Surface cooling, advection and the development of different surface textures on active lavas on Kilauea, Hawai'i

Ball, Matthew R.; Pinkerton, Harry; Harris, Andrew

doi:10.1016/j.jvolgeores.2008.01.004

Cited by 27 publications

(20 citation statements)

References 36 publications

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“…Remotely observed terrestrial pāhoehoe flows exhibit surface cooling rates of thousands of °C h −1 (e.g., Ball et al. ) to ≤900 °C h −1 (Flynn and Mouginis‐Mark ). Modeled cooling rates agree with the higher end of these measurements, yet predict cooling rates >1450°C h −1 only within the upper 2 cm of the flow.…”

Section: Discussionmentioning

confidence: 99%

Igneous cooling history of olivine‐phyric shergottite Yamato 980459 constrained by dynamic crystallization experiments

First

Hammer

2016

Meteorit & Planetary Scien

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Abstract-Dynamic crystallization experiments were performed on a liquid having the bulk composition of olivine-phyric shergottite Yamato 980459, to constrain the igneous thermal history of this meteorite. Key characteristics of the meteorite's mineralogy and texture, including several morphologically distinct olivine and pyroxene crystal populations and a glassy mesostasis devoid of plagioclase, were replicated upon cooling from 1435 to 909°C at 1 atmosphere under reducing conditions. Three sequential cooling ramps are required to produce synthetic samples with textures and compositions matching Yamato 980459. Olivine phenocrysts formed at <1°C h À1 , presumably at depth in the Martian crust. Pyroxene phenocrysts formed mainly at~10°C h À1 , consistent with crystallization within a lava flow at depths of 25-45 cm. Increased cooling rate (~100°C h À1 ) in a third stage suppressed the formation of plagioclase and produced groundmass crystals, consistent with crystallization at lava flow depths of 5-7 cm. Although Y 980459 is unique among Martian meteorites (i.e., preserving a primary glassy mesostasis), its emplacement did not require unique physical conditions. Rather, the second and third cooling stages may reflect cooling within the core of a p ahoehoe-like flow and subsequent breakout on the surface of Mars.

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Section: Discussionmentioning

confidence: 99%

Igneous cooling history of olivine‐phyric shergottite Yamato 980459 constrained by dynamic crystallization experiments

First

Hammer

2016

Meteorit & Planetary Scien

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“…See, for example, Ball et al . [, Figure ] which shows all four segments of the L&B system in an active pahoehoe lobe just 4 m long. These four segments that comprise an L&B channel system are as follows: A proximal, stable, channel zone where levées are well‐developed, static and of a mature, compound morphology [ Harris et al ., ]; that is, being a mixture of initial, rubble, overflow, and accretionary levees [ Sparks et al ., ]. A medial, transitional, channel zone where flow is channelized and movement is contained between two zones of quasi‐static, but still deformable, lava; so that the levées are not well formed. A distal dispersed flow zone, where there are no levées so that lava is moving across its entire flow width. The terminus of the system is defined by a flow front.…”

Section: Introductionmentioning

confidence: 99%

A comparison of cooling‐limited and volume‐limited flow systems: Examples from channels in the Piton de la Fournaise April 2007 lava‐flow field

Rhéty

Harris

Villeneuve³

et al. 2017

Geochem Geophys Geosyst

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Channel‐fed lava‐flow systems lack detailed thermal and textural studies through the boundary between channelized and dispersed flow, and out to the flow front. Here chemical, textural, and morphological analyses were made to define cooling and crystallization rates down the entire system, especially through the zone of dispersed flow. We compare two channel systems active during the 2007 eruption of Piton de la Fournaise, one of which was cooling limited and one of which as volume limited. In the cooling‐limited case, rapid changes in rheology occurred across the zone of dispersed flow, where viscosity increased from 1000 to 1600 Pa s over the last 100 m of the channel system. This was due to an increase in cooling rate from 7°C km−1 over the first 500 m of the system, to 42°C km−1 over the last 100 m, and an increase in microcryst content from 13% to 25%. In the volume‐limited case, the exponentially increasing segment of the down‐flow cooling and viscosity trend is absent. Instead, lava arriving at the flow front is still relatively hot (1161°C compared with a near‐vent temperature of 1167°C) and is thus of relatively low viscosity (1125 Pa s). In the volume‐limited case, because the channel was still in extension when supply to the system was cut, the zone of dispersed flow was extremely short. However, because lava behind the stalled flow front was still hot and fluid, breakouts from the static front resulted in a complex flow front morphology.

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“…Detailed studies of basaltic or basaltic andesite lava flows have been dominated by investigations at only a few volcanoes, for example, Hawaiian volcanoes (Soule, Cashman & Kauahikaua, 2004;Harris et al 2009;Ball, Pinkerton & Harris, 2008), Longquimay, Chile (Naranjo et al 1992) and Etna, Italy (Polacci & Papale, 1997Calavari & Pinkerton, 1998Guest et al 1987;Guest & Stofan, 2005;Bailey et al 2006). There is need to examine case studies elsewhere.…”

Section: Introductionmentioning

confidence: 99%

Morphology and structure of the 1999 lava flows at Mount Cameroon Volcano (West Africa) and their bearing on the emplacement dynamics of volume-limited flows

et al. 2010

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-The morphology and structure of the 1999 lava flows at Mount Cameroon volcano are documented and discussed in relation to local and source dynamics. Structures are analysed qualitatively and more detailed arguments are developed on the processes of levee formation and systematic links between flow dynamics and levee-channel interface geometry. The flows have clear channels bordered by four main types of levees: initial, accretionary, rubble and overflow levees. Thermally immature pahoehoe lava units with overflow drapes define the proximal zone, whereas rubble and accretionary levees are common in the distal region bordering thermally mature aa clinker or blocky aa flow channels. Pressure ridges, squeeze-ups and pahoehoe ropes are the prevalent compressive structures. Standlines displayed on clinkery breccias are interpreted to represent leveechannel interactions in response to changing flow levels. These data complement previous knowledge on lava flow morphology, thus far dominated by Etnean and Hawaiian examples.

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Surface cooling, advection and the development of different surface textures on active lavas on Kilauea, Hawai'i

Cited by 27 publications

References 36 publications

Igneous cooling history of olivine‐phyric shergottite Yamato 980459 constrained by dynamic crystallization experiments

Igneous cooling history of olivine‐phyric shergottite Yamato 980459 constrained by dynamic crystallization experiments

A comparison of cooling‐limited and volume‐limited flow systems: Examples from channels in the Piton de la Fournaise April 2007 lava‐flow field

Morphology and structure of the 1999 lava flows at Mount Cameroon Volcano (West Africa) and their bearing on the emplacement dynamics of volume-limited flows

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