280 
average is given below: 
cm cm cm 
January 0.014 May =+0.008 September 0.007 
February ++0.014 June +0.006 October +0.007 
Mareh 40.012 July 0.005 November +0.605 
April +0.012 August 0.006 December +0.098 
It is apparent that the fluctuation is twice as great in 
winter as it is in summer and fall; in winter, as well as 
in spring, it is considerably greater at Troms6 than it 
= 
serceeees TROMSO 
SSS 
—AROSA 
0.220} 
0.21 Of 
0.200} °~ AUTUMN 10.250 
0.240 
0.230 
0.290} N SUMMER fp 220 
0.280} — 6 
0.270 
0.260} S 
iW SPRING [OBO 
S VW 0.240 
s WINTER J(Q-230 
(Ss) H 
aca | YEAR 
0.240} h 
0.230} Al? 
0.220} 
wit 41 AF DONRDODOHAMTDON 
AIKAIBOMMMMMMOMMITTIS SSS 
oO 
Fra. 8.—Secular fluctuation of the ozone amount. Vertical 
broken lines represent sunspot minima; vertical solid lines, 
sunspot maxima. 
is at Arosa; the series is thus subject to the same in- 
fluence which also causes the meteorological (imter- 
diurnal) variability. If one were to seek a direct cor- 
SMALL OZONE AMOUNT 
0.200 CM 
UMKEHR EFFECT AROSA 
MEDIUM OZONE AMOUNT 
0.260-0.270 CM 
SOUNDING BALLOON 
THE UPPER ATMOSPHERE 
relation between ozone and solar activity, then the 
double fluctuations of the Eurasian large-scale weather 
within the sunspot cycle according to Baur [7] would 
be of interest. In the lower yearly average curve of 
Fig. 8, the vertical solid lines represent sunspot maxima, 
the vertical broken lines represent sunspot minima. 
For the yearly averages the following correlation co- 
efficients are obtained. 
Correlation 
coefficient 
Ozone and relative sunspot number........... +0.01 
Ozone and air pressure....................... —().43 
Ozone and solar constant..................... +0.48 
As regards the analysis of other long series of observa- 
tions, there exists only the attempt [11, 93] to determine 
ozone by means of the Chappuis band from the Smith- 
sonian measurements. Even though wide scattering of 
these values makes them seem rather unreliable, it is 
nevertheless interesting to note the very slight ozone 
amount during the year 1912 since it has been ascribed 
to an effect of the eruption of the Katmai Volcano [87]. 
Such a possibility has also been discussed by Hi. Regener 
[84]. 
The Vertical Distribution of Ozone. The vertical dis- 
tribution of ozone, first of all shows a high primary layer 
of maximum ozone content at an altitude of 20 to 25 
km. Its stratified character is more pronounced the 
smaller the total ozone amount. The layer thickens as 
the ozone amount increases, owing to meteorological 
HIGH OZONE AMOUNT 
0.340 AND 0.400 CM 
UMKEHR EFFECT TROMSO 
STUTTGART 
--—-— STRATOSPHERE 
FLIGHT U.S.A. 
secoseeee THE SAME, REVISED 
KILOMETERS 
O 0.004 0.008 0.012 0.016 
--—- V-2 WHITE SANDS 
0 0.004 0.008 0.012 0.016 
0.340 CM 03 
---= 0.400 CM 03 
I 
eee — — 
QO 0.004 0.008 0.012 0.016 
CM O3 PER KM 
Fig. 9.—Vertical ozone distribution. 
