Seismic tomography of the Tongariro Volcanic Centre, New Zealand

Rowlands, D. P.; White, R. S.; Haines, A. J.

doi:10.1111/j.1365-246x.2005.02716.x

Cited by 45 publications

(47 citation statements)

References 35 publications

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“…This is seems likely that the conductive feature continues northward beneath the Tongariro volcano. Such a continuation of this dyke like structure marking the route by which hot gases, and potentially, magma are transported to the volcanic cones is consistent with an observed area of low P-wave velocity at depths down to ∼10 km, noted by Rowlands et al (2005). Their preferred interpretation of this feature was in terms of a hot open conduit beneath Ruapehu, remnant partial melt left over from previous eruptions beneath Ngauruhoe, and the hot source body for the hydrothermal systems on Tongariro, each of which would be characterized by high conductivity.…”

Section: Deep Structuresupporting

confidence: 85%

A magnetotelluric study of Mount Ruapehu volcano, New Zealand

Ingham¹,

Bibby²,

Heise³

et al. 2009

Geophysical Journal International

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S U M M A R YMt Ruapehu is an active andesite cone volcano, which marks the southern termination of the Kermadec volcanic arc. Results from 40 broad-band magnetotelluric soundings have been analysed using the phase tensor. This approach provides a way of determining dimensionality, allowing for distortion removal, and visualizing data in a 3-D situation. The phase tensor analysis suggests that the shallow resistivity structure is largely 1-D in character, but that the deeper structure requires a 3-D interpretation. 1-D inversions show that at sites on Ruapehu a shallow conductive layer lies between a high resistivity layer, of a few hundred metres thickness, and higher resistivity layer corresponding to basement greywacke. The low resistivity layer is contiguous with the waters of the highly acidic Crater Lake, and thus is believed to be the hydraulically controlled upper limit of a zone of acid alteration overlain by dry volcanic rock and ash. To the southwest of the volcano the conductive layer merges with a surface conductor associated with Tertiary sediments. Following initial 2-D inversions, the deep resistivity structure has been derived through 3-D inversion of data from 38 sites. This indicates the existence of a dyke-like low resistivity zone that persists to at least 10 km depth and extends from beneath the summit of Ruapehu to the northeast where it appears to connect to a poorly constrained region of high conductivity, which lies outside the network of measurement sites. The low resistivity dyke-like feature may be identified with a volcanic feeder system, which also supplies the other volcanoes of the Tongariro Volcanic Centre and marks the conduit by which hot gases and (occasionally) magma reach the surface.

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Section: Deep Structuresupporting

confidence: 85%

A magnetotelluric study of Mount Ruapehu volcano, New Zealand

Ingham¹,

Bibby²,

Heise³

et al. 2009

Geophysical Journal International

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“…Previous passive‐ and active‐source velocity tomography studies of other volcanoes have found a variety of types of features in the subsurface. Compiling results from 23 active arc volcanoes (Aso [ Sudo and Kong , ], Augustine [ Syracuse et al ., ], Mount Etna [ Aloisi et al ., ; Laigle et al ., ], Mount Fuji [ Nakamichi et al ., ], Great Sitkin [ Pesicek et al ., ], Iwate [ Tanaka et al ., ], Katmai [ Murphy et al ., ], Kirishima [ Tomatsu et al ., ], Klyuchevskoy [ Koulakov et al ., ], Long Valley Caldera [ Seccia et al ., ], Montserrat [ Paulatto et al ., ], Mount St. Helens [ Lees , ; Waite and Moran , ], Naruko [ Nakajima and Hasegawa , ], Nevado del Ruiz [ Londoño and Sudo , ], Okmok [ Masterlark et al ., ; Ohlendorf et al ., ], Popocatépetl [ Berger et al ., ; Kuznetsov and Koulakov , ], Rainier [ Moran et al ., ], Redoubt [ DeShon et al ., ], Taranaki [ Sherburn et al ., ], Tongariro [ Rowlands et al ., ], Tungurahua [ Molina et al ., ], Unzen [ Ohmi and Lees , ], and Vesuvius [ Piana Agostinetti and Chiarabba , ]) show that upper crustal low‐velocity regions, potentially indicative of hotter or melt‐rich areas, are as common as high‐velocity regions, generally interpreted to be cooled basaltic rocks intruded during previous eruptions and near which magma travels to the surface. It is possible that all volcanoes contain both these features, but resolution limitations prevent their observation.…”

Section: Resultsmentioning

confidence: 99%

Seismicity and structure of Akutan and Makushin Volcanoes, Alaska, using joint body and surface wave tomography

et al. 2015

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Joint inversions of seismic data recover models that simultaneously fit multiple constraints while playing upon the strengths of each data type. Here we jointly invert 14 years of local earthquake body wave arrival times from the Alaska Volcano Observatory catalog and Rayleigh wave dispersion curves based upon ambient noise measurements for local V p , V s , and hypocentral locations at Akutan and Makushin Volcanoes using a new joint inversion algorithm. The velocity structure and relocated seismicity of both volcanoes are significantly more complex than many other volcanoes studied using similar techniques. Seismicity is distributed among several areas beneath or beyond the flanks of both volcanoes, illuminating a variety of volcanic and tectonic features. The velocity structures of the two volcanoes are exemplified by the presence of narrow high-V p features in the near surface, indicating likely current or remnant pathways of magma to the surface. A single broad low-V p region beneath each volcano is slightly offset from each summit and centered at approximately 7 km depth, indicating a potential magma chamber, where magma is stored over longer time periods. Differing recovery capabilities of the V p and V s data sets indicate that the results of these types of joint inversions must be interpreted carefully.

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“…Applications followed in seismology [Claerbout, 1968], in helioseismology [Rickett and Claerbout, 2000] and in acoustics [Lobkis and Weaver, 2001], but it is only in the last decade that this method has received widespread attention within the broader seismological community (see, for example, Wapenaar et al [2008] for a comprehensive overview). [8] In this study, we construct Rayleigh and Love wave phase and group velocity dispersion curves from cross-correlation functions of ambient seismic noise recorded at stations of the Central North Island Passive Seismic Experiment (CNIPSE; 33 stations; 6 months) [Reyners and Stuart, 2002], the Western Central North Island Passive Seismic Experiment (WCNIPSE; 6 stations; 9-11 months) [Greve et al, 2008], the Seismic Tomography Around Ruapehu and Tongariro deployment (START; 28 stations; 5 months) [Rowlands et al, 2005], the RF2004 deployment (7 stations; 10 months) [Bannister et al, 2004] and three permanent broadband stations that started operating in 2001 (see Figure 1). We also include correlations between 20 permanent broadband stations operated by GeoNet (http://www.geonet.…”

Section: Introductionmentioning

confidence: 99%

Crustal shear wave tomography of the Taupo Volcanic Zone, New Zealand, via ambient noise correlation between multiple three‐component networks

Behr

Townend

Bannister

et al. 2011

Geochem Geophys Geosyst

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[1] The central North Island of New Zealand is characterized by extension, high heat flow, and active volcanism caused by the Pacific plate subducting beneath the Australian plate off the east coast of the North Island. The Taupo Volcanic Zone (TVZ) is the current locus of rifting and active volcanism. The shear velocity structure derived here from short-period surface wave analysis fills a gap in the geophysical information obtained in previous active and passive source studies. Using ambient noise correlation techniques, we reprocess data from four three-component temporary seismic arrays that were deployed between 2001 and 2005 in the central North Island and data from permanent seismic stations operational at the same time. Special attention has been paid to the correction of timing errors and incomplete instrument response information. Low shear velocities in the top 15-20 km of the crust inferred from Rayleigh wave dispersion analysis coincide with the presumed source regions of rhyolitic magma in the TVZ and are correlated with conductive bodies inferred from a 3-D magnetotelluric survey. Based on the observed changes in shear velocity we use empirical relations to infer an average percentage of partial melt in the upper crust of <4%. Comparison of our shear velocity model with compressional wave cross sections from active and passive source studies and shear velocities derived from previous 3-D V p and V p /V s models reveals several consistent features, especially in the lower crust. The greater sensitivity of shear velocity than compressional velocity to the presence of melt and other fluids aids in linking seismic and electromagnetic observations and provides additional constraints on the distribution of magmatic structures in active continental rifting environments.

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Seismic tomography of the Tongariro Volcanic Centre, New Zealand

Cited by 45 publications

References 35 publications

A magnetotelluric study of Mount Ruapehu volcano, New Zealand

A magnetotelluric study of Mount Ruapehu volcano, New Zealand

Seismicity and structure of Akutan and Makushin Volcanoes, Alaska, using joint body and surface wave tomography

Crustal shear wave tomography of the Taupo Volcanic Zone, New Zealand, via ambient noise correlation between multiple three‐component networks

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