Subaqueous, basaltic lava dome and carapace breccia on King George Island, South Shetland Islands, Antarctica

Smellie, John L.; Millar, Ian L.; Rex, D. C.; Butterworth, Peter J.

doi:10.1007/s004450050189

Cited by 33 publications

(30 citation statements)

References 52 publications

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“…The lines show the least squares linear regression best fit to the height:radius ratio of small Icelandic lava shields ( h = 0.038 r ) [ Rossi , 1996] and basaltic lava domes on the southern East Pacific Rise (SEPR) ( h = 0.2 r ) [ White et al , 2000]. Two stars show the sizes of small submarine basaltic lava domes (LH) at Low Head‐on King George Island [ Smellie et al , 1998] and (B) at Bogoslof in the Aleutians [ Miller et al , 1998]. The NEPR pillow constructions are too small and steep to be classified as lava shields but are very similar to other documented small basaltic lava domes.…”

Section: Volcanic Structures Imaged By Dsl‐120 Sonarmentioning

confidence: 99%

Correlation between volcanic and tectonic segmentation of fast‐spreading ridges: Evidence from volcanic structures and lava flow morphology on the East Pacific Rise at 9°–10°N

et al. 2002

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[1] Combined analyses of volcanic features in DSL-120 sonar data and Argo I images along the ridge crest of the East Pacific Rise, 9°09 0 -54 0 N reveal a consistent decrease in inferred lava effusion rate toward the ends of third-order segments. The correlation of tectonic segmentation and volcanic style suggests that third-order segmentation corresponds to the volcanic segmentation of the ridge. Along-axis changes in volcanic structures (from collapse troughs to basaltic lava domes) and lava morphology (from sheet to pillow flows) coincide with the boundaries of morphologically defined third-order tectonic segments of the ridge crest visible in shipboard multibeam bathymetry. Pillow lava flows cover 25% of the surveyed area of the ridge crest and are closely associated with small lava domes that occur primarily at third-order segment ends. An additional 25% of the surveyed area of the ridge crest is covered by sheet lava flows found in close association with an axial collapse trough. The remaining terrain consists of lobate lava flows. We interpret the spatial correlations of morphologic, structural, seismic, and petrologic data as evidence that individual volcanic plumbing systems are organized at $20 km spacing along the ridge axis (third-order segment scale) in agreement with the hypothesis that volcanic and tectonic segmentations are correlated. For fast spreading ridges, we estimate that the longevity of volcanic segments is $10 4 -10 5 years, 1-3 orders of magnitude longer than fourth-order segments ($10 2 -10 3 years). This implies the present pattern of hydrothermal activity may reorganize tens or hundreds of times while volcanic segmentation remains fairly stable.

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Section: Volcanic Structures Imaged By Dsl‐120 Sonarmentioning

confidence: 99%

Correlation between volcanic and tectonic segmentation of fast‐spreading ridges: Evidence from volcanic structures and lava flow morphology on the East Pacific Rise at 9°–10°N

et al. 2002

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“…Shallow subaqueous dome complexes (Smellie et al 1998) of low volume (0.01 km 3 ) are commonly associated with mafic volcanic fields. Direct observation of subaqueous dome formation and associated processes are commonly restricted to submersible investigations and based on photo-interpretation of small areas of view (S. M. .…”

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confidence: 99%

Hyaloclastites, peperites and soft-sediment deformation textures of a shallow subaqueous Miocene rhyolitic dome-cryptodome complex, Pálháza, Hungary

Németh

Pécskay

Martin

et al. 2008

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The NE Tokaj Mountains at Pálháza in NE Hungary are made up of a complex association of Miocene rhyolitic shallow intrusions, cryptodomes and endogenous lava domes emplaced into and onto soft, wet pelitic sediment in a shallow submarine environment. The intrusiveextrusive complex shows a range of interaction textures with the host muddy sediment, ranging from blocky peperites, formed on a 0.1 m-scale, through to irregular contacts closely resembling globular mega-peperites, on a .10 m-scale. The over 200 m-thick igneous succession is interpreted to result from the pulsatory growth of shallow cryptodomes through muddy saturated host sediment. The intrusions eventually breached the sedimentary cover to build up thick in situ hyaloclastite piles in the shallow subaqueous environment. The coherent rhyolitic cryptodome facies is surrounded by intrusive hyaloclastite in the contact zone to the pelitic host sediment. In the upper level of the complex, rhyolitic dome rock is capped and surrounded by hyaloclastite formed due to quench fragmentation upon contact of the lava surface with sea water.

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“…(f, g) glacially modified surfaces below mafic volcanic sequences at Tucker Glacier (T5.33) and W Edisto Inlet (T5.27), respectively. The surfaces are polished, striated (parallel to the hammer head in (f) and pencil in (g)) and moulded by ice steam-driven explosions caused by water trapped in pockets overridden by the lava or trapped in pores in the autobreccia and flashing to steam (Kokelaar 1986;Smellie et al 1998) will generate additional hyaloclastite breccia and provide a mechanism to physically mix the newly formed hyaloclastite with the passively advected subaerial autobreccia. Thus, the abundance of breccia relative to coherent lava will be substantial in a subaqueous setting compared with subaerial counterparts (e.g.…”

Section: Lithofacies Sequence Types and Eruptive Modelsmentioning

confidence: 99%

Late Miocene volcanic sequences in northern Victoria Land, Antarctica: products of glaciovolcanic eruptions under different thermal regimes

2010

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Late Miocene (c. 13-5 Ma) volcanic sequences of the Hallett Volcanic Province (HVP) crop out along >250 km of western Ross Sea coast in northern Victoria Land. Eight primary volcanic and six sedimentary lithofacies have been identified, and they are organised into at least five different sequence architectures as a consequence of different combinations of eruptive and/or depositional conditions. The volcanoes were erupted in association with a Miocene glacial cover and the sequences are overwhelmingly glaciovolcanic. The commonest and most representative are products of mafic aa lava-fed deltas, a type of glaciovolcanic sequence that has not been described before. It is distinguished by (1) a subaerially emplaced relatively thin caprock of aa lavas lying on and passing down-dip into (2) a thicker association of chaotic to crudely bedded hyaloclastite breccias, water-chilled lava sheets and irregular lava masses, collectively called lobe-hyaloclastite. A second distinctive sequence type present is characterised by water-cooled lavas and associated sedimentary lithofacies (diamictite (probably glacigenic) and fluvial sands and gravels) similar to some mafic glaciovolcanic sheet-like sequences (see Smellie, Earth-Science Reviews, 74, 241-268, 2008), but including (for the first time) examples of likely sheet-like sequences with felsic compositions. Other sequence types in the HVP are minor and include tuff cones, cinder cones and a single ice-marginal lacustrine sequence. The glacial thermal regime varied from polar, characterised by sequences lacking glacial erosion, glacigenic sediments or evidence for free water, to temperate or sub-polar for sequences in which all of these features are conspicuously developed.

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Subaqueous, basaltic lava dome and carapace breccia on King George Island, South Shetland Islands, Antarctica

Cited by 33 publications

References 52 publications

Correlation between volcanic and tectonic segmentation of fast‐spreading ridges: Evidence from volcanic structures and lava flow morphology on the East Pacific Rise at 9°–10°N

Correlation between volcanic and tectonic segmentation of fast‐spreading ridges: Evidence from volcanic structures and lava flow morphology on the East Pacific Rise at 9°–10°N

Hyaloclastites, peperites and soft-sediment deformation textures of a shallow subaqueous Miocene rhyolitic dome-cryptodome complex, Pálháza, Hungary

Late Miocene volcanic sequences in northern Victoria Land, Antarctica: products of glaciovolcanic eruptions under different thermal regimes

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