Little Tahoma Peak Rockfalls and Avalanches, Mount Rainier, Washington, U.S.A.

Fahnestock, Robert K.

doi:10.1016/b978-0-444-41507-3.50013-1

Cited by 21 publications

(10 citation statements)

References 4 publications

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“…1) that started on an inaccessible suspended glacier. Cases have been presented among the others by Barla et al (2000), Bottino et al (2002), Evans et al (1989), Evans and Clague (1988), Fahnestock (1978), Hewitt (2009), Sosio et al (2008. The Sherman landslide is another famous example of landslide fallen on a glacier.…”

Section: General Considerationsmentioning

confidence: 90%

Introduction to the Physics of Landslides

Blasio¹

2011

124

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Section: General Considerationsmentioning

confidence: 90%

Introduction to the Physics of Landslides

Blasio¹

2011

124

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“…Many other avalanches have been inferred to have slid into place in a similar manner (e.g. , Fahnestock 1978;Erismann 1979;Shaller 1991 and references therein;Clavero et al 2007). Of course in detail significant departures from ideal plug flow would have occurred due to effects such as avalanche heterogeneity, temporal and spatial variations or pore pressure, and/or local topography, and we stress that this is certainly only a crude approximation of the real behaviour.…”

Section: Implications For Rheological Behaviourmentioning

confidence: 95%

Topographic reflection of the Socompa debris avalanche, Chile

et al. 2008

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International audienceOne of the most remarkable features of the exceptionally well preserved 26 km3 Socompa debris avalanche deposit is the evidence for topographically driven secondary flow. The avalanche formed by sector collapse of Socompa stratovolcano and spread 40 km across a preexisting basin, forming a sheet of ∼50 m average thickness. As the avalanche impinged on the western and northern margins of the basin, it was reflected back, forming a secondary flow that continued to travel 15 km down a gentle slope at an oblique angle to the primary flow, the front of the return wave being preserved frozen on the surface of the deposit as a prominent escarpment. Satellite images, aerial photos, digital elevation models and field observations were used to reconstruct the sequence of events during avalanche emplacement, and in particular during secondary flow. The avalanche sheet was divided into distinct terrane groups, each believed to have experienced a particular strain history during emplacement. Evidence for avalanche reflection includes clearly recognizable secondary slide masses, sub-parallel sets of curvilinear shear zones, headwall scarps separating the (primary) levée from the secondary terranes, extensional jigsaw breakup of surface lithologies during return flow, and cross cutting, or deflection, of primary flow fabrics by secondary terranes. Reflection off the basin margin took place in an essentially continuous manner, most major return motions being simultaneous with, or shortly following, primary flow. The secondary flow occurred as a wave that swept obliquely across the primary avalanche direction, remobilizing the primary material, which was first compressed, then stretched, as it passed over and rearward of the wave front. As return flow occurred, surface lithologies were rifted in a brittle manner, and the slabs were sheared pervasively as they glided and rotated back into the basin; some sank into the more fluidal interior of the avalanche, which drained out into a prominent distal lobe. Extension by factors of up to 1.8 took place during return flow. Secondary flow took place on slopes of only a few degrees, and the distal lobe flowed 8 km on a slope of ∼1°. Overall the avalanche is inferred to have slid into place as a fastmoving sheet of fragmental rock debris, with a leading edge and crust with near-normal friction and an almost frictionless, fluidal interior and base. The avalanche emplacement history deduced from field evidence is consistent with the results of a previously published numerical model of the Socompa avalanche

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“…On another hand, mechanisms involving lubrication reduce internal friction only in the basal part of the flow. They are based on the presence of an air cushion [ Shreve , ; Fahnestock , ], water‐saturated basal layer [ Johnson , ; Voight and Sousa , ], molten basal layer [ Erismann , ; De Blasio and Elverhøi , ], or sliding sediment layer beneath the flow [ Watson and Wright , ].…”

Section: Introductionmentioning

confidence: 99%

The extreme mobility of debris avalanches: A new model of transport mechanism

et al. 2015

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Large rockslide‐debris avalanches, resulting from flank collapses that shape volcanoes and mountains on Earth and other object of the solar system, are rapid and dangerous gravity‐driven granular flows that travel abnormal distances. During the last 50 years, numerous physical models have been put forward to explain their extreme mobility. The principal models are based on fluidization, lubrication, or dynamic disintegration. However, these processes remain poorly constrained. To identify precisely the transport mechanisms during debris avalanches, we examined morphometric (fractal dimension and circularity), grain size, and exoscopic characteristics of the various types of particles (clasts and matrix) from volcanic debris avalanche deposits of La Réunion Island (Indian Ocean). From these data we demonstrate for the first time that syn‐transport dynamic disintegration continuously operates with the increasing runout distance from the source down to a grinding limit of 500 µm. Below this limit, the particle size reduction exclusively results from their attrition by frictional interactions. Consequently, the exceptional mobility of debris avalanches may be explained by the combined effect of elastic energy release during the dynamic disintegration of the larger clasts and frictional reduction within the matrix due to interactions between the finer particles.

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Little Tahoma Peak Rockfalls and Avalanches, Mount Rainier, Washington, U.S.A.

Cited by 21 publications

References 4 publications

Introduction to the Physics of Landslides

Introduction to the Physics of Landslides

Topographic reflection of the Socompa debris avalanche, Chile

The extreme mobility of debris avalanches: A new model of transport mechanism

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