284. 
E. Regener concerning separation in the atmosphere; 
for the equatorial zone it is assumed that the turbulence 
extends to higher altitudes corresponding to the greater 
altitude of the tropopause. The result of this calculation 
indicates a constant downward stream of ozone caused 
by turbulence. It follows that ozone must constantly 
be destroyed in the layers near ground level. The mean 
ozone distribution in the lowermost 15 to 20 km is de- 
termined essentially by the austausch. The small 
amount of total ozone in the tropical zone (O; = 0.185 
cm) is due to high-reaching turbulence combined with 
a rapid destruction of the downward transported ozone 
in the layers near the ground level, which seems plau- 
sible for tropical conditions. Disregarding the possibility 
of achieving a better agreement between theory (as 
indicated in Table III) and observation by making 
TasxeE III. Amount or Ozone AccorDING TO HQuation (31) 
(mm O3) 
p I Ut |) IONE) ihyy Vv VI | VII} VIIL| Ix xXx XI | XII 
45° |2.02/2.05)2.09/2.11/2.07|2.00}1.97|1.96)1.96/1.99/2.01)2.00 
60° |2.16)2.17)2.20)2.22)2.22/2.16/2.14)2.15)2.15}2.17/2.18)2.16 
80° |1.73/1.73)1.77/1.85]1.88}1.91)1.86)1.89}1.76)1.75)1.73)1.72 
Corresponding values, assuming a hypothetical circulation: 
60° |2.28/2.53/2.69}2.68}2. 53/2. 18/1.88}1.75)1.68)1.69)1.78|2.02 
different assumptions concerning several as yet un- 
certain quantities entering the calculations, it is possi- 
ble to improve agreement by assuming a meridional 
circulation. The last line of Table III is calculated under 
the assumption of an ascending flow in the higher lati- 
tudes of the summer hemisphere, and a descending 
flow in the higher latitudes of the winter hemisphere, 
the seasonal variations occurring primarily in the lower 
layers. 
Another circulation hypothesis by Craig [17] has not 
yet been calculated. Reed [80], on the other hand, sug- 
gests an explanation of the seasonal and zonal ozone 
fluctuations based on the variable large-scale atmos- 
pheric turbulence with a maximum in winter and at a 
latitude of 60°. Between fall and spring, this is supposed 
to cause more ozone to be transported down into the 
protected regions than can be. destroyed at ground 
level. During this period an increase in the total amount 
of ozone would consequently occur since the ozone 
transported to low altitudes is replaced at high altitudes. 
Between spring and fall, on the other hand, decomposi- 
tion at ground level presumably predominates so that 
there is a drop in the total ozone content. The discussion 
by Schr6er and Moser [71] will be dealt with in the fol- 
lowing section. 
OZONE AND WEATHER 
Ozone in the Stratosphere. According to Dobson, the 
amount of ozone varies with the atmospheric pressure 
distribution, that is, the synoptic situation. In western 
Hurope a maximum in the ozone amount is found on the 
rear side of a cyclone, aminimum of ozone is found above 
the southwest side of a high [25]. More recent studies 
concerning the connections between ozone amount and 
THE UPPER ATMOSPHERE 
the surface weather map and fronts have supported 
this observation [23, 94] and have shown that the 
center of high ozone amount on the rear side of a 
cyclone is particularly the property of a newly develop- 
ing depression (Fig. 12). Since its axis is inclined back- 
Soe ISOBARS Paes SS 
OZONE oe ‘S 
Fie. 12.—Depression with warm sector. 
wards, Palmén [72] was able to point out that the region 
of maximum ozone coincides with the tropopause vortex, 
that is, the trough at the tropopause, and that the 
ozone amount is symmetrical to the pressure distribu- 
tion at that height. Tropopause topography as well as 
ozone is explained as a common consequence of the 
three-dimensional air flow within a deepening cyclone. 
Thus, at the time at which one was still dependent upon 
statistical studies between ozone amount and the other 
atmospheric elements, Meetham [61] found the best 
correlations when referring all elements (variables) to 
a ‘“pseudo-center” 300 to 350 km to the southwest of 
the center of the surface pressure system; this pseudo- 
center corresponds to the tropopause vortex. According 
to Meetham, a 0.01-cm increase in the amount of ozone 
is accompanied bya 3C rise of the potential temperature 
at an altitude of 18 km and by a lowering of the tropo- 
pause by 1 km. The correlation coefficient between the 
ozone amount and potential temperature at an altitude 
of 18 km has the high value of 0.8, a fact which however 
should not induce us to seek the seat of ozone fluctu- 
ations at this altitude. Johansen [52], who conveniently 
groups the ozone measurements according to rise and 
fall regions of atmospheric pressure at ground level, 
also finds high ozone amounts with a low tropopause 
over Tromso. 
According to the preceding section, these conditions 
must be explained by the fact that meteorological 
transport processes displace the ozone from its source. 
Two main possibilities exist; the decision between them 
requires modern upper-air weather maps on the one 
