UNCONFOEMITY AT BASE OF LOWEK MARQUETTE SERIES. 559 



the Basement Complex. In all of the cases the detritus is inost distinctly 

 waterworn, and while the major portion of the material in each case must 

 have been derived from the immediately subjacent part of the Basement 

 Complex, other material not occurring in the immediate neighborhood is 

 found, thus showing conclusively that these rocks are not reibungs or 

 fault breccias. The evidence is therefore demonstrative that the Lower 

 Marquette series was deposited unconformably iipon the Basement Complex. 

 As explained later, it will be seen that locally, as a result of the power- 

 ful dynamic action to which the rocks have been subjected, the foliation of 

 the Basement Complex and that of the basal quai-tzite are in the same 

 direction, and that at certain localities the basal conglomerate and quartzite 

 have been so mashed as to pass into completely crystalline schists, which 

 appear to grade down into the foliated schist or gneiss of the Basement 

 Complex. As a consequence, the granites of the Basement Complex have 

 been described by certain geologists as intrusive within the Lower Marquette 

 series. Others have said that it is a case of downward-progressing meta- 

 morphism. Taking into account the above facts as to the contacts and 

 conglomerates, there is no escape from the conclusion that this apparent 

 conformity and gradation are illusory, being produced by the metamor- 

 phosing processes of profound dynamic action and metasomatic changes. 



DEPOSITION OF THE LOWER MARQUETTE SERIES. 



In the earlier part of Lower Marquette time, the sea steadily trans- 

 gressed southwestward from the northeast, depositing a basal conglomerate 

 as it advanced. As soon as the sea had progressed a little beyond a given 

 place, the deposition of sandstones there replaced that of the conglom- 

 erates. (See Atlas Sheet IV.) By the time the sea had transgi'essed as far 

 as Teal Lake on the north and Goose Lake on the south, argillaceous and 

 siliceous limestones began to be deposited in the east end of the district, and 

 hence the western limit of the Mesnard quartzite is placed at these localities. 

 The Koua dolomite probably marks deeper and quieter waters, and therefore 

 indicates that depression had been continuing. A thin layer of slate marks 

 intermediate conditions between those favorable to the deposition of sand- 

 stone and those in which the limestone was deposited. However, the area 



