Geology and eruptive history of the Rabaul Caldera area, Papua New Guinea

Nairn, I. A.; McKee, Chris; Talai, B.; Wood, C. P.

doi:10.1016/0377-0273(95)00035-6

Cited by 67 publications

(32 citation statements)

References 20 publications

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“…The general applicability of our model to Campi Flegrei and several other calderas that have erupted since the late 1980s highlights lateral propagation as an important, perhaps predominant, process for magma transfer43. Our conceptual model explains the shallow lateral transfer of magma below Campi Flegrei in the last ~5 ka and, as supported by the available evidence of recent caldera unrest, may provide a key to forecasting the location of future eruptions at Campi Flegrei and calderas with similar behaviour.…”

Section: Discussionsupporting

confidence: 61%

Magma transfer at Campi Flegrei caldera (Italy) before the 1538 AD eruption

Vito

Acocella

Aiello

et al. 2016

Sci Rep

132

117

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Calderas are collapse structures related to the emptying of magmatic reservoirs, often associated with large eruptions from long-lived magmatic systems. Understanding how magma is transferred from a magma reservoir to the surface before eruptions is a major challenge. Here we exploit the historical, archaeological and geological record of Campi Flegrei caldera to estimate the surface deformation preceding the Monte Nuovo eruption and investigate the shallow magma transfer. Our data suggest a progressive magma accumulation from ~1251 to 1536 in a 4.6 ± 0.9 km deep source below the caldera centre, and its transfer, between 1536 and 1538, to a 3.8 ± 0.6 km deep magmatic source ~4 km NW of the caldera centre, below Monte Nuovo; this peripheral source fed the eruption through a shallower source, 0.4 ± 0.3 km deep. This is the first reconstruction of pre-eruptive magma transfer at Campi Flegrei and corroborates the existence of a stationary oblate source, below the caldera centre, that has been feeding lateral eruptions for the last ~5 ka. Our results suggest: 1) repeated emplacement of magma through intrusions below the caldera centre; 2) occasional lateral transfer of magma feeding non-central eruptions within the caldera. Comparison with historical unrest at calderas worldwide suggests that this behavior is common.

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Section: Discussionsupporting

confidence: 61%

Magma transfer at Campi Flegrei caldera (Italy) before the 1538 AD eruption

Vito

Acocella

Aiello

et al. 2016

Sci Rep

132

117

View full text Add to dashboard Cite

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“…Analogous complexities in subsidence geometry appear to be present at the historically active Rabaul caldera in Papua New Guinea, where geologic relations document successive overlapping caldera subsidences during the past few hundred thousand years (Nairn et al 1995), even though present-day seismicity defines a geometrically simple ringstructure boundary for the active caldera (Mori et al 1989).…”

Section: Piecemeal Disruptionmentioning

confidence: 96%

Subsidence of ash-flow calderas: relation to caldera size and magma-chamber geometry

Lipman¹

1997

Bulletin of Volcanology

446

328

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Diverse subsidence geometries and collapse processes for ash-flow calderas are inferred to reflect varying sizes, roof geometries, and depths of the source magma chambers, in combination with prior volcanic and regional tectonic influences. Based largely on a review of features at eroded pre-Quaternary calderas, a continuum of geometries and subsidence styles is inferred to exist, in both island-arc and continental settings, between small funnel calderas and larger plate (piston) subsidences bounded by arcuate faults. Within most ring-fault calderas, the subsided block is variably disrupted, due to differential movement during ash-flow eruptions and postcollapse magmatism, but highly chaotic piecemeal subsidence appears to be uncommon for large-diameter calderas. Small-scale downsag structures and accompanying extensional fractures develop along margins of most calderas during early stages of subsidence, but downsag is dominant only at calderas that have not subsided deeply. Calderas that are loci for multicyclic ash-flow eruption and subsidence cycles have the most complex internal structures. Large calderas have flared inner topographic walls due to landsliding of unstable slopes, and the resulting slide debris can constitute large proportions of caldera fill. Because the slide debris is concentrated near caldera walls, models from geophysical data can suggest a funnel geometry, even for large plate-subsidence calderas bounded by ring faults. Simple geometric models indicate that many large calderas have subsided 3-5 km, greater than the depth of most naturally exposed sections of intracaldera deposits. Many ring-fault platesubsidence calderas and intrusive ring complexes have been recognized in the western U.S., Japan, and elsewhere, but no well-documented examples of exposed eroded calderas have large-scale funnel geometry or chaotically disrupted caldera floors. Reported ignimbrite "shields" in the central Andes, where large-volume ash-flows are inferred to have erupted without caldera collapse, seem alternatively interpretable as more conventional calderas that were filled to overflow by younger lavas and tuffs. Some exposed subcaldera intrusions provide insights concerning subsidence processes, but such intrusions may continue to evolve in volume, roof geometry, depth, and composition after formation of associated calderas.

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“…or the control of regional faults (case 8), as at the above-mentioned Los Azufres caldera, and at the Rabaul caldera (Papua New Guinea) where eruptive activity simultaneously occurred at opposite sides in 1878 and 1937 (Mori and McKee, 1987;Nairn et al, 1995). Finally, distributed vents inside the caldera may suggest conduits and dykes of different geometries linked to a highly-fractured caldera block (case 9), as for example at the resurgent Ischia Island caldera (Italy) (Tibaldi and Vezzoli, 1998).…”

Section: Accepted Manuscriptmentioning

confidence: 99%