Stratigraphic constraints on the timing and emplacement of the Alika 2 giant Hawaiian submarine landslide

McMurtry, Gary M.; Herrero‐Bervera, Emilio; Cremer, Maximilian D; Smith, John R.; Resig, Johanna M.; Sherman, Clark; Torresan, Michael E.

doi:10.1016/s0377-0273(99)00097-9

Cited by 59 publications

(42 citation statements)

References 42 publications

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“…Flank seismicity, for example, of the magnitude of the great 1868 Ka'u (M $ 8.0) or the 1975 Kalapana earthquakes (M7.2) would certainly shake the submarine flanks, dislodging precarious slope deposits, but such seismicity accompanies flank sliding and must be ongoing, at least for an extensive period of volcanic evolution. Catastrophic flank collapse of the scale observed here, and documented around the islands, is thought to occur relatively late in the evolution of the volcano [e.g., Moore et al, 1989], and may coincide with unusually energetic volcanic eruptions, perhaps explosive in nature [Clague and Dixon, 2000;McMurtry et al, 1999]. Kilauea volcano has experienced at least two extraordinary phreatomagmatic eruptions within the last 50,000 years, both associated with collapse of the summit caldera, and responsible for massive ash deposits dated at 49 and 23-29 ka [Clague et al, 1995].…”

Section: Collapse Of the Central Flank And Growth Of The Outer Benchmentioning

confidence: 86%

Slope failure and volcanic spreading along the submarine south flank of Kilauea volcano, Hawaii

2003

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[1] New multichannel reflection data and high-resolution bathymetry over the submarine slopes of Kilauea volcano provide evidence for current and prior landsliding, suggesting a dynamic interplay among slope failure, regrowth, and volcanic spreading. Disrupted strata along the upper reaches of Kilauea's flank denote a coherent slump, correlated with the active Hilina slump. The slump comprises mostly slope sediments, underlain by a detachment 3-5 km deep. Extension and subsidence along the upper flank is compensated by uplift and folding of the slump toe, which surfaces about midway down the submarine flank. Uplift of strata forming Papa'u seamount and offset of surface features along the western boundary of Kilauea indicate that the slump has been displaced $3 km in a southsoutheast direction. This trajectory matches coseismic and continuous ground displacements for the Hilina slump block on land, and contrasts with the southeast vergence of the rest of the creeping south flank. To the northeast, slope sediments are thinned and disrupted within a recessed region of the central flank, demonstrating catastrophic slope failure in the recent past. Debris from the collapsed flank was shed into the moat in front of Kilauea, building an extensive apron. Seaward sliding of Kilauea's flank offscraped these deposits to build an extensive frontal bench. A broad basin formed behind the bench and above the embayed flank. Uplift and back tilting of young basin fill indicate recent, and possibly ongoing, bench growth. The Hilina slump now impinges upon the frontal bench; this buttress may tend to reduce the likelihood of future catastrophic detachment.

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Section: Collapse Of the Central Flank And Growth Of The Outer Benchmentioning

confidence: 86%

Slope failure and volcanic spreading along the submarine south flank of Kilauea volcano, Hawaii

2003

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“…Volcaniclastic turbidite layers in abyssal-plain are important records of catastrophic failures (e.g. Moore and Holcomb 1994;Garcia 1996;Masson 1996;McMurtry et al 1999). Some of them may not directly reflect the actual failure event but mainly record secondary reworking of unconsolidated matrix facies.…”

Section: South Kona Slide and Debris-avalanche Matrixmentioning

confidence: 99%

“…The volume of the slides derived from the west flank of ancestral Mauna Loa volcano has been estimated at 1,500-2,000 km 3 (Lipman et al 1988). The age of the South Kona landslide is considered to be no older than about 250 ka , while the Alika-2 debris avalanche is the youngest among major slides, at about 105 ka (McMurtry et al 1999). Because the South Kona landslide has been considered to be a complex slide area involving multiple failure events Moore and Chadwick 1995), we use the name "South Kona slide complex."…”

Section: Introductionmentioning

confidence: 99%

Emplacement mechanisms of the South Kona slide complex, Hawaii Island: sampling and observations by remotely operated vehicle Kaiko

Yokose

Lipman

2004

Bull Volcanol

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Emplacement of a giant submarine slide complex, offshore of South Kona, Hawaii Island, was investigated in 2001 by visual observation and in-situ sampling on the bench scarp and a megablock, during two dives utilizing the Remotely Operated Vehicle (ROV) Kaiko and its mother ship R/V Kairei. Topography of the bench scarp and megablocks were defined in 3-D perspective, using high-resolution digital bathymetric data acquired during the cruise. Compositions of 34 rock samples provide constraints on the landslide source regions and emplacement mechanisms. The bench scarp consists mainly of highly fractured, vesiculated, and oxidized a'a lavas that slumped from the subaerial flank of ancestral Mauna Loa. The megablock contains three units: block facies, matrix facies, and draped sediment. The block facies contains hyaloclastite interbedded with massive lava, which slid from the shallow submarine flank of ancestral Mauna Loa, as indicated by glassy groundmass of the hyaloclastite, low oxidation state, and low sulfur content. The matrix facies, which directly overlies the block facies and is similar to a lahar deposit, is thought to have been deposited from the water column immediately after the South Kona slide event. The draped sediment is a thin high-density turbidite layer that may be a distal facies of the Alika-2 debris-avalanche deposit; its composition overlaps with rocks from subaerial Mauna Loa. The deposits generated by the South Kona slide vary from debris avalanche deposit to turbidite. Spatial distribution of the deposits is consistent with deposits related to large landslides adjacent to other Hawaiian volcanoes and the Canary Islands.

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“…The most studied examples are from the Hawaiian and Canary islands (McMurtry et al, 1999). Eruption-generated events are fewer, with the most devastating from Krakatau, 1883 (Francis and Self, 1983).…”

Section: Volcanic Tsunamismentioning

confidence: 99%

The Generation of Tsunamis

Tappin

2017

Encyclopedia of Maritime and Offshore Engineering

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Tsunamis are gravity‐driven water waves. Most are generated by vertical displacement of the seabed that propagates through the water column to the sea surface. The resulting elevated surface wave collapses through gravity and then propagates outward from the source. Dispersion of the initial wave generates a multiple wave train. Tsunamis are mainly (∼80%) generated by earthquakes, but other mechanisms include subaerial and submarine landslides and volcanic collapse and eruption. Other, less frequent, tsunami mechanisms include bolide (asteroid) impact and weather events (meteotsunamis), but these are generated at the water surface, respectively, from external impact and from wind friction. The magnitude of a tsunamigenic earthquake has the main control on the tsunami, although “tsunami” earthquakes generate tsunamis much larger than expected from their earthquake source magnitude. Tsunamigenic earthquake mechanisms include interplate boundary rupture, splay faulting, and intraplate rupture. Landslide tsunami mechanisms include slumps and translational failures that may be initiated from either the bottom or the top. Landslide volume, water depth, and initial acceleration are the main controls on tsunami magnitude, although other factors such as the failure mechanism and the location of initiation are influential. There are three main aspects of a tsunami; (i) initial wave generation, (ii) propagation, and (iii) onland run‐up. Initial wave generation from earthquakes is mainly from seabed vertical displacement, and a rule of thumb suggests that in most instances the maximum initial wave elevation is up to twice this. The maximum initial wave elevation from a landslide tsunami is theoretically determined by the ocean depth and thus could be thousands of meters. Local tsunami run‐up elevations vary with source mechanism and vary considerably. Although dependent on local bathymetry and topography, these are likely to be more elevated and focused from submarine landslides than from earthquakes. The different mechanisms generate different tsunami wave frequencies; these determine travel distances, with the low frequency tsunamis from earthquakes traveling much farther than tsunamis from landslides, which are much higher frequency. Final onland run‐up is mainly dependent on source mechanism as well as local offshore bathymetry and coastal topography.

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Stratigraphic constraints on the timing and emplacement of the Alika 2 giant Hawaiian submarine landslide

Cited by 59 publications

References 42 publications

Slope failure and volcanic spreading along the submarine south flank of Kilauea volcano, Hawaii

Slope failure and volcanic spreading along the submarine south flank of Kilauea volcano, Hawaii

Emplacement mechanisms of the South Kona slide complex, Hawaii Island: sampling and observations by remotely operated vehicle Kaiko

The Generation of Tsunamis

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