ACPAtmospheric Chemistry and PhysicsACPAtmos. Chem. Phys.1680-7324Copernicus PublicationsGöttingen, Germany10.5194/acp-17-3445-2017An Atlantic streamer in stratospheric ozone observations and SD-WACCM simulation dataHockeKlemensklemens.hocke@iap.unibe.chhttps://orcid.org/0000-0003-2178-9920SchranzFranziskaMaillard BarrasElianeMoreiraLorenahttps://orcid.org/0000-0002-4791-8500KämpferNiklausInstitute of Applied Physics, University of Bern, Bern, SwitzerlandOeschger Centre for Climate Change Research, University of Bern, Bern, SwitzerlandFederal Office of Meteorology and Climatology, MeteoSwiss, Payerne, SwitzerlandKlemens Hocke (klemens.hocke@iap.unibe.ch)10March2017175344534529November201630November201615February201728February2017This work is licensed under a Creative Commons Attribution 3.0 Unported License. To view a copy of this license, visit http://creativecommons.org/licenses/by/3.0/This article is available from https://acp.copernicus.org/articles/17/3445/2017/acp-17-3445-2017.htmlThe full text article is available as a PDF file from https://acp.copernicus.org/articles/17/3445/2017/acp-17-3445-2017.pdf
Observation and simulation of individual ozone streamers are important for
the description and understanding of non-linear transport processes in the
middle atmosphere. A sudden increase in mid-stratospheric ozone occurred
above central Europe on 4 December 2015. The GROund-based Millimeter-wave
Ozone Spectrometer (GROMOS) and the Stratospheric Ozone MOnitoring RAdiometer
(SOMORA) in Switzerland measured an ozone enhancement of about 30 % at 34 km
altitude (8.3 hPa) from 1 to 4 December. A similar ozone increase is
simulated by the Specified Dynamics Whole Atmosphere Community Climate
(SD-WACCM) model. Further, the global ozone fields at 34 km altitude (8.3 hPa) from SD-WACCM and the satellite experiment Aura/MLS show a remarkable
agreement for the location and timing of an ozone streamer (large-scale
tongue-like structure) extending from the subtropics in northern America over
the Atlantic to central Europe. This agreement indicates that SD-WACCM can
inform us about the wind inside the Atlantic ozone streamer. SD-WACCM shows
an eastward wind of about 100 m s-1 inside the Atlantic streamer in the
mid-stratosphere. SD-WACCM shows that the Atlantic streamer flows along the
edge of the polar vortex. The Atlantic streamer turns southward at an
erosion region of the polar vortex located above the Caspian Sea. The spatial
distribution of stratospheric water vapour indicates a filament outgoing from
this erosion region. The Atlantic streamer, the polar vortex erosion region
and the water vapour filament belong to the process of planetary wave
breaking in the so-called surf zone of the northern midlatitude winter
stratosphere.
Introduction
Rossby wave breaking contributes to the mean meridional circulation and to
the horizontal mixing of tropical, subtropical and extratropical air masses
in the middle atmosphere . Rossby wave
breaking occurs in the middle and upper stratosphere during the winter season.
In particular, the midlatitudes are regarded as the surf zone of the
stratosphere where the material erosion of the polar vortex takes place
. The material erosion of the vortex leads to water
vapour filaments at midlatitudes since the vortex air is rich in water
vapour which has a long lifetime in the stratosphere.
utilized simulation and observation data of stratospheric water vapour as a
tracer for vortex filamentation in the Arctic winter.
Strong planetary waves shift the stratospheric polar vortex equatorwards, and
subtropical air is drawn in tongue-like structures (streamers) from the
subtropics to the extratropics. observed the formation
of the so-called Atlantic streamer in the trace gases N2O and HNO3.
derived climatological features of stratospheric streamers
by means of the FUB-CMAM model with increased horizontal resolution
(2.8∘×2.8∘). They found that tropical–subtropical
streamers mainly occur over the Atlantic and the east Asia/west Pacific
region during Arctic winter. They emphasized that stratospheric streamers
have nothing to do with ozone laminae (small-scale structures in vertical
space) in the lower stratosphere. reproduced the streamer
distribution observed by the CRISTA experiment on board Space Shuttle
with the Chemical Lagrangian Model of the Stratosphere
(CLaMS) and the Karlsruhe Simulation Model of the Middle Atmosphere (KASIMA).
These model-observation intercomparisons indicate that planetary wave
breaking and induced stratospheric streamers are an excellent test for
non-linear wave–mean-flow interactions in middle atmospheric chemistry climate
models.
In the following, we investigate whether the Specified Dynamics Whole
Atmosphere Community Climate Model (SD-WACCM) can simulate an individual
Atlantic streamer event which was observed by the GROund-based Millimeter-wave
Ozone Spectrometer (GROMOS) at Bern and the satellite experiment Aura
Microwave Limb Sounder (Aura/MLS). Further, we look in detail on the role of
the Atlantic streamer in the process of planetary wave breaking and polar
vortex erosion.
Data setsThe microwave radiometers GROMOS and SOMORA
The study is partly based on stratospheric ozone profiles observed by GROMOS and the Stratospheric
Ozone MOnitoring RAdiometer (SOMORA). The instruments are ground-based ozone
microwave radiometers which are part of the Network for the Detection of
Atmospheric Composition Change (NDACC). They continuously observe the middle
atmosphere above Bern, Switzerland (46.95∘ N, 7.44∘ E, 577 m
above sea level) and Payerne, Switzerland (46.82∘ N,
6.95∘ E, 471 m a.s.l.). While the routine observations of
GROMOS started in 1994, SOMORA has been taking measurements since the year 2000. Both radiometers
measure the thermal microwave emission of a rotational transition of ozone at
142.175 GHz. In our study, we use ozone profiles with an integration time of
2 h for GROMOS and 1 h for SOMORA. The hourly ozone profiles of SOMORA
are averaged with a 3 h running mean in order to get close to the 2-hourly
data of GROMOS and SD-WACCM. The valid altitude range of the ozone profiles
is from 25 to 70 km with a vertical resolution of about 12 km in the
stratosphere. The measurement response between 50 and 0.5 hPa (20 to 52 km)
is higher than 0.8 (corresponding to a priori contributions less than
20%). Therefore, the retrieved ozone values at these altitudes are
primarily based on the measured line spectrum. For technical details,
measurement principle and retrieval procedure of the instruments; see, for
example, , , ,
and references included therein. An
intercomparison study of indicated that the relative
differences between SOMORA and Aura/MLS are less than 10%. Similar values
of uncertainty are obtained for GROMOS. The SOMORA instrument is quite
similar to GROMOS and was also upgraded with a FFT spectrometer in 2009. The
vertical ozone profiles from GROMOS and SOMORA have been validated by means
of nearby ozone sondes, ground stations and collocated satellite
measurements, the data sets have been used for studies of ozone–climate
interaction, middle atmospheric dynamics as well as for long-term monitoring
of the stratospheric ozone layer and for detection of trends
.
The Aura Microwave Limb Sounder
The Microwave Limb Sounder is an instrument on board the NASA Aura satellite
which was launched in July 2004. The level2 data of Aura/MLS consist of
atmospheric vertical profiles with a spacing of 165 km (1.5∘ along
the satellite orbit, which is sun-synchronous with an inclination of
98∘ and a period of 98.8 min) . This
relatively dense, horizontal sampling should be sufficient for observing
ozone streamers. The vertical resolution of the ozone profiles of Aura/MLS
ranges from 3 km in the stratosphere to 6 km in the mesosphere
. The present study utilizes Aura/MLS data of the version
4.2. The global ozone maps of Aura/MLS were computed by interpolating the
valid ozone profiles of 1 day to a horizontal grid (2∘×2∘) using a Delaunay triangulation (Matlab function
TriScatteredInterp.m). The validity of the ozone or water vapour values from
Aura/MLS is limited by uncertainty thresholds which are described in the data
quality document for each species .
The SD-WACCM model
The Specified Dynamics Whole Atmosphere Community Climate Model (SD-WACCM)
was described and evaluated in detail by . Here, we use
the Community Earth System Model (CESM) version 1.2.2 WACCM component set
which is a coupled chemistry climate model of the National Center for
Atmospheric Research (NCAR). The WACCM chemistry module is taken from the
Model for OZone And Related chemical Tracers (MOZART)
but is extended to include 122 species . SD-WACCM is a
modified version of WACCM in which the meteorology is constrained to match
observations to within a user-defined tolerance
. SD-WACCM is nudged with winds,
temperature, surface pressure, surface wind stress and heat fluxes from the
Goddard Earth Observing System 5 (GEOS5) analysis . The
nudging coefficient is in our study 0.1; i.e. the winds, temperature and
surface pressure are defined by a linear combination of 10 % from GEOS5 and
90 % from the model. Nudging is applied every 30 min. The model run was
initialized on 1 July 2015 by means of a former WACCM run and GEOS5 data.
The model output files are written every 2 h, the horizontal resolution
is 1.9∘×2.5∘ (latitude × longitude), and the
vertical resolution is about 1 km in the stratosphere. The altitude range of
SD-WACCM is from the surface to 140 km whereby nudging is only applied below
50 km. In the present study, we work with SD-WACCM output data which have a
time resolution of 2 h. SD-WACCM can resolve planetary waves while
short-term gravity waves are parameterized .
Time series of ozone volume mixing ratio and zonal wind
at 34 km altitude above Bern, Switzerland from October to December 2015. The
vertical red line is at 4 December 2015 12:00 UT when
the ozone streamer reached Bern. (a) Time series of ozone observed
by GROMOS (Bern) and SOMORA (Payerne) versus the simulated SD-WACCM ozone
series at the grid point nearest to Bern. (b) Time series of eastward wind
simulated by SD-WACCM at 34 km altitude.
Results
The initial point of the present study was the occurrence of an ozone peak in
mid-stratospheric ozone at Bern on 4 December 2015. Figure a
shows the time series of ozone at 34 km altitude (8.3 hPa) above Bern as
observed by the GROMOS microwave radiometer at Bern and the SOMORA microwave
radiometer at Payerne. Ozone suddenly increases by about 30 % from 1
to 4 December. The time series of ozone from SD-WACCM is included in Fig. a. Generally the ozone time series of SD-WACCM is smoother than
those of GROMOS and SOMORA. SD-WACCM reproduces the increase in ozone around
4 December 2015. The maximum in zonal wind of SD-WACCM (Fig. b)
is at the time of the ozone peak observed by GROMOS (Fig. a). In
summary, ozone-rich air passed above Bern with a velocity of about 90 m s-1 at 34 km
altitude.
The next step is to derive the vertical ozone profiles of GROMOS, SD-WACCM,
and Aura/MLS above or close to Bern which are shown on the left-hand-side of
Fig. for 1 December 2015 (dashed lines) and 4 December 2015
(solid lines). Ozone reaches a maximum of 9 ppm at 37 km altitude with
GROMOS and a maximum of about 8 ppm at the same altitude with SD-WACCM
and Aura/MLS. The ozone increase takes place in the mid-stratosphere between
30 and 45 km. This layer thickness of 15 km is given by the full width at
half maximum of the ozone peaks of the difference profiles of SD-WACCM,
Aura/MLS and GROMOS at the right-hand-side of Fig. . The double-peak structure in the difference profile of SD-WACCM is confirmed by the
Aura/MLS observation. The vertical resolution of GROMOS (12 km) is not
sufficient for resolving such a double peak. The profiles of Aura/MLS and
SD-WACCM are not folded with the averaging kernels of GROMOS since we do not
like to degrade the vertical resolution of the ozone profiles of Aura/MLS and
SD-WACCM.
Left-hand side: vertical ozone profiles at Bern (or
close to Bern) before the streamer arrival on 1 December 2015 12:00 UT (dashed
line) and at the streamer arrival on 4 December 2015 12:00 UT. The GROMOS
observations are indicated by the blue lines, the SD-WACCM results are given
by the red lines, and Aura/MLS is shown by the green lines. Right-hand side:
difference between the ozone profiles from 4 and 1 December 2015. The relative
uncertainties of GROMOS, SOMORA and Aura/MLS are about 10 %.
(a) Beginning of an ozone streamer extending from Mexico over
the Atlantic to Morocco on 1 December 2015 at 8.3 hPa (ca. 34 km altitude) and
simulated by SD-WACCM. (b) The ozone streamer narrows and extends to central Europe on 4 December 2015.
(c) The ozone streamer is shifted southward and fades away on 8 December 2015. The graphs (d), (e) and (f) are based on
all valid ozone profiles of Aura/MLS measured during the days 1, 4 and 8 December 2015.
The formation and the decay of the Atlantic streamer is shown in Fig. a, b and c which show the global ozone field at 8.3 hPa (ca.
34 km altitude) as simulated by SD-WACCM for 1, 4 and 8 December 2015. We selected the polar stereographic
projection in order to be in the same position as an observer in space who
would be looking at the Earth. The Atlantic streamer starts with a tongue-like
structure, stretching from Mexico over the Atlantic to Morocco. Later, on 4 December 2015,
a narrow ozone streamer was formed from Mexico to central
Europe. The ozone streamer is moved southward and fades away in Fig. c. The SD-WACCM simulation of the formation and the decay of the
Atlantic streamer is confirmed by the Aura/MLS observations in Fig. d, e and f. Please note that the ozone field of Aura/MLS was not
used for nudging the SD-WACCM model run. The structures of the Atlantic
streamer in the pure Aura/MLS ozone fields are quite similar to those in the
SD-WACCM ozone fields. This is a confirmation of the non-linear wave–mean-flow interactions in the stratosphere as simulated by SD-WACCM. Generally,
the streamer is clearer in the SD-WACCM simulation than in the Aura/MLS
observations. There are at least two reasons which may explain this result.
The SD-WACCM model simulation does not resolve all inertia-gravity waves
which may disturb the formation and duration of streamers and filaments.
Secondly, the limited horizontal and temporal sampling of the Aura/MLS
observations may render a clear detection of streamers and filaments.
Figure a shows the ozone distribution at 8.3 hPa during a Rossby
wave breaking process which can be recognized by the comma-shaped polar
vortex with an outflow of ozone-poor air from the polar region to northern
Africa. Figure b zooms into the Atlantic streamer over Europe on
4 December 2015. The colour shading gives the ozone value and the arrows
depict the horizontal wind vector. The largest arrows correspond to wind
speeds of about 100 m s-1. The figure clearly shows that a narrow stream of
ozone-rich air extends over the Atlantic to France, and it turns southward
over eastern Europe.
Figure a utilizes water vapour as a tracer of polar vortex air and
shows the spatial distribution of stratospheric water vapour at 8.3 hPa on
4 December 2015. Small arrows indicate the horizontal wind. An erosion
region of polar, water vapour-rich air appears above the Caspian Sea, ending
in a long filament of water vapour pointing in a south-westerly direction. This
finding is in a qualitative agreement with the vortex filamentation studies
of and and the Rossby wave breaking study of
. Comparison with Fig. a) shows that the
Atlantic ozone streamer is located at the edge of the polar vortex. In
addition the ozone streamer in Fig. a turns southward before
reaching the vortex erosion region above the Caspian Sea. Figures a and a are appropriate for visualizing the surf zone
of the midlatitude stratosphere in winter . Figures a and a also show the anti-correlation of the spatial
distributions of ozone and water vapour in the mid-stratosphere since
stratospheric polar air is rich in water vapour and poor in ozone.
Finally, we like to compare the water vapour distribution of SD-WACCM (Fig. a) with the observations of the satellite experiment Aura/MLS on
4 December 2015. Figure b shows the result of Aura/MLS at 8.3 hPa
which is close to 34 km altitude. The water vapour distributions of Aura/MLS
and SD-WACCM are in a good agreement. The vortex erosion region over the
Caspian Sea is unclear in the case of Aura/MLS. The water vapour filament over
northern Africa in Fig. b indicates that there was a transport of
water-vapour-rich air from the polar vortex to the subtropics.
(a) Ozone distribution at 8.3 hPa (ca. 34 km altitude)
on 4 December 2015 based on the SD-WACCM simulation. The figure indicates
the effects of a breaking Rossby wave in the polar wintertime stratosphere.
(b) Zoomed-in image of (a): the Atlantic ozone streamer reaches central Europe and turns
southward over eastern Europe. The largest arrows correspond to wind speeds of
about 100 m s-1 within the Atlantic streamer at 8.3 hPa (34 km).
Water vapour distribution at 8.3 hPa (34 km) on 4 December
2015 simulated by SD-WACCM. Water vapour is a tracer of polar vortex air.
It indicates an erosion region of the polar vortex located above Caspian Sea.
A comma-shaped, helical tongue of water vapour-rich air reaches
northern Africa. The water vapour distribution is anti-correlated to the ozone
distribution in Fig. a. (b) Water vapour distribution at 8.3 hPa
(34 km) on 4 December 2015 observed by Aura/MLS. The water vapour filaments
above northern Africa agree with the SD-WACCM simulation result in (a).
Discussion
Rossby waves propagate from the troposphere into the stratosphere during
winter. They propagate along the polar vortex edge where the horizontal
gradient of potential vorticity (PV) is maximal. The Rossby wave amplitude
increases with height, and the Rossby wave can break in the mid-stratosphere.
According to three-dimensional simulations of the Rossby wave breaking
process by the process has a duration of 10–20 days. With
zonal wave-number 1 forcing, wave breaking usually initiates a deep helical
tongue of PV that is extruded from the polar vortex .
Our SD-WACCM simulation of the water vapour distribution in Fig. a confirms the generation of a deep helical tongue of PV since
water vapour is known as a good tracer of PV in the stratosphere. Figure a clearly shows the comma-shaped vortex erosion region which
ends in a narrow water vapour filament over northern Africa. This filament is
also present in the observations by Aura/MLS (Fig. b). However
in the Aura/MLS observations the water vapour filament over northern Africa is
not connected to the polar vortex. It remains open as to whether this is a substantial
difference between the simulation and the observation since the
spatio-temporal sampling of Aura/MLS is limited – particularly the sampling
in longitude which is about 24∘ while the sampling in latitude is
about 1.5∘. Thus, the vortex erosion region is a bit undersampled by
Aura/MLS so that the vortex erosion and the filaments are clearer in the
SD-WACCM simulation than in the Aura/MLS observations. Figure b
does not change much if we reduce the time interval of the collected water
vapour profiles from 24 to 12 h, centred at 12:00 UTC. The limited
temporal sampling of the Aura/MLS maps seems to not be critical.
On the other hand, a realistic representation/parameterization of gravity
waves in climate models is quite challenging. A link between
poleward-breaking Rossby waves in the upper troposphere and the generation of
stratospheric inertia-gravity waves was shown by . Such
links of waves across the scales could be a reason for a substantial
deviation between the model and observation in the vortex erosion region. We
suggest that, in reality, inertia-gravity waves which are not resolved or
imperfectly parameterized in the model simulation may disturb the formation
and duration of streamers, filaments and vortex erosion regions. Because of
the importance of the Rossby wave breaking process for the circulation,
dynamics and composition of the middle atmosphere, we think that further
intercomparisons between the models and remote sensing observations are
needed. In particular, the occurrence of streamers, filaments and vortex
erosion regions should be intercompared in further observational and
simulation studies. Atlantic streamers regularly occur in simulations such as in the
statistical simulation study by . Satellite and
ground-based observations indicate that the polar vortex edge is often
shifted by a zonal wave-number 1 forcing towards the European longitude sector
in wintertime. Thus, our selected case study is possibly representative for a
major part of the Rossby wave breaking processes in the mid-stratosphere.
Conclusions
An Atlantic streamer was detected in stratospheric ozone observations of the
space-based microwave radiometer Aura/MLS and the ground-based microwave
radiometers GROMOS and SOMORA in Switzerland. These observations were
compared to SD-WACCM simulation data. Generally, the simulations of SD-WACCM
are realistic and agree with the observed ozone maps and ozone time series.
The timing of the streamer event on 4 December 2015 and the global structure
of the Atlantic streamer agree well for Aura/MLS, SD-WACCM, GROMOS and
SOMORA. One can see the extension of the tongue-like structure which
transports subtropical ozone-rich air from Mexico to central Europe. The
Atlantic streamer is strongest at altitudes between 30 and 45 km. Eastward
wind speeds of about 100 m s-1 are reached inside the narrow streamer.
The SD-WACCM simulation of the spatial distributions of horizontal wind,
water vapour and ozone in Figs. and show details of
planetary wave breaking in the surf zone at 8.3 hPa at northern midlatitudes
on 4 December 2015. The Atlantic ozone streamer flows eastward at the edge of the polar vortex. The ozone streamer turns southward before
reaching the Caspian Sea where a vortex erosion region is located. The vortex
erosion region shows an increase of water-vapour-rich polar air. A water
vapour filament flows from this region in southwesterly direction. Generally, the
spatial distributions of water vapour and ozone are anti-correlated so that
the ozone streamer contains water-vapour-poor air and the water vapour
filament contains ozone-poor air. The SD-WACCM simulation shows that the
Atlantic streamer is a part of the planetary wave breaking process in the
surf zone of the midlatitude stratosphere in winter. This result is in
agreement with , who reported that transport out of the
tropics occurs in Rossby wave breaking events in which streamers of tropical
air are drawn into middle latitudes in the winter season. The streamers and
filaments at 8.3 hPa (34 km) are clearer in the SD-WACCM simulation than in
the Aura/MLS observations. We suggest that in reality, inertia-gravity waves
which are not resolved in the model simulation may disturb the formation and
duration of streamers and filaments. Another reason is the limited longitude
sampling of the Aura/MLS limb sounding observations since two subsequent
orbits of Aura are spaced by about 24∘ in longitude.
Routines for data analysis and visualization are available
upon request by Klemens Hocke.
The ground-based ozone measurements of SOMORA and GROMOS
are available in the data centre of the Network for the Detection of
Atmospheric Composition Change (http://www.ndacc.org, NDACC, 2017). The Aura/MLS level2
data are available at the Aura Validation Data Center
(http://avdc.gsfc.nasa.gov/, AVDC, 2017). The SD-WACCM simulation data of winter
2015/2016 are available by the author Franziska Schranz.
Franziska Schranz performed the SD-WACCM model simulation. Klemens Hocke carried out the plots. Eliane Maillard Barras took care on
the SOMORA data. All authors contributed to the interpretation of the data sets.
The authors declare that they have no conflict of interest.
Acknowledgements
We thank the Aura/MLS team and NASA/JPL for the microwave limb sounding measurements and the provision of the level2 data set at the Aura Validation
Data Center (http://avdc.gsfc.nasa.gov/). We are grateful to the National Center for Atmospheric Research (Boulder) for providing the SD-WACCM model.
The study was supported by the Swiss National Science Foundation under grant number 200020-160048 and 200021-165516.
Edited by: F. Khosrawi
Reviewed by: two anonymous referees
ReferencesAura Validation Data Center (AVDC): Level-2 data, available at: http://avdc.gsfc.nasa.gov/, last access: 1 February 2017.Brakebusch, M., Randall, C. E., Kinnison, D. E., Tilmes, S., Santee, M. L., and
Manney, G. L.: Evaluation of Whole Atmosphere Community Climate
Model simulations of ozone during Arctic winter 2004/2005, J.
Geophys. Res.-Atmos., 118, 2673–2688, 10.1002/jgrd.50226,
2013.Brasseur, G. P., Hauglustaine, D. A., Walters, S., Rasch, P. J., Müller,
J.-F., Granier, C., and Tie, X. X.: MOZART, a global chemical transport
model for ozone and related chemical tracers: 1. Model description, J.
Geophys. Res.-Atmos., 103, 28265–28289,
10.1029/98JD02397, 1998.
Dumitru, M. C., Hocke, K., Kämpfer, N., and Calisesi, Y.: Comparison and
validation studies related to ground-based microwave observations of ozone in
the stratosphere and mesosphere, J. Atmos. Solar Terr. Phys., 68, 745–756,
2006.Flury, T., Hocke, K., Haefele, A., Kämpfer, N., and Lehmann, R.:
Ozone depletion, water vapor increase, and PSC generation at midlatitudes by
the 2008 major stratospheric warming, J.
Geophys. Res.-Atmos., 114, D18302, 10.1029/2009JD011940, 2009.Hocke, K., Kämpfer, N., Ruffieux, D., Froidevaux, L., Parrish, A., Boyd,
I., von Clarmann, T., Steck, T., Timofeyev, Y. M., Polyakov, A. V., and
Kyrölä, E.: Comparison and synergy of stratospheric ozone measurements by
satellite limb sounders and the ground-based microwave radiometer SOMORA,
Atmos. Chem. Phys., 7, 4117–4131, 10.5194/acp-7-4117-2007, 2007.Keckhut, P., Hauchecorne, A., Blanot, L., Hocke, K., Godin-Beekmann, S.,
Bertaux, J.-L., Barrot, G., Kyrölá, E., van Gijsel, J. A. E., and
Pazmino, A.: Mid-latitude ozone monitoring with the GOMOS-ENVISAT experiment
version 5: the noise issue, Atmos. Chem. Phys., 10, 11839–11849,
10.5194/acp-10-11839-2010, 2010.Khosrawi, F., Grooß, J.-U., Müller, R., Konopka, P., Kouker, W.,
Ruhnke, R., Reddmann, T., and Riese, M.: Intercomparison between Lagrangian
and Eulerian simulations of the development of mid-latitude streamers as
observed by CRISTA, Atmos. Chem. Phys., 5, 85–95, 10.5194/acp-5-85-2005,
2005.Koh, T.-Y. and Legras, B.: Hyperbolic lines and the stratospheric polar vortex,
Chaos, 12, 382–394, 10.1063/1.1480442, 2002.Krüger, K., Langematz, U., Grenfell, J. L., and Labitzke, K.:
Climatological features of stratospheric streamers in the FUB-CMAM with
increased horizontal resolution, Atmos. Chem. Phys., 5, 547–562,
10.5194/acp-5-547-2005, 2005.Kunz, A., Pan, L. L., Konopka, P., Kinnison, D. E., and Tilmes, S.: Chemical
and dynamical discontinuity at the extratropical tropopause based on
START08 and WACCM analyses, J. Geophys. Res.-Atmos.,
116, D24302, 10.1029/2011JD016686, 2011.Lamarque, J.-F., Emmons, L. K., Hess, P. G., Kinnison, D. E., Tilmes, S.,
Vitt, F., Heald, C. L., Holland, E. A., Lauritzen, P. H., Neu, J., Orlando,
J. J., Rasch, P. J., and Tyndall, G. K.: CAM-chem: description and evaluation
of interactive atmospheric chemistry in the Community Earth System Model,
Geosci. Model Dev., 5, 369–411, 10.5194/gmd-5-369-2012, 2012.Leovy, C. B., Sun, C.-R., Hitchman, M. H., Remsberg, E. E., Russell,
III, J. M., Gordley, L. L., Gille, J. C., and Lyjak, L. V.: Transport
of ozone in the middle stratosphere – Evidence for planetary wave breaking,
J. Atmos. Sci., 42, 230–244,
10.1175/1520-0469(1985)042<0230:TOOITM>2.0.CO;2, 1985.
Livesey, N. J., Read, W. G., Wagner, P. A., Froidevaux, L., Lambert, A.,
Manney, G. L., Valle, L. F. M., Pumphrey, H. C., Santee, M. L., Schwartz,
M. J., Wang, S., Fuller, R. A., Jarnot, R. F., Knosp, B. W., and Martinez,
E.: EOS Aura-MLS Version 4.2x Level 2 data quality and description document,
JPL D-33509 Rev. B, 1–164, 2016.
Maillard Barras, E., Ruffieux, D., and Hocke, K.: Stratospheric ozone
profiles over Switzerland measured by SOMORA, ozonesonde and MLS/AURA
satellite, Int. J. Remote Sens., 30, 4033–4041, 2009.Maillard Barras, E., Haefele, A., Stübi, R., and Ruffieux, D.: A method to
derive the Site Atmospheric State Best Estimate (SASBE) of ozone profiles
from radiosonde and passive microwave data, Atmospheric Measurement
Techniques Discussions, 8, 3399–3422, 10.5194/amtd-8-3399-2015, 2015.McIntyre, M. E. and Palmer, T. N.: The 'surf zone' in the stratosphere,
J. Atmos. Terr. Phys., 46, 825–849,
10.1016/0021-9169(84)90063-1, 1984.Moreira, L., Hocke, K., Eckert, E., von Clarmann, T., and Kämpfer, N.:
Trend analysis of the 20-year time series of stratospheric ozone profiles
observed by the GROMOS microwave radiometer at Bern, Atmos. Chem. Phys., 15,
10999–11009, 10.5194/acp-15-10999-2015, 2015.Müller, M., Neuber, R., Fierli, F., Hauchecorne, A., Vömel, H., and
Oltmans, S. J.: Stratospheric water vapour as tracer for Vortex filamentation
in the Arctic winter 2002/2003, Atmos. Chem. Phys., 3, 1991–1997,
10.5194/acp-3-1991-2003, 2003.Network for the Detection of Atmospheric Composition Change (NDACC): Stratospheric ozone profiles, available at: http://www.ndacc.org/, last access: 1 February 2017.Offermann, D., Grossmann, K.-U., Barthol, P., Knieling, P., Riese, M., and
Trant, R.: Cryogenic Infrared Spectrometers and Telescopes for the Atmosphere
(CRISTA) experiment and middle atmosphere variability, J. Geophys.
Res.-Atmos., 104, 16311–16325,
10.1029/1998JD100047, 1999.
Peter, R.: The ground-based millimeter-wave ozone spectrometer GROMOS,
IAP Research Report 97-13, Institut für angewandte Physik,
Universität Bern, Bern, Switzerland, 1997.Polvani, L. M. and Saravanan, R.: The Three-Dimensional Structure of
Breaking Rossby Waves in the Polar Wintertime Stratosphere, J.
Atmos. Sci., 57, 3663–3685,
10.1175/1520-0469(2000)057<3663:TTDSOB>2.0.CO;2, 2000.Randel, W. J., Gille, J. C., Roche, A. E., Kumer, J. B.,
Mergenthaler, J. L., Waters, J. W., Fishbein, E. F., and Lahoz,
W. A.: Stratospheric transport from the tropics to middle latitudes by
planetary-wave mixing, Nature, 365, 533–535, 10.1038/365533a0, 1993.
Rienecker, M., Suarez, M., Todling, R., Bacmeister, J., Takacs, L., Liu, H.-C.,
Gu, W., Sienkiewicz, M., Koster, R., Gelaro, R., Stajner, I., and Nielsen,
J.: The GEOS-5 Data Assimilation System – Documentation of Versions
5.0.1, 5.1.0, and 5.2.0, Tech. Rep. NASA/TM-2007-104606, vol. 27, NASA
GSFC, 2008.Schwartz, M. J., Lambert, A., Manney, G. L., Read, W. G., Livesey, N. J.,
Froidevaux, L., Ao, C. O., Bernath, P. F., Boone, C. D., Cofield, R. E.,
Daffer, W. H., Drouin, B. J., Fetzer, E. J., Fuller, R. A., Jarnot, R. F.,
Jiang, J. H., Jiang, Y. B., Knosp, B. W., Krüger, K., Li, J.-L. F.,
Mlynczak, M. G., Pawson, S., Russell, J. M., Santee, M. L., Snyder, W. V.,
Stek, P. C., Thurstans, R. P., Tompkins, A. M., Wagner, P. A., Walker, K. A.,
Waters, J. W., and Wu, D. L.: Validation of the Aura Microwave Limb Sounder
temperature and geopotential height measurements, J. Geophys.
Res.-Atmos., 113, D15S11, 10.1029/2007JD008783, 2008.Steinbrecht, W., Claude, H., Schönenborn, F., McDermid, I. S., Leblanc, T.,
Godin-Beekmann, S., Keckhut, P., Hauchecorne, A., Van Gijsel, J. A. E.,
Swart, D. P. J., Bodeker, G. E., Parrish, A., Boyd, I. S., Kämpfer, N.,
Hocke, K., Stolarski, R. S., Frith, S. M., Thomason, L. W., Remsberg, E. E.,
Von Savigny, C., Rozanov, A., and Burrows, J. P.: Ozone and temperature
trends in the upper stratosphere at five stations of the Network for the
Detection of Atmospheric Composition Change, Int. J. Remote
Sens., 30, 3875–3886, 10.1080/01431160902821841, 2009.
Studer, S., Hocke, K., and Kämpfer, N.: Intraseasonal oscillations of
stratospheric ozone above Switzerland, J. Atmos.
Sol.-Terr. Phys., 74, 189–198, 2012.Studer, S., Hocke, K., Schanz, A., Schmidt, H., and Kämpfer, N.: A
climatology of the diurnal variations in stratospheric and mesospheric ozone
over Bern, Switzerland, Atmos. Chem. Phys., 14, 5905–5919,
10.5194/acp-14-5905-2014, 2014.Waters, J. W., Froidevaux, L., Harwood, R. S., Jarnot, R. F., Pickett, H. M.,
Read, W. G., Siegel, P. H., Cofield, R. E., Filipiak, M. J., Flower, D. A.,
Holden, J. R., Lau, G. K. K., Livesey, N. J., Manney, G. L., Pumphrey, H. C.,
Santee, M. L., Wu, D. L., Cuddy, D. T., Lay, R. R., Loo, M. S., Perun, V. S.,
Schwartz, M. J., Stek, P. C., Thurstans, R. P., Boyles, M. A., Chandra,
K. M., Chavez, M. C., Chen, G. S., Chudasama, B. V., Dodge, R., Fuller,
R. A., Girard, M. A., Jiang, J. H., Jiang, Y. B., Knosp, B. W., LaBelle,
R. C., Lam, J. C., Lee, K. A., Miller, D., Oswald, J. E., Patel, N. C.,
Pukala, D. M., Quintero, O., Scaff, D. M., Van Snyder, W., Tope, M. C.,
Wagner, P. A., and Walch, M. J.: The Earth Observing System Microwave Limb
Sounder (EOS MLS) on the Aura satellite, IEEE T. Geosci.
Remote, 44, 1075–1092, 2006.
Waugh, D. W.: Seasonal variation of isentropic transport out of the tropical
stratosphere, J. Geophys. Res.-Atmos., 101,
4007–4023, 10.1029/95JD03160, 1996.
Zülicke, C. and Peters, D. H. W.: Parameterization of Strong
Stratospheric Inertia-Gravity Waves Forced by Poleward-Breaking Rossby
Waves, Mon. Weather Rev., 136, 98–119,
2008.