IQO T. C. CHAMBERLIN 



into the Florida Current (Gulf Stream) and similarly the tropical 

 waters of the Pacific into the Japan Current, and by so doing restrain 

 their spreading in their journey to the north, they would fail to raise 

 the temperature of any given area in high latitudes as effectively 

 as they do now. On the other hand, if the warm waters from the 

 low latitudes are concentrated into deep streams by convergent 

 lands, or better still if they are forced to flow poleward as deep cur- 

 rents protected from surface agitation by winds and from the radi- 

 ation enhanced by these winds, they will be more effective carriers 

 of heat to the high latitudes. 



While some other theoretical considerations might be added, 

 the foregoing confirm the inductions drawn from the preceding 

 comparisons and give them great cogency. Observation and theory 

 together make a clear and decisive case. The conclusion may 

 therefore be drawn with great firmness that extension of sea in high 

 latitudes, in itself considered, normally renders the climate cooler 

 than it would he if no extension took place. It is to be scrupulously 

 noted that this conclusion applies simply to the alternative of sea 

 and land, not to special influences super-added on either side, such 

 as warm currents, on the one side, or cold currents and great eleva- 

 tions of land surface, on the other. These super-added features are 

 of course to be dealt with on their own account as special influences 

 arising from super-imposed causes. 



While the evidence is thus decisive against the assumed warming 

 effects of sea extension in itself, a study of the evidence makes it 

 clear that the ocean is a very effective climatic agency both in raising 

 and in lowering regional temperatures in response to co-operating 

 conditions. 



This influential action has two phases that are to be distinguished 

 in the study of geologic climates: (i) transient effects, and (2) 

 secular effects. It is obvious that the superficial effects of the 

 ocean are transient because the resulting temperature of the air 

 is soon changed by radiation and the moisture supplied to the air is 

 soon precipitated. If an effect is to be perpetuated by these means 

 there must be a constant renewal of the activity. On the other hand, 

 a prolonged effect may be produced by the great capacity of the 

 ocean to store and retain heat, and this stored heat may be trans- 



