At Syowa Station in Antarctica, the author observed the wind velocity profile from March to September in 1970 and the temperature profile from March 1970 to February 1971.The results are summarized as follows:(1) The frequency distribution of the stable temperature gradient is about 88 per cent in winter (from May to September) and about 75 per cent throughout the year. The variation pattern of the requency distribution of the temperature is nearly symmetric in autumn (March and April) and spring (October and November), and is distorted in other seasons, namely the peak of the frequency distribution shifts to the small temperature gradient in winter and to the great temperature gradient in summer.(2) The phenomenon of Kernlose type also appears at the annual variations of TX (tropospheric maximum temperature), T20 (temperature at 20m height) and T1 (temperature at 1m height) which are averaged of the observations with inversion. The temperature differences between Tx, T20, and T1 increases in winter.(3) The more the thickness of an inversion layer increases, the less the rate of an inversion appearance increases.(4) The value of the temperature difference decreases in order of Tx-T1, T20-T1 and T10-T1. The maximum value of the temperature difference is found in July and the minimum value of the temperature difference in January and February.(5) The ratio of (T10-T1)/(T20-T1) is great in autumn and is small in summer. The ratio of (T10-T1)/(T20-T1) in winter and spring is nearly equal to the mean of the summer-value, which shows the maximum in the year, and the autumn-value, which shows the minimum in the year. The observation results, described above make clear that the temperature profile in winter and spring shows a linear variation and that the temperature gradient in the lower atmospheric surface layer remarkably increases in autumn and decreases in summer.(6) To make clear the relation between the wind velocity and the temperature gradient, the observed data are plotted on the Fig. 9. From the distribution of the plotts, it is possible to estimate the maximum value of the temperature gradient related with the wind velocity. This maximum value is called maximum limit of the relation between the wind velocity and the temepreture gradient. The curve shape of the maximum limit looks like an orthogonal hyperbola. The temeprature gradient remarkably increases in the case of the wind velocity at 10m (U10) below 5m/sec and decreases in the case of the wind velocity above 8m/sec, with which the snow cover begins to drift.