Touchet Formation

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Touchet Formation
Touchet-formation-2.JPG

Touchet beds in the "Little Grand Canyon" near Lowden in the Walla Walla valley. Note distinct layers.
Type Geological formation
Underlies Loess
Overlies Columbia River Basalt Group
Area 7,000 square miles (18,000 km2)
Thickness up to 330 feet (100 m)[1]
Lithology
Primary sediment
Other Basalt, Loess
Location
Coordinates Walla Walla Basin
46°15′49″N 120°31′00″W / 46.26361°N 120.51667°W / 46.26361; -120.51667
Touchet Basin
46°06′00″N 118°39′00″W / 46.10000°N 118.65000°W / 46.10000; -118.65000
White Bluffs
46°42′25″N 119°27′23″W / 46.70694°N 119.45639°W / 46.70694; -119.45639
Yakima Basin
46°20′30″N 119°27′23″W / 46.34167°N 119.45639°W / 46.34167; -119.45639
Region Columbia Basin of
Western North America
Country USA
Type section
Named for Touchet, Washington
Named by Richard Foster Flint, 1938[1]
Lake Lewis Basin.jpg
Map showing the elevations of the Mid-Columbia region. The lowland areas in brown routinely were flooded during the Missoula Floods, creating lakes.

The Touchet Formation or Touchet beds consist of large quantities of gravel and fine sediment which overlay almost a thousand meters (several thousand feet) of volcanic basalt of the Columbia River Basalt Group in south-central Washington and north-central Oregon. The beds consist of between 6 to 40 distinct rhythmites - horizontal layers of sediment, each clearly demarcated from the layer below. These Touchet beds are often covered by windblown loess soils which were deposited later; the number of layers varies with location.[2][3] The beds vary in depth from 330 ft (100 m) at lower elevations where a number of layers can be found to a few extremely thin layers at the maximum elevation where they are observed (1,150 ft (350 m)).[1]

The Touchet beds are one element in a chain of evidence which helped identify and define the progression of the Missoula Floods, which occurred around 16,450 to 13,750 years BCE.[4][5] During the floods, flow through the Wallula Gap was slow enough such that water pooled in a temporary lake, Lake Lewis. Lake Lewis back-flooded up the Yakima, Walla Walla, Touchet and Tucannon River Valleys. In these relatively calm arms of the lake, the slack waters deposited the suspended materials eroded from the scabland regions north of Lake Lewis, and redeposited them in pronounced layers before receding.[3]

Discovery and interpretation[edit]

 This photo shows a series of horizontal layers of soil in a road cut. In the center of the photo - barely visible - there is a geologist's hammer and a leather glove to establish perspective - they suggest that the layers are about 1 meter thick. In geology the type locale is a location where the first example of a newly described object was found - this is the type locale. This set of layered beds, although nowhere near as clearly pronounced in layering as in several of the other photos, shows the first location where the Touchet Formation was identified in the published literature.
Touchet beds in the Touchet River valley.

Although visible along the Walla Walla and Touchet rivers, the Touchet Beds were not subjected to study until the early 20th century. They remain at the center of scientific analyses to characterize the Missoula Floods.

Type locality[edit]

The type locality for the Touchet Formation is the confluence of the Touchet River with the Walla Walla River, originally noted by Richard Foster Flint[6] in 1938.[7] Numerous other exposures were subsequently identified throughout the basins of the former Lake Lewis and Lake Condon.[8] Touchet-equivalent slackwater deposits are also present in the Willamette Valley near Portland (former Lake Allison).

Early interpretation[edit]

In 1923 J Harlen Bretz published a paper arguing that the channeled scablands in Eastern Washington were caused by massive flooding in the distant past. This view, which was seen as arguing for a Catastrophic explanation for the geologic development, which ran counter the then prevailing view of uniformitarianism, and Bretz's views were initially decried. Bretz defended his theories, setting off a forty-year debate over the Missoula Floods before Bretz’s view of a catastrophic flood finally prevailed.[8][9] Waitt extended Bretz's argument, arguing for a sequence of multiple Missoula Floods — 40 or more.[10][11][12] Waitt's proposal was based mainly on analysis from glacial lake bottom deposits in Ninemile Creek and the Touchet Formation deposits in Burlingame Canyon. This represented a move away from a single catastrophic flood toward a series of catastrophic floods, but with the flood source still ascribed to Glacial Lake Missoula.[12]

The controversy whether the Channeled Scabland landforms were formed mainly by multiple periodic large floods or by a single grand-scale cataclysmic flood from either late Pleistocene Glacial Lake Missoula or an unidentified Canadian source reappeared in 1999.[13] Shaw’s team reviewed the sedimentary sequences of the Touchet beds and concluded that the sequences do not automatically imply multiple floods separated by decades or centuries. Rather, they proposed that sedimentation in the Glacial Lake Missoula basin was the result of jökulhlaups draining into Lake Missoula from British Columbia to the north. Shaw's team proposed that the rhythmic Touchet beds are the result of multiple pulses, or surges, within a single larger flood.[13] In response, Atwater’s team observed that there is substantial evidence for multiple large floods, including evidence of mud cracks and animal burrows in lower layers of the Touchet beds, which were filled by sediment from later floods.[14]

Causes[edit]

 This photo shows several layers of the horizontal Touchet beds - the layers are not as clearly demarked as they were in some of the prior photos. There is a geologist’s hammer and a glove in the photo to establish perspective - it suggests the layers are about 1 meter thick. Most significantly, there is a thin, white horizontal line running through the top of one of the layers. This layer consists of two layers of ash deposited by an eruption of Mount St. Helens separated by a thin layer. The ash allows an alternative confirmation of the dating the layer.
Touchet beds in the Touchet River valley. Note distinct white line, which consists of two layers of Mount St. Helens "S" ash that fell in eastern Washington between 13,350 and 14,400 years BCE.

Recent scientific investigations support Waitt’s proposed separation of layers into records of sequential flood events.[15][16] Although the various sources support temporal separation of floods, they do not definitively identify the source of water for all of the floods, though they all agree that Lake Missoula was source for at least some of them.

Formation[edit]

The Touchet beds are formed of sediment which deposited during the various Missoula Floods, around 16,450 to 13,750 BCE,[4] and during the Bonneville Flood that occurred in approximately 12,500 BCE.[17] Another potential source for periodic flooding, still somewhat controversial, is flood release by jökulhlaups from subglacial lakes in British Columbia, but no specific source for these jökulhlaups has yet been identified.[4]

During the floods, flow through the narrow Wallula Gap was restricted such that water pooled in a temporary lake, Lake Lewis, which formed in the lowlands of the Columbia Plateau. Lake Lewis backflooded up the Yakima, Walla Walla, Touchet and Tucannon River valleys. This flooding lasted for a period of 4–7 days. In the relatively calm arms of the lake, the slack waters were thick with suspended materials eroded from the scablands above. Some of the suspended materials settled out, creating thick Touchet Formation layers, or rhythmites, which are found throughout these valleys. The larger clasts settled out first, followed by the finer ones. This resulted in layers with graded bedding, or bedding in which the larger particles are at the bottom and the smaller ones are at the top.[8]

Periodicity[edit]

  This photo shows four profiles of Lake Lewis at various flood levels. It illustrates that the lake back flooded several valleys in which the Touchet Beds were found.
Lake Lewis was formed when the restricted flow of waters[18] from periodic cataclysmic floods from Glacial Lake Missoula, pluvial Lake Bonneville, and perhaps from subglacial outbursts, backed up through the constriction formed by the Wallula Gap in the Horse Heaven Hills (southern Washington).[19]

In 1980, R. B. Waitt studied the Touchet Formation in the wall of the Burlingame Canyon west of Walla Walla, Washington, where he counted at least 41 distinct flood deposit layers. He postulated that these floods could occur only when glacial Lake Missoula existed,[10] which estimates place at 16,450 to 13,750 BCE.[4] More recent studies have used radiocarbon dating to establish the approximate ages of deposition for the various layers.[12]

The side valleys were protected from the violent currents of the main channel; as a result the flood strata laid down by earlier floods were not eroded away by subsequent floods, but were buried and preserved. The average period between flood episodes is estimated to be 20 to 60 years. The periodicity estimates are based on a number of constraints:

  • The time to recharge Lake Missoula depends upon the level at which the dam is breached releasing the flood as well as upon the adjusted precipitation rate in the drainages flowing into Lake Missoula. For the volumes which correspond to calculated maximum flow rates, this is estimated to take from 20 to 80 years.[12]
  • Paleomagnetic orientations from beds of tephra (volcanic ash) that lie between the layers of the Touchet Formation show secular variation, which indicates that the beds must have been formed by many floods. The purity of the tephra suggests subaerial deposition (the tephra could be mixed with the surrounding sediment if it was deposited in moving water), which indicates a dry period during the ash falls (and hence a hiatus between floods).[15]
  • Offshore deposits on the bed of the Pacific at the mouth of the Columbia River include 120 m (390 ft) of material deposited over a several thousand year period that corresponds to the period of multiple scabland floods seen in the Touchet Beds. Since there are at least 40 floods, this would give an average separation between floods of 50 years.[16]
  • The number of layers deposited varies with location in the Lake Lewis basin. This can best be understood as the result of multiple floods; the variable levels correspond to Lake Missoula breaching the ice dam at varying lake levels, releasing different volumes of flood waters. This would suggest the time between floods is variable.[20]
  • Flood beds in other locations upstream of Lake Lewis such as Ninemile Creek in Montana and the Sanpoil arm of glacial Lake Columbia show a corresponding regularity of flood deposits as well as deposit grading and rhythmical repetition to those in Lake Lewis. Since Glacial Lake Columbia remained filled, annual deposits (varves) can be observed between flood deposits. The flood deposits can be distinguished from annually-deposited varves by both their thickness and the presence of materials foreign to the immediate drainage. Atwater reports from 35 to 55 annual varves between flood deposits in Lake Columbia, supporting a period of 35 to 55 years between ice dam failures.[20]
  • Additional varve counts from the Lake Missoula Basin, Sanpoil River, and Latah Creek suggest that the time between floods was 30-40 years on average.[11][21]

Locations[edit]

Touchet river valley[edit]

 This photo shows several layers of the Touchet formation, as seen close-up. There is a geologist's hammer and a leather glove in the photo to provide perspective - they suggest the layers are about 1 meter deep. There is a vertical seam of a different material running through the horizontal layers – this is the clastic dike which was introduced by later geologic processes.
Carson and Pogue identified these as clastic dikes penetrating Touchet layers.[8] Photo taken in a road cut several miles up the Touchet Valley.

The Touchet Formation was originally identified at the confluence of the Touchet River with the Walla Walla River. It is also found at some distance up the Touchet River Valley. The number of layers observed decreases as one progresses up-valley, indicating that the floodwater lakes varied in depth and distance upstream from the various flood dams. Clastic dike intrusions are observed in some locations penetrating the layers vertically; the dikes are infilled with uniform-size fine-grained materials and are indications that the period between floods was long enough that the deposits dried, forming vertical cracks and allowing wind-blown eroded materials to infill the cracks.[8]

Walla Walla river valley[edit]

 This photo shows another canyon cut into the surrounding flat soil with about 30 distinct horizontal layers of sediment, each clearly demarked from the layer below. Above the canyon a telephone pole can be seen in the distance – the pole provides the perspective that helps the viewer establish that the cut is 30–40 ft (9.1–12.2 m) deep. In the foreground one observes the near edge of the canyon, which help one establish that the canyon is quite narrow and steep walled.
Touchet beds near Lowden in the Walla Walla valley. Note distinct layers.

The Walla Walla River Valley is a closed basin. The river passes through a narrow gap near its confluence with the Columbia River and then widens into a broad open valley floor about 8 mi (13 km) above the confluence with the Columbia. This area was filled to varying depths by the successive Missoula Floods, and sediments settled out to form the Touchet beds over much of the basin, creating what is today a fertile farmland region. In the lowest part of the broader valley, to the east of the Columbia River and west of the city of Walla Walla, Washington, soils commonly form on Touchet beds. In several locations erosion has exposed these beds. One outcrop, the Gardena Terrace segment of the rhythmites, can be seen along the highway west of Walla Walla. The Touchet Formation is also extensively exposed at Burlingame Canyon, just southwest of the town of Touchet near the confluence of the Touchet and Walla Walla Rivers. The deposits are also found along tributaries to the Walla Walla, extending some distance south into Oregon.[3][7]

Yakima river valley[edit]

 This photo shows a canyon cut into the surrounding flat soil with over 20 distinct horizontal layers of sediment, each clearly demarked from the layer below. Above the canyon lip a number of boxes used for transporting harvested apples are stacked; the size of these boxes indicates that the layers each are 0.5-1 meter in depth.
Touchet beds on the Yakima River in Zillah, Washington. Note distinct layers. Apple crates at top provide scale (each is 1 meter high) for layer thickness.

Lake Lewis extended up the Yakima Valley, flooding an area of about 600 sq mi (1,600 km2) of the valley and covering the area now occupied by the city of Yakima by about 200 ft (61 m). The valley extends for 80 mi (130 km), widening westwards above the Chandler Narrows and then narrowing again at Union Gap just below Yakima. The Toppenish Basin and Benton Basin of the lower Yakima River both contain large amounts of Touchet Formation deposits. Rhythmites are extensively exposed 1 mi (1.6 km) north of Mabton and at Zillah. Ice rafted erratics are also commonly found in these beds.[7][22]

Tucannon river valley[edit]

The Tucannon River and its tributary, the Pataha Creek also have valleys partially filled with alluvial deposits from the Missoula and Bonneville floods. Although they lie some distance up the Snake River drainage, the flood waters of Lake Lewis backed up this drainage far enough to deposit sediments. Floodplain deposits consist of up to six distinct Touchet Beds, as well as loess silt and fine sand. These alluvial and loess deposits narrow as they approach the basalt valley walls, and thicken into the central valley, with a maximum sediment thickness of between 20 and 100 ft (6 and 30 m). Due to the elevation of the valley, only six of the flooding events caused water to back into the Tucannon Valley in sufficient volume to deposit distinct layers.[3][23]

Columbia River Basin[edit]

Rhythmites from the Missoula Floods have also been observed in the Columbia River valley. One notable location is the White Bluffs, which are made up of more thickly bedded deposits from the eddy that formed in the floodwaters behind the Saddle Mountains.[3] Another location is at Trinidad, WA located approximately 8 miles west of Quincy (Crescent Bar Road).

Willow Creek Valley[edit]

The Touchet Formation is also found in Oregon, in areas flooded by Lake Condon. This lake back-flooded into the Umatilla and John Day River Valleys as well as other tributaries.[8] As one example, silt-sand rhythmites associated with the Missoula Floods are present along Willow Creek, a valley tributary to the Columbia River. Willow Creek conflues with the Columbia a few miles west of Boardman, Oregon. Excellent exposures of the unit (which contains abundant clastic dikes) can be found in roadcuts along Hwy 74 (Heppner Highway) near the ranching community of Cecil, Oregon. These deposits are associated with former Lake Condon.

References[edit]

  1. ^ a b c Baker, Victor R. (Ed.); Nummedal, Dag (Ed.) (1978). The Channeled Scabland: A Guide to the Geomorphology of the Columbia Basin, Washington. Washington, D.C.: Planetary Geology Program, Office of Space Science, National Aeoronautics and Space Administration, Washington, D.C. pp. 173–177. ISBN 0-88192-590-X. 
  2. ^ "Walla Walla Level 1 Watershed Assessment" (PDF). WRIA 32 Watershed Plan. Walla Walla Watershed Management Partnership. Retrieved September 2009. 
  3. ^ a b c d e Bjornstad, Bruce (2006). On the Trail of the Ice Age Floods: A Geological Guide to the Mid-Columbia Basin. Keokee Books; San Point, Idaho. ISBN 978-1-879628-27-4. 
  4. ^ a b c d Lopes, C; A. C. Mix (January 2009). "Pleistocene megafloods in the northeast Pacific". Geology. v. 37: 79–82. doi:10.1130/G25025A. 
  5. ^ Actual source states timing of Missoula floods is constrained between 18.4 and 15.7 cal. ka B.P. (subtract 1950 for BCE)
  6. ^ Richard Foster Flint was a geology professor from Yale University, who was one of the most prominent critics of the catastrophic flood hypothesis.
  7. ^ a b c J.E.Allen and M. Burns with S.C. Sargent (2009). Cataclysms on the Columbia. Portland State University, Open Book. ISBN 0-88192-215-3. 
  8. ^ a b c d e f Carson, Robert J.; Pogue, Kevin R. (1996). Flood Basalts and Glacier Floods: Roadside Geology of Parts of Walla Walla, Franklin, and Columbia Counties, Washington. Washington State Department of Natural Resources (Washington Division of Geology and Earth Resources Information Circular 90). 
  9. ^ Bretz, J Harlen (1925). "The Spokane flood beyond the Channeled Scablands". Journal of Geology 33 (2): 97–115, 236–259. Bibcode:1925JG.....33...97B. doi:10.1086/623179. 
  10. ^ a b Waitt, R.B., Jr (1980). "About 40 last-glacial Lake Missoula jökulhlaups through southern Washington". Journal of Geology (Web of Science) 88 (6): 653–679. Bibcode:1980JG.....88..653W. doi:10.1086/628553. 
  11. ^ a b Waitt, R.B., Jr (1984). "Periodic jökulhlaups from Pleistocene Glacial Lake Missoula—New evidence from varved sediment in northern Idaho and Washington". Quaternary Research 22: 46–58. Bibcode:1984QuRes..22...46W. doi:10.1016/0033-5894(84)90005-X. 
  12. ^ a b c d Waitt, R.B., Jr (1985). "Case for periodic, colossal jökulhlaups from Pleistocene glacial Lake Missoula". Geological Society of America Bulletin 96 (10): 1271–1286. Bibcode:1985GSAB...96.1271W. doi:10.1130/0016-7606(1985)96<1271:CFPCJF>2.0.CO;2. 
  13. ^ a b Shaw, J.; Munro-Stasiuk, M., Sawyer, B., Beaney, C., Lesemann, J.-E., Musacchio, A., Rains, B., and Young, R.R., (1999). "The Channeled Scabland: Back to Bretz?". Geology 27 (7): 605–608. Bibcode:1999Geo....27..605S. doi:10.1130/0091-7613(1999)027<0605:TCSBTB>2.3.CO;2. 
  14. ^ Atwater, Brian F.; Gary A. Smith; Richard B. Waitt (June 2000). "The Channeled Scabland: Back to Bretz?: Comment and Reply: COMMENT". Geology 28 (6): 574. Bibcode:2000Geo....28..574A. doi:10.1130/0091-7613(2000)28<576:TCSBTB>2.0.CO;2. 
  15. ^ a b Clague, John J.; Barendregt, Rene, Enkin, Randolph J. and Franklin F. Foit, Jr. (March 2003). "Paleomagnetic and tephra evidence for tens of Missoula floods in southern Washington". Geology (The Geological Society of America) 31 (3): 247–250. Bibcode:2003Geo....31..247C. doi:10.1130/0091-7613(2003)031<0247:PATEFT>2.0.CO;2. 
  16. ^ a b Brunner, Charlotte A.; Normark, William R., Zuffa, Gian G. and Serra, Francesca (1999). "Deep-sea sedimentary record of the late Wisconsin cataclysmic floods from the Columbia River". Geology 27 (5): 463–466. Bibcode:1999Geo....27..463B. doi:10.1130/0091-7613(1999)027<0463:DSSROT>2.3.CO;2. 
  17. ^ Bishop, Ellen Morris (2003). In search of ancient Oregon: a geological and natural history. Portland, Oregon: Timber Press, Inc.,. ISBN 0-88192-590-X. 
  18. ^ Flow was restricted by a hydraulic dam—a restriction to the flow rate caused by a narrowed reach in a river valley.
  19. ^ Last, George V.; Bjornstad, Bruce N. and Gessel, Byron M. (2009). "Distribution of Mammoth (Mammuthus) and Erratic Finds Relative to the Size of Ice Age Floods in Southeastern Washington State". Pacific Northwest National Laboratory. PNNL-SA-68903 
  20. ^ a b Atwater, Brian F. (1984). "Periodic floods from glacial Lake Missoula into the Sanpoil arm from of glacial Lake Columbia, northeastern Washington". Geology (The Geological Society of America) 12: 464–467. Bibcode:1984Geo....12..464A. doi:10.1130/0091-7613(1984)12<464:PFFGLM>2.0.CO;2. 
  21. ^ Atwater, Brian F. (1986). "Pleistocene glacial-lake deposits of the Sanpoil River valley, northeastern Washington". U.S. Geological Survey Bulletin (U.S. Geological Survey) 1661: 39. 
  22. ^ Jones,, M.A.; J.J. Vaccaro, and A.M. Watkins (2006). "USGS publication: Scientific Investigations Report 2006–5116". U.S. GEOLOGICAL SURVEY. Retrieved 6 September 2009. 
  23. ^ Easterbrook, Don J. (2003). Quaternary geology of the United States: INQUA 2003 field guide volume. Reno, Nevada: The Desert Research Institute. p. 131. ISBN 978-94-592-0504-4. 

Coordinates: 46°01′59.13″N 118°41′03.63″W / 46.0330917°N 118.6843417°W / 46.0330917; -118.6843417