Wichita Mountains

Wichita Mountains

Elk Mountain, in the eastern Wichita Mountains
Highest point
Peak Haley Peak (officially unnamed)
Coordinates 34°50′22″N 98°48′13″W / 34.83944°N 98.80361°W / 34.83944; -98.80361Coordinates: 34°50′22″N 98°48′13″W / 34.83944°N 98.80361°W / 34.83944; -98.80361
Dimensions
Length 60 mi (97 km) northwest-southeast
Width 10 mi (16 km)
Geography

Color digital elevation map of southwestern Oklahoma; the Wichita Mountains are highlighted.

Country United States
State Oklahoma
Geology
Orogeny Ouachita orogeny
Age of rock Cambrian and Pennsylvanian (geology)
Type of rock granite, rhyolite and gabbro

The Wichita Mountains are located in the southwestern portion of the U.S. state of Oklahoma.[1] The mountains are a northwest-southeast trending series of rocky promontories, many capped by 540 million-year old granite. These were exposed and rounded by weathering during the Permian Period. The eastern end of the mountains offers 1,000 feet (305 m) of topographic relief in a region otherwise dominated by gently rolling grasslands. The mountains are home to numerous working ranches and quarry operations, the state reformatory, recreational homes and campsites, and scenic parklands. Fort Sill, home of the U.S. Army Field Artillery School, occupies a large portion of the southeastern end of the mountains.

Recreation

The Wichita Mountains National Wildlife Refuge, a favorite for hikers and rock climbers in the region, is located adjacent to Cache, Medicine Park, Indiahoma, and historic Meers while just a short drive from Lawton and Walters. Bison, elk and deer are protected on the 59,020-acre (23,880 ha) wildlife refuge. The refuge also manages a herd of longhorn cattle. A scenic highway traversing the park permits leisurely views of these and other fauna. Backcountry camping is available in the Charon Gardens Wilderness area.[2] The park is home to a small number of popular fishing lakes. There are numerous trails for hiking. It is also home to Treasure Lake Job Corps. Additional points of interest are the refuge's visitors center, Holy City of the Wichitas, Quanah Parker Lake & Dam, Lake Jed Johnson, and Lake Lawtonka.

Great Plains State Park is located near the geographic center the Wichita Mountains, north of the town of Mountain Park.

Quartz Mountain Nature Park and Arts Center is a noteworthy recreation area located north of the city of Altus.

Geography

At 2,464 ft (751 m) Mount Scott is the second highest mountain within the Wichita Mountains National Wildlife Refuge boundary. Mount Pinchot in the Special Use Area [lower-alpha 1] is 12 feet (4 m) taller.[3][4]A paved road leads to the summit of Mount Scott, offering a stunning view of the granite promontories to the west, the wind farm on the Slick Hills to the north, the lakes to the south and east, Fort Sill, and Lawton. The highest peak in the Wichita Mountains (including areas outside the refuge) is Haley Peak, at 2,481 ft (756 m). Haley Peak (officially unnamed) is located on private property just outside the northwest corner of the refuge.[5]

Wichita Mountains Narrows

History

When the area was part of Indian reservations and therefore off-limits to non-Native Americans, the Wichita Mountains were rumored to contain rich gold deposits. When the area was first opened up for settlement, many prospectors staked mining claims, and towns were laid out to serve the presumed bonanzas, but no economic deposits were found. The gold boom was prolonged by some unscrupulous assayers who found gold in every sample, but the miners eventually gave up, leaving behind ghost towns such as Wildman, Oklahoma.[6][7]

Geology

Granite knob in the Wichita Mtns.
Granite overlying gabbro - a view of Mount Sheridan from the northeast
American Bison

Overview

In simplest terms, the Wichita Mountains are rocky promontories and rounded hills made of red and black igneous rocks, light-colored sedimentary rocks, and boulder conglomerates. The Wichita Mountains were formed in four distinct geologic episodes.

  1. Magmatism induced by continental rifting just prior to and in the Cambrian Period produced the granites and rhyolites (the red rocks), gabbroic rocks, anorthosites, and diabases (the black rocks).
  2. Subsidence resulted in burial by sandstones and carbonates (the light-colored rocks) during the early Paleozoic.
  3. Uplift during the Pennsylvanian Ouachita Orogeny brought these rocks to the surface as mountains.
  4. Weathering and erosion during the Permian Period flattened the mountains and produced a mantle of conglomerates.

The mountains themselves are Permian landforms covered and preserved by river-borne sediments in the Permian and partially excavated only in recent geological times. Exposure of these fossil mountains is greatest towards the southeast; much of the western part of the Permian range remains buried under sandstones and shales.

Details

The geologic history of the region began with the deposition of late Precambrian to early Cambrian sandstones collectively known as the Tillman metasedimentary group.[8] These sediments were intruded by a coarse mafic layered complex about 575 million years ago[9][10] as the region began to rift apart in an aulacogen during breakup of the Neoproterozoic continent, Pannotia.[11] The exposed portion of this unit, named the Glen Mountains Layered Complex, consists of gabbro, anorthosite and troctolite. These are the dark gray rocks found throughout the Raggedy Mountains, the central region of the wildlife refuge, and to the immediate north of the refuge.[12]

Uplift and erosion followed, as the layered complex is uncomfomably overlain by the extensive lava flows of the Carlton Rhyolite.[8] This is an brown-red to orange porphyritic rock with 5–10 mm orange-colored alkali feldspar crystals. Most of the rounded hills on Fort Sill are made of this rhyolite, including Medicine Bluffs. Additional exposure of the rhyolite is found in Blue Creek Canyon, where Oklahoma Highway 58 cuts through the Slick Hills. Tabular intrusions of granite and hydrous gabbro exploited the boundary between the layered complex and the rhyolites.[13] The granites, collectively named the Wichita Granite Group, vary slightly in composition and texture. The granites form the peaks and highlands in the eastern Wichitas and the isolated peaks of the western Wichitas. Some are equigranular, others are porphyritic. The Mount Scott Granite is the most extensively exposed Wichita Granite. It forms the topographic feature from which it takes it name, and it is distributed throughout the northern half of the wildlife refuge. Dark rounded alkali feldspars, typically one centimeter or less in diameter, dominate this rock.[14]

Relatively small and compositionally distinct plutons, known as the Roosevelt Gabbros, are found in the eastern and central Wichita Mountains. Like the layered complex, these are dark rocks. Unlike the layered complex, they contain appreciable amounts of biotite, a mineral that forms in magmas with elevated dissolved water. One of these bodies, the Mount Sheridan Gabbro, is exposed in roadcuts at Meers and underlies the Mount Scott Granite on the north side of the wildlife refuge. Weathered gabbroic soils are thicker and support more vegetation than those generated on weathered granite, so the tree line on the north side of Mount Sheridan approximates the contact between the Mount Sheridan Gabbro and the Mount Scott Granite. Geologic relationships suggest that the granites and gabbros intruded at depths no greater than half a kilometer in the crust.[8] Minor uplift ensued, and magmatism concluded with the intrusive emplacement of subvolcanic features: rhyolite and diabase dikes.[8] These are poorly exposed, with the exception of a large diabase dike in the Mount Scott Granite revealed during the recent widening of Oklahoma State Highway 49, just west of Interstate 44. Following the cessation of magmatism, the region subsided and was inundated by a shallow sea, resulting in the deposition of detrital sediments followed by carbonates.[15] The light-colored rocks exposed in the Slick Hills are lower Paleozoic marine sediments.

During the Pennsylvanian Period (330–290 million years ago) the region was subjected to intense pressure during the continental collision or orogeny which produced the Ouachita Mountains to the east.[16] This resulted in faulting and folding striking along a WNW direction and includes the Arbuckle and Wichita Mountains of southern Oklahoma and the Amarillo Uplift of the Texas Panhandle.[16] Up to 20,000 feet (6,100 m) of local uplift occurred during this time.[17]

This uplift locally created rugged mountains reduced by erosion to their present state largely during the Permian Period. Extensive weathering produced the tors of the Charon Gardens region and the "river" of boulders that descends the west slope of Mount Scott. Likewise, weathering produced the bowling-ball sized boulders in the Permian-age Post Oak Conglomerate locally found in and around the mountains. In addition to outcrops of the conglomerate, the boulders are preserved in the distinctive rock buildings of Medicine Park. As the Permian progressed, river sediments buried the Wichita Mountains, preserving them from further weathering. Recent geological erosion has removed these sediments, excavating these once buried fossil landforms.[8]

Notes

  1. ↑ The Special Use Area is a part of the WMNWR that is closed to the public.


References

  1. ↑ U.S. Geological Survey Geographic Names Information System: Wichita Mountains
  2. ↑ U.S. Geological Survey Geographic Names Information System: Wichita Mountains Charons Garden Area
  3. ↑ U.S. Geological Survey Geographic Names Information System: Wichita Mountains North Mountain Area
  4. ↑ Splinter, Dale K. and Marston, Richard A. "Wichita Mountains". Encyclopedia of Oklahoma History and Culture. Oklahoma Historical Society. Accessed May 16, 2016.
  5. ↑ Haley Peak Elevation information from records stored at USGS/NSDI Standards Team/NGTOC III/Mid-Continent Mapping Center, Rolla, Missouri.
  6. ↑ Plazak, Dan (January 31, 2010). "A Hole in the Ground with a Liar at the Top: Fraud and Deceit in the Golden Age of American Mining". University of Utah Press. pp. 198–200. ISBN 978-1607810209.
  7. ↑ Morris, John W (March 15, 1978). "Ghost Towns of Oklahoma". University of Oklahoma Press. pp. 204–205. ISBN 978-0806114200.
  8. 1 2 3 4 5 M. Charles Gilbert, 1982, Geologic setting of the eastern Wichita Mountains with a brief discussion of unresolved problems, in Gilbert, M.C. and Donovan, R.N., eds., Geology of the Eastern Wichita Mountains, Southwestern Oklahoma, Oklahoma Geological Survey Guidebook 21, p. 1-30.
  9. ↑ David D. Lambert and Unruh, D. M., 1986, Isotopic constrains on the age and source history of the Glen Mountains Layered Complex, Wichita Mountains, in Gilbert, M.C. ed., Petrology of the Cambrian Wichita Mountains Igneous Suite, Oklahoma Geological Survey Guidebook 23, p. 53-59.
  10. ↑ http://www.fws.gov/southwest/REFUGES/oklahoma/wichitamountains/geology.html US Fish and Wildlife Service, Wichita Mountains Wildlife Refuge, Geology
  11. ↑ D.A. McConnell and Gilbert, M.C., 1990, Cambrian extensional tectonics and magmatism within the Southern Oklahoma Aulacogen, Tectonophysics, 174 p. 147-157.
  12. ↑ Roger W. Cooper, 1986, Platinum-group-element potential of the Glen Mountains Layered Complex, in Gilbert, M.C. ed., Petrology of the Cambrian Wichita Mountains Igneous Suite, Oklahoma Geological Survey Guidebook 23, p. 65-72.
  13. ↑ Hogan, John P., Price, J.D., and Gilbert, M.C., 1998, Magma traps and driving pressure: consequences for pluton shape and emplacement in an extensional regime., Journal of Structural Geology, 20 pp. 1155-68.
  14. ↑ Clifford A. Merritt, 1965, Mt. Scott Granite, Wichita Mountains, Oklahoma, Oklahoma Geology Notes, 25, pp. 263-72.
  15. ↑ R. Nowell Donovan, Ragland, D., Rafalowski, M., McConnell, D., Beauchamp, W., Marcini, W.R., and Sanderson, D.J. 1988, Pennsylvanian deformation and Cambro-Ordovician sedimentation in the Blue Creek Canyon, Slick Hills, southwestern Oklahoma, in Hayward, O.T., ed., Geological Society of America, Centennial Field Guide, 4, p. 127-34.
  16. 1 2 Kiver, Eugene P; Harris, David V (June 15, 1999). "Geology of U.S. Parklands". Wiley. pp. 732–743. ISBN 978-0471332183.
  17. ↑ USGS America's Volcanic Past
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