44 
described presently. The five higher formations of the Chaleur series 
continue the earliest Clinton of the Clemville formation without inter- 
ruptions, probably to the close of Lockport time. On Anticosti there is 
now nothing younger than the Clinton and Rochester equivalents, all 
the younger formations having been eroded away. The proof of this 
erosion is seen in the presence of the Chaleur series, which lies in the same 
trough as that on Anticosti, and the various faunas of the Chaleur show 
that the Niagaran ones of interior America probably came largely from 
the St. Lawrence geosyncline and northwestern Europe. When the 
Silurian faunas of Anticosti and Quebec are fully described, it probably will 
be seen, that many of the species now best known from the Chicago-Racine 
area are also common to the St. Lawrence trough. All of us have heretofore 
been inclined to agree with Weller that most of the interior faunas came 
from the Arctic realm, and whereas some of them did, most of them were 
in connexion with the St. Lawrence sea and so on to Europe. 
Clemville Formation 
The “Ordovician” strata of Little Port Daniel river, about Clemville, 
appear to go unbroken into the earliest Silurian strata now to be described. 
This probably means that the basal beds of the Silurian have not been seen, 
and it is certain that the boundary with the graptolitic Ordovician has 
not been delimited. 
The fossiliferous Clemville formation is at least 385 feet thick and goes 
unbroken into what Ells has mapped as Ordovician. No difference was 
seen in the dips and strikes between them. Moreover, the lithology 
changes gradually from these higher, more or less calcareous rocks, to the 
older greenish shales that are interbedded with feldspathic sandstones 
and conglomerates having large pebbles of the Macquereau series. It 
may well be, therefore, that much more of Ells’ Ordovician is also Silurian, 
and it may be shown that the whole of his Ordovician is early Silurian 
and highest Ordovician (Richmondian and Gamachian). 
The Clemville formation outcrops in the banks of Little Port Daniel 
river at Clemville, which is about a mile north of Port Daniel Centre, or 
less than 2k miles in an air-line northwest of the Catholic church of St. 
Georges de Port Daniel. Here, where the wagon road crosses this stream, 
beneath the bridge, are exposed the so-called Ordovician strata of dark 
greenish, thick-bedded, feldspathic and conglomeratic sandstones; the 
pebbles are mainly of older Ordovician slate with admixtures of the older 
Macquereau series. A few hundred feet upstream from the bridge, on 
the northern bank, occur blue-green shales with scattering thin-bedded 
sandstones having a strike of north 60 degrees east, dip 75 degrees north- 
west. These strata, of undetermined age, are also seen in a high bank 
one-fourth to one-half mile downstream, and all are below the fossiliferous 
Clemville formation to be next described. 
About one-fourth mile upstream from the above-mentioned bridge 
across Little Port Daniel river, there is a low but fine exposure along the 
southern bank, and here some of the beds are rich in fossils. The following 
descending series was measured: 
