Upper Elk River valley, British Columbia

1921 ◽  
Author(s):  
J R Marshall
Keyword(s):  
British Columbia ◽  
River Valley ◽  
Elk River

scholarly journals Landslides in weakly cemented glaciolacustrine sediments, Morkill River valley, British Columbia

2001 ◽  
Vol 38 (4) ◽  
pp. 889-900 ◽  
Author(s):  
Corey R Froese ◽  
David M Cruden
Keyword(s):  
British Columbia ◽  
River Valley ◽  
Carbonate Content ◽  
Canadian Rocky Mountains ◽  
Density Profiles ◽  
Frost Action ◽  
Dominant Component ◽  
Freeze And Thaw ◽  
Calcite Cement ◽  
The Relationship

Slopes in weakly cemented glaciolacustrine sediments in the Morkill River valley in the Canadian Rocky Mountains stand at up to 70°. Based on field and laboratory observations it appears that a contributing factor to instability is the softening of the soils by frost action and the leaching of calcite cement. Field density profiles demonstrated increased density and carbonate content with an increase in depth. Laboratory tests of carbonate content indicated a positive correlation between calcium carbonate and density in the glaciolacustrine sediments. The relationship was strongest in sands, in which leaching and dissolution were important components of softening. In clays, frost action was the dominant component of softening. Freeze-thaw tests showed a 50% decrease in strength after one cycle of freeze and thaw in the silts and clays.Key words: landslide, cemented, glaciolacustrine sediments, British Columbia.

Control of artesian pressure by bleeder wells

1979 ◽  
Vol 16 (3) ◽  
pp. 488-496 ◽  
Author(s):  
N. H. Wade ◽  
H. Taylor
Keyword(s):  
British Columbia ◽  
River Valley ◽  
Seasonal Peak ◽  
Clayey Silt ◽  
Artesian Aquifer ◽  
Sand And Gravel ◽  
Site Test ◽  
Gravel Aquifer

Deep test bleeder wells were installed in an artesian aquifer underlying the Bridge River No. 1 hydroelectric generating station in southern British Columbia to determine whether seasonal peak artesian pressures could be controlled.The Bridge River complex, built in the early 1950's, consists of two powerhouses located about a kilometre apart on the shore of Seton Lake, a system of power tunnels, and surface penstocks, which conduct water from the Carpenter Lake reservoir in Bridge River valley to the powerhouses. The No. 1 powerhouse is founded on consolidated deposits of clayey silt, underlain by sand and gravel. Shortly after the powerhouse was constructed, ground and powerhouse movements occurred. It was later determined that such movement was caused by high artesian pressures in the sand and gravel aquifer under the powerhouse.Attempts to install bleeder wells in 1952 were unsuccessful and an offshore fill was constructed as a toe weight, which functioned adequately until 1974 when additional ground cracking was observed. After further study and additional drilling at the site, test bleeder wells and piezometers were installed in 1976.Tests conducted to assess the effect of the bleeder wells indicated that control of excessive artesian pressures by a system of bleeder wells was feasible.

Eocene paleo-physiography and drainage directions, southern Interior Plateau, British Columbia

2005 ◽  
Vol 42 (2) ◽  
pp. 215-230 ◽  
Author(s):  
Selina Tribe
Keyword(s):  
British Columbia ◽  
Middle Eocene ◽  
Regional Scale ◽  
River Valley ◽  
Coast Mountains ◽  
Base Level ◽  
The North ◽  
Bedrock Geology ◽  
River Valleys ◽  
Early Cenozoic

A map of reconstructed Eocene physiography and drainage directions is presented for the southern Interior Plateau region, British Columbia south of 53°N. Eocene landforms are inferred from the distribution and depositional paleoenvironment of Eocene rocks and from crosscutting relationships between regional-scale geomorphology and bedrock geology of known age. Eocene drainage directions are inferred from physiography, relief, and base level elevations of the sub-Eocene unconformity and the documented distribution, provenance, and paleocurrents of early Cenozoic fluvial sediments. The Eocene landscape of the southern Interior Plateau resembled its modern counterpart, with highlands, plains, and deeply incised drainages, except regional drainage was to the north. An anabranching valley system trending west and northwest from Quesnel and Shuswap Highlands, across the Cariboo Plateau to the Fraser River valley, contained north-flowing streams from Eocene to early Quaternary time. Other valleys dating back at least to Middle Eocene time include the North Thompson valley south of Clearwater, Thompson valley from Kamloops to Spences Bridge, the valley containing Nicola Lake, Bridge River valley, and Okanagan Lake valley. During the early Cenozoic, highlands existed where the Coast Mountains are today. Southward drainage along the modern Fraser, Chilcotin, and Thompson River valleys was established after the Late Miocene.

RECORDS OF ADDITIONAL EUROPEAN SAWFLIES IN AMERICA AND DESCRIPTIONS OF NEW VARIETIES OF NORTH AMERICAN SPECIES

1932 ◽  
Vol 64 (11) ◽  
pp. 247-251 ◽  
Author(s):  
Herbert H. Ross
Keyword(s):  
British Columbia ◽  
North American ◽  
West Coast ◽  
River Valley ◽  
North American Species ◽  
Alnus Rubra ◽  
Fraser River ◽  
The West ◽  
New Varieties ◽  
The Common

This species has apparently been introduced in recent years and become established as a pest of the common native alder (Alnus rubra) on the west coast of Washington and British Columbia, particularly in the lower part of the Fraser River Valley. The earliest specimens I have at hand are a series of 15 females taken at White Rock, B. C., June 28, 1929, collected by Mr. G. Beall.

Late Pleistocene stratigraphy and chronology of lower Chehalis River valley, southwestern British Columbia: evidence for a restricted Coquitlam Stade

2004 ◽  
Vol 41 (7) ◽  
pp. 881-895 ◽  
Author(s):  
Brent C Ward ◽  
Bruce Thomson
Keyword(s):  
British Columbia ◽  
Late Pleistocene ◽  
River Valley ◽  
Glacial Lakes ◽  
Coast Mountains ◽  
Source Areas ◽  
Definitive Evidence

Sediments in lower Chehalis valley span middle Wisconsin (Olympia nonglacial interval) to Holocene time. Sediments are divided into six units with chronological control provided by 14 new radiocarbon ages. Fluvial gravel spans the transition from the late Olympia nonglacial interval to the early Fraser Glaciation. Glaciolacustrine sedimentation represents the first definitive glacial activity in the valley and indicates that Vashon ice in the Fraser Lowland blocked the mouth of the Chehalis valley at ca. 18–17 ka BP. Ice then flowed down the Chehalis valley. The Chehalis valley deglaciated while ice persisted in the Fraser Lowland, forming another lake. After this lake drained, terraces and fans formed. This style of glaciation–deglaciation is typical of many watersheds peripheral to the Fraser Lowland in that local valley ice was slightly out of phase with ice in the lowland. This resulted in glacial lakes forming during both advance and retreat phases. However, in contrast to watersheds in the northwestern Fraser Lowland, no definitive evidence of a Coquitlam ice advance was found within the Chehalis valley. Although glaciers in the area were likely active and advancing, data from the Chehalis valley indicates that they were not as extensive as previously thought. Since ice source areas in the northeastern Fraser Lowland are in the leeward area of the Coast Mountains, it is suggested that lower precipitation resulted in limited glacier activity there during the Coquitlam Stade.

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