Camas prairie

Nez Perce chiefs, 1899

Named for the blue flowering camas—an important food source for all Native Americans in the interior Northwest—the Camas Prairie is a traditional Nez Perce gathering place in north central Idaho.[1]

From the Nez Perce National Historical Park: Camas Prairie is interpreted at a highway pullout on the north side of U.S. Highway 95, about six miles (10 km) south of Grangeville.[2] This large prairie was a Nez Perce gathering place, where camas roots were harvested for thousands of years. Several nontreaty bands gathered at Tolo Lake in early June 1877 in anticipation of moving to the Nez Perce reservation. In response to the forced move and other hostile actions, several young Nez Perce people took actions that precipitated the Nez Perce War.

Camas Prairie is a large area, mostly privately owned, that extends many miles between the Salmon and Clearwater River drainages. Most of the area is agricultural and the northern section is within the Nez Perce Indian Reservation. Similar to the opening of lands in Oklahoma, the U.S. government opened the reservation for white settlement on November 18, 1895. The proclamation had been signed less than two weeks earlier by President Cleveland.[3][4][5][6]

The area was home to the second subdivision of the Camas Prairie Railroad,[7] known as the "railroad on stilts" due to its numerous trestles, most of which were timber. Breakheart Pass, a 1975 film starring Charles Bronson, was filmed on portions of the railroad on the Camas Prairie. The railroad ceased operations in the late 1990s.[8]

For more information:

• National Park Service - Nez Perce
• U.S. Forest Service - Nez Perce

In southern Idaho, east of Mountain Home, the high plain of Camas County around Fairfield is locally called the "Camas Prairie."[9][10][11]

• Camas Prairie Centennial Marsh Wildlife Management Area[9][10]

The basin in which the Camas Prairie lies is a low-relief valley surrounded by mountains composed of metasedimentary strata that belong to the Prichard Formation of the Belt Supergroup. These strata are intensively folded and thrust faulted. The basin is filled with undifferentiated Cenozoic red, greenish, and bluish siltstone and mudstone and volcanic rock. A few sandy and gravelly beds are also present. These strata outcrop at the surface around the perimeter of the basin. Within the basin, they are cover by 15 to 30 m (49 to 98 ft) of Quaternary deposits that accumulated within glacial Lake Missoula.[12][18]

The Camas Prairie is well-known for the large fields of Late Pleistocene giant current ripples that cover a substantial part of its surface.[19] They were created during one of the many times when glacial Lake Missoula drained when its ice dam failed. From the northern edge of the Camas Basin, the fields of giant current ripples extend south (downcurrent) from four mountain passes that were once submerge inlets into the flooded Camas Basin. Southward, these fields of giant current ripples spread out and merge on the basin floor. These sedimentary bedforms are best seen in aerial images and at low sun angles.[20][21]

These giant current ripples are large-to-very-large, subaqueous gravel dunes and antidunes. Although they once covered a significantly larger area, they cover about 26 km² (10 sq mi) of the Camas Prairie basin. The wavelength of these dunes and antidunes ranges from 90 to 951 m (295 to 3,120 ft) and their height ranges from 0.3–17 m (0.98–55.77 ft). They are all two-dimensional, flow transverse, sinuous, sedimentary bedforms. The wavelength and height of these giant current ripples decrease away (downcurrent) from the former inlets. Correspondingly, the size of the gravels comprising them decreases south (downcurrent) from boulder and cobble gravels to pebble gravels. Their foreset bedding is poorly defined and their dip varies from 14 to 23 degrees. In addition to the gravel dunes and antidunes, delta-like, expansion bars accumulated below each of the former subaqueous inlets. They consist of foreset beds that consist of boulder-cobble-pebble gravels.[19][20][21]

The Pleistocene deposits and bedforms in the basin have not been dated using radiometric dating methods. The lack of absolute dates prevents the construction of a reliable geochronology for Lake Missoula lake drainage events in the Camas Prairie basin and correlation of the giant current ripples with bedforms and sedimentary deposits outside of it.[21]

The exposed gravel deposits underlying the giant current ripples at Camas Prairie exhibit at least two beds of gravelly deposits that are indicative of deposition by separate Missoula floods. They are separated by an erosional unconformity with a buried and dismembered calcrete, carbonate soil horizon. The calcrete is 15 to 25 cm (5.9 to 9.8 in) thick. It provides empirical evidence of at least two separate periods of giant current ripple activity and associated with separate Missoula Floods that occurred thousands of years apart based the thickness and development of the calcrete.[22][23]

The giant current ripples of the Camas Prairie are analogous to similar giant Pleistocene bedforms described form Channeled Scablands of Washington. They are identical to the giant subaqueous bedrooms that formed on the bottom of Lake Kuray-Chuya during the Altai flood in Siberia, Russia. These giant bedforms, which are rare or unknown outside of theoretical and experimental studies, preserved a unique record of the paleohydraulology of a Missoula Flood associated with the catastrophic emptying of Lake Missoula.[19][20]