246 MALKUS [chap. 4 



Now equations (27a) and (28a) are used in the form 



Qs = Cp \\ pdu-nda -^ Cpy M^O (27d) 



and 



Qe = {{ pLqu-ndG = 2 Jf.Lg, (28d) 



where a steady state is assumed in the inflow layer ; radiation terms are negli- 

 gible over these short times, and condensation conversion only affects the air 

 vertically exported from the box of surface area a. As in the trades case, Qs 

 and Qe are for the whole oceanic area below the air considered and must be 

 divided by this area to compare with the transfer formulas. On the right sides 

 of the expressions actually used for the calculation, M„ is the mass flux in 

 g/sec through each face of the box considered. 



Radial and vertical fluxes of sensible and latent heat may be computed from 

 the data in Tables XVII and XVIII. These fluxes and the heat sources required 

 for balance are shown in Table XX and Fig. 71, These diagrams were derived 

 as follows : the mass flux through each vertical face (at r = 90, 70, 50 and 30 km) 

 was obtained from M = Ur- r'lrr 8plg, where Ur-r is taken from the dynamic 

 calculation (Table XVII, column 5). The mass flux through the top face, AM, 

 is the difference between the horizontal fluxes through the successive vertical 

 faces. Mass leaving through the top of each box was assumed to go out with the 

 mean property of the air in the box. Heat sources were calculated as residuals 

 to meet continuity. Over the area within the core, the source is 5.38 x 10^2 cal/ 

 sec latent heat of water vapor and 1.60 x lO^^ cal/sec sensible heat, a total of 

 6.98 X 1012 cal/sec. It is interesting to note that this is nearly 1% (Table I) of 

 the entire heat energy exported from the tropics and 3|% of the poleward 

 transport of the Atlantic ocean-current systems (Fig. 12)! It corresponds to a 

 total heat increment to the air of 2.50 cal/g, within computational error of the 

 result of Table XIX. 



Table XXI compares the sensible and latent heat fluxes in cal/cm^ per day 

 from the budget method with those computed from transfer formulas (20) and 

 (21). Agreement is extremely good. The most important result of Table XXI is 

 that the ordinary formulas and coefficients are easily adequate to meet the exchange 

 requirements of the moderate hurricane. No special demand is created during 

 transition from trade-wind speeds of 5-7 m/sec to hurricane velocities for an 

 increase of the transport efficiency of the energy spectrum near the ground. 

 No impossible or difficult restriction is made when it is postulated that the 

 lowering of surface pressure in hurricanes depends upon an "extra" oceanic 

 heat source in a storm's interior, although it would be extremely interesting to 

 pursue further the effects upon the ocean-surface layers of the abstraction of 

 this much heat during hurricane passage. 



Comparison with Table II shows that the actual transports in the hurricane 

 are very large indeed compared to the trades. Sensible heat pick-up is 720 cal/ 

 cm2 per day, an increase of sixty times over the trades ; the increase in Tq — Ta 



