Rev | Vol 10 • Issue 10 • May 2018
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