The Difference of the Slope Wind Between Day and Night

Kumakura, Hiroaki

doi:10.2151/jmsj1965.62.2_224

Cited by 15 publications

(11 citation statements)

References 12 publications

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“…The wind inland was a little stronger at the places where the mountains were located closer to the coastline, which was the same feature pointed out by Asai and Mitsumoto (1978). From the results of the linear theory on the slope wind (Asai and Mitsumoto, 1978;Kondo, 1984;Niino and Kondo, 1989), there was little difference in the phase between surface heating and up-slope ' wind when the slope angle (cr) satisfied the relation, a» w/N. Here, w is the frequency of diurnal variation and N is the Brunt-Vaisala frequency.…”

Section: Description Of the Modelsupporting

confidence: 69%

A Numerical Experiment of the "Extended Sea Breeze" over the Kanto Plain

Kumakura¹

1990

Journal of the Meteorological Society of Japan

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Numerical experiments have been employed to simulate the "extended sea breeze (ESB)" over the Kanto Plain in a three-dimensional mesoscale model. Through some observations in the field, it has been found that there are two characteristics of ESB which distinguish ESB from a typical sea breeze.(1) The thickness of the ESB is 1-1.5 km, which is almost two times the thickness of a typical sea breeze. (2) The wind direction throughout the Kanto Plain shifts northward in the early afternoon.The numerical experiments reproduced these two characteristics rather well in both cases with no general wind and with a SW general wind (5 m/s). Some additional experiments with artificial topography indicated that when there was no general wind an ESB-like wind was generated from the combination of the sea breeze and the thermally and orographically induced flow over the mountainous area of the central part of Japan. However, when there was a SW general wind, another type of ESBlike wind was formed in combination with the general wind and the thermally and orographically induced flow. It was very difficult to distinguish the two types of ESB by observation, because there were southerly winds in the south of the Kanto Plain in both cases.

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Section: Description Of the Modelsupporting

confidence: 69%

A Numerical Experiment of the "Extended Sea Breeze" over the Kanto Plain

Kumakura¹

1990

Journal of the Meteorological Society of Japan

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“…The presence of nonlinear terms involved with the evaluation of the L WR flux divergence prevents a simplified analytical solution for Equation (1); some authors have even neglected the L WR flux divergence term (e.g., Rao and Snodgrass, 1981;Kondo, 1984). However, in order to overcome this limitation, a diagnostic equation of 8 can be established which is based upon observational data for 8, and so, indirectly, includes the contributions from long-wave radiative flux divergence terms to 8.…”

Section: Analytical Methodologymentioning

confidence: 99%

On the impact of atmospheric thermal stability on the characteristics of nocturnal downslope flows

Garratt

Segal

et al. 1990

Boundary-Layer Meteorol

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.... Abstract. The impacts of background (or ambient) and local atmospheric thermal stabilities, and slope steepness. on nighttime thermally induced downslope flow in meso-(3 domains (i.e., 20-200 km horizontal extent) have been investigated using analytical and numerical model approaches. Good agreement between the analytical and numerical evaluations was found. It was concluded that: (i) as anticipated, the intensity of the downslope flow increases with increased slope steepness, although the depth of the downslope flow was found to be insensitive to slope steepness in the studied situations; (ii) the intensity of the downslope flow is generally independent of background atmospheric thermal stability; (iii) for given integrated nighttime cooling across the nocturnal boundary layer (NBL), Qs, the local atmospheric thermal stability exerts a strong influence on downslope flow behavior: the downslope flow intensity increases when local atmospheric thermal stability increases; and (iv) the downslope flow intensity is proportional to Q~/2.

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“…The eddy-viscosity concept has led to useful qualitative descriptions of a variety of turbulent geophysical flows including atmospheric Ekman layers (Clarke, 1970;Houghton, 1977;Lettau, 1983), oceanic Ekman layers (Price et al, 1987;Chereskin, 1995;Ralph and Niiler, 1999), sea breezes (Walsh, 1974;Sun and Orlanski, 1981), and anabatic and katabatic flows (Defant, 1949;Egger, 1981;Kondo, 1984;Papadopoulos et al, 1997;Oerlemans, 1998). However, despite the successes of some appropriately tuned models based on the eddy-viscosity concept, it should always be borne in mind that eddy viscosity is a rather ad hoc concept.…”

Section: Governing Equationsmentioning

confidence: 99%