## 2 Methods  
In this paper, we analyze the possibility of simulation of the wind speed and temperature fields with a sufficiently high spatial and temporal resolution within the Baikal Astrophysical Observatory (BAO) region. The region includes three domains. The horizontal resolution in the internal domain is 500 m. The region is distinguished by a complex relief with strongly dissected mountains and plateaus. In calculations, we used the non-hydrostatic WRF model [25]. This model is a powerful tool for the study of mesoscale phenomena in the atmosphere, precipitation and cloudiness. The basic equations of the WRF model are written as follows:  
\[ \begin{cases}\frac{\partial U}{\partial t}+m[\frac{\partial(Uu)}{\partial x} +\frac{\partial(Vu)}{\partial y}]+\frac{\partial(Wu)}{\partial y}+\left(u_{ d}a^{\prime}\frac{\partial\overline{n}}{\partial x}+u_{d}a\frac{\partial p^{ \prime}}{\partial x}\right)+\left(\frac{\alpha}{\alpha_{d}}\right)\left(\mu_{ d}\frac{\partial H^{\prime}}{\partial x}+\frac{\partial y^{\prime}}{\partial y} \frac{\partial H}{\partial x}-\mu_{d}^{\prime}\frac{\partial H}{\partial x} \right)=F_{U},\\ \frac{\partial V}{\partial t}+m[\frac{\partial(Uv)}{\partial x}+\frac{\partial (Vv)}{\partial y}]+\frac{\partial(Wv)}{\partial y}+\left(\mu_{d}a^{\prime} \frac{\partial\overline{n}}{\partial y}+\mu_{d}a^{\prime}\frac{\partial p^{ \prime}}{\partial y}\right)+\left(\frac{\alpha}{\alpha_{d}}\right)\left(\mu_{ d}\frac{\partial H^{\prime}}{\partial y}+\frac{\partial p^{\prime}}{\partial y} \frac{\partial H}{\partial y}-\mu_{d}^{\prime}\frac{\partial H}{\partial y} \right)=F_{V},\\ \frac{\partial W}{\partial t}+m[\frac{\partial(Uv)}{\partial x}+\frac{\partial (Vu)}{\partial y}]+\frac{\partial(Wv)}{\partial y}-\frac{\alpha}{\alpha_{d}} \left(\frac{\alpha}{\alpha_{d}}\right)\left(\frac{\partial p^{\prime}}{ \partial y}-\overline{\mu_{d}}(q_{vapor}+q_{cloud}+q_{rain})\right)+\frac{ \delta}{m}\mu_{d}^{\prime}=F_{W},\\ \frac{\partial H^{\prime}}{\partial t}+\frac{1}{\mu_{d}}\left(m^{2}\left(U[ \frac{\partial H}{\partial x}+V\frac{\partial H}{\partial y}\right)+mW\frac{ \partial H}{\partial y}-gW\right)=0,\\ \frac{\partial H^{\prime}}{\partial t}+m^{2}\left(\frac{\partial U}{\partial x }+\frac{\partial V}{\partial y}\right)+m\frac{\partial W}{\partial y}=0,\\ \frac{\partial\theta}{\partial t}+m^{2}\left(\frac{\partial U}{\partial x}+ \frac{\partial(V\theta)}{\partial y}\right)+m\frac{\partial(W\theta)}{\partial y }=F_{\theta},\\ \frac{\partial Q_{0n}}{\partial t}+m^{2}\left(\frac{\partial(Uq)}{\partial x}+ \frac{\partial(Vq)}{\partial y}\right)+m\frac{\partial(Wq)}{\partial y}=F_{ \Omega_{n}},\\ \frac{\partial T}{\partial\eta}=-\overline{\mu}\cdot\overline{\kappa},\\ \frac{\partial H^{\prime}}{\partial\eta}=-\overline{\mu}\cdot\alpha^{\prime}- \mu^{\prime}\overline{\kappa},\\ \eta=(p_{h}-p_{hupper})/\mu;\mu=p_{hsurface}-p_{hupper}\end{cases} \]  
where \(u\), \(v\), \(w\) are the wind speed components \(U=\mu_{d}u/m\), \(V=\mu_{d}v/m\), \(W=\mu_{d}\dot{\eta}/m\), \(\mu_{d}\) is the mass of dry air, \(\dot{\eta}\) is the vertical velocity, \(m\) is the scale coefficient (of the map). \(\alpha=\alpha_{d}(1+q_{vapor}+q_{cloud}+q_{rain})\) is the specific volume of dry air \(\alpha_{d}\), water vapor, cloudiness and rain, \(q\) is the ratio of mixture of water vapor, cloudiness and rain. The knowledge of these parameters within the region and at different heights makes it possible not only to estimate the vertical profiles of the structure constant of air refractive index fluctuations \(C_{n}^{2}\), but also to determine the influence of mesoscale processes on the structured optical turbulence under different atmospheric conditions and the quality of astronomical images. Interest in studies of mesoscale structures is supported by several factors. On the one hand, mesoscale structures arising in the atmosphere (mesoscale jets in the atmospheric boundary layer, mountain waves) distort the energy spectrum of turbulence and can enhance optical turbulence.