Field Trip Guide to Mt. Rainier
Additional Information for IES: Mt. Rainier
Winter, 2000

 

Ancient History

Volcanism has dominated Cascade Range for the past 40 million years and eruptions continue to this day, a product of subduction of the Pacific Plate beneath the North American continental plate (Vance and Naeser, 1977; McBirney and others, 1974; Hammond and others, 1977; Duncan and Kulm, 1989; Evart and Swanson, 1994). The rocks exposed in this region can be divided into the following four groups: (1) pre-Tertiary units, (2)Western Cascade volcanic and sedimentary strata, (3) lava flows of the Miocene Columbia River Basalt group and associated sedimentary and volcanic rocks, and (4) late Cenozoic volcanics of the High Cascades (see table for geologic time designations). Mt. Rainier National Park is dominated by groups (2) and (4), Western Cascade volcanic and sedimentary strata and the late Cenozoic volcanics of the High Cascades.

The continental crust below the arc of volcanoes in the southern Washington Cascades is complex and poorly understood but appears to consist of complex accretionary structures formed during late Mesozoic and early Tertiary plate convergence between an oceanic plate to the west and the North American continental crust (Stanley et al., 1990). Gravity and aeromagnetic data suggests that oceanic basement (Siletzia terrane) extends at shallow depths beneath the volcanic arc as far east as Mount St. Helens (Finn, 1990).

During the middle Eocene (55 to 43 Ma) rivers drained a granitic highland to the east and northeast, they flowed westward across a subdued landscape and deposited sediment into two large marine basins, creating the Cowlitz Fm. and Puget Group. Sediments were deposited over the basaltic Crescent Terrane during the later part of this interval. Clastic sediments and coal were deposited in flood plains, swamps, deltas and coastal lagoons (Buckovic, 1979; Armentrout and Suek, 1985; Vance et al., 1987; Heller et al., 1987). These Eocene coal deposits have been exploited all along the western Cascade foothills and towns such as Black Diamond, Carbonado, and Centralia grew up around the coal mines. Eastern correlative fluvial and lacustrine units include the Naches, Roslyn, and Chumstick Fms. (Tabor et al., 1984; Vance et al., 1987; Walsh et al., 1987). A volcanic arc (Challis volcanics) was active several hundred kilometers to the east in eastern Washington and Idaho, later it migrated westward (Pringle, 1993).

In the late Eocene (42 to 36 Ma) volcanic activity was initiated in the Cascade region. The westward relocation of the magmatic arc may have been a consequence of the accretion of the Crescent Terrane (now the Washington Coastal Range and Olympic Mtns.) and the development of a new subduction zone further to the west or, more likely, a shift in the tectonic regime replaced a diffusely distributed extensional magmatic arc (of the Challis episode) with a more focused compressional arc (Heller et al., 1987; Evarts and Swanson, 1994). Throughout most of the western Washington these isolated volcanoes produced silica-rich eruptive products including rhyolites and pyroclastics but to the west, in the present location of Mount St. Helens, shield volcanoes erupted basaltic and andesitic lavas that became interbedded with fluvial deposits (Northcraft Fm.) (Gard 1968; Vine, 1969; Phillips et al., 1989; Pringle, 1993). The Rainier region was part of a broad, low-lying coastal plain that extended along the site of the present day Cascades. Much of this lowland was submerged beneath large lakes or embayments of the sea (Fiske and others, 1964).

The middle Tertiary volcanic rocks (Western Cascade Group from the lithologically similar Western Cascade volcanic rocks of Oregon) are deformed, intruded, hydrothermally altered and metamorphosed regionally to zeolite facies (Peck and others, 1964; Grant, 1969; Wise, 1961; Fiske and others, 1963; Hartman, 1973). The rocks are calc-alkaline and consist of pyroxene andesite, basalt, rhyodacite, dacite and rhyolite in the form of lava flows, laharic breccias, ash-flow tuffs and volcanic rocks. The volcanic sources of these rocks (stratovolcanoes) are not well defined (Hammond and others, 1977). In the Mount Rainier-Tieton River region these are represented by the Ohanapecosh (late Eocene - early Oligocene), Stevens Ridge (Oligocene - lower Miocene) and Fifes Peak (lower Miocene) Formations. All of these units are exposed in Mt. Rainier National Park.

The Ohanapecosh Fm. is the oldest formation exposed in Mt. Rainier National Park. This unit is widely exposed in southern Washington between the Columbia River Gorge and Snoqualmie Pass and represents the first volcanic expression of the Tertiary Western Cascade magmatic arc in southern Washington and marks the end of the Eocene tectonic regime in the Pacific Northwest (Vance, 1982). The facies have been interpreted as debris flows and turbidites generated by subaqueous eruptions (Fiske and others, 1963) but evidence, such as the lack of pillow basalts, accumulations of pumice and accretionary lapilli, carbonized wood and nonmarine vertebrate fossils suggest a terrestrial source, if not subaerial deposition (Vance and others, 1987; Fiske and others, 1963). Vents of the volcanoes which produced the Ohanapecosh Fm. are found throughout the park region. The Ohanapecosh Fm. is suggested to have been folded, regionally altered (zeolite facies), uplifted, and deeply eroded prior to the deposition of the Stevens Ridge rocks (Fiske and others, 1963) but recent mapping cast doubts on the existence of the unconformity at the top of the Ohanapecosh (Smith, 1993; Evarts et al., 1993). Fission-track data indicate that the Ohanapecosh Fm. spans the age range of at least 36 to 28 Ma (late Eocene - early Oligocene).

The Fifes Peak Fm. overlays the Ohanapecosh Fm. in the White Pass-Tieton River region but an intermediate unit, the Stevens Ridge Fm., has been identified in the park to the north (Fiske and others, 1963). The Stevens Ridge Fm. attains a thickness of up to 1,000 m and consists mainly of massive welded pyroclastic flows. The "ash" is now devitrified and altered. Age data and lateral correlations indicate that the Stevens Ridge unit differs significantly in stratigraphic position, lithology, and age with the type Stevens Ridge and, thus, can not be physically correlated. The Stevens Ridge Fm., which is a silicic pyroclastic unit, is probably laterally discontinuous and lithologically equivalent to many units within the Fifes Peak Fm. and not unique to a single stratigraphic interval in the Washington Cascades outside of the park region (Vance and others, 1987). The Stevens Ridge Fm. was deposited during the Oligocene or Miocene (Fiske and others, 1964).

The long interval of subsidence which allowed the Ohanapecosh Fm. to accumulate ended by 27 Ma with an episode of folding, uplift and erosion. The Fifes Peak activity was initiated by violent, large-volume eruptions of silicic pyroclastics from a number of vents, at least one of which was a major caldera (Fiske and others, 1963; Vance and others, 1987). Fifes Peak volcanism lasted from 25.5 to at least 22 Ma (late Oligocene), ceasing prior to extrusion of the Columbia River Basalts (16 Ma). The Fifes Peak Fm. consists of lava flows, subordinate mudflows, and minor quantities of tuffaceous clastic rocks (Fiske and others, 1963). The lavas are predominantly olivine basalts and basaltic andesite, but they also include a little rhyolite (Fiske and others, 1963). The upper part of this unit is generally eroded in the Mt. Rainier region but dikes that fed the eruptions are common. Sills of the Fife Peak Fm. occur commonly along the contact between the Ohanapecosh and Stevens Ridge Fms.

The was a gentle deformational (folding, uplift and erosion) event prior to the emplacement of the late Miocene Tatoosh Pluton. This created gentle northwest-trending folds. The folding occurred largely between 21 and 12 Ma (Vance et al., 1987). The emplacement of the pluton was accompanied by the injection of a variety of satellitic stocks, sills, and dikes. In several places magma reached the surface initiating violent eruptions (The Palisades). The Tatoosh Range represents the eroded roots of a volcanic complex (Fiske et al., 1963).

In the middle Miocene (14 to 3 Ma) there was a decrease in the amount of volcanism in the Cascades, or evidence of the magmatism may have been subsequently eroded. During this interval the region was being actively uplifted, gentle folding may have continued into the late Miocene (10 Ma) (Pringle, 1993). Several interesting events occurred in the middle Miocene:

(a) the decline of volcanic activity

(b) change in petrology of the magmatic arc

(c) shift from regional subsidence to uplift of the Cascade Range

(d) folding of Tertiary strata

(e) eruption of the Columbia River Basalts

These events could be linked to a change in the tectonic regime of the Pacific Northwest at about 17 Ma, perhaps driven by initial activity of the Yellowstone plume (Brandon and Goles, 1988; Pringle et al., 1994).

Erosion of the unroofed Tatoosh pluton occurred prior to the development of the Rainier (Ta-co-man: "snow-covered mountain") volcano, probably in early Pleistocene time (Fiske and others, 1963). The first evidence of proto-Mount Rainier, referred to as the Lily Creek Fm., consists of a thick sequence of volcaniclastic debris that has been dated between 2.9 and 0.84 Ma (Easterbrook et al., 1981; Smith, 1987, Pringle et al., 1994). Early inter-canyon lava flows (pyroxene andesite) leveled the topography, filling the dissected surface of the Tertiary basement and produced a base for the present volcano (Rampart Ridge). Despite rapid erosion by streams and glaciers, the lava, mudflows, and thin pyroclastic deposits built a cone that was about 300 m higher than the present volcano. The summit either collapsed or was eroded and a subsequent small cone formed which culminates in Columbia Crest along the SE edge of the old summit rim. During the growth of this cone a pumice sheet was deposited, the age of the youngest deposit (600 - 500 years) records the last activity of the mountain (Fiske and others, 1963; Mullineaux, 1974). An estimated 140 km3 of lava has been erupted from Mount Rainier in the past 1 my (Sherrod and Smith, 1989).

Hazards

Rainier has the potential to be the most dangerous volcano in the Cascade Range because of the large (and increasing) population living along its lowland drainage. More than 100,000 people live on young volcanic mudflows that have flowed down the various drainage systems, away from the volcano, in the past 10,000 years. Because of the tremendous hazards associated with this volcano, Mt. Rainier was designated as a Decade Volcano study area by the National Research Council in 1994. The mountainís high relief and volume of ice and snow on the cone (4.4x109 m3) have the potential to generate enormous lahars and debris flow (especially during eruption) (Driedger and Kennard, 1986; Pringle et al., 1994). Six or seven such flows have occurred since the Mount Mazama ash of 6,845 ybp including the Osceola, Round Pass, and Electon Mudflows (Bacon, 1983). Mudflow hazard is enhanced by the mountains steep, glacially carved slopes, hydrothermally altered core, active hydrothermal system, bedding dipping downslope, and frequency of tectonic and magmatic pulses. Recent efforts have been made to map hydrothermally altered materials using remotely sensed data and field mapping (Crowley and Zimbelman, 1997).

Postglacial deposits at Mt. Rainier are dominated by lahars (more than 60 have been identified) and they have been interpreted as eruption induced, particularly the Paradise Lahar and Osceola Mudflow (Crandell, 1971; Dragovich et al., in press). The 5,600 ka Osceola Mudflow had a volume of more than 4 km3, inundating at least 485 km2, and flowing more than 110 km to the Puget Sound. The Electron Mudflow has been dated at 530 ybp and appears to have been induced by a failure of part of the western slope and incorporated 0.26km3 of material (Scott et al., 1992). The Kautz lahar of 1947 moved 0.4 km3 of debris several miles downstream and redeposited it in a huge fan that temporarily blocked the Nisqually River.

Glacial outburst floods are frequent events. Floods from South Tahoma Glacier have repeatedly scoured Tahoma Creek during the past 30 years. These floods are usually associated with seasonally extremely weather (warm or wet conditions) (Walder and Driedger, 1994). Similar events have occurred in Kautz Creek and the Nisqually River (Driedger and Fountain, 1989).

The hydrothermal system on Mount Rainier suggests a substantial heat emission along a narrow, central zone which creates snow-free areas at the summit crater (Moxham et al., 1965; Frank, 1985). The hydrothermal system alters (argillization and silicification) and weakens the rock. Four Quaternary hydrothermal systems have been identified on Mt. Rainier:

(a) Summit craters (temperatures 76° - 86° C)

(b) Upper flank (max. temperature 60° C)

(c) Lower flank (max. temperature 9° - 24° C)

(d) Longmire Springs (max. temperature 25° C)

All sets of springs could be derived from similar acidic sulfate-chlorite waters that originate in a central hydrothermal system. Cooling of the water during flow away from the system toward lower elevation could be caused by dilution with meteoric water (Pringle et al., 1994).

Approximately 30 small earthquakes occur under Mt. Rainier annually, making it the most seismically active volcano in the Cascade Range after Mt. St. Helens (Malone and Swanson, 1986). These events may trigger slope failure and lahars. An important north-northwest-trending zone of seismicity is the Western Rainier seismic zone (National Resource Council, 1994; Goter, 1994).

References Cited

Armentrout, J. M., and Suek, D. H., 1985, Hydrocarbon exploration in western Oregon and Washington: AAPG Bull., v. 69, p. 627-643.

Bacon, C. R., 1983, Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A: J. of Volcan. and Geotherm. Res., v. 18, p. 57-115.

Brandon, A. D., and Goles, G. G., 1988, A Miocene subcontinental plume in the Pacific Northwest: geochemical evidence: Earth and Plan. Sci. Lett. v. 88, p. 273-283.

Buckovic, 1979, The Eocene deltaic system of west-central Washington: in Armentrout, J. M., Cole, M. R., and TerBest H., eds., Cenozoic paleogeography of the western United States: Los Angeles, Soc. Econ. Paleont. and Min., Pacific Section, Pacific Coast Paleogeog. Symposium 3, p. 147-163.

Campbell, N. P., 1975, A geologic road log over Chinook, White Pass and Ellensburg to Yakima highways: WA Div. of Geol. and Earth Resources Inf. Circular 54, 81pp.

Crandell, D. R., 1971, Postglacial lahars from Mount Rainier volcano, Washington: USGS Prof. Paper 677, 75pp.

Crowley, J. K., and Zimbelman, D. R., 1997, Mapping hydrothermally altered rocks on Mount Rainier, Washington, with airborne visible/infared imaging spectometer (AVIRIS) data: Geology, v. 25, p. 559-562.

Driedger , C. L., and Fountain, A. G., 1989: Glacier outburst floods at Mount Rainier, Washington State, U.S.A.: in Wold, B. ed., Proceedings of the symposium on snow and glacier research relating to human living conditions: Annals of Glaciology, v. 13, p. 51-55.

Driedger, C. L., and Kennard, P. M., 1986, Ice volumes on Cascade volcanoes-Mount Rainier, Mount Hood, Three Sisters, and Mount Shasta: USGS Prof. Paper 1365, 28pp.

Duncan, R. A., and Kulm, L. D., 1989, Plate tectonic evolution of the Cascades arc-subduction complex: in Winterer, E. L., Hussong, D. M., and Decker, R. W., eds., The eastern Pacific Ocean and Hawaii, The geology of North America, GSA, v. N, p. 413-438.

Evarts, R. C., and Swanson, D. A., 1994, Geologic transect across the Teritary Cascade Range, southern Washington: in Swanson, D. A., and Haugerud, R. A., eds., Geologic field trips in the Pacific Northwest: 1994 GSA Annual Meeting, ch. 2H.

Finn, C., 1990, Geophysical constraints on Washington convergenct margin structure: J. of Geophys. Res., v. 95, p. 19533-19546.

Fiske, R. S., Hopson, C. A., and Waters, A. C., 1963, Geology of Mount Rainier National Park, Washington: USGS Prof. Paper 444, 93pp.

Frank, D. G., 1985, Hydrothermal processes at Mount Rainier, Washington: U of WA PhD thesis, 195pp.

Gard L. M. Jr., 1968, Bedrock geology of the Lake Tapps quadrangle, Pierce County, Washington: USGS Prof. Paper 388-B, 33pp.

Goter, S. K., 1994, Earthquakes in Washington and Oregon, 1872-1993: USGS Open-file Report 94-226A, scale 1:1,000,000

Hartman, D. A., 1973, Geology and low-grade metamorphism of the Greenwater River area, central Cascade Range, Washington: U of WA doctoral thesis, 99pp.

Heller, P. L., Tabor, R. W., and Suczek, C. A., 1987, Paleogeographic evolution of the United States pacific northwest during Paleogene time: Can. J. of Earth Sci., v. 24, p. 1652-1667.

Millineaux, D. R., 1974, Pumice and other pyroclastic deposits in Mount Rainier National Park, Washington: USGS Bull. 1326, 83pp.

National Research Council, 1994, Mount Rainier, active Cascade volcano: National Academy Press, Washington D. C., 114pp.

Peck, D. L., Griggs, A. B., Schlicker, H. G., Wells, F. G., and Dole, H. M., 1964, Geology of the central and northern parts of the western Cascade Range in Oregon: USGS Prof. Paper 449, 56pp.

Phillips, W. M., Korosec, M. A., Schasse, H. W., Anderson, J. L., and Hagen, R. A., 1986, K-Ar ages for volcanic rocks in southwest Washington: Isochron/West v, 47, p. 18-24.

Pringle, P. T., 1993, Roadside geology of Mount St. Helens National Volcanic Monument and vicinity: WA Div. of Geol. and Earth Resources Inf. Circular 88, 120pp.

Pringle, P. T. and others, 1994, Mount Rainier, a decade volcano GSA field trip: in Swanson, D. A., and Haugerud, R. A., eds., Geologic field trips in the Pacific Northwest: 1994 GSA Annual Meeting, ch. 2G.

Scott, K. M., Pringle, P. T., and Vallance, J. W., 1992, Sedimentology, behavior, and hazards of debris flows at Mount Rainier, Washington: USGS Open file report 90-385.

 

Sherrod, D. R., and Smith, J. G., 1989, Quaternary extrusion rates from the Cascade Range, northwestern United States and British Columbia: in Muffler, L. J. P., Weaver, C. S., Blackwell, D. D., eds., Proceedings of workshop XLIV - Geological, geophysical, and tectonic setting of the Cascade Range: USGS Open-file report 89-178, p. 94-103.

Smith, J. G., 1990, Geologic map of upper Eocene to Holocene volcanic and related rocks in the Cascade Range, Washington: USGS Miscellaneous investigations Map I-2005, scale 1:500,000.

Stanley, W. D., Mooney, W. D., and Fuis, G. S., 1990, Deep crustal structure of the Cascade Range and surrounding regions from seismic refraction and magnetotelluric data: J. of Geophys. Res., v. 95, p. 19419-19438.

Tabor, R. W., Fizzell, V. A., Vance, J. A., and Naeser, C. W., 1984, Ages and stratigraphy lower and middle Tertiary sedimentary and volcanic rocks of the central Cascades, Washington: applications to the tectonic history of the Straight Creek fault: GSA Bull., v. 95, p. 26-44.

Vance, J. A., 1982, Cenozoic stratigraphy and tectonics of the Washington Cascades (abstract): Geol. Soc. of Am. Abstracts with Programs, v. 14, p. 241.

Vance, J. A., Clayton, G. A., Mattinson, J. M., and Naeser, C. W., 1987, Early and Middle Cenozoic stratigraphy of the Mount Rainier-Tieton River area, southern Washington Cascades: in Schuster, J. E., ed., Selected papers on the geology of Washington: WA Div. of Geol. and Earth Resources Bull. 77, p. 269-290.

Vine, J. D., 1969, Geology and coal resources of the Cumberland, Hobart, and Maple Valley quadrangles, King County, Washington: USGS Professional Paper 624, 67pp.

Walder, J. S., and Driedger, C. L., 1994, Geomorphic changes caused by outburst floods and debris flows at Mount Rainier, Washington, with emphasis on Tahoma Creek valley: USGS Water Resources Invest. Report 93-4093, 93pp.

Walsh, T. J., Korosec, M. A., Phillips, W. M., Logan, R. L., and Schasse, H. W., 1987, Geologic map of Washington - southwest quadrant: WA Div. of Geol. and Earth Res. Map GM-34, scale 1:250,000

Wise, W. S., 1970, Cenozoic volcanism in the Cascade Mountains of southern Washington: WA Div. of Geol. and Earth Resources Bull. 60, 45pp.