152 



possible that the difference in the quaHty of the Gravels a and 

 B, is due to a change of climate, the disintegration being less 

 as the climate became milder. The upper Gravel bed may, 

 therefore, be comparatively modern. The surface of the Lake 

 is now about 20 feet below the bottom of the Gravel Pit. 



[Fig. 2. Gravel Pit at Hyde House.] 



The peculiar situation of this deposit has been already 

 described. If we suppose an accumulation of snow to have 

 taken place periodically in the angle formed by the steep face 

 of the Great Oolite, and the comparatively level surface of the 

 denuded Fuller's Earth, the spring rain, while it removed the 

 snow elsewhere, would leave a considerable drift, as shown by 

 the dotted line in the section, which becoming frozen, would 

 form a slippery incline, down which the detritus from the Great 

 Oolite would be easily carried by the surface water, to the site 

 of the gravel beds below ; while the disappearance of the snow 

 lower down the hill would, by presenting a rougher surface, 

 retard, if not wholly prevent, its further transport. 



[Fig. 3. Deposit of Gravel at Pitchcomhe.] 



This must have taken place before the valley was worn down 

 to its present depth. The gravel was probably brought down 

 the Combe, and deposited at its junction with the Painswick 

 valley. It was clearly not derived from the disintegration of 

 the rocks forming the spur, inasmuch as in the upper part of 

 the bed the gravel is on the top of the spur. 



Sections might be multiplied, but the above examples are 

 given by way of illustration of the various situations in which 

 the Gravel is found, and the manner in which it has been 

 deposited. It more generally occurs just below the base of the 

 Freestone beds of the Inferior Oolite, where that formation has 

 no capping of Great Oolite ; but in other instances, it is more 

 abundant upon the slopes of the Fuller's Earth. 



