Physics of auroral phenomena : proceedings of the 36th Annual seminar, Apatity, 26 February – 01 March, 2013 / [ed. board: A. G. Yahnin, A. A. Mochalov]. - Апатиты : Издательство Кольского научного центра РАН, 2013. - 215 с. : ил., табл.

I. V. Mingalev et al. atmospheric parameters with time were calculated until they become stationary. The steady-state distributions of the atmospheric parameters were obtained on condition that inputs to the model and boundary conditions correspond to 10.30 UT. The temperature distributions, corresponding to this moment, were taken from the NRLMSISE-00 empirical model [Picone et al., 2002]. -180 -150 -120 -90 -60 -30 0 30 60 90 120 150 180 Longitude, deg Fig. 1 The global distributions of the atmospheric temperature (K) at 50 km altitude, obtained from the NRLMSISE- 00 empirical model for 16 January, UT=10.30 and calculated for two distinct values o f magnetic activity: Kp=l (top panel) and Kp=4 (bottom panel). It turns out that atmospheric temperatures, calculated with the help of the NRLMSISE-00 empirical model for two distinct values of magnetic activity (Kp=l and Kp=4), are very similar below approximately 80 km, while, above this altitude, they may be rather different. Fig. 1 shows the global distributions o f the atmospheric temperature at 50 km altitude, obtained from the NRLMSISE-00 empirical model for 16 January, UT=10.30 and calculated for two distinct values of geomagnetic activity: Kp=l and Kp=4. It is seen no distinctions between the results obtained for two different values of geomagnetic activity. Above 80 km, for example, at the altitude of 110 km, differences between temperatures, obtained for two considered values of magnetic activity, can achieve a few tens o f degrees at identical points of the globe. Thus, the application of the NRLMSISE-00 empirical model shows that the influence of level of magnetic activity on the global distribution of the atmospheric temperature ought to be absent at altitudes of the troposphere, stratosphere, and mesosphere, while this influence ought to be appreciable at altitudes of the lower thermosphere for the winter period in the northern hemisphere. Distributions o f the atmospheric parameters, calculated with the help of the mathematical model and obtained for 16 January, are partly shown in Figs. 2 and 3. The results of modeling illustrate both common characteristic features and distinctions caused by different values of magnetic activity. The calculated global distributions of the atmospheric parameters display the following common features. The horizontal and vertical components o f the wind velocity are changeable functions of latitude and longitude at levels o f the stratosphere, mesosphere, and lower thermosphere. The horizontal domains exist where the steep gradients in the horizontal velocity field take place. The horizontal wind velocity can have various directions which may be opposite at the near points. Moreover, the horizontal domains exist in which the vertical neutral wind component has opposite directions. Maximal absolute values of the horizontal and vertical components o f the wind velocity are larger at higher altitudes. At levels of the mesosphere, the horizontal wind velocity can achieve values of more than 150 m/s. 156