l/iiIc\s staled otherwise, the calculations assumed k = 0.35 (Businger cr
d., 197 I ) and 45 'N latitude.
5. I. Grosrroplric* Drug Law.
nekes, 1973) show that the "geostrophic drag law" is
Asyniptotic similarity arguments (Hlackadar and Tennekes, 1968; Ten(23)
+
(kZG' 11: - A2)I
G
G
In
= B + l n
12"
u*
where ,4 and B are constants defined by
(24)
A = - k k ; / i i + ,
B = In(ic,/f&,) - kU,/u,
Some use a different convention in which .4 and B are reversed.
Our calculations are consistent with this drag law and for the chosen
model constants gave A = 2.3, B = 1.8. They are somewhat sensitive to von
Karmhn's constant; for k = 0.40 the values were A = 2.5, B = 1.1. Similarity theory ignores any possible latitude dependence of A and B, but some
would be expected because both J' and j c o t 4 appear in the stress
equations (3); hence, j'alone cannot completely account for latitude effects.
Between 15 and 9 0 ' . the calculated variations in A and B were only about
5 ?,,, however.
A and R are notoriously difficult to determine experimentally, and the
scatter in observations precludes any detailed testing of model calculations.
Caldwell el a/. (1972) have tabulated A and B values from several sources.
both experimental and model calculations. A values (in our convention)
range from 1.5 to about 5, and B from - 1.6 to 2.5.
5.2. Titrhitlcrice Distributions
Our calculated turbulence profiles are nondimensionalized with 11, and,f
in keeping with the asymptotic similarity theory prediction (Blackadar and
Tennekes. 1968) that these are the appropriate scales outside of the surface
layer.
Figure 1 shows calculated turbulent energy distributions for a range of
values of the transport coefficient a,. Below ;f;/u, = 0.1 (which corresponds
to z = 300 m i f 1 = 10 sec- ' and u* = 0.3 m scc- '), varying a, by a factor
of two from our normal value of 0.15 has negligible effect. Figure 1 also
shows good agreement between our curve for a, = 0.15 and Deardorffs
rcsult. Figure 2 shows the disiributions of energy components.
d., 197 I ) and 45 'N latitude.
5. I. Grosrroplric* Drug Law.
nekes, 1973) show that the "geostrophic drag law" is
Asyniptotic similarity arguments (Hlackadar and Tennekes, 1968; Ten(23)
+
(kZG' 11: - A2)I
G
G
In
= B + l n
12"
u*
where ,4 and B are constants defined by
(24)
A = - k k ; / i i + ,
B = In(ic,/f&,) - kU,/u,
Some use a different convention in which .4 and B are reversed.
Our calculations are consistent with this drag law and for the chosen
model constants gave A = 2.3, B = 1.8. They are somewhat sensitive to von
Karmhn's constant; for k = 0.40 the values were A = 2.5, B = 1.1. Similarity theory ignores any possible latitude dependence of A and B, but some
would be expected because both J' and j c o t 4 appear in the stress
equations (3); hence, j'alone cannot completely account for latitude effects.
Between 15 and 9 0 ' . the calculated variations in A and B were only about
5 ?,,, however.
A and R are notoriously difficult to determine experimentally, and the
scatter in observations precludes any detailed testing of model calculations.
Caldwell el a/. (1972) have tabulated A and B values from several sources.
both experimental and model calculations. A values (in our convention)
range from 1.5 to about 5, and B from - 1.6 to 2.5.
5.2. Titrhitlcrice Distributions
Our calculated turbulence profiles are nondimensionalized with 11, and,f
in keeping with the asymptotic similarity theory prediction (Blackadar and
Tennekes. 1968) that these are the appropriate scales outside of the surface
layer.
Figure 1 shows calculated turbulent energy distributions for a range of
values of the transport coefficient a,. Below ;f;/u, = 0.1 (which corresponds
to z = 300 m i f 1 = 10 sec- ' and u* = 0.3 m scc- '), varying a, by a factor
of two from our normal value of 0.15 has negligible effect. Figure 1 also
shows good agreement between our curve for a, = 0.15 and Deardorffs
rcsult. Figure 2 shows the disiributions of energy components.