On August 25, 2009 at approximately 1pm, a landslide along Porcupine Bay (part of the Coulee Dam Recreational Area) failed, probably something akin to a debris avalanche. The landslide plunged into the lake, creating a seiche, approximately 5-6 feet high. The seiche struck a camp dock across the bay, damaging some boats and destroying the dock. The landslide also injured two boys, who were thrust under the dock, resulting in minor injuries.

The landslide is reported to be up to an acre in size. The material of the landslide is probably Fraser age glaciolactustrine beds (equivalent to Vashon Stade in Western Washington). It is difficult to determine a trigger mechanism at this point, but this has been a fairly dry year and the lake level might have been dropping fairly rapidly, resulting in a rapid dewatering of the material, resulting in an increase in instability. Unfortunately, such things are hard to determine in photos.

Porcupine Bay Landslide

Photo from NWCN

Porcupine Bay Landslide Photo from KREM

Porcupine Bay Landslide Photo from KREM

I haven’t been able to imbed this within the website, but here is a link to the raw video by Karen Mustard, a camper at Porcupine Bay, who caught the landslide on video:
Watch Video

This is the second landslide this year to have caused a seiche in the Lake Roosevelt area. A landslide that moved in January caused a seiche and damaged docks. No injuries were reported. Link to the January Lake Roosevelt Landslide

Media Links:
Northwest Cable News
Seattle Times
Spokane Spokesman
KATU (Portland)
Seattle PI Washington GeoHazards Blog

Each week we will feature a new landslide in Washington State. Washington State is covered with dynamic and sometimes quirky landslides.

Greider Lake Landslide, Sultan Basin, Snohomish County

Greider Lake is located in the DNR Morningstar Natural Resources Conservation Area (NRCA).

Greider Lake Landslide Location Map

Greider Lake Landslide Location Map

Area: ~366,000 sq. ft.
Width: ~1,400 ft
Length: ~3,000 ft
Depth: ~ 250 ft
Volume: ~1,050,000,000 cu. ft.
Age: Unknown
Trigger: Earthquake

The Greider Lake Landslide splits Greider Lake into two separate lakes, Little Greider Lake and Big Greider Lake. The lake is probably a tarn, which formed during alpine glaciation in this cirque.

Greider Lake Landslide Toe

Greider Lake Landslide Toe

Greider Lake Landslide Scarp

Greider Lake Landslide Scarp

Although it is difficult to determine, the landslide may have moved after the lake was formed.

Greider Lake Landslide_lidar

Greider Lake Landslide 2006 NAIP Orthophoto

Greider Lake Landslide 2006 NAIP Orthophoto

The landslide would have created a large seiche in the lake and probably formed a hyperconcentrated flow or a debris slurry as it moved down hill. The reflection ponds at the base of the hill might be a plunge pool formed by the seiche outwash of Greider Lake.

Greider Lake Landslide Plunge Pool

Greider Lake Landslide Plunge Pool

The red lines in the map represent landslides mapped in the Sultan Basin.

Glacial lake bed deposits form much of the valley floor where Spade Lake is located. There is a faint terrace that might have been deposited after a debris dam formed from the Greider Lake seiche outwash.

Geology of the Sultan Basin

Regional Geology

Regional bedrock that includes the Sultan Basin watershed belongs to the Western Mélange Belt, part of the Western and Eastern Mélange Belts (WEMB) terrain. The WEMB includes Mesozoic (late Jurassic to early Cretaceous) marine sedimentary rocks, along with lenses of Paleozoic limestones, Mesozoic intrusives, and other rock types in fault-bounded bodies that were tectonically juxtaposed (Tabor et al, 1993). The WEMB rocks underwent high pressure, low temperature metamorphism in the late Cretaceous orogeny at about the time they were juxtaposed against the Northwest Cascade System terrain to the North.

Local Geology

Bedrock in the Sultan Basin watershed is mainly composed of the Western and Eastern Mélange Belt (Phipps et al., 2003; Dragovich et al., 2002; Tabor et al., 1993). The oldest units in this watershed are derived from the Stillaguamish Ophiolite (a slice of oceanic crust that has been thrust onto continental crust) suite. Sedimentary rocks were deposited during the late Jurassic to early Cretaceous (170 to 100 million years ago) periods (Carithers and Guard, 1945). The older sedimentary rock formed from thick silt and mud deposited in a marine setting. This unit appears to have had subsequent submarine landslides, resulting in chaotic bedding called mélange (Tabor et al., 1993; Cowan, 1985). Most of the units in the Sultan Basin have been metamorphosed so such features are locally difficult to discern. Younger, continentally derived sediments composed of mostly sand and gravel, of the late Cretaceous and early Paleocene lay unconformably (above a time break in a depositional sequence) on the older rocks (Hedderly-Smith, 1975). Peridotite (dark green to black granite-like rock) intruded around this time into the older marine sedimentary rocks. Hydrothermal systems and submarine eruptions (similar to black smokers) formed from intruding magma, creating large pyritic deposits (such as the Lockwood Pyrite deposit) and overlaid the marine sediment with volcanic (for example, ash and basalt) material (Olson, 1995; Snohomish County, 1979). These rocks were then exposed to regional metamorphism (exposed to heat and pressure). The metamorphism changed the marine sediments into primarily argillite (metamorphosed siltstone), phyllite (metamorphosed mudstone) and chert (white to gray rock) (Yeats, 1964). Sedimentary continental rocks changed primarily into argillite, quartzitic sandstone and meta-conglomerates. Peridotite has metamorphosed into serpentinite (light green to dark green and black dense rock with waxy luster) and talc.

This unit was imbricated (thrust as slivers) into the North American plate by an accretionary wedge (Wells and Heller, 1988; Jett, 1986). The timing for this event is not well known, but is constrained to somewhere between early Cretaceous to the early Eocene (Tabor et al., 1993; Frizzell et al., 1987). This was primarily done by faults, many of the faults responsible for this imbrication can still be seen trending northwesterly within the watershed, where they form saddles and linear drainages. Most or all of these faults are no longer active. Severe folding also occurred during imbrication.

The Bald Mountain pluton is composed of granodiorite (light gray granitic rock) intruded into the area in the early to mid-Eocene (55 to 49 Ma). Contact metamorphism can be seen near the edges of the pluton and marine metamorphic rock, resulting in gneissic margins (light gray large grained metamorphic rock) (Dungan, 1974; Carithers and Guard, 1945). This unit locally occurs around Bald Mountain and no further outcrops occur to the east.

Miocene batholiths (Vesper Peak stock and the Index batholith) intruded into the Stillaguamish Ophiolitic suite. These intrusions are primarily composed of tonalite (light gray granitic rock). The Index batholith caused widespread hydrothermal alteration and metamorphism throughout the ophiolitic units in the Sultan Basin (Baum, 1968). It appears, either a product of weathering or regional intrusive patters, that the southern part of the Sultan Basin experienced higher temperature metamorphism than the northern part, as seen by the minerals at the Sultan King mine and the .45 mine. High temperature minerals, such as magnetite and molybdenite are found at the Sultan King mine. Low temperature minerals are found in the .45 mine, such as galena and ruby silver (Carithers and Guard, 1945).

As the batholiths cooled, metal-bearing solutions and subsurface waters flowed into the metamorphic sedimentary rocks, following cracks from the intruding batholiths, sheer zones and faults. As these solutions lost pressure and temperature, they precipitated ore minerals in veins (Carithers and Guard, 1945). Due to the long history within the watershed of faulting, shearing and intrusion, no common structure exists for these veins to follow.

Glacial Material and Recent History

The Sultan Basin consists of continental glacial drift, alpine glacial drift, alluvium and talus. About 14,000 years ago, the Puget Lobe of the Cordilleran ice sheet, which represents the most recent advance of continental ice sheet, flowed into surrounding valleys. The deposits of this glaciation are called the ‘Vashon Drift’ locally. Tongues of the Vashon glacier dammed valleys that were tributaries to the Puget Lowlands, creating large ice dammed lakes. Glaciers advanced up the Pilchuck River system and the Sultan valley, covering the northwestern portion of the watershed (Tabor et al., 1993; Booth, 1990). This blocked the paleo-Pilchuck River, creating a large ice-dammed lake, known as glacial Lake Sultan and depositing outwash (deltas) and lacustrine (lake deposits) on the north flanks of Blue Mountain to Bald Mountain and upstream to midway on the south fork of the Sultan River, Elk Creek and Williamson Creek drainage. This rising lake eventually overflowed, washed over Olney Pass, and deposited fluvial outwash across the plains in the west and south parts of the Sultan River watershed.

As the glaciers retreated, the terminal moraine (sediment collected at the end of the glaciers) locally called the ‘Pilchuck Plug’ blocked the upper drainage of the Pilchuck River, creating the new Sultan River watershed (Coombs, 1969; Bliton, 1989). The Sultan River established a channel, rapidly incised into the glacial material, cut into the bedrock, and became entrenched. This incision is probably due to easily eroding glacial material and isostatic rebound of the bedrock in the area. Relict meander bends and channels can be seen near the main channel of the present Sultan River.

Alpine glaciation, predominately after the last of the major continental glaciation, formed much of the topography in the upper Sultan Basin. Alpine glaciation deposits make up most of the river valleys (beneath river alluvium). Alpine drift can also be traced up much of the valleys, from Bear Creek to the upper mountain peaks of the Sultan Basin. A steady decline in alpine glaciation has occurred within the watershed and almost all alpine glaciers have disappeared. Currently, only one major glacier northeast of Copper Lake exists.

Slope Stability and Geology

Geologic units within this area have affected general slope stability. The marine metasedimentary units (including the Stillaguamish Ophiolite suite), present predominately in the southwest section of the watershed, have beds striking between N 5 to W 20 with a variety of dipping beds (due to tightly folded and faulting). This unit has been observed in field and aerial photo interpretation to have a higher landslide frequency, specifically when bedding is near vertical. Historically, hundreds of debris flows have occurred in areas where these geology factors are present. Vertical beds are known to occur near Blue Mountain Ridge, but dips seem to gradually decrease towards the South Fork of the South Fork of the Sultan River. Bedding that is dipping into the mountain or at angles that are not at or near vertical have not been shown to produce landslides, but field verification should be considered in areas where this geology is present.

Regional metamorphic units observed within the watershed have not been shown to increase or decrease slope stability within the watershed. These rocks trend along the peaks and ridges along the eastern edge of the watershed, from Hard Pass to Crested Buttes and north to Gothic Peak and Headlee Pass. The beds strike N 15 to W 20 and dip from vertical at Headlee pass, to 35 E near Crested Buttes. These rocks are very resistant to erosion, have a lower landslide activity and can create steep cliffs above the valley (Carithers and Guard, 1945).

Altered peridotite and serpentinite (dark green to black rock that feels slippery), although it has not locally been shown to cause slope instability, has created major slope stability issues in other areas (for example, Blewett Pass). These ultramafic rock types occur primarily in a strip north of Red Mountain, 500 to 1,000 feet wide and striking northwest. However, pockets of ultramafic rock can occur throughout the watershed (Tabor et al, 1993).

Tonalite (light gray granitic rock) from the Index Batholith and Vesper Stock have caused major rock topples. A prominent feature present within the rock is three strong joint planes. These planes can aid in rocks breaking into rectangular blocks or wedges, as large as 15 feet on each side (Carithers and Guard, 1945). Most rock topples recorded were independent of harvest or road construction and are generated by erosion of the basin. However, two major rock avalanches were located in this area, one dividing upper and lower Greider Lakes, the other west of Vesper Peak. A brief field investigation of these rock avalanche sites has led to the theory that these landslides have been seismically triggered. Both landslides are located adjacent to fault zones. Large regional earthquakes from outside of the watershed could generate major rock topples within this watershed in the future.

Baum, L. F., 1968, Geology and mineral deposits, Vesper Peak stock area, Snohomish County, Washington: University of Washington Master of Science thesis, 75 p., 1 plate

Bliton, William S., 1989, Sultan River project. IN Galster, R. W., chairman, Engineering geology in Washington: Washington Division of Geology and Earth Resources Bulletin 78, v. I, p. 209-216.

Booth, Derek B., 1990, Surficial geologic map of the Skykomish and Snoqualmie Rivers area, Snohomish and King Counties, Washington: U.S. Geological Survey Miscellaneous Investigations Series Map I-1745, 2 sheets, scale 1:50,000, with 22 p. text.

Carithers, Ward; Guard, A. K., 1945, Geology and ore deposits of the Sultan Basin, Snohomish County, Washington: Washington Division of Mines and Geology Bulletin 36, 90 p., 1 plate.

Coombs, H. A., 1969, Leakage through buried channels: Association of Engineering Geologists Bulletin, v. 6, no. 1, p. 45-52.

Cowan, Darrel S., 1985, Structural styles in Mesozoic and Cenozoic mélanges in the western Cordillera of North America: Geological Society of America Bulletin, v. 96, no. 4, p. 451-462.

Dragovich, Joe D.; Logan, Robert L.; Schasse, Henry W.; Walsh, Timothy J.; Lingley, William S., Jr.; Norman, David K.; Gerstel, Wendy J.; Lapen, Thomas J.; Schuster, J. Eric; Meyers, Karen D., 2002, Geologic map of Washington–Northwest quadrant: Washington Division of Geology and Earth Resources Geologic Map GM-50, 3 sheets, scale 1:250,000, with 72 p. text.

Dungan, M. A., 1974, the origin, emplacement, and metamorphism of the Sultan mafic-ultramafic complex, North Cascades, Snohomish County, Washington: University of Washington Doctor of Philosophy thesis, 227 p., 3 plates.

Frizzell, Virgil A., Jr.; Tabor, Rowland W.; Zartman, Robert E.; Blome, Charles D., 1987, Late Mesozoic or early Tertiary mélanges in the western Cascades of Washington. IN Schuster, J. E., editor, Selected papers on the geology of Washington: Washington Division of Geology and Earth Resources Bulletin 77, p. 129-148.

Hedderly-Smith, D. A., 1975, Geology of the Sunrise breccia pipe, Sultan Basin, Snohomish County, Washington: University of Washington Master of Science thesis, 60 p., 2 plates.

Jett, Guy A., 1986, Sedimentary petrology of the western mélange belt, north Cascade Range, Washington: University of Wyoming Master of Science thesis, 85 p.

Olson, Duane F., 1995, Geology and Geochemistry of the Lockwood Volcanogenic Massive Sulfide Deposit, Snohomish County, Washington: Western Washington University Master of Science thesis, 118 p., 8 plates.

Phipps, Richard W.; McKay, Donald T., Jr.; Norman, David K.; Wolff, Fritz E., 2003, Inactive and abandoned mine lands–Spada Lake and Cecile Creek watershed analysis units, Snohomish and Okanogan Counties, Washington: Washington Division of Geology and Earth Resources Open File Report 2003-3, 36 p.

Snohomish County Public Utility District No. 1; Washington Department of Ecology, 1979, Sultan River project, Stage II; Application for amended license, FERC project no. 2157–State of Washington final SEPA EIS and FERC environmental report (exhibit W): Snohomish County Public Utility District No. 1, 2 v.

Tabor, R. W.; Frizzell, V. A., Jr.; Booth, D. B.; Waitt, R. B.; Whetten, J. T.; Zartman, R. E., 1993, Geologic map of the Skykomish River 30- by 60-minute quadrangle, Washington: U.S. Geological Survey Miscellaneous Investigations Series Map I-1963, 1 sheet, scale 1:100,000, with 42 p. text.

Wells, Ray E.; Heller, Paul L., 1988, The relative contribution of accretion, shear, and extension to Cenozoic tectonic rotation in the Pacific Northwest: Geological Society of America Bulletin, v. 100, no. 3, p. 325-338.

Yeats, R. S., 1964, Crystalline klippen in the Index district, Cascade Range, Washington: Geological Society of America Bulletin, v. 75, no. 6, p. 549-561, 1 plate.

Trying to keep track of all of the landslides occurring in Washington State is a difficult task. Normally, I hear about most of the important ones via media reports, but this one escaped me, probably because of all of the activities following the January 7-8th storm.

National Park Service Morning Report

“On Friday, January 16th, a large landslide occurred adjacent to the Spokane River near Mill Canyon. Homeowners in the Mill Canyon area contacted the park and reported that their docks had been destroyed by a large wave. Responding rangers found that a section of hillside measuring approximately 17 acres in size had broken free across from Breezy Bay and that the subsequent landslide had fallen into the water, creating a wave that was about 30 feet high when it hit the southern shore about a thousand yards across the lake. The wave damaged or destroyed several private docks located at Breezy Bay, Moccasin Bay, Sunset Point and Arrowhead Point. Several vessels moored in the area were also swamped and left beached on land. The water reached one residence before receding and came just to the foundations of several others. The full extent of the damage caused by the landslide is not yet known. Damage to property was documented as far as a mile and a half downstream, and significant resource damage and erosion to the shoreline occurred as far as three miles downstream. The park has issued a general safety warning due to the debris in the water, which is making navigation difficult. Boaters in the area have been advised to use extreme caution when boating from Cayuse Cove to Breezy Bay on the Spokane River. Along with ice deposits in the lake, there are now large trees, dead heads, dock parts, and unknown sediment deposits that have made safe navigation difficult. Due to unknown conditions near the slide, visitors are also being advised to avoid going on land at the site, as the ground will be quite unstable for some time and sinkholes and falling debris may occur. [Submitted by Adam Kelsey, Acting Chief Ranger]”

Lake Roosevelt Landslide?

Lake Roosevelt Landslide?

I am attempting to contact Ranger Adam Kelsey in regards to the exact location and any additional information on the landslide.

A good friend of mine and coworker, Trevor Contreras, ran across this photo of the suspected bluff in Cruden and Varnes (1996) landslide processes paper:

Lake Roosevelt Landslide - Cruden and Varnes

Lake Roosevelt Landslide - Cruden and Varnes

This before photo clearly shows little debris at the base of the bluff. and gives an approximate idea of how large the landslide is in size.

Past History
Lake Roosevelt National Park has a long history of landslides. I recall a document by the Emergency Management Division of Washington Military Department regarding landslide histories in this document
“• 1944 to 1953 – Massive landslides generated a number of inland tsunamis in Lake Roosevelt in Eastern Washington:
• April 8, 1944 – A four to five million cubic yard landslide from Reed Terrace generated a 30-foot wave, 5,000 feet away on the opposite shore of the lake about 98 miles above Grand Coulee Dam.
• July 27, 1949 – A two to three million cubic yard landslide near the mouth of Hawk Creek created a 65-foot wave that crossed the lake about 35 miles above Grand Coulee Dam; people 20 miles away observed the wave.
• February 23, 1951 – A 100,000 to 200,000 cubic yard landslide just north of Kettle Falls created a wave that picked up logs at the Harter Lumber Company Mill and flung them through the mill 10 feet above lake level.
• April 10 – 13, 1952 – A 15 million cubic yard landslide three miles below the Kettle Falls Bridge created a 65-foot wave that struck the opposite shore of the lake. People observed some waves six miles up the lake.
• October 13, 1952 – A landslide 98 miles upstream of Grand Coulee Dam created a wave that broke tugboats and barges loose from their moorings at the Lafferty Transportation Company six miles away. It also swept logs and other debris over a large area above lake level.
• February 1953 – A series of landslides about 100 miles upstream from Grand Coulee Dam generated a number of waves that crossed the lake and hit the opposite shore 16 feet above lake level. On average, observed waves crossed the 5,000-foot wide lake in about 90 seconds.
• April – August 1953 – Landslides originating in Reed Terrace caused waves in the lake at least 11 different times. The largest wave to hit the opposite shore was 65 feet high and observed six miles away. Velocity of one of the series of waves was about 45 miles per hour.”

Some more history from Stevens County in chapter 5 of their Multi-Hazard Mitigation Plan

“• April 8, 1944 – A four to five million cubic yard landslide from Reed Terrace generated wave, 5,000 feet away on the opposite shore of the lake about 98 miles above Dam.
• April 10 – 13, 1952 – A 15 million cubic yard landslide three miles below the Kettle created a 65-foot wave that struck the opposite shore of the lake. People observed six miles up the lake.
• February 1953 – A series of landslides about 100 miles upstream from Grand generated a number of waves that crossed the lake and hit the opposite shore lake level. On average, observed waves crossed the 5,000-foot wide lake in about
• April – August 1953 – Landslides originating in Reed Terrace caused waves in the 11 different times. The largest wave to hit the opposite shore was 65 feet high and miles away. Velocity of one of the series of waves was about 45 miles per hour.”

So, what is causing all of these landslides? The USGS in their report on significant landslide events in the United States summarizes:

“In summary the shores of Roosevelt Lake have been subject to several hundred landslides since the reservoir began to be filled during construction of Grand Coulee Dam during the 1930’s and early 1940’s. The greatest percentage of landslide activity occurred during initial filling of the reservoir, but many slope failures also have been caused by intermittent drawdown of the reservoir level. In addition, occasional slope failures have occurred as natural phenomena, related more to wet winters than to fluctuation of the reservoir.”

Static Liquification from water level changes and changes the surrounding hydrology probably does play a big roll in landslides, it is something that you can see in most of our major dammed lakes. There might be other triggers as well.

Lake Roosevelt Landslide

Lake Roosevelt Landslide

In eastern Washington, there are certain triggers when looking at landslides. Potentially, agriculture can play a role in landslides along bluffs and in the long-term, the watering of crops above these bluffs does play a role. Chances are, they weren’t watering in January. The area also had a huge amount of snow this winter and January 16th was in that period where we had a warming trend. So, perhaps snow melt helped to increase the amount of water into the subsurface as well.