Ultimately the winds are driven almost entirely by the sun’s energy, causing differmential surface heating. The heating ismost intense on landmasses closer to the equator, and obviously the greatest heating occurs in the daytime,whichmeans that the region of greatest heating moves around the earth’s surface as it spins on its axis. Warm air rises and circulates in the atmosphere to sink back to the surface in cooler areas. The resulting large-scale motion of the air is strongly influenced by coriolis forces due to the earth’s rotation. The result is a large-scale global circulation pattern. Certain identifiable features of this such as the trade winds and the ‘roaring forties’ are well known. The non-uniformity of the earth’s surface, with its pattern of land masses and oceans, ensures that this global circulation pattern is disturbed by smaller-scale variations on continental scales. These variations interact in a highly complex and nonlinear fashion to produce a somewhat chaotic result, which is at the root of the day- to-day unpredictability of the weather in particular locations. Clearly though, under-
lying tendencies remain which lead to clear climatic differences between regions. These differences are tempered bymore local topographical and thermal effects.
Hills and mountains result in local regions of increased wind speed. This is partly a result of altitude – the earth’s boundary layer means that wind speed generally increases with height above ground, and hill tops and mountain peaks may ‘project’ into the higher wind-speed layers. It is also partly a result of the acceleration of the wind flow over and around hills and mountains, and funnelling through passes or along valleys aligned with the flow. Equally, topography may produce areas of reduced wind speed, such as sheltered valleys, areas in the lee of a mountain ridge or where the flow patterns result in stagnation points. Thermal effects may also result in considerable local variations. Coastal regions are often windy because of differential heating between land and sea. While the sea is warmer than the land, a local circulation develops in which surface air flows from the land to the sea, with warm air rising over the sea and cool air sinking over the land. When the land is warmer the pattern reverses. The land will heat up and cool down more rapidly than the sea surface, and so this pattern of land and sea breezes tends to reverse over a 24 h cycle. These effects were important in the early development of wind power in California, where an ocean current brings cold water to the coast, not far from desert areas which heat up strongly by day. An intervening mountain range funnels the resulting air flow through its passes, generating locally very strong and reliable winds (which are well correlated with peaks in the local electricity demand caused by air-conditioning loads). Thermal effects may also be caused by differences in altitude. Thus cold air from high mountains can sink down to the plains below, causing quite strong and highly stratified ‘downslope’ winds.
The brief general descriptions of wind speed variations in Sections 2.1 to 2.5 are illustrative, and more detailed information can be found in standard meteorological texts. Section 9.1.3 describes how the wind regimes at candidate sites can be assessed, while wind forecasting is covered in Section 2.9.
Section 2.6 presents amore detailed description of the high-frequencywind fluctua tions known as turbulence, which are crucial to the design and operation of wind turbines and have a major influence on wind turbine loads. Extreme winds are also important for the survival of wind turbines, and these are described in Section 2.8.
READ MORE - Geographical Wind resourcess
lying tendencies remain which lead to clear climatic differences between regions. These differences are tempered bymore local topographical and thermal effects.
Hills and mountains result in local regions of increased wind speed. This is partly a result of altitude – the earth’s boundary layer means that wind speed generally increases with height above ground, and hill tops and mountain peaks may ‘project’ into the higher wind-speed layers. It is also partly a result of the acceleration of the wind flow over and around hills and mountains, and funnelling through passes or along valleys aligned with the flow. Equally, topography may produce areas of reduced wind speed, such as sheltered valleys, areas in the lee of a mountain ridge or where the flow patterns result in stagnation points. Thermal effects may also result in considerable local variations. Coastal regions are often windy because of differential heating between land and sea. While the sea is warmer than the land, a local circulation develops in which surface air flows from the land to the sea, with warm air rising over the sea and cool air sinking over the land. When the land is warmer the pattern reverses. The land will heat up and cool down more rapidly than the sea surface, and so this pattern of land and sea breezes tends to reverse over a 24 h cycle. These effects were important in the early development of wind power in California, where an ocean current brings cold water to the coast, not far from desert areas which heat up strongly by day. An intervening mountain range funnels the resulting air flow through its passes, generating locally very strong and reliable winds (which are well correlated with peaks in the local electricity demand caused by air-conditioning loads). Thermal effects may also be caused by differences in altitude. Thus cold air from high mountains can sink down to the plains below, causing quite strong and highly stratified ‘downslope’ winds.
The brief general descriptions of wind speed variations in Sections 2.1 to 2.5 are illustrative, and more detailed information can be found in standard meteorological texts. Section 9.1.3 describes how the wind regimes at candidate sites can be assessed, while wind forecasting is covered in Section 2.9.
Section 2.6 presents amore detailed description of the high-frequencywind fluctua tions known as turbulence, which are crucial to the design and operation of wind turbines and have a major influence on wind turbine loads. Extreme winds are also important for the survival of wind turbines, and these are described in Section 2.8.
