Wind Energy Meteorology: Atmospheric Physics for Wind Power by Stefan Emeis

By Stefan Emeis

This publication is meant to offer an advent into the meteorological boundary stipulations for energy iteration from the wind, onshore and offshore. it's to supply trustworthy meteorological info for the making plans and working of this significant form of renewable strength. This comprises the derivation of wind legislation and wind profile descriptions, particularly these above the logarithmic floor layer. Winds over advanced terrain and nocturnal low-level jets are regarded as good. a different bankruptcy is dedicated to the potency of huge wind parks and their wakes.

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By Stefan Emeis

This publication is meant to offer an advent into the meteorological boundary stipulations for energy iteration from the wind, onshore and offshore. it's to supply trustworthy meteorological info for the making plans and working of this significant form of renewable strength. This comprises the derivation of wind legislation and wind profile descriptions, particularly these above the logarithmic floor layer. Winds over advanced terrain and nocturnal low-level jets are regarded as good. a different bankruptcy is dedicated to the potency of huge wind parks and their wakes.

Show description

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Extra info for Wind Energy Meteorology: Atmospheric Physics for Wind Power Generation

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Equating the first two equations of the wind profile Eq. 55) for z = zp gives an equation for the friction velocity: uà ¼ jug ðÀ sin a0 þ cos a0 Þ lnðzp =z0 Þ ð3:56Þ and from equating the respective equations for the vertical wind shear at the same height z = zp we get a second equation for u*:   ð3:57Þ uà ¼ 2ug cjzp sin a0 These two equations must be valid simultaneously. Equating the right hand sides of these two Eqs. 57) yields the desired relation for the turning angle, a0: a0 ¼ arctg 1 1 þ 2czp lnðzp =z0 Þ ð3:58Þ Unfortunately, Eq.

For small negative values of z/L* the vertical wind profiles in the surface layer can be described by introducing a correction function Wm(z/L*) (Paulson 1970; Högström 1988):     1þx 1 þ x2 p ð3:15Þ Wm ¼ 2 ln þ ln À 2arctgðxÞ þ 2 2 2 where x = (1-b z/L*)1/4 and b = 16. This leads to the following description of the vertical wind profile which replaces Eq. 6): uðzÞ ¼ uà =jðlnðz=z0 Þ À Wm ðz=Là ÞÞ ð3:16Þ While the surface layer mean wind profile in the unstable surface layer depends on the local stability parameter z/L*, turbulence partly depends on non-local parameters as well.

Therefore, wind resource and load assessment cannot be done solely with the vertical profile relations and laws given in Sect. 1. The more complicated wind regime in the Ekman layer is to be considered as well. The equilibrium of forces changes when moving upward from the surface layer or Prandtl layer into the Ekman layer. In addition to the pressure gradient force and the surface friction, the Coriolis force due to the Earth’s rotation becomes important here as well. 4) must balance each other.

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