55 
The second terrace about Gascons is as a rule very narrow and rises 4 
feet to the second cliff of about 10 feet elevation. On much of this terrace 
the railway is placed. The inshore cliffs of the first and second terraces 
are drawn on the map, the second terrace going west to An se-A-la-B arb e . 
East of Chouinard brook other and higher terraces are seen. The 
slope of the third terrace here rises 10 feet, with a cliff back of it 20 feet high. 
There is a fourth but much eroded terrace, the first to come out of the 
Pleistocene submergence. The height of the three terraces up to the 
base of the fourth is about 90 feet above the present sea-level. 
East of Gascons along the King’s road, ascending the Macquereau 
strata, two sets of glacial strise are seen, one striking north 20 degrees west, 
the other north 30 degrees east. Both sets strike into Chaleur bay. 
Along the entire shore of the Port Daniel-Gascons area may be seen 
somewhat large, erratic stones that have come from the interior highland 
to the north. Most of these are of ancient metamorphosed formations, 
like greenstones, schists, and arkosic conglomerates. Granites are rare, 
but one grey granite mass was seen with dimensions of 10 by 7 by 5 feet. 
There are also boulders of the Ordovician and Macquereau. Nowhere, how- 
ever, does one see moraines or glacial deposits, only the scattered erratics, 
and sea-fill material. 
IGNEOUS ROCKS 
The only igneous rock seen in our area forms a dyke 15 feet across, 
cutting vertically the deformed Silurian strata near the northern end of 
anse aux Gascons beach. On either side of the dyke rock, the Silurian 
shales are baked red and hardened. The age of this intrusive is, therefore, 
later than the Devonian deformation. The composition of this dyke has 
been determined by Professor Adolph Knopf of Yale University to be 
that of an anorthosite porphyry. He describes it as follows: 
“The dyke from Gascons cove proves to be a rock of uncommon type and is best 
designated an anorthosite porphyry. It is a grey rock containing numerous phenocrysts 
of glassy plagioclase in a microgranular groundmass. The plagioclase crystals constitute 
roughly 20 per cent of the bulk of the rock; they are of thin, tabular habit, averaging one 
centimetre in diameter, and are roughly m parallel alignment. Under the microscope, 
they are found to be a sodic labradorite (Ab^An^). The groundmass is composed largely 
of tabular plagioclase in seriate development, the largest individuals, however, being 
much smaller than any of the phenocrysts. Chlorite occurs in small amount in the 
triangular interspaces between the plagioclase laths and is undoubtedly derived from 
what little ferromagnesian mineral was originally present. Secondary calcite is more 
or less abundant and has resulted from alteration of the feldspar. Magnetite in small 
octahedrons, ilmenite in thin plates, and apatite in aeicular prisms are relatively abundant 
accessory minerals. They appear to have separated out at a late stage of magmatic 
consolidation, as none of them occurs as inclusions in the large porphyritic crystals. 
“On account of the marked preponderance of plagioclase in the makeup of this rock, 
the most appropriate name for it appears to be anorthosite porphyry.” 
THE SILURIAN SUCCESSION OF BLACK CAPE 
About 45 miles west of the Port Daniel area occurs a most interesting 
Silurian sequence that is exposed continuously along the seashore for nearly 
2 miles. The strata have an average dip of 60 degrees southeast, and are 
a part of one limb of an extensive anticline. The section begins near the 
base of the Silurian and appears to go without repetition or break into the 
higher Silurian of the Port Daniel sequence, our West Point or Crotalocrinus 
