The summit of Ice Peak is about 280 metres (920 feet) lower than that of Mount Edziza, but it still rises well above the general level of the Big Raven Plateau.

[12][13] Mount Edziza Provincial Park is in the Tahltan Highland, a southeast-trending upland area extending along the western side of the Stikine Plateau.

[18][19] Between Tennaya, Nido and Tenchen creeks are pie-shaped, gently sloping interfluves which represent the remains of the original eastern flank of the Ice Peak stratovolcano.

[1][20] The southern and western flanks of the Ice Peak stratovolcano are approximal to those of the original volcano and merge with the Big Raven Plateau which is one of the main physiographic features of the Mount Edziza volcanic complex.

[21] Most of the vents in this lava field are at elevations above 1,800 metres (5,900 feet) near the terminus of outlet glaciers of the Mount Edziza ice cap, five of which named.

Both cones are younger than the main edifice of Ice Peak, but they have been greatly modified by glaciation, slumping and rockfalls due to their location near the steep headwalls of active cirques.

[8][31] Also on the western flank of Ice Peak where it merges with the surrounding Big Raven Plateau are the Koosick and Ornostay bluffs, which lie adjacent to the head of Sezill Creek.

[25][33] Ice Peak is part of the Northern Cordilleran Volcanic Province, a broad area of shield volcanoes, lava domes, cinder cones and stratovolcanoes extending from northwestern British Columbia northwards through Yukon into easternmost Alaska.

[9][34] The dominant rocks comprising these volcanoes are alkali basalts and hawaiites, but nephelinite, basanite and peralkaline phonolite, trachyte and comendite are locally abundant.

Another period of volcanic activity 0.3 million years ago deposited the Kakiddi Formation on the southwestern and eastern parts of the Ice Peak pile during the fourth magmatic cycle.

[43][44] Ice Peak Formation basalt flows on the northwestern flank of Mount Edziza are interbedded with diamictites recording a regional glaciation that occurred during the Early Pleistocene.

[45] The lowermost basalt flow contains basal pillows, directly overlies hyaloclastites and is brecciated and deformed, suggesting it may have been extruded onto a glacier or an ice sheet.

[45][46] Its extrusion onto glacial ice is also evident due to the lack of fluvial and lacustrine sediments at the base of the basalt flow which suggests it did not extrude into lakes or streams.

[45] The steep sides and unusually large thicknesses of the trachyte flows comprising Koosick and Ornostay bluffs is attributed to them having been extruded through glacial ice.

[48] The source of this Kakiddi flow remains unknown, but the tributary branch that descended Tennaya Valley probably originated from a vent near the summit of Ice Peak that is now covered by glaciers.

[49] A relatively small trachyte flow descended from Punch Cone on the western flank of Ice Peak and spread onto the Big Raven Plateau.

[56] Ice Peak is underlain by the Pyramid Formation, which consists mainly of Pleistocene rhyolite and trachyte flows, domes and thick piles of pyroclastic breccia.

[8][59] The southern edge of the Ice Peak pile laps out against Miocene comenditic or trachytic pumice and ash flows of the Armadillo Formation.