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Portneuf River (Idaho)

Coordinates: 42°57′06″N 112°45′02″W / 42.95167°N 112.75056°W / 42.95167; -112.75056
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Portneuf River
The Portneuf River, as seen from U.S. Route 30 west of Lava Hot Springs, October 2004
Portneuf River (Idaho) is located in Idaho
Portneuf River (Idaho)
Location of the mouth of the Portneuf River
Portneuf River (Idaho) is located in the United States
Portneuf River (Idaho)
Portneuf River (Idaho) (the United States)
Location
CountryUnited States
StateIdaho
CountiesBannock, Caribou, Bingham, & Power
Physical characteristics
Source 
 • locationnorth of Chesterfield, Bingham County
 • coordinates43°06′10″N 112°00′13″W / 43.10278°N 112.00361°W / 43.10278; -112.00361[1]
 • elevation6,253 ft (1,906 m)[2]
MouthSnake River
 • location
American Falls Reservoir, Bannock/Power counties
 • coordinates
42°57′06″N 112°45′02″W / 42.95167°N 112.75056°W / 42.95167; -112.75056[1]
 • elevation
4,357 ft (1,328 m)[1]
Length124 mi (200 km)[3]
Basin size1,329 sq mi (3,440 km2)[4]
Discharge 
 • locationat Tyhee[5]
 • average418 cu ft/s (11.8 m3/s)[5]
 • minimum32 cu ft/s (0.91 m3/s)
 • maximum1,730 cu ft/s (49 m3/s)

The Portneuf River is a 124-mile-long (200 km)[3] tributary of the Snake River in southeastern Idaho, United States. It drains a ranching and farming valley in the mountains southeast of the Snake River Plain. The city of Pocatello sits along the river near its emergence from the mountains onto the Snake River Plain.

The river is part of the Columbia River Basin.

Course

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The Portneuf River rises in western Caribou County, approximately 25 miles (40 km) east of Pocatello, along the eastern side of the Portneuf Range. It flows initially south, passing westward around the southern end of the 60-mile (100 km) range, and then turning north to flow between the Portneuf Range to the east and the Bannock Range to the west. It flows northwest through downtown Pocatello and enters the Snake at the southeast corner of American Falls Reservoir, approximately 10 miles (16 km) northwest of Pocatello.

Watershed and discharge

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The Portneuf watershed drains 850,290 acres (3,441.0 km2) in southeastern Idaho and is bounded by Malad Summit to the south, the Bannock Range to the west, the Portneuf Range to the southeast, and the Chesterfield Range to the northeast. Marsh Creek is the only major tributary to the Portneuf River. Other creeks in this watershed include Mink, Rapid, Garden, Hawkins, Birch, Dempsey, Pebble, Twentyfourmile, and Toponce creeks. The total area of the Chesterfield Reservoir is estimated at 1,236 acres (500 ha).[6]

The Portneuf River's drainage basin is approximately 1,329 square miles (3,442 km2) in area.[4]

Its mean annual discharge, as measured by USGS gauge 13075910 (Portneuf River at Tyhee), is 418 cubic feet per second (11.8 m3/s), with a maximum daily recorded flow of 1,730 cu ft/s (49.0 m3/s) and a minimum of 32 cu ft/s (0.906 m3/s).[5]

History

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The Portneuf River was given its name sometime before 1821 by French Canadian voyageurs working for the Montreal-based fur trading North West Company.[7]

The valley of the Portneuf provided the route of the Oregon Trail and California Trail in the middle 19th century. After the discovery of gold in Montana and Idaho, it became a significant stage route for the transportation of people and goods. In 1877 the valley was used as the route of the Utah and Northern Railway, the first railroad in Idaho.

Recreation Status

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Biogeochemistry of the watershed

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The Portneuf River watershed is a heavily used and anthropogenically altered system. After a series of heavy floods in the early 1960s the Army Corps of Engineers designed and constructed a concrete channel to control flooding in 1965. The channelization followed the river's route and cut through the west side of Pocatello, drastically altering the natural river processes.[8] One common result of human activity is the loading of nutrients into the water system through both point and non-point sources.[9] The river is subjected to use by four municipalities (Lava Hot Springs, McCammon, Inkom, and Pocatello) over its length.[10] The dynamic geology of the region and the heavy use by the local populations have produced a unique set of chemical characteristics associated with both the biological processes and the interactions with the local geology.

Nitrates

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Nutrient runoffs from intensive agriculture and ranching along the route of the river have noticeably increased the nitrate loads in the stream. This is compounded by the addition of treated effluent from the city of Pocatello's wastewater treatment facility and the waste associated with the phosphate processing plant, Simplot. This increased nutrient load supports an increased biomass within the system.[10] The DEQ in collaboration with the City of Pocatello, the Soil Conservation Commission, and USDA are developing tools and practices designed specifically to alleviate the nitrogen issues associated with agriculture and its waste. Known as Best Management Practices (BMPs), these methodologies are designed and modified for varying situations and have proven themselves effective through prior implementation projects.[11]

Carbon exchange

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The exchange of inorganic carbon between the solid earth and the atmosphere in the Portneuf watershed has produced deposits of CaCO3 throughout the system. Known as travertine and tufa, these deposits are formed as a function of the dynamic groundwater and geology of the region. Tufa is known throughout the geologic collective as the soft and porous CaCO3 deposits associated with moving freshwater environments.[12] Travertine is a related deposit separated by the fact that it is associated with thermal waters.[13] Deposition of tufa is complex, involving processes of dissolution, saturation, subsurface transport, emergence and precipitation.[14] Both versions of precipitated CaCO3 are present in the Portneuf watershed. Several very different but related processes control the precipitation of CaCO3 in natural aqueous systems. The chemical processes are driven by the chemical properties of the elements and molecules involved. The physical processes are driven by characteristics of the watershed system (gradient, flow, substrate, groundwater flow properties). The biotic processes are driven by the activities of living organisms.

Chemical processes

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Calcium carbonate formations are associated with regions where meteoric waters become enriched with calcium carbonate by direct dissolution of CaCO3-rich rocks underground only to resurface and re-precipitate calcite. It is well known that the geology of the Portneuf watershed contains large thicknesses of limestone and dolomite strata that are mostly Paleozoic.[10][15] Enrichment of CaCO3 in the meteoric waters is due to the addition of CO2 either through interaction with the atmosphere, or infiltrating through organic compound containing soil layers. This saturation of CO2 in the groundwater allows for the dissolution of carbonate rocks as it drives pH down.[12] As the water reemerges it is exposed to the atmosphere and the concentration gradient of CO2 associated with it. As the enriched waters attempt to achieve equilibrium they precipitate calcite,[14] through the reaction of Ca+2 + 2HCO− ⇔ CO2↑ + H2O+ CaCO3↓. The mountains surrounding the Portneuf are characterized by thick Paleozoic limestone deposits rich in carbonates,[15] and many springs do emerge along the reach associated with Lava Hot Springs.

Physical processes

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Another factor affecting the precipitation of tufa is the physical aspects of the river system. The gradient of the Portneuf through Lava Hot Springs is such that this reach is dominated by a series of riffles with some larger falls. This turbulence and increased surface area caused by aeration facilitate the out gassing of CO2, thus increasing the saturation of CaCO3 to the point of precipitation. This is a phenomenon noticed throughout the world as the development of waterfall tufa[16] and is a relevant explanation for at least some formation through the region, especially through the town site of Lava Hot Springs. The figure below is a schematic representation of the stream gradient of the Portneuf from just below Chesterfield Reservoir and above American Falls Reservoir adapted from Minshall, 1973.

Biotic processes

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The third recognized mechanism for tufa development is the active role played by the biota. Algae and mosses, along with higher plants and some insects, often trap tiny particles within their sinuous roots, fronds, and shelter/feeding structures, acting as nucleation points for further precipitation.[16] This may explain some of the deposition locations, but the biota plays a larger role as photosynthetic plants remove CO2 from the water, further concentrating the Ca2+ and CO32− and driving precipitation. The Portneuf through this reach is rich in plant life not only due to the nutrient accumulation as it travels through farmland but from the warm water inputs that protect the stream from the effects of the harsh cold of winter temperatures. This could be a mechanism for potentially increasing tufa formation through the reach. An interesting study completed in 1972 showed evidence that the development of tufa and travertine filled the interstices normally found on the rocky river. This had implications for some burrowing organisms as well as nutrient cycling.[10]

Precipitation of tufa in the Portneuf drainage is produced through the combination of four complex mechanisms: dissolution of limestones by meteoric waters containing carbonic acids, degassing of CO2 at turbulent sites, the removal of CO2 by photosynthetic plants, and the trapping of particles of CaCO3 by the biota. The complex interactions between these different mechanisms may never be fully understood but offer insight into the occurrence of formations.

See also

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References

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  1. ^ a b c "Portneuf River". Geographic Names Information System. United States Geological Survey, United States Department of the Interior. June 21, 1979. Retrieved July 22, 2013.
  2. ^ Source elevation derived from Google Earth search using GNIS source coordinates.
  3. ^ a b "National Hydrography Dataset". United States Geological Survey. Retrieved July 22, 2013.
  4. ^ a b Upper Snake, Headwaters, Closed Basin Subbasins Plan Plan Archived 2012-02-13 at the Wayback Machine, Northwest Power and Conservation Council
  5. ^ a b c Upper Snake River basin between Idaho Falls and Neeley (includes Willow Creek, Blackfoot and Portneuf River basins), Water Resources Data, Idaho, 2005
  6. ^ "Archived copy" (PDF). Archived from the original (PDF) on 2012-02-13. Retrieved 2008-09-14.{{cite web}}: CS1 maint: archived copy as title (link)
  7. ^ Mackie, Richard Somerset (1997). Trading Beyond the Mountains: The British Fur Trade on the Pacific 1793–1843. Vancouver: University of British Columbia (UBC) Press. p. 26. ISBN 0-7748-0613-3.
  8. ^ Link, Paul, et al. 2010. /about.htm Digital Atlas of Idaho
  9. ^ Royer, T. V., M. B. David & L. E. Gentry, 2006. "Timing of riverine export of nitrate and phosphorus from agricultural watersheds". in "Illinois: implications for reducing nutrient loading to the Mississippi River." Environmental Science and Technology 40: 4126–4131
  10. ^ a b c d Minshall, Wayne G., Douglas A. Andrews, 1973. "An Ecological Investigation of the Portneuf River, Idaho: A Semiarid Land Stream Subjected to Pollution". Freshwater Biology 3:1–30
  11. ^ DEQ, 2003. "Portneuf River Total Maximum Daily Load Agricultural Implementation Plan" 1–159
  12. ^ a b Chen, Jingan, David D. Zhang, Shijie Wang, Tangfu Xiao, and Ronggui Huang, 2004. "Factors controlling tufa deposition in natural waters at waterfall sites." Sedimentary Geology 166: 353–66.
  13. ^ Ford, T.D., and H.M. Pedley, 1996. "A review of tufa and travertine deposits of the world", Earth-Science Reviews, 41 (3–4), 117–175
  14. ^ a b Crosby, 2002. "An Evaluation of Fossil Tufa as a Geochronologic and Paleoclimatic Tool: Naukluft Mountains, Namibia" Unpublished works
  15. ^ a b Crane, Tracy J., P. K. Link, Steven S. Oriel, Diana Boyack, and Beau Johnson. 2001. "Geologic Map of the Lava Hot Springs Quadrangle, Bannock County, Idaho" Map. Moscow, Idaho: Idaho Geological Survey, University of Idaho
  16. ^ a b Zhang, David D., Yingjun Zahng, An Zhu, and Xing Chen, 2001. "Physical Mechanisms of Fiver Waterfall Tufa (Travertine) Formation". Journal of Sedimentary Research 71: 205–16
  • Bond, M.M. 2000, Characterization and Control of Selenium Releases From Mining in the Idaho Phosphate Region. Master's Thesis, Pages 1–58.
  • Babbitt, B. (Ed.). (1998). Guidelines for Interpretation of the Biological Effects of Selected Constituents in Biota, Water and Sediment.
  • D.E.Q. 2007, Preparing Your 2006 IDAHO Drinking Water Consumer Confidence Report (CCR). Page 21.
  • Piper, D.Z. et al.2000, The Phosphoria Formation at the Hot Springs Mine in Southeast Idaho: A Source of Selenium and Other Trace Elements to Surface Water, Ground Water, Vegetation, and Biota: U. S. Geological Survey Open File Report 00-050.
  • Link et al. Lava Hot Springs Quadrangle geologic map, http://www.idahogeology.com/PDF/Technical_Reports_%28T%29/PDF/T-01-3-m.pdf
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