A Lake Breeze over Southern Lake Ontario

Effects of long-term deforestation and remnant forests on rainfall and temperature in the Central Rift Valley of Ethiopia

“…Distance to lakes was another predictor, but it was not included in the analysis because the stations on the valley floor were in similar proximities to the lakes, but the stations in the escarpments/highlands were in different climatic zones, and most stations in the highlands were far from the range of lake penetration distances of 15-45 km (e.g. Estoque et al 1976;Ryznar and Touma 1981).…”

Sea and Lake Breezes: A Review of Numerical Studies

“…The earliest hydrostatic models used simple boundary-layer schemes and neglected moisture, latent heating, radiation, and land-surface parametrisations. Some later models included radiation, moisture and latent heating, with increasingly sophisticated schemes for surface heating and the turbulent Neumann andMahrer (1971, 1974) 5 , Pearson (1973) Pielke (1974a,b) 4 1975-1979 2D 2.5-8 9 Neumann and Mahrer (1975) 5 , Sheih and Moroz (1975) 1 , Estoque et al (1976) 1 , Pielke (1976, 1977) 3 , Physick (1976) 4 , Anthes (1978) 2 , Asai and Mitsumoto (1978) 1 , Ookouchi et al (1978) 3 1980-19842D 3-10 8 Physick (1980 4 , Estoque and Gross (1981) 1985-1989 2D 1-10 14 Garratt and Physick (1985) 2 , Mahrer and Segal (1985) 1 , Physick and Smith (1985) 3 , Neumann and Savijarvi (1986) 1 , Noonan and Smith (1986) 2 , Segal et al (1986) 3 , Arritt (1987Arritt ( , 1989 4 , Briere (1987) 1 , Anthes (1987, 1988) Freitas et al (2007) 8 , Srinivas et al (2007) 8 , Talbot et al (2007) 8 , Thompson et al (2007) 8 , Cheng and Byun (2008) transport of heat, moisture, and momentum. Through the 1970s, turbulence in the surface layer was generally treated using simple K-theory, assuming constant fluxes, and with empirical formulations for turbulent transport in the overlying transition layer.…”

Numerical studies of neutrally stratified planetary boundary-layer flow above gentle topography

“…One which has been studied fairly extensively is the interaction of surface temperatures with a vertical temperature gradient to produce thermal slope winds (see, for example, Defant, 1951or Munn, 1966. These effects are usually considered on a rather larger horizontal scale than that considered here and can then be simulated by hydrostatic models (e.g., Danard, 1972;Mahrer and Pielke, 1975;Estoque et al, 1976). In the present study, potential temperatures are assumed to be uniform everywhere and we are concerned solely with what might be termed the 'dynamic pressure' effects of topography.…”