Nerushev A.F., Barkhatov A.E. Research and Production Association "Typhoon" 4 Pobedy Street, , Obninsk, Kaluga Region, Russia.
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1 DETERMINATION OF ATMOSPHERIC CHARACTERISTICS IN THE ZONE OF ACTION OF EXTRA-TROPICAL CYCLONE XYNTHIA (FEBRUARY 2010) INFERRED FROM SATELLITE MEASUREMENT DATA Nerushev A.F., Barkhatov A.E. Research and Production Association "Typhoon" 4 Pobedy Street, , Obninsk, Kaluga Region, Russia Abstract Based on the data of atmospheric soundings from the geostationary satellite (Meteosat-9) and Polar Orbital satellites (Terra, Aqua) studied were the dynamical characteristics of the atmosphere and cloud systems structures in the zone of generation and development of extra-tropical cyclone Xynthia (February 2010). The storm impacted the major part of Western Europe, caused a considerable damage along the trajectory of its motion and resulted in the deaths of more than 60 people. Spatial distributions of the horizontal wind speed module ( V ), the coefficient of horizontal meso-scale turbulent diffusion (K d ), vorticity (rotv) and the horizontal wind speed vector (V)under different atmospheric conditions at the stages of the cyclone generation and development were obtained. Significant differences of all the characteristics indicated were revealed in the upper and lower troposphere at the stage of the cyclone maximum development (pressure in the center p 967 HPa) with their small differences at the initial stage (p > 990 HPa). It is shown that the field of horizontal wind speed in the upper troposphere at temporal scales of several hours has noticeable inertia, that can be used for wind speed nowcasting on the basis of satellite measurement data. INTRODUCTION The tropical and extra-tropical cyclones come into the general atmospheric circulation and thus determine the climate characteristics of the global and regional scale. At the same time, they belong to hazardous atmospheric phenomena resulting at their landfalls in enormous economic losses and human deaths. The fields of the atmospheric dynamic characteristics play an important role in the processes of cyclone formation, evolution and motion. The information on the wind fields in the zones of cyclone action is obtained by different methods. The most efficient is remote sensing of the atmosphere from space platforms. In leading forecasting centers satellite winds are successfully assimilated into the schemes of numerical weather forecasts, that positively affects on the quality of the forecasting skills. Satellite methods used for cyclone characteristics studies and their monitoring are in the scope of essential scientific and practical problems. The goal of the present paper is to study, with an example of the severe extra-tropical cyclone Xynthia (February 2010), the peculiarities of the atmospheric dynamic characteristics, the structure and dynamics of cloud systems at different stages of cyclone evolution. The data of multi-wave atmospheric soundings made with the radiometer SEVIRI of the European geostationary meteorological satellite Meteosat-9 and the data of spectroradiometer MODIS of Polar satellites Terra and Aqua were used for this purpose. For calculations of atmospheric dynamic characteristics the method developed earlier (Nerushev, Kramchaninova, 2011) was used. The method allowed to determine not only the wind speed field vector (V) but also the coefficient of meso-scale turbulent diffusion (K d ) and vorticity (rotv) in one scale of air mass motion. A new and more flexible software was used.
2 A SHORT DESCRIPTION OF STORM XYNTHIA AND OF THE DATA USED FOR CALCULATIONS According to (Bissolli, 2010) cyclone Xynthia was the result of the development of the low pressure system formed to the south of the Azores on Friday, 26 February, During several days before the formation of Xynthia (22 24 February) a zonal transport was observed (from west to east). It was caused by a large system of a low pressure (a trough) located over the sub-tropic regions of the Atlantics to the south of the Azores. On 25 February, one branch of the flow obtained at the upper levels the meridional direction from north to south, and within the limits of the vast trough existing earlier a short-wave but very active trough was formed. This trough (with colder air at the top) interacting with the vast mother-trough (with warm and humid air at the bottom) resulted in the intensification of the latter. The short-wave trough and a big difference in temperatures between extremely warm air over Africa and colder air over the eastern Atlantics induced a very fast development of cyclone Xynthia. When moving towards north-east, the storm passed Portugal, the north-western Spain, the Bay of Biscay and reached western regions of France on February 27. It was very quickly intensified and reached maximum stage of development on February 28 at 00 UTC with the pressure p = 967 HPa near the ground in the center. During the day the pressure decreased by 20 HPa (Figure 1). The cloud system of Xynthia occupied the whole west and the center of Europe during this time. During the next three days the storm weakened while moving towards the west-north along the coastal line of France and the North Sea. Then it crossed the south of the Baltic Sea and continued its breakdown. The trajectory of cyclone Xynthia was rather unusual. In the most of the cases, such storms develop in the northern part of the Atlantics and then move towards the east over the western and central Europe. Figure 1:Trajectory of cyclone Xynthia on 26 February 3 March 2010 according to (Bissolli, 2010). Figures at the curve pressure near the ground in the center, HPa The storm Xynthia brought hurricane winds. According to the Deutscher Wetterdienst (DWD) wind gusts were maximal in its south-western sector especially after the passage of the cold front (Bissoli, 2010). In the Canaries maximal wind gusts (about 200 km/hr) were observed at night from 26 to 27 February. During the following week wind gusts still reached the full-gale force ( km/hr) at many stations of France. On Sunday in the morning (on February 28), the wind gust of the same force were registered in the north of France, in Luxemburg, Belgium, in the south-west of Germany and in Switzerland. Maximal wind gusts in Germany (DWD stations) made 180 km/hr on Sunday in the evening in the mountain of Brocken. At the stations located below the local wind gusts were about km/hr. In the Western Europe maximal gusts of 238 km/hr were registered on 27 February on Pic du Midi in the French Pyrenees (2877 m above the sea level), in the central region of France at the
3 altitude of 1415 m wind gusts of 209 m/hr were registered. High wind speeds caused an increase of the sea level by about 1.2 m on the Atlantic coast of France (Monthly Bulletin, 2010). During its whole lifetime cyclone Xynthia was in the satellite Meteosat-9 surveillance zone. The information from radiometer SEVIRI was transmitted to RPA Typhoon from the RC Planeta every 15 minutes. The calculations of dynamic characteristics in the zone of cyclone action were made with the grid having the space step of 5 pixels (about 15 km at the sub-satellite point) in the range within a radius of 10 degrees from the cyclone center. Such a step in space was needed for the construction of maps of corresponding physical values (parameters). Constructed were the maps of horizontal wind speed module ( V ) fields, of coefficient of meso-scale turbulent diffusion (K d ) and vorticity (rotv), of horizontal wind speed vectors (V). Not making a detailed binding of calculated fields over altitudes (due to the absence of atmospheric aerological sounding data for the terms indicated), we note that the data of the 6.2 micrometers channel make it possible to obtain the dynamic characteristics of the upper troposphere (in the layer with a pressure of 200 HPa p 400 HPa) and of the 0.8 micrometers channel data at the level of the cloud upper boundary, as a rule, in the average (400 HPa < p 700 HPa) or in the lower (700 HPa < p 1000 HPa) atmospheric layers (Nerushev, Kramchaninova, 2011). CALCULATION RESULTS AND DISCUSSION Figure 2 presents the fields of horizontal wind speed module ( V ) for February at 12:30 UTC calculated with the data of 6.2 and 0.8 micrometers channels of radiometer SEVIRI. A characteristic feature of the fields V shown in figure 2 is in high wind speeds on 27 February when the cyclone practically reached its maximum activity (pressure in the center p 969 HPa, see figure 1). (a) (b) (c) (d) Figure 2: Wind speed module field in cyclone Xynthia on 26 (a,b) and 27 (c,d) February 2010 at 12:30 UTC according to measurement data in the visible (0.8 micrometers) channel (a,c) and in the water vapor (6.2 micrometers) channel (b,d). The location of the cyclone center is marked by a circle. In the upper left angles color scale of wind speed in m/s.
4 According to the calculations, the wind speed in the upper troposphere in the central part of the cyclone over the north-western Pyrenean Peninsula, the Bay of Biscay and the north-west of France reached 70 m/s (252 km/h) and more. At the same time, at lower atmospheric levels (channel 0.8 micrometers) the wind speed was practically within the limits of m/s ( km/hr) over all the territories mentioned. Such a situation was not observed on 26 February, when the cyclone did not still reach the maturity stage (p 994 HPa). Thus, one can conclude that at the stage of maximum cyclone development the wind speed in the cyclone increased with altitude. As indirect confirmation of this can serve the data of the French Meteorological Service indicating that maximum wind speeds, as it was said above, were registered at night from 27 to 28 February at high meteorological stations: 238 km/hr at the altitude of 2877 m and 209 km/hr at the altitude of 1415, and at the stations located in the plains the wind speed did not exceed 160 km/hr. In Figure3 for the same time period, presented are the fields of the coefficient of horizontal meso-scale turbulent diffusion (K d ). At the early stage of cyclone development the fields of K d in the upper troposphere and at the cloud upper boundary differ slightly. Here the values of K d do not exceed m 2 /s in the major portion of the region. At the stage of maximum cyclone development the differences are rather noticeable. At lower levels of cloud medium (0.8 micrometers channel) the values of K d are significantly higher as compared to those in the upper troposphere. (a) (b) (c) (d) Figure 3: The field of horizontal coefficient of turbulent diffusion K d in cyclone Xynthia on 26 (a,b) and 27 (c,d) February at 12:30 UTC according to measurement data in the visible (0.8 micrometers) channel (a,c) and in the water vapor (6.2 micrometers) channel (b,d). The location of the cyclone center is marked by a circle. In the upper left angles color scale of K d*10-4 values in m 2 /s. Considerable differences at the stage of cyclone maximal development are observed in the vorticity fields (the data of 6.2 and 0.8 micrometers channels) (Figure 4). If in the upper troposphere in the cyclone center and in the range with a radius of about 3 degrees the zero or weak positive vorticity (anticyclonic, as it is named here) is registered, then in the middle and lower layers in the cyclone center negative (cyclonic) vorticity is observed. At the distances of about 3 degrees in the western and south-western directions the ranges with increased positive vorticity (rotv s -1 ) are observed.
5 The analysis of calculated fields of horizontal wind speed in the zones of cyclone action shows that their main peculiarity, besides the difference in wind vector modules in the upper (6.2 micrometers) and in the middle and lower (0.8 micrometers) tropospheric layers (that is shown in figure 2), is in distinctly seen differences of vector directions at different atmospheric levels in different cyclone regions. If in the frontal part of cyclone the directions of vectors in the tropospheric upper and lower layers practically coincide, then in the cyclone rear the directions of wind vectors significantly differ. It is especially noticeable at the stage of cyclone development on 26 February in the western and northwestern cyclone regions, where the vectors are practically orthogonal. (a) (b) (c) (d) Figure 4: Vorticity field in cyclone Xynthia on 26 (a,b) and 27 (c,d) February at 12:30 UTC according to measurement data in the visible (0.8 micrometers) spectrum range in the visible (0.8 micrometers) channel (a,c) and in the water vapor (6.2 micrometers) channel (b,d). The location of the cyclone center is marked by a circle. In the upper left angles color scale of vorticity in s -1. The analysis of calculations for different time moments (the difference in several hours) made it possible to reveal significant wind field inertia. In rather a large territory the wind in the upper troposphere of the extra-tropical cyclone changes insignificantly both in value and in direction. This obstacle can be used for nowcasting of the wind speed field based on satellite data. An interesting peculiarity in the cyclone structure is traced in the images made from the geostationary satellite in the visible spectrum range. During several days of its lifetime up to the maximum stage of development the cyclone was connected with the tropical zone by an extensive bank of clouds. A thin cloud thread stood out against its background. It varied slightly during several days (Figure 5). The length of this thread made more than 4000 km, the width 50 km. The measurement data of the spectroradiometer MODIS indicated that the altitude of the cloud upper boundary of the thread did not exceed 3 km, the optical depth in the visible wavelength range varied within the limits of 25 30, effective radius of cloud drops made about 20 micrometers. The cause of this phenomenon is likely to be connected with the peculiarities of the wind field in the lower troposphere.
6 Figure 5: Image of cyclone Xynthia in the visible spectrum range on 26 February 2010 at 12:30 UTC from the satellite Meteosat-9. CONCLUSION The construction of maps of atmospheric dynamic characteristics in the zone of the severe cyclone of the moderate latitudes based on the data of multi-wave remote sensing from the European geostationary satellite Meteosat-9 with the use of the method developed by the authors and the software allowed us to reveal a series of peculiarities of these characteristics. Most important of them are: a) significant differences of all the dynamic characteristics (V, K d, rotv) in the upper and lower troposphere in the cyclone action zone at the stage of its maximum development and slight differences at the cyclone early stage; b) noticeable inertia of the horizontal wind speed field in the upper troposphere in the time scales of several hours, that can be used for nowcasting of wind speeds on the basis of satellite measurement data. REFERENCES Bissolli P. (2010) Severe Storm Xynthia over southwestern and western Europe. Monthly Bulletin on the Climate in WMO Region VI. (February 2010). Deutscher Wetterdienst. Nerushev A. F., and E. K. Kramchaninova. (2011) Method for Determining Atmospheric Motion Characteristics Using Measurements of Geostationary Meteorological Satellites. Izvestiya, Atmospheric and Oceanic Physics, 47, No. 9, pp
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