HEAT BUDGET OF THE LOWER ATMOSPHERE IN THE KANTÔ PLAIN, WITH SPECIAL EMPHASIS ON MESO-CLIMATOLOGY

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The author has already reported papers on the meso-climatology of temperature distribution patterns in this area. In this present paper, the same theme is discussed based on the results of heat budget of the lower atmosphere. In the formation of meso-scale temperature distribution, areal differences in diurnal temperature change play an important role. In the Kantô Plain, which is situated in central Japan and facing to the Pacific Ocean, such a difference is especially marked between inland and coastal areas. As this difference is caused by the difference in the heat budget of lower atmosphere up to 850-mb, it is necessary to consider it for analyzing meso-scale temperature distribution theoretically. Heat budget equations (6) for the air column above the land surface and (7) for the sea surface are considered and terms are estimated based on observed meteorolgical data. In the above equations, Q is the heat absorbed into or exhausted from the lower atmosphere, I: total short-wave radiation at the surface, R: albedo of the surface, r: effective long wave radiation of the atmosphere under 850-mb level, α: evaporation ratio of unsaturated surface to the saturated, L: latent heat, E: amount of evaporation from the surface, G: heat absorbed into ground and W: heat absorbed into water. Suffixes L and W are added to terms relating to land- and water-surfaces respectively. Calculations of heat budget were done for days with daily cloudiness of less than two-tenths and in an anti-cyclonic condition in order to eliminate the effect of macro-scale advection. According to these standards stated above, 114 days were selected for computation from odd months of the years 1951 to 1960. Figure 2 shows the curves of estimated (I) for each hour of the day and the other calculated terms in the equations are tabulated in Tables 2, 3, 4, 5, 6 and 10. Heat budgets were calculated for the periods of day (0-24), morning-(O-12) and afternoon-hours (12-24). Results are summarized in Table 13 and Figure 3 where Q' denotes Q-value calculated diagrammatically from emagram (Figure 1), QW and QW' were assumed to be equal for all periods and Q was assumed to be zero for the period of day. If all the assumptions considered are right, QL and QL' must coincide with each other, at least theoretically, but results are as such seen in Figure 3. The main factor affecting this discrepancy may be due to inaccuracy of evaporation amount which is estimated by Penman's equation for open water. Among the results obtained, the following points may be the most important. Warming effect in the coastal area by the heat flux from the sea water, which has the order of 20-35 langley per day for the colder season, is evaluated. During summer, amount of heat consumed to evaporation is nearly equal to 50% of energy by total short-wave radiation, and this means that evaporation process is very important for making our moist climate milder. May is the only month having QL which is greater than QL'. This might be the result of strong sea breere invasion, because the most typical pattern of temperature distribution showing the narrow colder zone along the coast, on which the author has reported in the previous paper, also appeared on clear calm days in May. Rough estimate of evaporation ratio (α) for the natural surface in the Kanto Plain (Figure 6) is obtained for odd months. The ratio shows a marked seasonal variation.
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HEAT BUDGET OF THE LOWER ATMOSPHERE IN THE KANTÔ PLAIN, WITH SPECIAL EMPHASIS ON MESO-CLIMATOLOGY

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