first interpolated in time, and then vertically

averaged through the layer from the grid point

mixing height to the selected level (e.g., 700

mb). The winds at grid point (i,j) are obtained

from the previous equation, with the summation

over rawinsonde stations instead of surface

stations. Only rawinsonde stations within a

'scan-radius' of the grid point are considered.

Level 1 winds are the layer average between the surface and the

mixing depth.


Figure 2b - Wind Vector Plot for July 21, 1984, 1200 LST.

Level 2 winds are between the mixing depth and 700 mb.

Figures 2a and 2b are examples of the wind fields generated by

the MESOPUFF processor for July 21, 1984 at 1200 LST. The

effects of the 'scan-radius' and the influence of a deviant

surface station on the calculation of mixed layer average

(Level 1) winds can be seen in the vicinity of Richmond. There

are also some aberrant winds generated in the vicinity of

Philadelphia. It appears, however, that the model is

generating a sea breeze along the coastal areas. The Level 2

winds are generally fairly smooth and uniform.

The ARM3 takes a somewhat different approach to

calculating the wind field for the region of interest. The

ARM3 meteorological processor was designed to account for the

influence of terrain on the wind fields over a data sparse

area. The ARM3 processor computes a three dimensional wind

field. The ARM3 air quality model can use the vertical

velocities, generated by the meteorological processor, to

transport puffs. However, vertical velocities generated by

diagnostic wind models over complex terrain are highly suspect

and are not recommended for use in the air quality model.

Therefore, the remaining discussion will only pertain to the

formulation of the horizontal components of the wind, although

some of the procedures for calculating the vertical component

can influence the calculation of the horizontal components.



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