Pahoehoe Flows from the 1969–1971 Mauna Ulu Eruption, Kilauea Volcano, Hawaii

Swanson, Donald A.

doi:10.1130/0016-7606(1973)84<615:pfftmu>2.0.co;2

Cited by 232 publications

(154 citation statements)

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“…10b); glassy rims ~4 cm thick & lacking vesicles; generally pillow interiors also lack vesicleshowever, large former gas cavities are found in pillow interiors (Fig. 10b, white spot in the central pillow); similar gas pockets are observed in certain types of degassed pahoehoe lavas in Hawaii (Swanson, 1973).…”

Section: B 40 M-thick Sequence Of Pillow-palagonite Brecciamentioning

confidence: 85%

Geological evolution of the Coombs–Allan Hills area, Ferrar large igneous province, Antarctica: Debris avalanches, mafic pyroclastic density currents, phreatocauldrons

Ross

White

McClintock

2008

Journal of Volcanology and Geothermal Research

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The Jurassic Ferrar large igneous province of Antarctica comprises igneous intrusions, flood lavas, and mafic volcaniclastic deposits (now lithified). The latter rocks are particularly diverse and well-exposed in the Coombs-Allan Hills area of South Victoria Land, where they are assigned to the Mawson Formation. In this paper we use these rocks in conjunction with the pre-Ferrar sedimentary rocks (Beacon Supergroup) and the lavas themselves (Kirkpatrick Basalt) to reconstruct the geomorphological and geological evolution of the landscape. In the Early Jurassic, the surface of the region was an alluvial plain, with perhaps 1 km of mostly continental siliciclastic sediments underlying it. After the fall of silicic ash from an unknown but probably distal source, mafic magmatism of the Ferrar province began. The oldest record of this event at Allan Hills is a ≤180 m-thick debris avalanche deposit (member m 1 of the Mawson Formation) which contains globular domains of mafic igneous rock. These domains are inferred to represent dismembered Ferrar intrusions emplaced in the source area of the debris avalanche; shallow emplacement of Ferrar magmas caused a slope failure that mobilized the uppermost Beacon Supergroup, and the silicic ash deposits, into a pre-existing valley or basin.The period which followed ('Mawson time') was the main stage for explosive eruptions in the Ferrar province, and several cubic kilometres of both new magma and sedimentary rock were fragmented over many years. Phreatomagmatic explosions were the dominant fragmentation mechanism, with magma-water interaction taking place in both sedimentary aquifers and existing vents filled by volcaniclastic debris. At Coombs Hills, a vent complex or 'phreatocauldron' was formed by coalescence of diatreme-like structures; at Allan Hills, member m 2 of the Mawson Formation consists mostly of thick, coarse-grained, poorly sorted layers inferred to represent the lithified deposits of pyroclastic density currents. Meanwhile at Carapace Nunatak, mafic clasts were mixed with detrital material to form the Carapace Sandstone in alluvial and eventually lacustrine environments.Eruptions then became largely effusive, producing hundreds of metres of flood lavas that covered the landscape ('Kirkpatrick time'). In places, lava flowed into ephemeral lakes to form pillow-palagonite breccias (base of sequence, Carapace Nunatak) or pillow lavas (top of sequence, Coombs Hills). Several generations of Ferrrar intrusions were emplaced during the course of these events; at least three can be distinguished based on field relations. New geochemical data indicates that for the Ferrar province, magma involved in the explosive eruptions had the same major element composition as that which produced shallow intrusions and lavas. We also note the possibility that flood lavas were fed by plugs cross-cutting the Mawson Formation at Coombs Hills, rather than by major dikes extending to the surface. Finally, we infer that eruption plumes were limited to the troposphere and that direct...

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Section: B 40 M-thick Sequence Of Pillow-palagonite Brecciamentioning

confidence: 85%

Geological evolution of the Coombs–Allan Hills area, Ferrar large igneous province, Antarctica: Debris avalanches, mafic pyroclastic density currents, phreatocauldrons

Ross

White

McClintock

2008

Journal of Volcanology and Geothermal Research

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“…If such relationships do exist, they provide an avenue for inferring the character of prehistoric eruptions from the morphology of lava flows they produced. It is this approach to flow morphology that has been especially significant to the work reported here; of particular interest is the conclusion drawn from Kilauea's Mauna Ulu eruption that the development of lava tubes and a particular variety of "tube fed" pahoehoe results from stable effusion rates of long duration (Swanson, 1973;Peterson and Swanson, 1974). It is generalizations of this type that form the basis for interpretations of flow morphology made in this report.…”

Section: Lava-flow Morphologymentioning

confidence: 99%

“…Examples of this approach are the work by Walker (1973) concerning the relationship between effusion rate and length of lava flows, and the observations of Swanson (1973) on the relationships between eruptive behavior and different varieties of pahoehoe. If such relationships do exist, they provide an avenue for inferring the character of prehistoric eruptions from the morphology of lava flows they produced.…”

Section: Lava-flow Morphologymentioning

confidence: 99%

Kilauea Volcano, Hawaii: chronology and morphology of the surficial lava flows

Holcomb¹

1981

Open-File Report

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“…Holocene obsidian flows in the western US preserve evidence of a cooled surface crust in folding, crease structures and large gas cavities (Fink 1980a;Anderson and Fink 1989;Castro and Cashman 1999;Castro et al 2002;Lescinsky and Merle 2005). Crustal development increases the strength of the flow (Hon et al 1994;Griffiths and Fink 1997;Griffiths 2000;Lyman et al 2005), insulates the flow and reduces heat loss (Swanson 1973;Fink and Griffiths 1998;Keszthelyi and Self 1998;Harris and Rowland 2009;Tuffen et al 2013). When the crust fractures during lava movement, blocky lava is formed (Finch 1933;Macdonald 1953;Fink 1980a;Harris et al 2017), defined as being made up on distinct blocks without some of the key characteristics of an 'a'a flow, such as a spiny or clinker surface (Finch 1933).…”

Section: Crust Formationmentioning

confidence: 99%

“…For instance, the development of a cooled surface crust promotes crustal folding during flow advance (Fink 1980a;Castro and Cashman 1999) and crease structure development (Anderson and Fink 1992;Lescinsky and Merle 2005). Crusts influence lava flow growth (Griffiths and Fink 1992;Fink and Griffiths 1998), and thermally insulate the flow, facilitating prolonged mobility and advance (Swanson 1973;Manley 1992;Fink and Griffiths 1998;Keszthelyi and Self 1998;Harris and Rowland 2009;Tuffen et al 2013). This has been previously observed in dacitic lava flow emplacement at Santiaguito (Harris et al 2002(Harris et al , 2004, and active rhyolitic flow emplacement at Puyehue-Cordón Caulle Magnall et al 2017).…”

Section: Introductionmentioning

confidence: 99%

Emplacement of the Rocche Rosse rhyolite lava flow (Lipari, Aeolian Islands)

2018

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The Rocche Rosse lava flow marks the most recent rhyolitic extrusion on Lipari island (Italy), and preserves evidence for a multi-stage emplacement history. Due to the viscous nature of the advancing lava (10 8 to 10 10 Pa s), indicators of complex emplacement processes are preserved in the final flow. This study focuses on structural mapping of the flow to highlight the interplay of cooling, crust formation and underlying slope in the development of rhyolitic lavas. The flow is made up of two prominent lobes, small (< 0.2 m) to large (> 0.2 m) scale folding and a channelled geometry. Foliations dip at 2-4°over the flatter topography close to the vent, and up to 30-50°over steeper mid-flow topography. Brittle faults, tension gashes and conjugate fractures are also evident across flow. Heterogeneous deformation is evident through increasing fold asymmetry from the vent due to downflow cooling and stagnation. A steeper underlying topography mid-flow led to development of a channelled morphology, and compression at topographic breaks resulted in fold superimposition in the channel. We propose an emplacement history that involved the evolution through five stages, each associated with the following flow regimes: (1) initial extrusion, crustal development and small scale folding; (2) extensional strain, stretching lineations and channel development over steeper topography; (3) compression at topographic break, autobrecciation, lobe development and medium scale folding; (4) progressive deformation with stagnation, large-scale folding and refolding; and (5) brittle deformation following flow termination. The complex array of structural elements observed within the Rocche Rosse lava flow facilitates comparisons to be made with actively deforming rhyolitic lava flows at the Chilean volcanoes of Chaitén and Cordón Caulle, offering a fluid dynamic and structural framework within which to evaluate our data.

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Pahoehoe Flows from the 1969–1971 Mauna Ulu Eruption, Kilauea Volcano, Hawaii

Cited by 232 publications

References 0 publications

Geological evolution of the Coombs–Allan Hills area, Ferrar large igneous province, Antarctica: Debris avalanches, mafic pyroclastic density currents, phreatocauldrons

Geological evolution of the Coombs–Allan Hills area, Ferrar large igneous province, Antarctica: Debris avalanches, mafic pyroclastic density currents, phreatocauldrons

Kilauea Volcano, Hawaii: chronology and morphology of the surficial lava flows

Emplacement of the Rocche Rosse rhyolite lava flow (Lipari, Aeolian Islands)

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