Cross-correlation analysis of seismic and volcanic data at Mt Etna volcano, Italy

Cardaci, C.; Falsaperla, S.; Gasperini, Paolo; Lombardo, Giuseppe; Marzocchi, Warner; Mulargia, Francesco

doi:10.1007/bf00301812

Cited by 23 publications

(14 citation statements)

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“…Etna has yielded valuable information on the long-term (e.g., from months to years) as well as short-term (days to weeks) changes in the volcanic system (e.g., COSENTINO et al, 1989;CARDACI et al, 1993;ALPARONE Vol. 162, 2005 Volcanic Tremor at Mt.…”

Section: Discussionmentioning

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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Section: Discussionmentioning

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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“…Values for r r must range between almost zero, when the magma enters a void opened shortly before its arrival, and the mean density of the host rock. Using the empirical relation of Nafe and Drake (1963), seismic tomographic data for Etna (Cardaci et al 1993) indicate a mean host rock density of 2400 kg m -3 at 4-4.5 km below sea level, the nominal depths for the centers of mass of the 1989 and 1992 anomaly sources (Figs. 9, 10).…”

Section: Passive Magma Ascentmentioning

confidence: 99%

Temporal variations in gravity at Mt. Etna (Italy) associated with the 1989 and 1991 eruptions

Budetta

Carbone

1998

Bulletin of Volcanology

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“…A host of studies of volcano-tectonic earthquakes including source mechanisms (Zollo and Bernard 1992;Foulger and Long 1992;Robson 1992), stress patterns from focal mechanisms (Jolly et al 1994), configuration of the brittle (seismogenic) crust (Hill 1992;Jolly et al 1994), propagation rates of intrusion events (Klein et al 1987;Koyanagi et al 1988;Castellano et al 1993), coda wave attenuation (Chouet 1976;Del Pezzo et al 1983Fehler et al 1988;Ortiz et al 1992), and statistical analyses (Gasperini et al 1990(Gasperini et al , 1992Patan et al 1992;Cardaci et al 1993) have also been used to further our understanding of volcanic systems. Along with those studies various seismological techniques such as velocity tomography (Ellsworth and Koyanagi 1977;Thurber 1984;Benz and Smith 1984;Ankeny et al 1986; Aster and Meyer 1988;Achauer et al 1988; Lees and Crosson 1989;Toomey and Foulger 1989;Dawson et al 1990), attenuation tomography (Young and Ward 1980;Evans and Zucca 1988;Sanders et al 1988), reflection and refraction profiling Brown et al 1980;Schilly et al 1982;Smith et al 1982;Zucca et al 1982;Hill et al 1985), diffraction mapping , surface-wave dispersion inversion , and seismicity mapping Ryan et al 1981;Klein et al 1987;) have been applied to obtain crude information...…”

Section: Introductionmentioning

confidence: 98%

New Methods and Future Trends in Seismological Volcano Monitoring

Chouet

1996

Monitoring and Mitigation of Volcano Hazards

186

168

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Volcanic processes operate over a wide range of time scales that require a variety of instruments and techniques for their study. Short-period seismology typically covers the band 0.1-1 s, while broadband seismology can extend that band to 0.1-100 s. Borehole strainmeters may be used to cover the very wide band from 0.1 s to 100 days and Global Positioning System (GPS) surveys are useful to track deformation over time scales ranging from days to decades. Arrays of threecomponent broadband seismographs coupled with arrays of borehole strainmeters are required to monitor the dynamics of magmatic and hydrothermal fluids prior to and during eruptions. Inversions of broadband data may be performed to image the forces operating at a source and infer the fluid pathway geometry and mass transport balance in a volcano. The accuracy of such inversions depends on the degree of resolution achieved for the volcanic structure. High-resolution tomography based on iterative inversions of seismic travel-time data can image three-dimensional structures at a scale of a few hundred meters provided adequate local short-period earthquake data are available. Hence, forces in a volcano are potentially resolvable for periods longer than a few seconds. Studies of long-period events and tremor at periods ~ I s offer constraints on pressure fluctuations resulting from unsteady mass transport, and observations of volcano-tectonic activity tell us about hydraulic fracturing processes, as well as brittle response of the rock matrix to stress changes induced by rapid injection and/or withdrawal of fluids. Short-period networks are routinely used to monitor, locate, and assess the source properties of volcano-tectonic earthquakes and long-period events, while small-aperture seismic antennas are required to track tremor and separate source, path, and site effects in tremor wavefields. This chapter reviews quantitative methods used in the interpretation of source processes and structures in volcanoes and discusses some of the major challenges faced by volcano seismologists in their quest to understand eruptive behavior.

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Cross-correlation analysis of seismic and volcanic data at Mt Etna volcano, Italy

Cited by 23 publications

References 11 publications

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

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

Temporal variations in gravity at Mt. Etna (Italy) associated with the 1989 and 1991 eruptions

New Methods and Future Trends in Seismological Volcano Monitoring

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