Wind around a building causes driving rain on the envelope of the building. Without wind there is no driving rain. The atmospheric boundary layer (a.b.l.) is the layer close to the Earth's surface, in which wind is directly influenced by friction with the Earth's surface. Its height ranges from hundreds of metres to a few kilometres and depends on the intensity of thermal mixing (convection), terrain roughness and latitude. The atmospheric surface layer (a.s.l.) is the lowest 1020% of the a.b.l., where shear is approximately constant with height and production of turbulence is high. The a.s.l. over a uniform flat terrain in a neutral boundary layer is characterised by a wind velocity increasing with height and a wind direction being nearly constant with height.
Due to spatial changes in surface roughness, internal boundary layers (i.b.l.) develop, in which wind speed and direction are modified by the properties of the surface (obstacles), while the top of the i.b.l. flow is the wind velocity adjusted to the terrain conditions before the roughness change. The thickness of the i.b.l. increases downstream of the roughness change.
In the following we will only pay attention to a neutral boundary layer, i.e. an atmospheric situation in which vertical heat transfer is negligible.
The mean wind speed in the a.s.l. as
a function of height is expressed by the socalled ``logarithmic law'':
The friction velocity is defined by:
(2.3) 
Displacement height and roughness length are measures for the roughness of a terrain. A classification of typical values is presented in Wieringa ([Wieringa 1992], [Wieringa 1996]). Some typical values are listed here:
[m]  landscape 
0.0002  open sea or lake 
0.03  flat terrain with grass, airport runways 
0.10  moderately open country with low vegetation and occasional obstacles separated by more than 20 obstacle heights (e.g. low hedges, single rows of trees) 
1.0  closed and regularly covered terrain; open spaces up to (e.g. city, mature forests) 
The logarithmic law (eq. 2.1) applies only for:
In the literature one finds several approaches for a relation between wind above two adjacent terrains with different roughness properties. Here, we investigate an abrupt roughness change according to two models. Figure 2.1 sketches the situation. The quantities on the terrain upwind from the change will be denoted by index 1, downwind by index 2.
Internal boundary layer model According to the internal boundary layer model described in [Simiu and Scanlan 1996], it is suggested that the wind velocity at the top of the i.b.l. ( ) on the second terrain equals the velocity at the same height on the first terrain.
The height of the i.b.l. at a distance [m] from the roughness change
is [Simiu and
Scanlan 1996, p. 73]:
An example is given to calculate the wind speed at a position A at 45 m above
ground level in a town (denoted by ) with a known wind
speed at 10 m height at a weather station outside the town
().
The distance from A to the town border is km. The weather station is
on grass covered terrain, so
m. The roughness of the
town is m and the displacement height is m. So,
position A at 45 m height is above
.
According to equation 2.4,
equals
250 m. The relationship between the mean wind speeds at 10 m and 250 m height
at the weather station is calculated from the logarithmic law:
This yields .
According to the i.b.l. model the wind velocity at A at i.b.l. height
approximates the wind velocity at the weather
station at the same height, so:
The wind speed at 45 m height at A is:
Similarity model
The second approach is referred to as the similarity model
[Simiu and
Scanlan 1996, p. 48]; the ratio of friction
velocities is empirically estimated from the ratio of roughness lengths:
(2.5) 
For the above example, this approach yields .
The present example shows that the two methods yield different results. The example reflects the site used in the study reported in this thesis. Measurements at this site yield according to [Geurts 1997] and according to our own measurements (see section 5.2.1). These values differ 20% from each other and the estimations differ to a similar extent. This is an indication of the error that has to be taken into account when estimating weather station vs. local wind speed ratios. (Note that for this example changing into 1.5 m and/or into 0.1 m will yield a difference of 310% in the estimated ratios.) The ratio at our site is discussed in [de Wit et al. 2002] too.
Turbulence in wind causes variation of wind velocity in time and space.
Turbulence is often considered as a superposition of eddies with different sizes
transported by the mean flow. The simplest characterisation of turbulence is by
turbulence intensity, defined as the ratio of the rootmeansquare of the
fluctuating component of the longitudinal wind velocity and its timeaveraged
value:
(2.6) 
Similarly one defines lateral and vertical turbulent intensities and , respectively.
The total mean turbulent kinetic energy (per unit of mass) is
defined as:
(2.7) 
As shear is approximately constant with height in the a.s.l., the friction velocity is also approximately constant. The standard deviation of wind speed normalised by is therefore also a measure of turbulence in the a.s.l. Typical values, obtained by measurements, are presented in table 2.1.
[Panofsky and Dutton 1984]  [Geurts 1997]  
2.4  2.41  
1.9  1.91  
1.25  1.37  
5.5 
In the previous subsections we focussed on undisturbed wind. Describing wind patterns nearby buildings and in urban canopies (i.e. beneath the average roof height in towns) is quite difficult because many parameters and especially topography and building geometry are involved. Beranek ([Beranek 1994b], [Beranek 1994a]) and [Bottema 1993b] discuss this topic. We will first discuss the most important characteristics of the flow nearby a free standing building, bearing in mind that these characteristics should be useful for the evaluation of CFD simulations and that for a study on driving rain the lee side of a building is less interesting. Figure 2.2 shows a sketch of the time averaged wind pattern nearby a wide building in the atmospheric boundary layer. Its characteristics are (for more details, see e.g. []p. 80 and further]bottema:1993):

The complexity of flows in building groups is of course larger than near a single building on an unbuilt plane. Yet three typical flow regimes are distinguished, depending on the ratio of building height and distance between the buildings. Figure 2.3 shows these for a two dimensional configuration.
We use two definitions for the wind velocity vector. The first one, which we will use most frequently, is a globally defined axis system, i.e. relative to north (see figure 2.4):
The following quantities are derived from the wind velocity components:
(2.8) 
(2.9) 
The second definition is related to the mean wind direction:
© 2002 Fabien J.R. van Mook