Temporal and spatial characteristics of volcanic tremor wave fields

Gordeev, E.; Салтыков, В. А.; Sinitsyn, Valerii I.; Чебров, В. Н.

doi:10.1016/0377-0273(90)90108-r

Cited by 38 publications

(20 citation statements)

References 8 publications

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“…Visual/acoustic observation Reference Pavlof Lava fountaining related to high-amplitude tremor McNutt, 1986;Garce ¤s and Hansen, 1998 Klyutchevskoy Variation of tremor spectral amplitude envelope whenever the eruptive activity changed Gordeev et al, 1990 Kilauea Gas-piston events associated with cycles of ponding and withdrawal of lava from the crater followed by high-amplitude tremor Ferrazzini and Aki, 1992 Mt. Semeru Pumping and explosion sounds with durations of 40 s^16 min that coincided with tremor episodes Schlindwein, 1994 Stromboli Gas bursts at the top of the magma column coincide with highamplitude tremor Ripepe et al, 1996;Ripepe, 1996 Arenal Di¡erent explosion sounds that are accompanied by ash plumes and precede tremor episodes Benoit and McNutt, 1997;Hagerty et al, 2000 White Island Eruptive/intrusive activity always followed by inharmonic tremor Sherburn et al, 1998 Satsuma-Iwojima Strong tremor occurring while vent emmits high-temperature volcanic gas Ohminato and Ereditato, 1998 Karimsky/Sangay 'Chugging' tremor episodes followed by steam locomotive-like sounds Johnson and Lees, 2000 Fig.…”

Section: Regionmentioning

confidence: 99%

Nature, wavefield properties and source mechanism of volcanic tremor: a review

Konstantinou

Schlindwein

2003

Journal of Volcanology and Geothermal Research

184

129

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Volcanic tremor has attracted considerable attention by seismologists because of its potential value as a tool for forecasting eruptions and better understanding the physical processes that occur inside active volcanoes. However, unlike tectonic earthquakes where the dominant source process is brittle failure of rock, the driving mechanism of tremor seems to involve complex interactions of magmatic fluids with the surrounding bedrock. These interactions are responsible for the following distinct characteristics found in volcanic tremor recorded at many volcanoes worldwide: (a) the onset of tremor may be emergent or impulsive, with its amplitude showing in many cases a direct relationship to the volcanic activity; (b) in the frequency domain the spectra consist of a series of sharp peaks in the band 0.1^7 Hz, representing either a fundamental frequency and its harmonics, or a random distribution, while quite often they exhibit temporal variations in their content; (c) the depth of the source can vary considerably from one volcano to another in the range of a few hundred metres to 40 km; (d) tremor may occur prior to and/or after eruptions with a duration that ranges from several minutes to several days or months. The methods used to study tremor include spectral analysis using both the Fast Fourier Transform and the Maximum Entropy Method, polarisation analysis of the wavefield and methods that make use of array data to deduce the backazimuth and type of the seismic waves as well as the location of the source. Visual and/or recorded acoustic observations of the ongoing volcanic activity have assisted in many cases to further constrain proposed physical mechanisms for the generation of tremor. The models suggested as possible sources of tremor can be grouped as follows: (a) fluid-flow-induced oscillations of conduits transporting magmatic fluids; (b) excitation and resonance of fluid-filled cracks; (c) bubble growth or collapse due to hydrothermal boiling of groundwater; (d) a variety of models involving the oscillations of magma bodies with different geometries. It has been proposed by many authors that the source of tremor is not unique and may differ from one volcano to another, a fact that adds more difficulty in the source modelling efforts. As data quality, computer power and speed are improving, it may be possible in the near future to decipher and accurately model tremor source processes at different volcanic environments. ß 2002 Elsevier Science B.V. All rights reserved.

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Section: Regionmentioning

confidence: 99%

Nature, wavefield properties and source mechanism of volcanic tremor: a review

Konstantinou

Schlindwein

2003

Journal of Volcanology and Geothermal Research

184

129

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“…McNutt 1986;Gordeev et al 1990;Gordeev 1992;Goldstein and Chouet 1994;Ripepe et al 1996). We made particle motion plots for the station HAU.…”

Section: Particle Motion At the Onset Of The Eruptionmentioning

confidence: 99%

Volcanic tremor related to the 1991 eruption of the Hekla volcano, Iceland

Soosalu

Einarsson

Jakobsdóttir

2003

Bulletin of Volcanology

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Volcanic tremor at the Hekla volcano is directly related to eruptive activity. It starts simultaneously with the eruptions and dies down at the end of them. No tremor at Hekla has been observed during noneruptive times. The 1991 Hekla eruption began on 17 January, after a short warning time. Local seismograph stations recorded small premonitory earthquakes from 16:30 GMT on. At 17:02 GMT, low-frequency volcanic tremor became visible on the seismograph records, marking the onset of the eruption. The initial plinian phase of the eruption was short-lived. During the first day several fissures were active but, by the second day, the activity was already limited to a segment of one principal fissure. The eruption lasted almost 53 days. At the end of it, during the early hours of 11 March, volcanic tremor disappeared under the detection threshold and was followed by a swarm of small earthquakes. At the start of the eruption, the tremor amplitude rose rapidly and reached a maximum in only 10 min. The tremor was most vigorous during the first hour and started to decline sharply during the next hour, and later on more gently. During the eruption as a whole, the tremor had a continuous declining trend, with occasional increases lasting up to about 2 days. Spectral analysis of the tremor during the first 7 h of the eruption shows that it settled quickly, within a couple of minutes, to its characteristic frequency band, 0.5-1.5 Hz. The spectrum had typically one dominant peak at 0.7-0.9 Hz, and a few subdominant peaks. Hekla tremor likely has a shallow source. Particle motion plots suggest that it contains a significant component of surface waves. The tremor started first when the connection of the magma conduit with the atmosphere was reached, suggesting that degassing may contribute to its generation.

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“…Tremor is commonly addressed to as RMS amplitude of the seismic signal measured over a certain time window and frequency band (e.g., STEPHEN et al, 1994;GORDEEV et al, 1990;FALSAPERLA et al, 1998). In this note, we focus our attention on the seismic radiation in the time and frequency domains from July to .…”

Section: Introductionmentioning

confidence: 99%

Volcanic Tremor at Mt. Etna, Italy, Preceding and Accompanying the Eruption of July – August, 2001

Falsaperla

Alparone

D’Amico

et al. 2005

Pure appl. geophys.

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The July 17 -August 9, 2001 flank eruption of Mt. Etna was preceded and accompanied by remarkable changes in volcanic tremor. Based on the records of stations belonging to the permanent seismic network deployed on the volcano, we analyze amplitude and frequency content of the seismic signal. We find considerable changes in the volcanic tremor which mark the transition to different styles of eruptive activity, e.g., lava fountains, phreatomagmatic activity, Strombolian explosions. In particular, the frequency content of the signal decreases from 5 Hz to 3 Hz at our reference station ETF during episodes of lava fountains, and further decreases at about 2 Hz throughout phases of intense lava emission. The frequency content and the ratios of the signal amplitude allow us to distinguish three seismic sources, i.e., the peripheral dike which fed the eruption, the reservoir which fed the lava fountains, and the central conduit. Based on the analysis of the amplitude decay of the signal, we highlight the migration of the dike from a depth of ca. 5 km to about 1 km between July 10 and 12. After the onset of the effusive phase, the distribution of the amplitude decay at our stations can be interpreted as the overall result of sources located within the first half kilometer from the surface. Although on a qualitative basis, our findings shed some light on the complex feeding system of Mt. Etna, and integrate other volcanological and geophysical studies which tackle the problem of magma replenishment for the July-August, 2001 flank eruption. We conclude that volcanic tremor is fundamental in monitoring Mt. Etna, not only as a marker of the different sources which act within the volcano edifice, but also of the diverse styles of eruptive activity.

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Temporal and spatial characteristics of volcanic tremor wave fields

Cited by 38 publications

References 8 publications

Nature, wavefield properties and source mechanism of volcanic tremor: a review

Nature, wavefield properties and source mechanism of volcanic tremor: a review

Volcanic tremor related to the 1991 eruption of the Hekla volcano, Iceland

Volcanic Tremor at Mt. Etna, Italy, Preceding and Accompanying the Eruption of July – August, 2001

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