The intrusion was originally described as the “Rivière Boisvert Pluton” by Daigneault and Allard (1983, 1984) and Daigneault (1986). It is more simply described as “Boisvert Pluton” in more recent publications (Daigneault, 1991; Roy et al., 2005).

According to Roy et al.,, (2005, p. 12), the Boisvert Pluton is “composed of leucotonalite (trondhjemite) and two mica granodiorite with a minor amount of tonalite or diorite richer in mafic minerals. It is white, locally pinkish or brownish, in altered patina and light grey in fresh exposure. It is medium grained and foliated, highlighted by the alignment of micas that tend to concentrate in clusters. It is intensely foliated to mylonitic at its western contact with mafic volcanics of the Obatogamau Formation. This contact also corresponds to the Lac Dufresne Deformation Zone interpreted as the western limit of the Grenville Front Tectonic Zone. At its southeastern edge, banding gradually increases towards tonalitic gneiss and contact is diffuse. Along NNE faults that cut the Boisvert Pluton, leucotonalite is heavily altered in epidote, hematite and chlorite and has undergone brittle to ductile deformation. The Boisvert Pluton is cut by numerous intrusions or veins, usually of pegmatitic granite. Granitic mobilisate derived from partial melting is locally present but of minor importance (<5%). Amphibolite enclaves are common in the pluton and can reach up to 5 km long by several hundred metres thick. They consist of fine to medium-grained banded garnet amphibolite. In leucotonalite and granodiorite thin sections, microcline is observed as small interstitial grains, which highlights the relatively potassic character of the Boisvert Pluton in comparison to other felsic intrusions in the region. Quartz often forms lenticular grain clusters. The most important mafic minerals are green biotite, epidote and muscovite. Hornblende and garnet are scarce. The most common accessory minerals are titanite, allanite, magnetite, rutile, apatite and zircon.”