THE PHYSICAL EVOLUTION OE ACADIA. 
7 
The lower portion of this division of the Huronian system 
in New Brunswick is of granitic grits and coarse clay-slates, 
having numerous chloritic schists and igneous intrusions in the 
eastern exposures; but in the Passamaquoddy district dark 
clay-slates with whin-stone beds or diorites prevail. In this 
division are most .of the metallic mineral found around 
Passamaquoddy Bay. 
In the more central part of Charlotte County, to the west- 
ward, these slates are heavily charged with sulphurets, chiefly 
of iron, but having also copper and nickel ores. 
The upper division of the Huronian system (“ Kingston 
series or terrane”) consists chiefly of igneous rocks, and pre- 
vailingly of volcanic deposits. It does not everywhere run 
concurrently with the lower division for, though adjacent to it 
in Kings County, is separated in Charlotte County by a dome or 
ridge of Laurentian gneisses and limestones. This division is 
very uniform in the character of its rocks, and extends north- 
east in New Brunswick from Beaver Harbor for a distance of 
seventy miles with a width of about five miles, to where it 
passes beneath later Palaeozoic formations and is lost to view. 
The magnetic iron-ore deposits of Lepreau, or New River, 
are in this mass of volcanic rocks. 
The Huronian terranes in southern New Brunswick, as a 
whole, are intimately associated with the Laurentian and form 
bands of strata alternating with the Laurentian masses. Of 
these, the most easterly exposed extends from Bellisle, in Kings 
County, to Beaver Harbor, in Charlotte County; a branch of this 
passes to the islands of Passamaquoddy Bay. Another belt 
of these rocks lies to the north-west of the granitic and gneissic 
area at the St. Croix river, near St. Stephen, in the latter county. 
In the very remote age in which this system was deposited 
it would seem that the earth’s crust, in this region, was already 
being thrown into those parallel north-east to south-west folds, 
which have marked it in all subsequent time, and the causes 
which now operate to squeeze and disturb the strata here were 
active even then. Perhaps the most distinct proof of this 
pressure and consequent dislocation is the sharp line bordering 
