The predicted depth of the sea breeze inflow ranged between and m, while the depth of the return flow was in the range of — m. Some features of this site may not work without it. The pollutant concentration may increase in the SBCZs, but their ability to recirculate the pollutants requires more extensive research. Sea breeze fronts have been observed along the shore lines of the Great Lakes. An explanation of the graphs is available in the chapter Weather Events.
This resulted in measuring points close to the coast experiencing smaller temperature fluctuations than those further inland. The 2nd item, and , represents the vertical exchange of momentum between the surface and the layer above. At LT downslope winds start at Mond Mountain. Over vegetation where air is usually moist, sea breeze cumulus are the rule. Both bay breeze and mature sea breeze contribute towards development, extent and strength of the sea breeze convergence zones SBCZs.
The Evaluation of Estoque Model in Land/Sea Breezes Occurrence over Northern Persian Gulf
An example of a narrow peninsula is the northern tip of New Zealand, from Auckland northward 3. Maximum of sensible heat flux calculated by a mesoscale model. The up and down circulating cells associated with the land and sea breeze circulations are shown in Figure 8. These results corroborate those of Alpert et al. The relative humidity was higher near the sea and from there on decreased rapidly inland.
When convection is very deep, the frontal effect of a sea breeze may sometimes trigger cumulonimbus clouds provided the lifted air over land contains sufficient moisture. This may increase pollution concentration, especially in the evening hours, to unacceptable levels. The east coast sea breeze penetrated further inland but did not produce much deep convection, except near Lake Okeechobee, due to convergence with the lake breeze near the Lake's eastern shore. Higher ground level concentrations of pollutants are expected under coast-normal gradient winds, when SBCZs are formed in the middle of the land mass and the wind speed of the sea breeze inflow and the sea breeze front is relatively low. This control of the sea breeze circulation on deep convection is only possible when synoptic-scale forcing is negligible, i.