Challis Magmatic Episode

By Laura DeGrey and Paul Link of Idaho State University

Extent and timing of the Challis Magmatic Episode

Geologic History of the Challis Magmatic Episode

Geology of the Challis Volcanics

Trans-Challis Mineralization

PDF Slideshows: Challis Volcanics
Flythroughs: Big Lost River, Salmon River, Middle Fork Salmon, Big Wood River, Clearwater, North Fork Payette, South Fork Payette, Boise, Henry's Fork , Snake River , Blackfoot

Vocabulary Words

extensional tectonics







Extent and timing of the Challis Magmatic Episode

The Challis volcanic episode was active during the Eocene, between ~52-39 Ma, with the bulk of the eruption between 51-45 Ma. The Challis volcanic episode is part of a wide-spread Eocene volcanic belt that covered a large part of the Eocene northwestern United States and southwestern British Columbia (Figure 1).

Geologic History of the Challis Magmatic Episode

The Challis Volcanic Group covers approximately 25,000 square kilometers in Idaho , making it the largest of the Eocene volcanic fields (Figure 2). The Eocene geologic setting of the Challis volcanics is commonly accepted as an extensional basin related to the subduction of the oceanic Farallon Plate beneath the continental North American Plate. Prior to Eocene time, before ~60 Ma, the convergence rate of the Farallon and North American Plates was very fast.

The angle of subduction was shallow and the subducting slab of the Farallon Plate reached as far as eastern Wyoming underneath the North American Plate (Figure 3). This far-reaching subducting slab set the stage for widespread volcanism along the northwestern side of the United States and southwestern British Columbia.

Around 56 Ma, the subduction rate slowed and the angle of subduction became much steeper. During the steepening of subduction, the subducting slab migrated westward (Figure 3). Following the westward migration of subduction, backarc extensional basins developed and triggered widespread igneous activity that youngs in a westward direction. The extensional zone is oriented northeast-southwest and contains many high-angle and low-angle normal faults, which commonly dip toward each other, and form rift-grabens (Figure 3). These normal faults make up the Trans-Challis Fault Zone.



Figure 1. Eocene volcanic belt in the northwestern United States. From Moye et al.,1988.



Challis Volcanic Field

Figure2. Extent of Challis volcanism in Idaho. From Link and Janecke, 1999.


Figure 3. Drawing showing shallow subduction and then migration and steepening of the subducting plate.

Igneous activity occurred in two main phases. The first phase began around 52 Ma and included the intrusion of shallow granitic plutons 3 4 miles below the surface. The second phase included volcanic eruptions. The main phase of eruption occurred between 51 45 Ma, and consisted of effusive and voluminous intermediate and mafic lava flows as well as highly explosive silicic ash-flows. Less violent and less voluminous silicic eruptions continued until approximately 39 Ma. Intrusive activity in the form of rhyolitic domes, rhyolitic plugs, rhyolitic dikes, and rhyolitic stocks accompanied the later stage volcanism. The violent eruptions of rhyolitic ash tuffs and ignimbrites caused the collapse of many calderas between 49 45 Ma. Upon collapse, two of the calderas, the Van Horn Peak and Twin Peaks caldera complexes formed a linear graben oriented in a northeast-southwest direction that corresponds to the most eruptive part Trans-Challis fault zone (Figure 4).

Fault Zone

Figure 4. Map showing the linear graben that is related to the Trans-Challis fault zone. From Link and Janecke, 1999.


Figure 5. Map from Moye et al.(1988).

Geology of the Challis Volcanics

The Challis Volcanic Group include scattered intrusive plutons, intermediate to mafic volcanic rocks, and silicic volcanic rocks. Intrusive plutons are mostly composed of granite with large pink crystals. Plutons are commonly found in the eastern side of the Atlanta Lobe of the Idaho Batholith and just east of the batholith. The bulk of the Challis Volcanic Group is divided into 2 areas (Moye et al., 1988), a Northern Challis Field and a Southern Challis Field. The Northern Challis Field lies north of the 44 degree latitude line, and the Southern Challis Field lies to the south of it (Figure 5). Explanations of these two Challis packages are summarized from Moye et al. (1988).

The Southern Challis Field stratigraphy is divided into four packages:

Volcanic rocks in the Northern Challis Field are subdivided into three packages: 1. intermediate to mafic rocks, 2. rhyodacite to rhyolite ash-flow tuffs, and 3. rhyodacite to rhyolite domes and plugs. The intermediate to mafic rocks contain dacite with phenocrysts of plagioclase, pyroxene, and/or amphibolite and biotite, as well as andesite to basalt with phenocrysts of pyroxene or olivine and plagioclase.

These intermediate to mafic rocks are early stage Challis Volcanic Group, and are mostly found in the northern and central areas of the Northern Challis volcanic field. Rhyodacite and rhyolite ash-flow tuffs erupted from the Van Horn Peak caldera complex, the Thunder Mountain caldera, and the Twin Peaks caldera. Explosive eruptions caused caldera collapse, which can be recognized by thick ignimbrites within the caldera boundaries and thinner surrounding units. The tuff of Ellis Creek is the largest of these ash-flow tuffs, with thickness up to 400 meters outside of the Van Horn Peak caldera, and up to 1,500 meters within the caldera. The last igneous activity in the Northern Challis Field was the emplacement of rhyolite to alkali rhyolite domes and the intrusion of the granitic Castro pluton (Figure 4).

The basal conglomerate is named the Smiley Creek Conglomerate and can be found in the southern part of the Southern Challis Field. It ranges between unconformable to locally conformable with the overlying Challis Volcanic Group, indicating that deposition occurred during local onset of Challis volcanism. The Smiley Creek Conglomerate is significant because it helps define age constraints on early Challis volcanism. It also helps to define pre-Challis paleotopography. The bottom volcanic unit contains andesitic lava flows and tuff breccias. The andesite lavas contain phenocrysts of olivine and clinopyroxene, with minor plagioclase; more felsic lavas contain hornblende or orthopyroxene.

These units are widespread in the Southern Challis Field, however they vary in thickness due to deposition over paleotopography, with flows up to 700 meters thick in paleovalleys. The dacitic and rhyodacitic ash flows and lava flows are the most voluminous units in the Southern Challis Field. This part of the volcanic stratigraphy contains, from bottom to top: lower andesite to rhyodacite ash-flow tuff and tuff breccias, lower rhyodacite to dacite lava flows, upper rhyodacite ash-flow tuffs, and upper rhyodacite lavas. This volcanic stratigraphic package contains compound and multiple-flow units, indicating many different explosive eruptions. These eruptions have not yet been traced back to calderas, and are thought to be primarily erupted from fissures and several other local eruptive centers. As in Northern Challis Field, the Southern Field contains late-stage dacite and rhyolite domes and associated lava flows.

Trans-Challis Mineralization


Mineralization within the Challis Volcanic Group is associated with volcanic and plutonic activity, such as the emplacement of the domes and plutons, caldera collapse, and widespread hydrothermal activity. Regional structures, such as faults and fractures, domes, and grabens, controlled the locations for vein-filling precious metals and hydrothermal activity. The most profitable materials mined from the Challis Volcanic Field include gold, silver, copper, lead, zinc, flourspar, uranium, and building stone. Also emplaced due to Challis igneous activity were beryllium, thorium, molybdenum, tin, mercury, and antimony. The map below shows locations of productive gold and silver deposits, which have been mined along the Trans-Challis fault zone (Figure 6).


Figure 6. Map showing the locations of productive gold and silver deposits, which have been mined along the Trans-Challis fault zone. From Johnson et al., (1988).



Continue to Module 9 - Basin and Range Province - Teritiary Extension


Fisher, F. S., and Johnson, K. M., 1995, Challis Volcanic Terrane, in Fisher, F. S. and Johnson, K. M., eds., Geology and Mineral Resource Assessment of the Challis 1 degree x 2 degree Quadrangle, Idaho: U.S. Geological Survey Professional Paper 1525, p. 41-43.

Johnson, K. M., Lewis, R. S., Bennett, E. H., and Kiilsgaard, T. H., 1988, Cretaceous and Tertiary Intrusive Rocks of South-Central Idaho, in Link, P. K. and Hackett, W. R., eds., Guidebook to the Geology of Central and Southern Idaho: Idaho Geological Survey Bulletin 27, p. 55-86.

Kiilsgaard, T. H. and Bennett, E. H., 1995, Eocene Plutonic Terrane, in Fisher, F. S. and Johnson, K. M., eds., Geology and Mineral Resource Assessment of the Challis 1 degree x 2 degree Quadrangle, Idaho: U.S. Geological Survey Professional Paper 1525, p. 44-47.

Link, P. K. and Janecke, S. U., 1999, Geology of East-Central Idaho: Geologic Roadlogs for the Big and Little Lost River, Lemhi, and Salmon River Valleys, in Hughes, S. S. and Thackray, G. D., eds., Guidebook to the Geology of Eastern Idaho: Idaho Museum of Natural History, p. 295-334.

Link, P. K. and Phoenix , E. C., 1996, Rocks, Rail, & Trails, Second Edition: Idaho Museum of Natural History, Pocatello, ID, 193 p.

McIntyre, D. H., Ekren, E. B., and Hardyman, R. F., 1982, Stratigraphic and structural framework of the Challis Volcanics in the eastern half of the Challis 1 x 2 degree quadrangle, in Bonnichson, B. and Breckenridge, R. M., eds., Cenozoic Geology of Idaho: Idaho Bureau of Mines and Geology Bulletin 26, p. 3-22.

Moye, F. J., Hackett, W. R., Blakey, J. D., and Snider, L. G., 1988, Regional geologic setting and volcanic stratigraphy of the Challis volcanic field, central Idaho, in Link, P. K., and Hackett, W. R., editors, Guidebook to the Geology of Central and Southern Idaho: Idaho Geological Survey Bulletin 27, p. 87-97.

Orr, W. N. and Orr, E. L., 2002, Geology of the Pacific Northwest, Second Edition, McGraw-Hill Higher Education, New York, NY, p. 168-170.