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The Chilcotin Group, also called the Chilcotin Plateau Basalts, is a medium-sized large igneous province that forms a volcanic plateau running parallel with the Garibaldi Volcanic Belt in south-central British Columbiamarker, Canadamarker.

Predominantly, during Miocene and Pliocene times, a medium sized volcanic field of overlapping vents occurred in British Columbia's Interior Plateaumarker. The distribution is assumed to engulf up to 50,000 km2 of the Pacific Northwest, forming a medium-sized large igneous province. Volcanism occurred as late as Oligocene time, but continues sporadically up to present. Eruptions were most vigorous 6-10 million years ago and 2-3 million years ago, when most of the basalt was released. Less extensive eruptions continued 0.01 to 1.6 million years ago.

These lava flows have been dominantly exposed by erosion resulting from the great floods that flowed in this region throughout the past ice ages, which laid bare many layers of the basalt flows along the Fraser Canyonmarker from Soda Creekmarker south to Canoe Creek elsewhere along the Chilcotin, Chilkomarker, Chilankomarker and Taseko Riversmarker at Chasm Provincial Park along Upper Deadman Rivermarker. Prior to Late Pleistocene glacial erosion these centers formed a series of coalesced, low-profile shield volcanoes of unknown volume and distribution.

The Chilcotin Group were thought to potentially be linked to the Columbia River Basalt Group in the United Statesmarker, which are coeval and lie across parts of the states of Washingtonmarker, Oregonmarker, and Idahomarker to the south. However, its morphology and geochemistry have been proven much similar to other volcanic plateaus such as the Snake River Plain in Idaho and parts of Icelandmarker (Bevier, 1983).

Formation of the Chilcotin Plateau Basalts

Cliffs made of low viscosity lava flows in Chasm Provincial Park suggest extensive volcanic activity in the Chilcotin Plateau Basalts
More basalt lava flows and tress in Chasm Provincial Park

The distribution and volume of the Chilcotin Group is unknown due to extensive Pleistocene glacial cover. This presumably glacial "drift" is very thick, and in most regions completely obscure the volcanism. Individual vents for basalt volcanism include small cinder cones, volcanic plugs, and gabbroic feeders, which locally crosscut lava flows. Recent studies indicate that the volume of the Chilcotin Group is much less than previously thought, and that the "Plateau" is likely Eocene in age. This means that the Chilcotin is likely composed of many local volcanic vents, that were of small volumes that fed into the paleo-landscape, and subsequently are found in the major river systems that we see at present.

Prior to 16 million years ago, the western Cascade Volcanic Arc stratovolcanoes erupted with periodic regularity for over 27 million years, even as they do today. The ultimate cause of this volcanism is still up for debate, however, the most widely accepted idea is that a back-arc basin behind the Cascadia subduction zone initied the widespread and voluminous basaltic volcanism. Some centers erupted along pre-existing brittle fault systems while volcanism along its northern portion is most widely believed to have been related to a center of upwelling magma called the Anahim hotspot (similar to that associated with present day Hawaii), creating the Rainbowmarker, Ilgachuzmarker and Itcha Rangemarker shield volcanoes which also in turn form part of the Anahim Volcanic Belt. The exact nature of the relationship between the Anahim hotspot and the Chilcotin Group is, however, unknown.

Notable vents

Volcanoes of the Chilcotin Group include:

See also


  1. National Resources Canada - Catalogue of Canadian volcanoes: Chilcotin Plateau basalts Retrieved on 2008-03-15
  2. Igneous rock associations in Canada 3. Large Igneous Provinces (LIPs) in Canada and adjacent regions: 3 Retrieved on 2008-03-15

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