LARGE-SCALE ASPECTS OF ENERGY TRANSFORMATION OVER THE OCEANS 
sponding zonal values in each hemisphere. It may be 
noted that, except in the Indian Ocean, there exists no 
zone of high Q, values within the Southern Hemisphere 
to correspond to the equatorial zone of maximum @, 
found in the Northern Hemisphere. This results in an 
approximate ten-degree poleward displacement of the 
analogous Q, zones in the North Atlantic and North 
Pacific compared to the South Atlantic and South 
Pacific. In the case of the Indian Ocean, the situation is 
reversed. In this case the equatorial region of high Q, 
values exists south of the equator. Also, the northern 
1 QV 
< 150 1¢ 
a 
>150; <200 
1067 
The results of the computations indicate that the 
principal sources of heat energy for maintaining the 
general circulation over the oceans are in the equatorial 
regions and at the higher latitudes. The subtropical 
latitudes appear as regions where very little heat energy 
is being supplied to the atmosphere. In these latter 
regions the very large rate of energy transfer which is 
indicated by the Q, data does not make itself felt until 
it is released in the zone of equatorial convergence (01 
along the polar front at higher latitudes). The principal 
sources of heat energy for maintaiming the circulation 
Fig. 4.—The annual values of the rate of total energy gain by the atmosphere Qp;, both through the exchange of sensible heat 
with the sea surface Q, and through condensation Q,. The results are expressed in calories per square centimeter per day. 
Tapue VII. Seasonar VAtces or Q,, IN DirFeRENT LATITUDE ZONES (in cal em? day!) 
North Atlantic North Pacific 
North latitude zone 
Dec.-Feb. Mar.—May June—Aug. Sept.—Nov. Dec.-Feb. Mar.—May June-Aug. Sept.-Nov. 
0°-10° 237 229 330 217 268 249 292 261 
10°-20° 85 38 93 97 109 108 171 177 
20°-30° 109 55 62 112 157 110 109 104 
30°-40° 213 120 52 129 238 151 100 137 
40°-50° 268 140 87 164 218 149 119 184 
50°-60° 265 135 83 189 246 193 130 202 
part of the Indian Ocean exhibits greater seasonal 
variations in Q, than does any other portion of the 
oceans. 
Of greater interest from an atmospheric energy point 
of view, however, are the data concerning the rate at 
which total convective energy is acquired by the at- 
mosphere in the Northern Hemisphere, both through 
the condensation of water vapor and through the ex- 
change of sensible heat with the sea surface. The total 
energy Qn, is quite obviously the sum of these two 
quantities, that is, 
Qon = Qp SF Oi, cal em? day—t. (20) 
The annual chart of QQ, is given as Fig. 4 and the 
seasonal zonal averages are given in Table VII. 
at the higher latitudes are probably the western portion 
of the oceans (particularly in winter) and the central 
and eastern portions of the oceans, poleward from 
latitude 40°N. 
The existence of the seasonal and annual Q, and Qp, 
data for the North Atlantic and North Pacific allows 
the determination of the important quantity repre- 
sented by their difference. Because 
Qa — Qon = Gi On) Cine Qi) = Li (ai = 12) 
(21) 
the difference (Q, — Q x), when positive, represents 
latent energy which is locally surplus and available 
for transport to the continents or other portions of the 
oceans where it is made available as real heat through 
