Journal of the Meteorological Society of Japan. Ser. II
Online ISSN : 2186-9057
Print ISSN : 0026-1165
ISSN-L : 0026-1165
Volume 27, Issue 10
Displaying 1-4 of 4 articles from this issue
  • M. Shiotani
    1949 Volume 27 Issue 10 Pages 295-303
    Published: 1949
    Released on J-STAGE: February 05, 2009
    Some characteristics of hot wire direction-sensitive meter, consisting of two hot wires stretched at right angles, are discussed. It shows linear characteristics up to 30 degrees, and less than 10% erorr in the indication when the mean velocity changes from 5 to 14m/s, and also this erorr is compensated when used only in measurin the mean velocity. With this direction meter angle of inclination of wind velocity was recorded by a electromagnetic oscillograph at the plain of Kashima, Ibaragi Prefecture. On the same recording chart, velocity fluctuation along the mean flow was also recorded. So the vertical fluctuation of the vertical component can be obtained from them. Numerical values of _??_ at 1 and 3 meters above the ground are shown. The author also shows that the vertical component of turbulence is larger than the component along the mean stream not only in its intensity but also in its scale.
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  • Y. Miyake, R. Saruhashi
    1949 Volume 27 Issue 10 Pages 304-311
    Published: 1949
    Released on J-STAGE: February 05, 2009
    The authors have assumed the fundamental reaction of formation and decomposition of ozone as follows: formation; decoposition; Where M means any molecule or atom in the atmosphere. From the above reactions the formula of the photochemical equilibrium of ozone and oxygen has been deduced. in which K is an equilibrium constant, P the atmospheric pressure at the height h above the ground, α and β the absorption coefficients of ozone ánd oxygen, q and q' the number of light quanta to produce excited oxygen molecules and to destroy ozone respectively.
    In the next place, we put, where, q, and q' are the number of light quanta coming into the atmosphere which is calculated under the assumption that the sun is a black body of 6000°K. αq and βq' at each height are calculated by the graphical integration with regard to the wave lepgth. Since the distribution of ozone is unknown, we put _??_. The relation between x and h can be deduced by the formula of equilibrium. The results are shown in Fig. 3 and Fig. 4, which are in good agreement with observations. The maximum absorption of the ultra-violet ray occurs at about 40 km at which it is expected that the remarkable elevation of temperature would begin. (A full report will be printed soon on The Geophysical Magazine.)
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  • K. Kano
    1949 Volume 27 Issue 10 Pages 311-318
    Published: 1949
    Released on J-STAGE: February 05, 2009
    L. F. Richardson obtained from physical considerations an integral equation for the change of kinetic energy of eddying flow, from which he introduced a criterion for the decrease or increase of turbulent energy in the atmosphere. Later, Rossby presented a differential equation.
    The purpose of the present paper is to show that it is possible to obtain the general eeqution for the change of the energy of eddy directly from the fundamental equations of motion of the wind in the free atmosphere. The result thus obtained involves the Richardson's criterionship. When eddy viscosity K is given as a function of height, the equation becomes linear. Therefore, it will become one of the fundamental equations to be used in the future study of the phenomena.
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  • G. Yamamoto
    1949 Volume 27 Issue 10 Pages 318-331
    Published: 1949
    Released on J-STAGE: February 05, 2009
    Experiments on evaporation were carried out in wind tunnels. The results were in fairly good agreement with the theoretical results by Yamamoto and Ogiwara.
    When the boundary layer on the surface of water is laminar, the mean rate of evaporation, E, is expressed by the formula, where E is measured in g. cm. sec., u1; the wind velocity outside of the boundary layer, in cm-2 sec-1., x; the length of the veesel along wind, in cm., c0, c1; vapour concentrations on water surface and in an air current outside the boundary layer respectively, in g. cm-3. When the boundary layer on the surface of water is turbulent:
    In our experiment where water was constrained by the blotting paper the surface remained in laminar condition until log_??_, and beyond then it changed into turbulent condition and no transition region could be seen. But, as is seen from Millar's experiment, if we use the ves. sel containing water only, the surface of water will turn to turbulent condition even when log_??_, and the rate of evaporation from free water surface will be
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