User talk:Williamborg/sandbox2
Rathdrum Prairie Sandbox (a work in progress)[edit]
The Spokane Valley–Rathdrum Prairie reach is immediately downstream of the breakout point of Lake Missoula, hence the estimated maximum discharge rate by O'Connor and Baker (1992) fairly accurately constrains the maximum possible outflow condition from Lake Missoula. We adopted the hydrograph proposed by O'Connor and Baker (1992) with the maximum discharge of 17 × 106m3/s and total amount of water (2184 km3) equal to the volume of Lake Missoula. We also assumed that the depth of flood erosion is small compared with the maximum water depth and the present-day topography is close to the late Pleistocene one.
We assumed that the discharge rate calculation (O'Connor and Baker, 1992) at the Spokane Valley–Rathdrum Prairie conducted by the 2-dimensional HEC-2 program using high-water marks obtained in the field is reliable.[1]
Geography[edit]
Geology[edit]
"The Rathdrum Prairie Aquifer (RPA) is a deposit largely made up of sand, gravel, cobbles, and boulders. The RPA extends south from the Bonner-Kootenai County boundary toward the cities of Coeur d'Alene and Post Falls and west to the Idaho-Washington state line. The aquifer extends into Washington and becomes part of the larger Rathdrum-Spokane Aquifer." [2]
." [3]
The MOTHER LODE of all material.[4]
History[edit]
"Kootenai and Coeur d'Alene Indian tribes were early inhabitants of the area. In the mid-1800s, settlers, miners, and explorers started to traverse the region. Between 1853 and 1861, Lieutenant John Mullen completed a 624-mile road between Fort Walla Walla in Washington and Fort Benton in Montana, connecting the Missouri and Columbia Watersheds. Completion of the road and discovery of gold brought an influx of settlers." [3][5]
"In 1879, Fort Sherman was established on the northern shore of Lake Coeur d'Alene as a trading post and later expanded as the railroad completed a line through the area and mining became more established. The photo above shows Fort Sherman around 1890. Blackwell Island and the Spokane River are in the foreground, and Lake Coeur d'Alene and Tubbs Hill are in the background. Agricultural development on the Rathdrum Prairie consisted of dry-farming hay and oats to meet the needs of the army and the mining and lumber industries."[3]
"As the population grew on the Rathdrum Prairie, so did agricultural development. Between 1889 and 1966, a number of irrigation districts were formed, supplying water for agriculture from Twin, Hayden, and Hauser Lakes. There were a total of five irrigation districts: 1) Interstate Irrigation District, which later became the Hayden Lake Irrigation District, 2) Avondale Irrigation District, 3) Dalton Gardens Irrigation District, 4) Post Falls Irrigation District, and 5) East Greenacres Irrigation District. Hayden Lake was used as a water supply for Hayden Lake, Avondale, Dalton Gardens, and Post Falls Irrigation Districts, while East Greenacres Irrigation District received water from Twin Lakes through Rathdrum Creek and associated ditches (U.S. Bureau of Reclamation 2007). Combined, the five districts provided water to irrigate over 10,000 acres on the Rathdrum Prairie."[3]
Hold[edit]
Hold[edit]
Hold[edit]
References[edit]
- ^ G. Komatsu1, H. Miyamoto2, K. Ito3, H. Tosaka4 and T. Tokunaga4; The Channeled Scabland: Back to Bretz?: Comment and Reply - COMMENT; doi: 10.1130/0091-7613(2000)28<573:TCSBTB>2.0.CO;2 ; Geology June 2000 v. 28 no. 6 p. 573-574,
- ^ link
- ^ a b c d Rathdrum Prairie Aquifer
- ^ [http://pubs.usgs.gov/sir/2007/5044/ Paul A. Hsieh, Michael E. Barber, Bryce A. Contor, Md. Akram Hossain, Gary S. Johnson, Joseph L. Jones, and Allan H. Wylie; Ground-Water Flow Model for the Spokane Valley-Rathdrum Prairie Aquifer, Spokane County, Washington, and Bonner and Kootenai Counties, Idaho; U.S. GEOLOGICAL SURVEY; Scientific Investigations Report 2007–5044; 08-May-2007
- ^ Bureau of Reclamation
Overdeepening Sandbox (a work in progress)[edit]
Overdeepening is a characteristic feature of glacially formed fjords.
Fjords are found in locations where current or past glaciation extended below current sea level. A fjord is formed when a glacier downwastes, or melts faster than it is moving, after carving its typical U-shaped valley, and the sea fills the resulting valley floor. This forms a narrow, steep sided inlet (plunging up to 1900 m or 6300 ft below sea level) connected to the sea. Overdeepening of the glacier bed is common, which when combined with the terminal moraine often deposited at the fjord's entrance, usually results in shallower water at the neck of the fjord than in the main body of the fjord. Overdeepenings form near glacier heads or anywhere along the length of a glacier, but are prominent in downglacier reaches (i.e., areas where the glacier dropped significantly tend to be overdeepened at the base of the ice descent).[1][2][3][4][5][6][7][8]>
- ^ a b Bell, Robin E. (27 April 2008). "The role of subglacial water in ice-sheet mass balance". Nature Geoscience. 1 (5802): 297–304. doi:10.1038/ngeo186.
{{cite journal}}:|access-date=requires|url=(help); Cite has empty unknown parameter:|coauthors=(help)</ - ^ a b Murton, Julian B. (17 November 2006). "Bedrock Fracture by Ice Segregation in Cold Regions". Science. 314 (5802): 1127–1129. doi:10.1126/science.1132127.
{{cite journal}}:|access-date=requires|url=(help); Unknown parameter|coauthors=ignored (|author=suggested) (help) - ^ a b Dash, G., (2006). "The physics of premelted ice and its geophysical consequences". Rev. Mod. Phys. 78 (695). American Physical Society. doi:10.1103/RevModPhys.78.695. Retrieved 30 November 2009.
{{cite journal}}: Unknown parameter|coauthors=ignored (|author=suggested) (help)CS1 maint: extra punctuation (link) CS1 maint: multiple names: authors list (link) - ^ a b Rempel, A.W.; Wettlaufer, J.S.; Worster, M.G. (2001). "Interfacial Premelting and the Thermomolecular Force: Thermodynamic Buoyancy". Physical Review Letters. 87 (8): 088501. doi:10.1103/PhysRevLett.87.088501.
{{cite journal}}: CS1 maint: multiple names: authors list (link) - ^ a b Rempel, A.W. (2007). "Formation of ice lenses and frost heave". Journal of Geophysical Research. 112 (F02S21). American Geophysical Union. doi:10.1029/2006JF000525. Retrieved 30 November 2009.
{{cite journal}}: Cite has empty unknown parameter:|coauthors=(help) - ^ a b Rempel, A. W. (2008). "A theory for ice-till interactions and sediment entrainment beneath glaciers". Journal of Geophysical Research. American Geophysical Union.: F01013. doi:10.1029/2007JF000870.
{{cite journal}}:|access-date=requires|url=(help); Check|doi=value (help); Cite has empty unknown parameters:|coauthors=and|issue 113=(help) - ^ a b Peterson, R. A., (2008). "Differential frost heave model for patterned ground formation: Corroboration with observations along a North American arctic transect". Journal of Geophysical Research. 113. American Geophysical Union.: G03S04. doi:10.1029/2007JG000559.
{{cite journal}}:|access-date=requires|url=(help); Check|doi=value (help); Unknown parameter|coauthors=ignored (|author=suggested) (help)CS1 maint: extra punctuation (link) CS1 maint: multiple names: authors list (link) - ^ a b >Walder, Joseph (March 1985). "A theoretical model of the fracture of rock during freezing". Geological Society of America Bulletin. 96 (3). Geological Society of America.: 336–346. doi:10.1130/0016-7606(1985)96<336:ATMOTF>2.0.CO;2. Retrieved 30 November 2009.
{{cite journal}}: Unknown parameter|coauthors=ignored (|author=suggested) (help); zero width space character in|doi=at position 24 (help)