Abstract
Since the 1919 foundation of the International Association of Volcanology and Chemistry of the Earth’s Interior (IAVCEI), the fields of volcano seismology and acoustics have seen dramatic advances in instrumentation and techniques, and have undergone paradigm shifts in the understanding of volcanic seismo-acoustic source processes and internal volcanic structure. Some early twentieth-century volcanological studies gave equal emphasis to barograph (infrasound and acoustic-gravity wave) and seismograph observations, but volcano seismology rapidly outpaced volcano acoustics and became the standard geophysical volcano-monitoring tool. Permanent seismic networks were established on volcanoes (for example) in Japan, the Philippines, Russia, and Hawai‘i by the 1950s, and in Alaska by the 1970s. Large eruptions with societal consequences generally catalyzed the implementation of new seismic instrumentation and led to operationalization of research methodologies. Seismic data now form the backbone of most local ground-based volcano monitoring networks worldwide and play a critical role in understanding how volcanoes work. The computer revolution enabled increasingly sophisticated data processing and source modeling, and facilitated the transition to continuous digital waveform recording by about the 1990s. In the 1970s and 1980s, quantitative models emerged for long-period (LP) event and tremor sources in fluid-driven cracks and conduits. Beginning in the 1970s, early models for volcano-tectonic (VT) earthquake swarms invoking crack tip stresses expanded to involve stress transfer into the wall rocks of pressurized dikes. The first deployments of broadband seismic instrumentation and infrasound sensors on volcanoes in the 1990s led to discoveries of new signals and phenomena. Rapid advances in infrasound technology; signal processing, analysis, and inversion; and atmospheric propagation modeling have now established the role of regional (15–250 km) and remote (> 250 km) ground-based acoustic systems in volcano monitoring. Long-term records of volcano-seismic unrest through full eruptive cycles are providing insight into magma transport and eruption processes and increasingly sophisticated forecasts. Laboratory and numerical experiments are elucidating seismo-acoustic source processes in volcanic fluid systems, and are observationally constrained by increasingly dense geophysical field deployments taking advantage of low-power, compact broadband, and nodal technologies. In recent years, the fields of volcano geodesy, seismology, and acoustics (both atmospheric infrasound and ocean hydroacoustics) are increasingly merging. Despite vast progress over the past century, major questions remain regarding source processes, patterns of volcano-seismic unrest, internal volcanic structure, and the relationship between seismic unrest and volcanic processes.
Similar content being viewed by others
Avoid common mistakes on your manuscript.
State of the art and introduction
Seismic and acoustic (collectively seismo-acoustic) geophysical technologies are complementary in volcano science and monitoring. Volcano seismology involves the analysis, interpretation, and modeling of seismic signals generated inside and around active volcanoes, as well as the application of seismic techniques to image internal volcanic structure (e.g., Aki 1992; Chouet 1996a, 1996b, 2003; McNutt 1992, 1996, 2005; Kumagai 2009; Lees 2007; Neuberg 2011; Wassermann 2012; Chouet and Matoza 2013; Thompson 2015; Kawakatsu and Yamamoto 2015; McNutt and Roman 2015; Nishimura and Iguchi 2011; Zobin 2016; Saccorotti and Lokmer 2021). Volcanic seismicity occurs from mantle depths to the surface, and elucidates magmatic, hydrothermal, and faulting processes occurring within and around volcanoes (e.g., McNutt 1996; Nishimura and Iguchi 2011; Chouet and Matoza 2013; Kawakatsu and Yamamoto 2015; Matoza 2020). Infrasound (atmospheric acoustic waves with frequencies ~ 0.01–20 Hz) is produced by shallow subsurface and subaerial processes, including explosive eruptions, shallow degassing, surface flow, and mass wasting (Johnson and Ripepe 2011; Fee and Matoza 2013; Allstadt et al. 2018; Matoza et al. 2019a). Infrasound from major explosive eruptions can propagate thousands of kilometers in atmospheric waveguides, enabling regional (15–250 km) and remote (> 250 km) ground-based detection and characterization of explosive eruptions (e.g., Wilson and Forbes 1969; Kamo et al. 1994; Liszka and Garces 2002; Evers and Haak 2005; Le Pichon et al. 2005; Campus and Christie 2010; Fee et al. 2010a; Matoza et al. 2011a, 2018; McKee et al. 2021; Perttu et al. 2020a). Seismo-acoustic wave conversion and coupling commonly occur (e.g., Ichihara et al. 2012; Matoza and Fee 2014; Fee et al. 2016); thus, collocated seismic and infrasonic sensor deployments reduce ambiguity in seismic-acoustic signal type identification and process discrimination (e.g., Iguchi and Ishihara 1990; Garcés et al. 1998; Ripepe et al. 2001; Lees et al. 2004; Johnson et al. 2005; Matoza et al. 2009a, b, 2019b; Ichihara et al. 2021) and in explosive eruption detection and localization (e.g., Matoza et al. 2007, 2017; Sanderson et al. 2020; Le Pichon et al. 2021). At present, seismic and infrasound networks have become indispensable components in tracking the geophysical signatures of unrest and eruption, enabling better monitoring and mitigation of volcanic hazards (e.g., Moran et al. 2008a; National Academies of Sciences, Engineering, and Medicine 2017; Alvarado et al. 2018; Power et al. 2020). In the marine environment, technological advances and increasing availability of hydroacoustic systems and ocean-bottom seismology are expanding volcano seismology and acoustics to partially submerged and submarine oceanic volcanoes (e.g., Talandier and Okal 1987; Yamasato et al. 1993; Caplan-Auerbach and Duennebier 2001; Dziak et al. 2005, 2011; Chadwick et al. 2008, 2012; Green et al. 2013; Metz et al. 2016; Caplan‐Auerbach et al. 2017; Metz and Grevemeyer 2018; Tepp et al. 2019, 2020; Fee et al. 2020; Talandier et al. 2020; Tepp and Dziak 2021; Rose and Matoza 2021).
In modern volcano seismology, quantitative source mechanism models based on full-waveform moment-tensor and single-force representations provide detailed source-time histories (e.g., Ohminato et al. 1998a, b; Nakano et al. 2003; Chouet and Matoza 2013; Kawakatsu and Yamamoto 2015). Interpretations of these observations are facilitated by laboratory and numerical experiments investigating a range of seismic source processes in volcanic fluid and solid frictional systems (e.g., Lane and James 2009; James et al. 2004; Lavallée et al. 2008; Arciniega-Ceballos et al. 2015; Spina et al. 2018). Further hypothesis testing is enabled through multi-parametric geophysical and geological field observations (e.g., Tuffen and Dingwell 2005; Pallister et al. 2012; Rasmussen et al. 2018; Unwin et al. 2021). The ability to accurately recover seismic source mechanisms depends on seismic station density and distribution along with known resolution of the internal seismic velocity structure of the volcanic edifice and upper crust (e.g., Bean et al. 2008; De Barros et al. 2011; Dawson et al. 2011; Chouet and Dawson 2016), which are all steadily improving with advances in (for example) portable compact broadband (e.g., Aster et al. 2005; Ibáñez et al. 2016; Lyons et al. 2016; Matoza et al. 2022a) and nodal (e.g., Kiser et al. 2016; Wu et al. 2017; Glasgow et al. 2018) seismic instrumentation, exploited by various tomographic implementations including ambient noise seismology (e.g., Obermann et al. 2016; Wang et al. 2017; Ulberg et al. 2020). Advances in broadband seismic and complementary geodetic instrumentation (e.g., tiltmeters, high-rate Global Navigation Satellite System (GNSS) receivers, and continuous gravity meters) and techniques are expanding the scope of volcano seismology to an increasingly wider bandwidth, including, at longer time-scales, ultra-long-period (ULP, > 100 s period) signals approaching static ground deformation (e.g., Green et al. 2006; Green and Neuberg 2006; Sturkell et al. 2008; Mattia et al. 2008; Maeda et al. 2011, 2017; Chouet and Dawson 2015; van Driel et al. 2015; Wauthier et al. 2013, 2016; Poland and Carbone 2018; Poland et al. 2019; Alvizuri et al. 2021; Soubestre et al. 2021; Bell et al. 2021). The boundary between volcano geodesy and volcano seismology is thus becoming seamless (e.g., Anderson et al. 2010; Segall 2013; Wauthier et al. 2016; Fernández et al. 2017; Segall and Anderson 2021; Neuberg et al. 2022). Rapid advances in computation are enabling more thorough processing and analyses of greater volumes of seismic waveform data and characterization of hundreds of thousands to millions of seismic events recorded during sustained episodes of volcanic unrest and eruption (e.g., Moran et al. 2008b; Rodgers et al. 2015a; Matoza et al. 2015, 2021). Machine learning methods were adopted relatively early in volcano seismology (e.g., Falsaperla et al. 1996; Langer et al. 2003; Scarpetta et al. 2005; Benítez et al. 2007; Ibáñez et al. 2009; Dawson et al. 2010, 2012) but are now in increasing use (e.g., Malfante et al. 2018; Carniel and Guzmán 2021; Dempsey et al. 2020; Shen and Shen 2021) and are poised for massive impact most immediately in event detection and association, classification, and forecasting.
In modern volcano acoustics, quantitative source mechanism models and source inversions have been developed for relatively simple volcano-acoustic sources such as impulsive explosions (Johnson et al. 2008a; Kim et al. 2012, 2015; Iezzi et al. 2019a) and rockfalls (Moran et al. 2008c). The acoustics of more complex sources such as sustained volcanic jet noise signals from sub-Plinian and Plinian eruptions (Matoza et al. 2009a; 2013a; Mckee et al. 2017) are being investigated by laboratory (Swanson et al. 2018; Fernández et al. 2020) and numerical (Cerminara et al. 2016; Brogi et al. 2018) experiments. Non-linearity in source and propagation is being examined in observations and by numerical simulation (Marchetti et al. 2013; Fee et al. 2013a; Maher et al. 2020, 2022; Watson et al. 2021). Acoustic full-waveform inversion methods take into account topographic effects, which are particularly significant at local ranges (< 15 km). Major advances in infrasound propagation theory and numerical implementations incorporating operational atmospheric specifications are enabling increasingly accurate models of regional range (15–250 km) and remote (> 250 km) infrasound propagation through atmospheric waveguides particularly in the troposphere, stratosphere, and thermosphere (e.g., Drob 2019; Waxler and Assink 2019; Schwaiger et al. 2019). In tandem, advances in infrasound technology and signal processing, discrimination, association, and location are improving abilities to detect signals from remote explosive eruptions within the plethora of interfering background ambient infrasound signals, which are sometimes termed clutter (e.g., Garces and Hetzer 2006; Matoza et al. 2013b; Ceranna et al. 2019), and wind noise (e.g., Hedlin and Raspet 2003; Walker and Hedlin 2010; Raspet et al. 2019) and localize these detections to remote volcanoes using sparse ground-based infrasound networks (e.g., Evers and Haak 2005; Arrowsmith et al. 2015; Matoza et al. 2017) or combined seismic and infrasonic networks (e.g., Fee et al. 2016; Matoza et al. 2018; Sanderson et al. 2020; Le Pichon et al. 2021). Infrasound early warning and eruption notification systems are in operation and undergoing testing and refinement (e.g., Garces et al. 2008; Fee et al. 2010b; De Angelis et al. 2012; Ripepe et al. 2018; Matoza et al. 2019a), augmenting spaceborne remote sensing methods for monitoring and quantifying global volcanism (e.g., Wright et al. 2004; Webley and Mastin 2009; Prata 2009; Ramsey and Harris 2013; Patrick and Smellie 2013; Poland 2015; Carn et al. 2017; Poland et al. 2020; Mckee et al. 2021). More broadly, volcano seismology and acoustics have seen progressive integration with a wide array of volcano-monitoring techniques (including, but not limited to) thermal, gas, electromagnetic, volcanic lightning, fumarole and hydrothermal, physical volcanological, and petrological methods utilizing ground-based and spaceborne instrumentation systems (e.g., Martini et al. 1991; Fischer et al. 1994; Harris and Ripepe 2007a; Marchetti et al. 2009; McNutt and Williams 2010; Saunders et al. 2012; Harris et al. 2012; Van Eaton et al. 2016; Neal et al. 2019; Poland et al. 2020).
The occasion of the IAVCEI Centennial (1919–2019) (Cas 2022) is a time to reflect on 100 years of scientific and technological advances in volcano seismology and volcano acoustics; advances which have led to the point at which we are today in 2022. One hundred years is a long time for modern science, and advances in volcano seismology and acoustics have been coupled more broadly to developments, in (including, but not limited to) geophysics, tectonics, volcanology, seismology (broadly), acoustics (broadly), physics, applied mathematics, electrical and mechanical engineering, material science, instrumentation, remote sensing, and computer science. For this necessarily finite review, we limit our scope to a highlight of major trends and changes in instrumentation and technology, new discoveries, and paradigm shifts from 1919 to the time of writing (2021 to 2022). Volcanology is an observational science; over the past 100 years, major technological advances have provided progressively sharper tools to make new observations (e.g., the transition from analog to digital recording, event-triggered to continuous waveform data, short-period to broadband), all of which have led to discoveries of new phenomena as well as major shifts in understanding. Similarly, larger eruptions (VEI > 4; Volcanic Explosivity Index; Newhall and Self 1982) and the associated seismo-acoustic unrest and eruption signatures are only available to observe relatively rarely, and instrumentation must be in place at suitable locations (Moran et al. 2008a). Large eruptions and those with societal consequences have generally provided impetus and catalyzed the implementation of new seismic (and more recently acoustic) instrumentation and led to operationalization of research methodologies (e.g., Alcaraz et al. 1952; Philippine Geodetic & Geophysical Institute 1952; Malone 1990; Tayag and Punongbayan 1994; De la Cruz-Reyna and Siebe 1997; Sparks and Young 2002; Yamasato 2005; Gudmundsson et al. 2010; Neal et al. 2019).
Herein, we use the following definitions to refer to observation period (s) or frequency (Hz) bands of volcano seismic and acoustic signals (Ohminato et al. 1998a, b; Chouet and Matoza 2013):
-
Ultra-long-period (ULP) > 100 s or < 0.01 Hz;
-
Very-long-period (VLP) 2–100 s or 0.01–0.5 Hz;
-
Long-period (LP) 0.2–2 s or 0.5–5 Hz; and
-
Short-period (SP) 0.05–0.2 s or 5–20 Hz.
Strictly speaking, this terminology refers just to the band of the signal. In addition to the classification based on frequency content, volcano-seismic signals have also been named according to the inferred physical source process (Lahr et al. 1994; Chouet 1996a). In this latter process-based classification system, the most important distinction is between brittle-failure shear or tensile sources that occur in the elastic solid Earth (including so-called volcano-tectonic or VT seismicity), and volumetric sources that actively involve a fluid (including long-period seismicity, which includes individual LP events and tremor). In general, different physical processes occur on different time and spatial scales, but observed volcanic signals often do not fall neatly into these frequency bands (such as ULP, VLP, LP, and SP). Thus, moment-tensor and single-force source-representations provide a more fundamental basis for signal and process discrimination (e.g., Kumagai 2009; Chouet and Matoza 2013; Kawakatsu and Yamamoto 2015).
Volcano seismology in 1919
Instrumental volcano seismology in 1919
By 1919, quantitative instrumental recording of seismic ground motions was well underway using the seismograph, that is, an instrument for measuring seismic ground motion as a continuous function of time as a waveform (Dewey and Byerly 1969). There was, for example, regular reporting of earthquakes since 1883 in Japan allowing early pioneering observational seismology works by Profs. Sekiya Seikei and Fusakichi Omori (e.g., Omori 1894; Dewey and Byerly 1969; Agnew 2002). A seismoscope is an instrument for recording only the occurrence, time, and in some cases duration of an earthquake, but not a waveform record of ground motion. Seismic monitoring using pendulum seismoscopes began at the Manila Observatory, Philippines in 1868 followed with seismographs during the 1880s (Saderra Masó, 1904; Repetti 1946; Udías and Stauder 1996; Bautista and Bautista 2004; Manila Observatory 2016). Mexico installed its first seismograph in 1904 (Pérez-Campos et al. 2018; Suárez and Pérez‐Campos 2020). A first national seismic network was deployed in Chile by 1909 (Brenner 1911; Barrientos and National Seismological Center (CSN) Team 2018).
The first dedicated instrumental volcano-seismological observations (Fig. 1) are typically attributed to Luigi Palmieri, with observations of “continuous tremor” at Vesuvius using his “sismografo elettro-magnetico” (developed by Palmieri around 1856), which is formally considered a collection of electromagnetic seismoscopes (Dewey and Byerly 1969). Osservatorio Vesuviano, the world’s first volcano observatory, was founded 1841 (Palmieri 1859; Imbò, 1949; Borgstrom et al. 1999; Giudicepietro et al. 2010). The Palmieri seismoscope ran continuously until 1906, and was replaced in 1914 (Giudicepietro et al. 2010). In Japan, Sakurajima was the first volcano to have a seismometer installed nearby (Fig. 1). A Milne-type seismometer was installed at Kagoshima Weather Station in 1888 and later recorded precursory earthquakes to the 1914 eruption (Omori 1916; Yamasato 2005; Iguchi 2013).
A landmark study by Omori (1912) on eruptions and earthquakes of Mount Asama used Omori’s two-component horizontal pendulum seismograph “tromometer” (Fig. 2), which was a modification of the earlier horizontal pendulum seismograph of John Milne (Omori 1899). This formed the basis of the Bosch-Omori seismograph, which was later deployed worldwide (e.g., Dewey and Byerly 1969; Klein and Koyanagi 1980; Moore et al. 2018; Suárez and Pérez‐Campos 2020; Ammon et al. 2020). The original Omori seismographs did not include viscous damping, which was added in the Bosch-Omori design (Klein and Koyanagi 1980; Okubo et al. 2014). Omori also conducted pioneering observational seismology studies recognizing the forecasting potential for eruptions of Mount Usu in 1910 (Omori 1911) and Sakurajima in 1914 (Omori 1916; Davison 1924). Omori established the first volcano observatory in Japan at Mount Asama in 1911 (Suwa 1980) (Fig. 1). Even in these earliest instrumental observations it was clear that volcano-seismic signals could be different in character to ordinary crustal earthquakes (Gasparini et al. 1992).
Continuous seismic monitoring at Mount Pelée, Martinique began in 1903 with the installation of a two-component (horizontal) Omori seismograph that operated until 1927 (Fig. 1). However, the station was too far from the volcano (located at a distance of 8.5 km) to detect any weak volcanic seismicity (Lacroix 1904; Hirn et al. 1987). Two of Omori’s original seismograph instruments, which were an “ordinary” seismograph and a “heavy” seismograph, were also purchased by Thomas Jaggar and installed at the newly established (founded 1912) Hawaiian Volcano Observatory (HVO) (Klein and Koyanagi 1980; Wright and Takahashi 1989, 1998; Okubo et al. 2014). Jaggar had traveled to Japan in 1909 and met with Omori to learn about the new seismological methods as part of laying the foundation for establishing the HVO (Hawaiian Volcano Observatory 2001; Jaggar 1956). Jaggar later (by July 1913) added two horizontal Bosch-Omori instruments that were operated by HVO until 1963 (Klein and Koyanagi 1980; Apple 1987; Okubo et al. 2014). For further information on the early development of the HVO, the reader is referred to the collections by Wright and Takahashi (1989, 1998) and “The Volcano Letter” collections (see Takahashi 1988).
Simultaneous with Omori’s work in Japan, similar pioneering research was conducted by Miguel Saderra Masó in the Philippines at the Weather Bureau (Manila Observatory) (Saderra Masó, 1911a; 1919). The 1911 eruption of Taal was documented in detail by Saderra Masó (1911a) including with observations from Vicentini and Omori seismographs, as well as ten Richard barograph stations installed out to a distance of 242 km (Fig. 3). In a 1911 publication summarizing observations at Taal, Mayon, and Camiguin (Saderra Masó, 1911b), Saderra Masó wrote:
“The exorbitant toll of human lives levied by the recent eruption of Taal Volcano is a lesson which must not be forgotten, so much the less in view of the fact that, under similar circumstances, on a likewise recent occasion (July, 1910) not a single life was lost in Japan [Usu]. These occurrences in Japan and those which we have recently witnessed in connection with the eruption of Taal Volcano, January 30, 1911, prove conclusively that some eruptions can be foreseen; a conclusion likewise stated by the eminent seismologist Prof. F. Omori.”
(Saderra Masó 1911b)
In a review of Saderra Masó’s paper (Saderra Masó 1911b), Harry O. Wood concluded:
“The moral drawn in the paper is that sundry volcanic eruptions, through the occurrence of earthquakes, or in other ways, can be anticipated in sufficient time to permit the escape of persons whose lives are threatened.”
(Wood 1912)
Wood was subsequently recruited by Jaggar to establish seismic monitoring at the HVO (Wood 1913), arriving there in summer 1912 (Okubo et al. 2014).
Saderra Masó established a small seismic observatory at Ambulong on the north shore of Lake Taal following the 1911 eruption (Saderra Masó 1911a, 1913; Repetti 1946, 1948). Bulusan volcano had a significant eruption in 1918 which was also documented, including with observations from a seismograph placed at about 8 km distance (Saderra Masó, 1919). In 1920, Saderra Masó represented the, then, world-famous Manila Observatory (Repetti 1948) at the First Pan-Pacific Scientific Conference held in Honolulu, Hawai‘i together with Omori and Jaggar who co-organized the seismology and volcanology section (Proceedings of the first Pan-Pacific Scientific Conference 1921).
Volcano seismology scientific framework in 1919
By 1919, it had been well established qualitatively that volcanic eruptions were generally preceded by observable, i.e., felt, seismicity (see, for example, the writings of Pliny the Younger; Sigurdsson et al. 1982), and also that earthquakes at volcanoes do not necessarily lead to eruption (Scrope 1825). Early ideas about the mechanisms by which magmatic processes drove earthquakes were heavily influenced by principles of structural geology. Scrope (1825) posited that earthquakes would occur most strongly at depths where expansive force of magma was strongest. According to Scrope (1825), this led to the, albeit possibly subtle, uplift of shallower strata and consequential, and possibly seismic, dilation/fissuring. This was a prescient connection with the modern continuum between volcano seismology and volcano geodesy. Scrope (1825) further posited that the position of a fissure with respect to its expansive force would control whether magma erupted or remained trapped in the crust, leading to a testable hypothesis about the location and timing of earthquakes with respect to the vent.
In the decades between Scrope’s pioneering treatise of 1825 and 1919, the beginnings of instrumental seismology led to debate and refinement of these ideas. Omori (1912) hypothesized that strong volcanic earthquakes resulted from energy released by subterranean explosions that were not simultaneously accompanied by eruption, and that an explosive eruption produced a lower quantity of seismic energy. That is, eruptions were “safety valves” that served to reduce pressure causing large earthquakes (Omori 1912). Omori further hypothesized that the former type of non-eruptive volcanic earthquake would be characterized by a deeper implosive source (“B-type”), and the latter explosion earthquake type by a shallow explosive source (“A-type”). Omori (1912) presented limited evidence for this pattern from a seismograph installed at Mount Asama, which was later refined by Minakami (1960) using data from volcanic and tectonic earthquakes, as shown in Fig. 4. Jaggar (1920), summarizing work by the nascent HVO (Wright and Takahashi 1998), posited that volcanic earthquakes could reflect a wide variety of processes alone or in combination. He hypothesized that volcanic earthquakes occur on existing rift faults stressed past their frictional limit. Jaggar’s point that multiple source processes could result in volcanic earthquakes was accompanied by early recognition of a variety of seismic signals such as harmonic and spasmodic tremor (Omori 1914; Jaggar 1920). The early classification scheme based on event depth made by Omori (1912) ultimately evolved into a spectral-based classification scheme, in which spectral differences were hypothesized to correspond to fundamentally different source mechanisms (Minakami 1974; Lahr et al. 1994).
Volcanic waves in the atmosphere in 1919
Atmospheric infrasound (frequency band ~ 0.01 to 20 Hz) is part of a broad spectrum of atmospheric waves produced by volcanic activity that includes gravity waves, acoustic-gravity waves, infrasound, and audible acoustic waves (Gossard and Hooke 1975). By 1919, low-frequency (< 1 Hz) pressure waves from eruptions had been captured instrumentally by meteorological barographs, and research was underway to understand the physics of these atmospheric pressure disturbances and their relation to atmospheric structure. This work based on instrumental observations had begun 36 years earlier with the eruption of Krakatau.
In 1883, over 50 weather barometers around the world recorded (ultra) long-period pressure disturbances from the cataclysmic, VEI 6, August 27 eruption of Krakatau, Indonesia (Scott 1883; Strachey 1884, 1888; Verbeek 1884). A Royal Society of London report compiled the barometric observations and reports of sounds heard (Strachey 1888). Audible cannon-like sounds were reported as far away as ~ 4800 km, similar to historical “earwitness” reports from the earlier 1815 eruption of Tambora (de Jong Boers 1995). The Krakatau atmospheric (ultra) long-period pressure wave propagated around the globe and was recorded as barometric pulses for four minor-arc passages and three major-arc (antipodal) passages (Strachey 1888). It took roughly 1.5 days to make each complete lap, with an average propagation speed of 300–325 m/s; the dominant periods at long range were ~ 100 to 200 min (Gabrielson 2010). These observations stimulated the development of theory to explain what were eventually termed acoustic-gravity waves, and more specifically the surface-guided Lamb wave, and to understand the effects of gravity, buoyancy, and atmospheric structure on their propagation (e.g., LeConte 1884; Lamb 1911; Taylor 1929, 1936; Pekeris 1939; Pierce 1963; Press and Harkrider 1962, 1966; Harkrider 1964; Harkrider and Press 1967; Bretherton 1969; Yeh and Liu 1974; Gabrielson 2010).
The pioneering study of Omori (1912) at Mount Asama, Japan, gave nearly equal emphasis to seismic and atmospheric pressure wavefields, using seismometers and barometers to discriminate between seismic signals associated with airborne explosions (“detonations” and “sound tremors”) and non-explosion earthquakes (Fig. 2). Many of the explosion events were audible in settlements at distances of ~ 200 to 300 km, and some were powerful enough to knock out doors and windows. Omori used this information to map the sound propagation and acoustic shadow zones, and began to consider the effects of wind and topography on the acoustic signals; these topics are again active research areas today. Omori continued the analysis of barograph records, for example, at Sakurajima (Omori 1916) (Fig. 2). Saderra Masó (1911a) made similar instrumental (seismograph and barograph) observations for the 1911 eruption of Taal, Philippines (Fig. 3).
The use of weather barometers and infrasonic microphone arrays to study low-frequency (< 1 Hz) atmospheric pressure waves from volcanic explosions at regional to global ranges (tens to thousands of kilometers) continued sporadically throughout the twentieth century, most commonly when large eruptions were recorded on remote barograph or infrasonic microphone arrays, for example, for the eruptions of Mount Pelee, Martinique, 1902 (Anderson and Flett 1903); Bezymianny, Russia, 1956 (Gorshkov 1960); Mount St. Helens, USA, 1980 (Reed 1987; Delclos et al. 1990); El Chichón, Mexico, 1982 (Mauk 1983); Mount Tokachi, Japan, 1988; Sakurajima, Japan, 1989; Pinatubo, Philippines, 1991; Ruapehu, New Zealand, 1995 (Morrissey and Chouet 1997), and Popocatépetl, Mexico (Raga et al. 2002).
Despite early pioneering instrumental studies giving near-equal emphasis to seismic and atmospheric pressure wavefields (e.g., Saderra Masó 1911a; Omori 1912; Perret 1950), advances broadly in seismology and specifically in volcano seismology rapidly outpaced those in atmospheric acoustics until the 1990s (Harris and Ripepe 2007a, b; Fee and Matoza 2013; Chouet and Matoza 2013; Matoza et al. 2019a).
Instrumentation changes 1919–2019
Volcano seismology and acoustics are highly observational fields. The phenomena that can be observed depends upon the available instrumentation. From 1919 to 2019, major advances were made (for example) (1) in instrument sensitivity, i.e., the smallest resolvable amplitude change of ground motion or air pressure that can be measured; (2) in bandwidth, i.e., the frequency range of signals that can be captured; (3) in the portability, compactness, ruggedness, and rapid deployability of instrumentation; (4) in the electronics systems for recording, storing, timing (e.g., GNSS), and telemetering the data; (5) in reducing instrumental power requirements, solar charging, and battery technology; and (6) with the computer revolution, the efficiency with which data could be processed and stored. A comprehensive history of seismometry, microbarograph, and infrasound sensor technology evolution from 1919 to 2019 is beyond our scope. For some of the details, we refer the reader to Dewey and Byerly (1969), Howell (1989), Ben-Menahem (1995), Agnew (2002), Evers and Haak (2010), Ponceau and Bosca (2010), Nief et al. (2019), Marty (2019), and references therein. Major milestones included the transition from analog to digital recording, event-triggered to continuous waveform data, and short-period to broadband, all of which collectively provided a progressively sharper, higher fidelity, wider bandwidth, higher sensitivity, and more temporally continuous capture of the seismic and acoustic signatures of volcanic unrest and eruption. Moreover, a net effect of these technological advances was that the operational seismological monitoring workflow became increasingly efficient, with real-time data transmission and processing enabling the results of seismological analyses to be available more rapidly to inform monitoring decisions (e.g., Klein and Koyanagi 1980; Okubo et al. 2014; Thompson 2015).
Although field logistics at volcanoes will always be demanding, these technological advances have generally also allowed steady expansion in the numbers of seismic and acoustic stations (i.e., increases in network density) at permanently monitored volcanoes (Fig. 5; Table 1) and in campaign research deployments, in turn permitting higher spatiotemporal resolution geophysical inference. Although operating and maintaining permanent seismic monitoring stations at volcanoes is still not straightforward, it is undoubtedly easier now in the days of digital waveform telemetry and low-power ruggedized systems compared to the laborious days of smoked paper or tape recorders. Another promising trend in volcano seismology and acoustics is the increased central archiving and public worldwide sharing of waveform data, which is beginning to allow systematic comparisons and hypothesis testing of seismic and acoustic source processes across varied volcanic systems and tectonic environments.
For operational volcano monitoring, a critical technological advance was the development of radio telemetry (e.g., Eaton 1977; Murray 1992; Lockhart et al. 1992; Thompson 2015). Prior to radio telemetry, data transmission utilized cables including telephone cables. At the HVO, this resulted in miles of overland cables by 1958 and a seismic station distribution limited by cable logistics (Klein and Koyanagi 1980; Klein et al. 1987; Okubo et al. 2014). Radio telemetry thus represented a monumental advance, permitting the expansion of volcano seismic monitoring networks worldwide (e.g., Klein and Koyanagi 1980; Ewert and Swanson 1992; Hill 1984; Castellano et al. 2002; Power and Lalla 2010; Giudicepietro et al. 2010; Senyukov et al. 2009; Nishimura and Iguchi 2011). Data from remote and widely distributed instruments could be collected at a central location and analyzed in real time (first on media such as smoked drum paper and later on computerized systems). This advance primarily occurred in the mid-1960s through the early 1970s.
As an illustration of other major technological changes, we consider selected time snapshots containing landmark studies or significant eruptions. We focus the remainder of this section on technological changes from 1970 to 2020, which was a time of major growth in quantitative volcano seismology.
Volcano seismology in the 1970s: limited portability
By the 1970s, field studies at volcanoes using portable seismic instrumentation and computational methods were underway, but the portability was highly limited by today’s standards. A 1959 eruption of Kīlauea, Hawai‘i, produced a stagnant lava pond at Kīlauea Iki, a pit crater adjacent to Kīlauea summit caldera in the upper east rift zone (Richter et al. 1970), and its slow cooling and solidification provided a landmark opportunity in volcanology (Kauahikaua and Poland 2012; Heiken 2013) and decades of studies including scientific drilling (e.g., Rawson 1960; Wright et al. 1976; Helz 1980, 1993; Helz and Thornber 1987). By the 1970s, the solidified crater floor also enabled seismological investigations, including a refraction experiment performed for a series of geophones deployed along the long axis of the crater floor (Aki et al. 1978) and passive seismic surveys capturing local seismic events originating in the cooling crust of the lake (Chouet 1979). Chouet (1979) developed a quantitative source model for the seismic signals originating within the cooling Kīlauea Iki magma body, parameterized as vertically aligned penny-shaped cracks between columnar basalt joints, with tensile failure (crack opening) due to cooling and solidification of magma. Chouet (1979) presented an analytical expression for the far-field pulse shape of vertical and horizontal ground displacements including attenuation, enabling forward modeling with the crack model to infer cavity volumes, which compared reasonably well with independent estimates based on thermodynamic considerations and a cooling model (also by Chouet 1979).
These were important early studies in quantitative (and computational) volcano seismology, but the limitations of seismic instrumentation technology at the time made installing and maintaining the field equipment highly laborious (B. Chouet, personal communication, 2019 & 2021). For example, a study on coda waves from earthquakes in Hawai‘i (Chouet 1976) involved the deployment of 4 mi (6.4 km) of military surplus Spiral-4 cable to connect station OTL (Outlet) on Sand Hill to the HVO. Spiral-4 came in spools weighing 100 lb. (45 kg) each; 40 spools were used. The data were stored on paper (recording at 1 mm/s for months on end), which had to be digitized by hand to be stored on punch cards. The seismic surveys described by Chouet (1979) (conducted in the summer of 1974) used a “portable” Sprengnether MEQ-800 smoke drum recorder with a vertical component (short-period) Mark products L-4C 1 Hz geophone as the sensor (Fig. 6a). All of the data were analog and had to be measured by hand with rulers (B. Chouet, personal communication, 2019 & 2021).
Volcano seismology in the 1980s: digital capture and storage
The 1980s saw the beginnings of digital data capture and storage, based on the recording of event-triggered digital waveforms. The 1980–1986 unrest and eruption sequences of Mount St. Helens, USA, provided opportunities to record signals with new technologies, with access to the crater floor exposed by the 18 May 1980 lateral blast allowing near-field high signal-to-noise ratio recording. A pioneering study by Fehler and Chouet (1982) and Fehler (1983) utilized a prototype 12-bit digital recorder which had been designed and built at the Massachusetts Institute of Technology, USA primarily for ocean bottom deployment (Fig. 6b, c). The deployment consisted of nine short-period seismometers (L4-C 1 Hz geophones with a rapid fall-off in response below 1 Hz) attached to the digital event recorders, which provided event-triggered recording. This involved event-windowed data recording on a magnetic tape that was initiated whenever seismic amplitude rose significantly above the background noise. There was thus no continuous digital recording, but continuous analog recording was made separately on paper chart recorders. The digital recording package for each station consisted of a 4-ft. (1.2 m) tall cylinder containing the signal processing electronics and recorder, but one station was nevertheless deployed in the crater of Mount St. Helens (Fehler and Chouet 1982; B. Chouet, personal communication, 2019 & 2021). Despite these limitations, this deployment provided digital capture of long-period (LP, 0.5–5 Hz) seismicity and tremor at Mount St. Helens (Fig. 6b) (Fehler and Chouet 1982; Fehler 1983), providing new and key observations that initiated a sustained research program to understand the quantitative source mechanism of long-period seismic events and tremor (Chouet and Julian 1985; Chouet 1981; 1985; 1986; 1988; 1992).
Digital recording facilitated digital signal processing, including the application of the Fast Fourier Transform (FFT) (Cooley and Tukey 1965; Cooley et al. 1969) for spectral estimation. Fehler and Chouet (1982) reported LP events with durations ∼30 s, spectra peaked in the range 1.7–2.3 Hz, and at depths of between 0 and 5 km. Production of the spectral peaks by a path effect (Malone 1983) was considered inconsistent with the data because the position of the spectral peaks did not change significantly with station location, and a VT earthquake located in the vicinity of the crater observed with the same instruments did not have the same spectral structure as the LPs (Fehler and Chouet 1982). Fehler and Chouet (1982) proposed that the spectral peaks originated from the excitation of a fixed cavity under the active crater. Following Latter (1979), Fehler (1983) also noted the spectral similarity of LP events and tremor, and proposed that tremor consisted of a superposition of randomly occurring LP events. These observations rejuvenated interest in LP event and tremor models in which the fluid plays an active role in generating the signal.
Computer-based earthquake data processing began at HVO in 1979 through digitizing analog tapes. Subsequently, by 1986, automated operational near-real-time seismic network processing with event-triggered digital storage was underway with the Caltech-USGS Seismic Processing (CUSP) system (Fig. 5), which received analog telemetered seismic data and converted it to a digital format (Okubo et al. 2014). Nevertheless, by the time of the 1991 eruption of Pinatubo, Philippines (Tayag and Punongbayan 1994; Punongbayan and Newhall 1999), analog systems remained standard in operational (especially rapid response) monitoring due to their low cost, simplicity of design, and ruggedness (Lockhart et al. 1996). However, digital acquisition, telemetry, and signal processing were becoming increasingly integrated in operations (e.g., Sabit et al. 1996; Ramos et al. 1996, 1999). The 1980s also saw steady expansion of volcano-seismic monitoring capacities worldwide. For example, in 1988, the Instituto Geofísico of the Escuela Politécnica Nacional (IGEPN) of Ecuador began continuous monitoring of Ecuadorian volcanoes with single telemetered seismic stations at Tungurahua, Cotopaxi, Cuicocha, Chimborazo, Antisana, and Cayambe, and seismic and geodetic networks were established at Guagua Pichincha (Alvarado et al. 2018). Several volcanological and seismological observatories were also established in Colombia by the Colombian Geological Survey (formerly Instituto Colombiano de Geología y Minería INGEOMINAS) in the late 1980s (Vargas et al. 2018).
Volcano seismology in the 1990s: portable broadband seismometry, infrasound, continuous digital waveform data
The 1990s saw the advent of portable broadband seismometry at volcanoes capturing waveforms in the VLP and ULP bands, immediately leading to the discovery of new signals and phenomena (Fig. 7) (e.g., Kawakatsu et al. 1992; Neuberg et al. 1994; Kaneshima et al. 1996; Arciniega-Ceballos et al. 1999). The reader is referred to the reviews by Chouet and Matoza (2013) and Kawakatsu and Yamamoto (2015) for an overview of VLP and ULP observations, inversions, and modeling studies during this time. Previously unobservable with standard short-period instrumentation, VLPs represented entirely new signals reflecting slower processes associated with unsteady mass transport, and commonly attributed to fluid–rock interaction or longer-term inertial volume changes in fluid-filled conduits (e.g., Kawakatsu et al. 1992; Ohminato et al. 1998a, b; Nishimura et al. 2000; Kumagai et al. 2003; Kumagai 2006; Chouet and Dawson 2011).
Advances in computer processing and storage by the 1990s also enabled the transition to continuous digital waveform recording and storage for an expanding number of stations, and made tractable full-waveform inversions using synthetic Green’s functions taking into account topography (Ohminato et al. 1998a, b; Kumagai et al. 2002a; Chouet et al. 2003, 2005; Nakano and Kumagai 2005). As a result, broadband observations rapidly became quintessential in volcano-seismic monitoring worldwide (e.g., Martini et al. 2007; De Cesare et al. 2009; Neuberg et al. 1998; Kawakatsu et al. 2000; Iguchi 2013). For example, a semi-permanent digitally telemetered (continuous data) 10-station broadband network was established at Kīlauea beginning November 1994, immediately capturing a variety of new signals and processes and augmenting monitoring capacity (Dawson et al. 1998).
Audio range volcanic sound microphone recordings (> 20 Hz)
Frank Perret made probably the first recordings of sounds in the audio range (frequencies > 20 Hz) from volcanoes using moving-coil microphones at Vesuvius in 1906, eventually also recording signals at Etna, Stromboli, Kīlauea, Sakurajima, Mount Pelée, and Soufrière Hills (Perret 1950). The first tape recordings of volcanic sounds were apparently made by the NHK (Nippon Hōsō Kyōkai) Broadcasting Bureau of Japan (Snodgrass and Richards 1956). In 1952, a program of volcanic acoustics was initiated by James Snodgrass at the Scripps Institution of Oceanography, USA, leading to a decade’s worth of underwater and airborne acoustic recordings of volcanic sounds with frequencies > 50 Hz (Richards 1963). The paper by Richards (1963) summarizes these observations, relating the various sounds to different idealized styles of volcanic activity.
A pioneering study of acoustic signals (> 20 Hz) by Woulff and McGetchin (1976) represents the first attempt at a quantitative link between acoustic radiation and fluid mechanics at volcanoes using equivalent source theory. This study introduced the idea of using radiated acoustic power and frequency content to infer erupted gas exit velocity for assumed equivalent monopole, dipole, and quadrupole source types. Woulff and McGetchin (1976) only considered audio range acoustic signals > 20 Hz, but later infrasound (< 20 Hz) studies built extensively upon this concept (e.g., Firstov and Kravchenko 1996; Vergniolle et al. 1996; Johnson 2003, Vergniolle and Caplan-Auerbach 2006; Matoza et al. 2009a; Caplan-Auerbach et al. 2010; Kim et al. 2012; Ripepe et al. 2013; Lamb et al. 2015; Delle Donne et al. 2016; Fee et al. 2017; Haney et al. 2018; Iezzi et al. 2019a, 2022; Perttu et al. 2020b). In a reexamination of the original formulation of Woulff and McGetchin (1976) in the context of the current understanding of jet noise, Matoza et al. (2013b) concluded that the formulation of Woulff and McGetchin (1976) can lead to large errors when inferring eruption parameters from acoustic data and thus requires modification.
Remote volcano infrasound observations from the 1960s to the 1990s
In volcano seismology, the frequency band from ~ 0.01 to 20 Hz (which includes VLP, LP, and SP), is particularly important for signals of volcanic unrest and eruption. In atmospheric acoustics, this band is termed infrasound (e.g., Pierce 1981; Bedard and Georges 2000; Hedlin et al. 2002; Evers and Haak 2010). Progress in the field of volcano (atmospheric) acoustics was therefore modest until microphones targeting these frequencies were deployed near active volcanoes. As we reviewed above, barograph records capturing atmospheric pressure wave signals with frequencies < 1 Hz were documented since the 1883 Krakatau eruption. However, the frequency limit of the barograph instrumentation (< 1 Hz), together with their prime usage as weather stations, resulted in an observational bias toward larger eruptions recorded at long ranges.
Reviews of some aspects of the history of general infrasound research can be found in Bedard and Georges (2000), Hedlin et al. (2002), and Evers and Haak (2010). The era of atmospheric nuclear testing from 1945 to 1963 (the 1963 Limited Test Ban Treaty then prohibited nuclear weapon tests in the oceans, atmosphere, and space) resulted in active research programs in infrasound, including the development of sensors, spatial wind-noise filtration systems, and array processing methods, particularly between the years 1945 and 1967 (Thomas et al. 1971). Between 1967 and 1985, infrasound research continued with geophysical studies of weather, meteors, aurorae, and volcanoes, and this time period saw the first utilization of low-frequency infrasound microphone arrays to detect remote volcanic eruptions (in the band 0.01–0.1 Hz).
Goerke et al. (1965), Wilson et al. (1966), and Wilson and Forbes (1969) provided some of the first infrasonic microphone array observations of volcanic eruptions in the low infrasound band (0.01–0.1 Hz). The 1963 eruption of Mount Agung, Bali, was recorded 14,700 km away in Boulder, Colorado (Goerke et al. 1965), and the 1967 eruptions of Redoubt and Trident Volcanoes, Alaska, were recorded in Fairbanks, Alaska (Wilson et al. 1966; Wilson and Forbes 1969). The main emphasis of these studies was the atmospheric propagation of the signals. Infrasonic microphone arrays were then installed at Kariya, Japan (Tahira 1982), and Windless Bight, Antarctica, 26 km from Mount Erebus (Dibble et al. 1984). Although limited to the 0.1–1 Hz band, the Kariya array routinely detected explosions from Sakurajima at a range of 710 km and also recorded the 1991 Pinatubo eruption at a range of 2770 km. These data were used to infer eruptive time-histories when visual or instrumental observations close to the volcano were impossible (Tahira et al. 1996).
The first proposal for an acoustic early warning system for explosive eruptions of which we are aware was that of Kamo et al. (1994). Kamo et al. (1994), following work by Tahira (1982), demonstrated that an array at Kariya, 710 km from Sakurajima, was capable of detecting infrasound from volcanoes thousands of kilometers distant and showcased example signals from the 1991 eruption of Pinatubo (see also Tahira et al. 1996). Kamo et al. (1994) concluded that “this capability forms the basis of a proposal for a worldwide network of air-wave sensors to monitor volcanic explosions,” proposing the “PEGASAS-VE” (“pressure gage system for air-shocks by volcanic eruptions”) early warning system for aviation safety that would consist of a set of infrasonic microphone arrays with a 500–1000 km spacing. Kamo et al. (1994) proposed that PEGASAS-VE “would be a very effective means of enhancing aviation safety and would be similar to the tsunami warning system, which is in worldwide operation.” Although PEGASAS-VE was not constructed, the International Monitoring System (IMS) infrasound network was initiated after the Comprehensive Nuclear-Test-Ban Treaty (CTBT) was opened for signature in 1996 (e.g., Christie and Campus 2010; Marty 2019; Le Bras et al. 2021). The proposed 500 km spacing of the PEGASAS-VE design was chosen to provide timely warnings of volcanic eruptions within 30 min based on infrasound propagation time. The average station spacing for the complete IMS infrasound network will be about 2000 km (Christie and Campus 2010), so additional stations will be needed to augment the IMS infrasound network (e.g., Matoza et al. 2007, 2011a,b; 2017, 2018; Garcés et al. 2008; Fee et al. 2010b; Tailpied et al. 2013, 2016; Nishida and Ichihara 2016; Ripepe et al. 2018; Taisne et al. 2019; Perttu et al. 2020a; Le Pichon et al. 2021) and achieve the vision outlined in the original PEGASAS-VE proposal (Kamo et al. 1994).
Volcano infrasound in the 1990s
Volcanic infrasound in the band 1–20 Hz (termed near-infrasound) was collected at local recording ranges (defined as < 15 km) during a small number of field studies in Kamchatka and Antarctica in the 1970s and 1980s (e.g., Dibble et al. 1984; Firstov and Kravchenko 1996; Gordeev et al. 1990). Observations of local volcano near-infrasound greatly expanded in the 1990s with field studies particularly in Japan and at Stromboli, Italy (Fig. 8). In Japan, Iguchi and Ishihara (1990) and Yamasato (1997) installed infrasonic microphones at distances of 2–5 km from Sakurajima, Suwanosejima, and Unzen, recording numerous explosions and pyroclastic flows (Yamasato 1997), harmonic infrasonic tremor (Sakai et al. 1996), and impulsive signals associated with LP seismic events (Iguchi and Ishihara 1990; Yamasato 1998). The study by Sakai et al. (1996) at Sakurajima is considered the first observation of infrasonic harmonic tremor, but this publication was followed rapidly by similar observations at Arenal (Hagerty et al. 1997, 2000; Garces et al. 1998) (Fig. 8) and Karymsky (Johnson et al. 1998). Acoustic studies began at Stromboli in the early 1990s (Braun and Ripepe 1993; Vergniolle and Brandeis 1994; Buckingham and Garcés 1996). Since then, it has become increasingly clear that an array of volcanic processes produces a variety of types of infrasound signals across the 0.01–20 Hz frequency range (e.g., Harris and Ripepe 2007a, b; Johnson and Ripepe 2011; Garces et al. 2013; Fee and Matoza 2013; Matoza et al. 2019a; Marchetti et al. 2019).
In 1996, the CTBT was opened for signature, leading to the construction of the IMS. The IMS included a global infrasound network with, as of 2022, 53 certified infrasound stations of a planned total 60 (Marty 2019). Construction of the IMS led to rapid advances in infrasound technology, such as improvements in instrumentation, signal-processing methods, and infrasound propagation modeling. These technologies have all been transferred and adapted to understand and monitor volcanic processes (Garces et al. 2003, 2008; McCormack et al. 2005; Matoza et al. 2007, 2019a; Matoza and Fee 2018).
Volcano seismo-acoustics: 2000 to 2020
During the past 20 years, the fields of volcano seismology and volcano acoustics have been progressively merging, as captured in the term volcano seismo-acoustics, and in-line more broadly with the emergence of the discipline of seismo-acoustics (Arrowsmith et al. 2010). These complementary geophysical technologies provide more complete capture of the signals of unrest and eruption, from the mantle to the surface, and reduce ambiguity in signal and process identification. From 2000 to 2020, high-quality, broadband, and well-calibrated infrasound sensors have become increasingly portable, lower power, and rapidly deployable, mirroring trends in portable broadband seismology. Digitizers, power systems, and other electronic components of the system are highly similar for infrasound and seismic stations, making these complementary channels easy to record together and leveraging general technological advances in seismology. Telemetry systems have also increasingly moved from analog to digital. The large community EarthScope USArray Transportable Array catalyzed advances in seismo-acoustic systems technology (Busby et al. 2018). For research campaign-style deployments relying on local data storage (no telemetry), high-volume data storage has increasingly permitted the collection of longer multi-year datasets, with more recording channels, at higher sample rates, and with easier field logistics (infrequent data downloads). In addition, cellular modems (where coverage is available) now make possible streaming of remote data without purpose-built telemetry systems (e.g., Busby et al. 2018; Sanderson et al. 2021; Shiro et al. 2021). Numerous other advances in instrumentation technology have driven progress. For example, for reviews of infrasound sensor and wind noise reduction system developments, the reader is referred to Ponceau and Bosca (2010), Nief et al., (2019), and Raspet et al. (2019).
Permanent volcano monitoring networks have progressively established denser seismic networks (Figs. 1 and 5), with continuous digital waveform acquisition, processing, and storage now being the standard. Infrasound technology has been increasingly integrated in volcano-seismic monitoring operations and is also rapidly becoming standard (e.g., Orazi et al. 2013; Ruiz et al. 2013; Iguchi 2016; Coombs et al. 2018; Alvarado et al. 2018; Yokoo et al. 2019; Taisne et al. 2019; Power et al. 2020).
The internet, central data archiving, and legacy data
A general trend in seismology has been toward increased central archiving and public sharing of waveform data facilitated by data management centers worldwide, e.g., IRIS (Incorporated Research Institutions for Seismology), founded 1987 (Smith 1987); GEOFON (GEOFOrschungsNetz), founded 1992 (Quinteros et al. 2021); GEOSCOPE (French Global Network of broad band seismic stations), founded 1982 (Roult et al. 2010); ORFEUS (Observatories and Research Facilities for European Seismology), founded 1988 (van Eck and Dost 1999); MEDNET (Mediterranean Very Broadband Seismographic Network), founded 1987 (Boschi et al. 1991); and POSEIDON (Pacific Orient Seismic Digital Observation Network), founded 1989 (Geller 1974; Shimazaki et al. 1992). The growth of the internet accelerated these trends (Malone et al. 1993; Malone 1995). These efforts have collectively had profound impacts on seismology (e.g., Malone et al. 1993; Malone 1995; Aster et al. 2004) and, more recently, infrasound (e.g., Hutko et al. 2017; Busby and Aderhold 2020; Stammler et al. 2021) technology and research. Data management centers have become increasingly important with the rise of continuous data streams and growing data volumes. In the past decade, volcano seismo-acoustics research infrastructure has increasingly moved toward the standards of FAIR (Findable, Accessible, Interoperable, and Reusable). The central archiving and public accessibility of seismo-acoustic data allows systematic comparisons across varied volcanic systems and tectonic environments. Preserving data for the future will further ensure that waveform details from landmark eruptions will be available for retrospective analyses with new processing methodologies, or in light of new paradigms and hypotheses.
For the same reasons, the preservation of legacy seismic data is an urgent priority (e.g., Bogiatzis and Ishii 2016; Richards and Hellweg 2020; Hwang et al. 2020; Pérez‐Campos et al. 2020). As seismic and acoustic waves propagate over distance, wave amplitude loss occurs from geometrical spreading, attenuation, and scattering, generally resulting in information loss about volcano seismic and acoustic unrest and eruption signals with increasing distance from the volcanic source. Thus, seismic and acoustic instrumentation provide the most information when deployed as dedicated monitoring instruments (< 50 km range). However, seismic signals from eruptions or unrest sequences have still been captured and usable, to some degree, by more distant stations on early instrumental records. For example, some seismicity from the 1943 eruption of Parícutin was recorded by a Wiechert seismograph at the Tacubaya seismic station in Mexico City at ~ 320 km distance from the source (Yokoyama and de la Cruz-Reyna 1990). Similarly, the 1963–1967 eruption of Surtsey, Iceland was recorded by two stations at distances > 100 km (Sayyadi et al. 2021). This underscores the importance of preserving and making available legacy seismic data, especially data from classic eruption case studies in volcanology (e.g., Malone 2020; Thompson et al. 2020; Lee et al. 2020; Sayyadi et al. 2021).
Progression in understanding of volcano seismic source processes 1919–2019
Volcano seismology involves both the analysis of seismic signals generated by volcanic processes and the application of seismic techniques to image internal volcanic structure. We focus our review in this section largely on the former (analysis of volcano-seismic signals). However, these objectives are closely related, since the ability to accurately recover seismic source mechanisms depends upon the resolution of the velocity structure of the volcanic edifice and upper crust (e.g., Bean et al. 2008; De Barros et al. 2011; Dawson et al. 2011). For reviews and perspectives on advances in seismic imaging of internal volcanic structure, we refer the reader to Lees (2007), Chouet and Matoza (2013), Saccorotti and Lokmer (2021), Koulakov and Shapiro (2021), and Thelen et al. (2022).
We also limit our primary focus to the progression in understanding over the past hundred years of volcano-tectonic (VT) and long-period (LP) seismicity (0.5–5 Hz), which includes individual transient LP events and more temporally continuous tremor. This choice is made since VLP seismicity was discovered as recently as the 1990s and has already been adequately reviewed by Chouet and Matoza (2013). Recent advances have also been made at the longer ULP time-scales approaching static. A review of ULP signals is also provided by Chouet and Matoza (2013) and these signals have been increasingly amenable to observation and analysis over the past decade. A primary advance for the ULP band has been the development of waveform inversion methods that account for contributions from both translation and tilt in horizontal seismograms through the use of Green’s functions representing the seismometer response to translation and tilt motions (Maeda et al. 2011, 2017; Chouet and Dawson 2015; van Driel et al. 2015; Waite and Lanza 2016; Jolly et al. 2017a). Thus, volcano seismology presently provides quantitative models of the seismic source process related to a variety of volcanic processes over an extremely wide band spanning the LP, VLP, and ULP bands (Maeda et al. 2017; Chouet and Dawson 2015). However, until the advent of broadband seismometry at volcanoes in the 1990s, LP and VT sources were a primary focus of volcano seismology.
Long-period seismicity: LP events and tremor
Long-period (LP, 0.5–5 Hz) seismicity includes individual transient LP events and more continuous tremor (e.g., Kawakatsu et al. 1992; Kaneshima et al. 1996; Narváez et al. 1997; Gil Cruz and Chouet 1997; Neuberg et al. 2000; Aki and Ferrazzini 2000; Saccorotti et al. 2001; Kumagai et al. 2002b; Nakano et al. 2003; Lesage et al. 2006; Waite et al. 2008; Nakamichi et al. 2009; Palo et al. 2009; Alparone et al. 2010; Matoza and Chouet 2010; Buurman and West 2010; D'Auria et al. 2011; Traversa et al. 2011; Arciniega-Ceballos et al. 2012; Rodgers et al. 2013; Matoza et al. 2014a; Unglert et al. 2016; Battaglia et al. 2016a; Lyons et al. 2016; Bell et al. 2017; Frank et al. 2018; Soubestre et al. 2018; Park et al. 2019). The escalation of LP seismicity at shallow depth (< 2 km) in a volcanic edifice is often explained in terms of the pressure-induced disruption of a shallow hydrothermal region, and is one of the most significant indicators of volcanic unrest (e.g., Chouet et al. 1994; Chouet 1996a; Chouet and Matoza 2013). Long-period events are transient signals characterized by a short-lived (∼10 s) broadband onset, followed by a coda of decaying harmonic oscillations lasting from tens of seconds to a few minutes in duration (Chouet 1996a). This is commonly interpreted as a broadband, time-localized pressure excitation mechanism (or trigger mechanism), followed by the response of a fluid-filled resonator (Chouet 1996a). Long-period events are typically associated with volumetric source mechanisms when moment-tensor representations are possible to determine (Chouet and Matoza 2013). Volcanic seismic tremor is a more continuous vibration of the ground with observed durations of minutes to hours, or even weeks to years in some cases (McNutt 1992). Observations of volcanic tremor are multifarious and tremor apparently results from a variety of fluid processes (e.g., McNutt 1992; Konstantinou and Schlindwein 2003; Chouet 1996b). Worldwide observations of volcanic tremor show a wide variability in temporal durations, signal amplitudes, and frequency contents. Accordingly, various terms have been introduced over the years to capture the variety in tremor observations and physical interpretations. These include, but are not limited to, harmonic tremor, monotonic/monochromatic tremor, spasmodic tremor, eruption tremor, banded tremor, and tremor storm (e.g., Seidl et al. 1990; McNutt 1992; Konstantinou and Schlindwein 2003). For example, “eruption tremor” is still commonly used to describe broadband tremor directly associated with sustained explosive eruptions (Scandone and Malone 1985; McNutt and Nishimura 2008).
The classification of seismic signals associated with processes operating in complex natural systems is not straightforward, and these descriptive terms have thus consequently been applied in various ways in the literature, and in some cases have evolved over time. One of the earliest distinctions made by Jaggar, following Omori in the early twentieth century, was that between “spasmodic” tremor (i.e., irregular vibrations) and “harmonic” tremor (i.e., more rhythmic vibrations) (Omori 1908, 1911, 1916; Jaggar 1920). However, since the advent of spectral analyzers and later digital signal processing from the 1970s onwards, the term “harmonic tremor” has evolved to generally imply tremor with sharply peaked spectra (Fig. 9), but the tremor spectral peaks do not always follow a simple harmonic progression (Lesage et al. 2006; Matoza et al. 2010). Whether the spectral character of LP and tremor events is related to a source, path, or site effect (Goldstein and Chouet 1994; Chouet et al. 1997) has been discussed extensively (e.g., Malone 1983; Fehler and Chouet 1982; Bean et al. 2014; Chouet and Dawson 2016). Untangling source, path, and site effects has, however, become progressively more robust with more recent data, for example, from denser broadband seismic networks (e.g., Waite et al. 2008; Chouet and Dawson 2016; Lyons et al. 2016; Matoza et al. 2022a). Clear multi-parameter evidence for source resonance includes infrasound signals recording the same spectral signature as co-located seismic instrumentation but for a different (atmospheric) path (Garcés et al. 1998) (Fig. 8d), video data capturing breathing mode gas oscillations from a vent coincident with a Helmholtz resonance spectral infrasonic signature (Fee et al. 2010c), and the observation of multiple gas eruption jets related to the production of dual overlapping gliding harmonic seismic spectral evolution (Lesage et al. 2006).
Previously, it was already noted from about the 1980s that LP events and tremor have similar spectral properties and are closely temporally related, with for example swarms of individual LP events merging into tremor and back into LP events (e.g., Latter 1979; Fehler 1983; Neuberg et al. 1998, 2000; Powell and Neuberg 2003; Hotovec et al. 2013). This particular type of tremor thus clearly has a common origin with the individual LP events. These observations led to the interpretation that LP events represent the impulse response of a resonant tremor-generating system, and that some types of tremor consist of the superposition of many individual LP events (Latter 1979; Fehler and Chouet 1982; Fehler 1983; Chouet 1985). This type of tremor would probably be classified as “spasmodic” tremor in the original terminology of Jaggar (1920).
We next briefly review the development of quantitative models of long-period events and tremor beginning from the 1950s, and again focusing most on the time since the 1970s.
Volcanic tremor: early quantification
Omer (1950) provided one early quantitative model for the source mechanism of volcanic tremor, attributing tremor observations at Kīlauea (Finch 1949) (Fig. 10a, b) to a path effect: the reverberation of near-surface strata excited into motion by magma moving though subsurface feeding conduits. Shima (1958) and Kubotera (1974) instead proposed that a peaked tremor spectrum at Mount Aso (Sassa 1935) (Fig. 10c) was a result of free oscillations of a spherical magma chamber, while Shimozuru (1961) considered the longitudinal resonance of a cylindrical magma column. Steinberg and Steinberg (1975) attributed tremor to pulsating “flow crises” of gas in volcanic vents undergoing the transition from subsonic to supersonic flow. However, these early models did not adequately quantify the driving force of the fluid or predict the elastic radiation from the source region (Chouet 1981). More critically, these models required implausibly large dimensions for the resonating cavities, as pointed out by Ferrazzini and Aki (1987). For example, Kubotera (1974) determined the source of 3.5–7 s period tremor at Aso (Fig. 10c) to be a resonating spherical magma chamber of 2–4 km radius.
Crack propagation source model of Aki
A rigorous quantitative and (early) computational treatment of volcanic tremor was given by Aki et al. (1977), who proposed a mechanism for volcanic tremor at Kīlauea consisting of the sudden extension of dry and fluid-filled tensile cracks (Fig. 11a). Two scenarios were proposed: (1) the jerky extension and propagation of a single crack; (2) the random jerky openings of narrow channels connecting a chain of pre-existing cracks. This simplified two-dimensional model considered both the driving excitation and crack geometry appropriate for magma transport, but the fluid did not support acoustic waves and merely acted as a passive cushion to the motion of the crack wall. Near-field and far-field displacements computed by finite-difference calculations replicated the general properties of the observed tremor. A key parameter in the formulation of Aki et al. (1977) was the crack stiffness, defined:
where b is the bulk modulus of the fluid in the crack, L is the crack length, μ is the elastic shear modulus, and d is the aperture of crack opening. The single-crack model (scenario 1, above) was rejected because the growing crack length predicted a significant increase in tremor period, inconsistent with the observations at Kīlauea. Aki et al.’s (1977) scenario 2 was further developed for deep tremor occurring at 30–50 km beneath Kīlauea by Aki and Koyanagi (1981). They defined a measure of tremor amplitude related to the magma flux known as reduced displacement:
where A is the peak-to-peak amplitude of ground motion (\(\frac{A}{2\surd 2}= {A}_{\mathrm{r}.\mathrm{m}.\mathrm{s}.}\), the root-mean-square amplitude), and r is the source-to-receiver distance. Measurement of the reduced displacement as a function of time implied a magma flow rate an order of magnitude lower than that implied by field observations of erupted lava effusion rates reported by Swanson (1972). Thus, Aki and Koyanagi (1981) concluded that most magma transport in the lithosphere takes place aseismically, with only particularly strong barriers to flow acting as seismic sources.
Later, Chouet (1981) further developed the crack model of Aki et al. (1977), calculating near-field and surface displacements for a single crack extension while accounting for interaction with the free-surface and near-surface velocity structure. The effects of varying the structure of the elastic media, source depth, and bulk modulus of the fluid in the crack were explored. This model was expanded into three-dimensions and further described in Chouet (1982, 1983). However, these models still assumed no active participation of the fluid. The fluid could not transmit acoustic waves, and the dynamics of the fluid were not considered in detail. Consequently, the spectral peaks obtained by these models were too weak and too broad, and the long duration of observed LP signals could not be reproduced (Chouet 1988).
Fluid resonance models and “crack waves”
The 1980–1986 unrest and eruptions of Mount St. Helens provided new digital observations of LP events and tremor (Fehler and Chouet 1982; Fehler 1983), rejuvenating interest in LP and tremor models in which the fluid plays an active role. Lawrence and Qamar (1979) and Ferrick et al. (1982) proposed a mechanism involving volcanic fluids analogous to the water-hammer effect in a cavity connecting a magma chamber to the surface. This model consisted of resonance of a conduit in response to unsteady flow conditions (i.e., “fluid transients”, resulting from an abrupt disturbance to a fluid system initially at steady state) (Ferrick et al. 1982). These studies were motivated by seismic observations of “icequakes” in glaciers and seismic events originating from a malfunctioning power plant that resembled volcanic LP events.
Chouet (1985) also recognized the importance of the fluid in sustaining resonance, and interpreted individual LP events as the impulse response of a tremor-generating system. Accordingly, he proposed a conceptual system consisting of a “trigger,” a “resonator,” and a “radiator”; in this case, a hemispherical trigger, overlying a cylindrical conduit resonator (with “organ pipe” modes), terminated at the base by a circular radiator (Fig. 11b). Chouet (1985) proposed that the trigger mechanism was the rapid exsolution of gases from the fluid phase during magma ascent, or flashing of a subsurficial layer of phreatic water to steam due to shallow magma intrusion. An LP event thus corresponded to a single triggering of the system, while continuous tremor would result from continuous triggering. Thus, the goal of understanding the complex source mechanism of volcanic tremor was superseded by the more tractable task of understanding individual LP events.
Chouet and Julian (1985) and Chouet (1986, 1988) further developed the crack models initiated by Aki et al. (1977) and Chouet (1981, 1982, 1983), now allowing the fluid to transmit acoustic energy (Fig. 11c). These models were formulated using the equations of elastodynamics in the elastic solid, as well as conservation of momentum and equations of continuity for the fluid. These fluid-filled crack models were applied to non-double couple earthquakes observed near Long Valley Caldera between 1978 and 1983, hydrofracture events used in hydrocarbon extraction (Bame and Fehler 1986), and volcanic LPs and tremor. The most significant feature of these models was the presence of an interface wave propagating through the fluid and reflecting back and forth at the crack tips. The velocity of this “crack wave” is slower than the acoustic velocity of the fluid at all wavelengths, and is inversely dispersive (i.e., velocity decreases as wavelength increases). The properties of the crack wave are analogous to those of tube waves propagating in a fluid-filled borehole (Biot 1952). However, unlike the tube wave, as the wavelength increases to infinity, the velocity of the crack wave approaches zero in inverse proportion to the square root of wavelength (Ferrazzini and Aki 1987). In the short wavelength limit, the crack wave reduces to the Stoneley wave propagating along a fluid–solid interface (Stoneley 1926; Ferrazzini and Aki 1987).
Ferrazzini and Aki (1987) found analytic expressions of the crack waves by considering normal modes in a fluid layer between two homogeneous half-spaces, producing dispersion relations in harmony with the numerical results of Chouet and Julian (1985) and Chouet (1986). These studies showed that “slow waves” or “crack waves” could produce long-period elastic radiation from only a modest-sized resonating cavity. For instance, Kubotera (1974) had previously determined the source of 3.5–7 s period tremor at Mount Aso (Fig. 10c) to be a resonating spherical magma chamber of 2–4 km radius. By considering crack waves, Ferrazzini and Aki (1987) and Chouet (1988) could model this same tremor signal as resulting from a modest-sized magma body 0.5-m thick and 0.5-km long.
Analysis of the radiation properties from the resonating crack by Chouet (1988) demonstrated the stability of the dominant period in the far-field, while the frequency and width of this spectral peak was a strong function of the crack stiffness and trigger amplitude, area, and location. The crack stiffness (Eq. 1) affects the dispersion characteristics and therefore the resonance frequencies of the crack, while the frequency and duration of the signals are also affected by the impedance contrast between solid and fluid:
where ρs and ρf are the density of the elastic solid and fluid, respectively, α is the P-wave velocity of the elastic solid, and a is the sound speed of the fluid in the crack (Chouet 1988). The duration of the LP signal is also related to the viscous damping loss at the fluid–solid boundary:
where η is the viscosity of the fluid and L and d are the crack length and aperture (see Eq. 1) (Chouet 1988). Accordingly, the LP coda contains information on the attenuation properties of fluids in the crack source volume. However, as formulated by Chouet (1988), the crack model accounts for radiation and viscous drag losses only. Intrinsic losses due to dissipation mechanisms within the fluid must be treated separately, and were the focus of follow-up work that examined attenuation in a fluid-filled crack.
Attenuation in volcanic fluid-filled cracks
Attenuation in a fluid-filled crack model (Fig. 11d) was investigated by Kumagai and Chouet (1999, 2000, 2001) and Morrissey and Chouet (2001). The Sompi autoregressive signal analysis method enabled estimates of the quality factor Q of observed LP waveforms (Kumazawa et al. 1990; Nakano et al. 1998). The resultant observed Q is composed of two components:
where \({Q}_{r}^{-1}\) and \({Q}_{i}^{-1}\) are the radiation and intrinsic losses, respectively. The radiation attenuation \({Q}_{r}^{-1}\) is a function of the resonator geometry, as well as the sound speed and density of the fluid, and can be evaluated using the fluid-filled crack model (Kumagai and Chouet 1999, 2000, 2001; Morrissey and Chouet 2001). In contrast, the intrinsic attenuation \({Q}_{i}^{-1}\) corresponds to intrinsic losses in the fluid, for example, viscous, thermal, and acoustic damping. Consequently, calculation of \({Q}_{i}^{-1}\) requires knowledge of the thermodynamic equations of state for multiphase fluids (e.g., Kieffer 1977; Commander and Prosperetti 1989; Temkin and Dobbins 1966).
Kumagai and Chouet (2000, 2001) evaluated \({Q}_{i}^{-1}\) and \({Q}_{r}^{-1}\) for various gas–gas mixtures, ash–gas mixtures, and liquid–gas mixtures. They found that \({Q}_{i}^{-1}\) was negligible compared to \({Q}_{r}^{-1}\) for gas–gas mixtures, but that \({Q}_{i}^{-1}\) could be important, for example, in bubbly liquids and in dusty and misty gases under certain bubble-size and particle-size conditions. Kumagai and Chouet (2000, 2001) also noted that the high observed Q (low attenuation) for long-lasting LP codas observed at several volcanoes could be explained by the high Q values of dusty and misty gases with small (∼1 μm) particles. This highlighted the importance of these fluids (dusty and misty gases) in generating LP events.
Trigger mechanisms of LP seismicity
The utility of the fluid-driven LP source models reviewed above was restricted to a quantification of the crack resonance and properties of the fluids. These numerical and analytic formulations did not address the excitation (trigger) mechanism of the LP events or tremor. For example, in the computational formulation of Chouet (1986), the spatiotemporal properties of the pressure transient triggering the crack resonance are parameterized as kinematic conditions (e.g., an arbitrary step function in pressure applied to a small patch of the crack wall). Quantifying the physics of the trigger or driving mechanism of LP seismicity, including individual LP events (discrete impulse) and tremor (sustained), remains a work in progress. A wide variety of trigger mechanisms have been proposed (Chouet and Matoza 2013; and references therein), including those ultimately arising from self-sustained oscillations (e.g., Julian 1994; Balmforth et al. 2005; Rust et al. 2008; Dunham and Ogden 2012; De Lauro et al. 2011; Lyons et al. 2013; Takeo 2021), magmatic-hydrothermal interactions (e.g., Latter 1981; Havskov et al. 1983; Chouet 1985, 1996a; Leet 1988; Almendros et al. 2001; Kumagai et al. 2002b; Nakano et al. 2003; Nakano and Kumagai 2005; Lin et al. 2005; Ohminato 2006; Petersen and McNutt 2007; Cusano et al. 2008; Waite et al. 2008; Nakamichi et al. 2009; Matoza and Chouet 2010; Alparone et al. 2010; Arciniega-Ceballos et al. 2012; De Lauro et al. 2012; Cannata et al. 2012; Maeda et al. 2013; Jousset et al. 2013; Syahbana et al. 2014; Matoza et al. 2015; Kato et al. 2015; Caudron et al. 2015; Rodgers et al. 2015b; Padrón et al. 2015; Sgattoni et al. 2016; Jolly et al. 2017a; Park et al. 2019; D'Auria et al. 2011, 2019; Dawson and Chouet 2019; Gresse et al. 2021; Butcher et al. 2021), magmatic degassing (e.g., Chouet and Shaw 1991; Kawakatsu et al. 1992; Neuberg et al. 1994; Benoit and McNutt 1997; Gil Cruz and Chouet 1997; Garcés et al. 1998; Hagerty et al. 2000; Ripepe et al. 2001; Falsaperla et al. 2002; Chouet et al. 2003; Rowe et al. 2004; Molina et al. 2004; Ruiz et al. 2006; Lesage et al. 2006; Saccorotti et al. 2007; Patanè et al. 2008; Arciniega-Ceballos et al. 2008; Johnson et al. 2008b; Palo et al. 2009; Buurman and West 2010; Traversa et al. 2011; Davi et al. 2012; Lyons et al. 2016; Battaglia et al. 2016b), and brittle failure of melt (e.g., Webb and Dingwell 1990; Goto 1999; Neuberg et al. 2006; Tuffen et al. 2003; Tuffen and Dingwell 2005; De Angelis and Henton 2011; Thomas and Neuberg 2012). We refer the reader to the work by Chouet and Matoza (2013) for a review of this literature discussing the various proposed mechanisms and the observational and modeling constraints.
Advances in fluid-driven source models
The fundamental significance of solid–fluid interface waves as possible sources of LP seismicity was demonstrated in the work reviewed above. Work since about 2000 has further explored the parameter space of solid–fluid interface waves, including consideration of other source geometries and investigation of the potential for self-sustained oscillation in volcanic fluid transport systems (e.g., Krauklis and Krauklis 1998; Jousset et al. 2003, 2004; Balmforth et al. 2005; Rust et al. 2008; Dunham and Ogden 2012; Lipovsky and Dunham 2015). Some of these studies have referred to the crack wave as the “Krauklis wave” after Krauklis (1962) (e.g., Korneev 2008, 2011; Frehner 2014; Cao et al. 2021). A series of papers by Maeda and Kumagai (2013, 2017), Taguchi et al. (2018, 2021), and Torres et al. (2021) provide empirical formulations and generalized equations for the frequencies and quality factors of crack resonance, enabling more rapid evaluation of source parameters (forward modeling) compared to previous formulations involving a numerical solution based on finite differences (Chouet 1988).
Volcano-tectonic (VT) seismicity
Since 1919, major advances in the understanding of VT earthquakes and their relationship to magmatic processes accompanied improved observations of event rates, locations, focal mechanisms, and magnitudes; as well as the development of the plate tectonics paradigm and corresponding ideas on magma generation. By the middle of the twentieth century, it was recognized that some volcanic earthquakes, termed “ordinary volcanic earthquakes” by Minakami (1950), and ultimately defined as “volcano-tectonic” or VT earthquakes by Lahr et al. (1994), were nearly indistinguishable from tectonic earthquakes in that their waveforms contained high-frequency P and S phases. However, following from earlier ideas linking volcanic earthquakes to tensile failure (Jaggar 1920; Reid 1929) and accumulating observations of “great earthquakes” prior to eruptions (MacGregor 1949), a protracted debate about causality, i.e., whether these earthquakes triggered or were triggered by magmatism, arose during the mid-twentieth century. One camp, speaking from an experimental perspective, supported a “stress release hypothesis” that “ordinary volcanic earthquakes” resulted in pressure decreases of sufficient magnitude to generate melting and magma formation, with magma then ascending along the earthquake fault to erupt (e.g., Yoder 1952; Uffen 1959; Uffen and Jessop 1963). Alternatively, others argued, in line with modern understanding, that melting resulted in volume (and thus pressure) changes which strain the crust to trigger VT earthquakes (e.g., Kuno 1958; Minakami 1960; Matsuzawa 1953). For a review of contemporaneous understanding of whether and how purely tectonic earthquakes may trigger magmatic unrest, which is beyond the scope of this article, we refer the reader to Manga and Brodsky (2006).
Deployments of multiple seismic instruments on active volcanoes, and the consequent possibility of locating VT earthquakes, led to both advances in fundamental understanding of VTs and their use in forecasting. An early example involves the recognition that an (ultimately non-eruptive) 1933–37 Montserrat swarm was shallow (e.g., Perret 1939) and of volcanic origin. Powell (1938) showed that this swarm comprised an elongated cluster of epicenters, which MacGregor (1949) linked to the trend of soufrières (recently active vents) on the island, suggesting that the VT earthquakes were connected to a plane of crustal weakness or deep-seated fracture. Due to the expansion of the HVO seismic network, earthquakes preceding the 1942 eruption of Mauna Loa were observed to migrate towards and along the volcano’s southwest and northeast rift zones, leading to an accurate forecast of an eruption along the volcano’s flanks rather than at its summit. Additional observations of propagating VT earthquakes were made in 1960 at Kīlauea, and at Krafla in 1977, among others. Ultimately, the new observations demonstrating linear elongation of VT clusters and temporal propagation lent support to a hypothesized close spatial relationship between VT earthquakes and migrating magma, culminating in the “mesh hypothesis,” i.e., the idea that VT swarms occur on faults connecting magma-filled tension cracks as proposed by Hill (1977). As the station densities of seismic networks increased, it became possible to detect and locate smaller seismic events, and thus expanding quantities of VT seismicity, more precisely. Toda et al. (2002), for example, documented the locations of over 7000 VT earthquakes, accompanying dike intrusion under the Izu islands, Japan, which propagated to ultimately form an elongated cluster. Later, Ágústsdóttir et al., (2016) described the locations of over 30,000 propagating VT earthquakes accompanying dike intrusion and propagation at Bárðarbunga–Holuhraun, Iceland, in 2014–2015.
The expansion of multi-instrument volcano-seismic networks also allowed calculation of VT earthquake focal mechanisms, ultimately shifting early hypotheses that these earthquakes occurred as tensile failure to a double-couple failure model. An early attempt to distinguish “push/pull” mechanisms on the basis of first motions from a single seismometer was made by Sassa (1936). However, later work by Wada and Sudo (1967), using first motions from five stations recording earthquakes during the 1965–1966 eruption of Aso, Japan, documented mixed first motions for “tectonic-type” earthquakes, suggesting a double-couple component of motion. Additional evidence for a double-couple mechanism, dominated by strike slip and/or normal slip, for VT earthquakes emerged in the 1970s (Fig. 12) (Zobin 1971; Minakami 1974; Filson et al. 1973; Francis 1974; Ward and Gregersen 1973). This led to the development of a theoretical framework for dike mechanics (e.g., Pollard 1987; Rubin 1993, 1995 and references therein) in the 1990s that linked VT earthquakes to stresses induced in the host rock by ascending and/or pressurizing magma. This theoretical framework established a new paradigm that VT earthquakes were not necessarily spatially close to their source magma. This paradigm was enforced by observational evidence that induced stresses controlled VT seismicity (Barker and Malone 1991), and included observations of “distal VT” earthquakes preceding eruptions at Pinatubo in 1991 (Harlow et al. 1996), Mount Spurr in 1992 (Power et al. 1995), and Soufrière Hills and Unzen in 1995 (Umakoshi et al. 2008; Roman et al. 2008). Based on a comparative analysis of distal VT seismicity preceding 111 eruptions at 83 volcanoes, in addition to distal VT swarms preceding intrusions at 21 other volcanoes, White and McCausland (2016) made a case that distal VT seismicity was an important precursor for Earth’s most explosive eruptions. In this regard, they argued that distal VT seismicity preceded all VEI ≥ 5 explosive eruptions that they considered. They additionally argued that pre-eruptive distal VT seismicity originated on tectonic fault structures up to tens of kilometers laterally from the eruption site, rather than directly beneath the eruption site.
Beginning in the early 1990s, more comprehensive VT focal mechanism catalogs (Barker and Malone 1991; Aspinall et al. 1998) began to show that many VT earthquake focal mechanisms had P-axes approximately perpendicular to regional maximum compressive stresses, linking VTs to stresses resulting from compression of the wall rock around a dike. Later work (Roman and Cashman 2006; Roman et al. 2021) demonstrated that this phenomenon corresponded to magmas with high bulk viscosities, and that VTs resulting from emplacement of low-viscosity magmas most likely represented induced stresses ahead of the dike tip rather than in the dike wall rock.
While VT earthquake magnitudes have not received nearly as much attention as their locations and focal mechanisms, several important observations about VT magnitudes have informed understanding of their mechanism and their utility in eruption forecasting. By the 1970s, it had been recognized that magnitudes of VT earthquakes were generally low M < 4 (Zobin 1971; McNutt and Roman 2015), although exceptions have since been found (e.g., Yokoyama 2001; Nishimura et al. 2001; Wauthier et al. 2013). Early examinations of temporal patterns of precursory seismic energy release noted that, while some eruptions take place immediately following a decrease in seismic energy (Minakami 1961; Gorshkov 1960), a general increase in earthquake magnitude and cumulative energy release may be useful for forecasting eruption onset (Tokarev 1963; 1966). Furthermore, concepts from earthquake statistics led to recognition that a VT swarm’s b-value may be abnormally high compared to “tectonic” earthquake sequences, suggesting that increases in fluid pressure in the seismogenic volume around a magma pocket may play a role in driving VT seismicity (e.g., Mogi 1962; Suzuki 1959; Warren and Latham 1970).
Advances in eruption forecasting using seismicity: 1919 to 2022
In this section, we follow recent terminology for the distinction between an eruption “forecast” and “prediction” using seismicity. This is stated by National Academies of Sciences, Engineering, and Medicine (2017) as follows:
“An eruption forecast is a probabilistic assessment of the likelihood and timing of volcanic activity. The forecast may also include information about the expected style of activity, the duration of an eruption, and the degree to which populations and infrastructure will be affected (Sparks 2003). A prediction, in contrast, is a deterministic statement about where, when, and how an eruption will occur, and a prediction will either be correct or incorrect”.
An ideal forecast of volcanic activity includes the location, timing, character, and magnitude of the potential eruption, and a quantitative estimate of the probability of each of these factors. While the potential of instrumental seismology to inform on eruption forecasting was recognized early-on, true forecasts (as opposed to hindcasts), were, and continue to be, limited by sparse and distant instrumentation (Hirn et al. 1987), lack of real-time telemetry, and inability to distinguish “false alarms” (e.g., MacGregor 1949; Macdonald 1954; Shepherd et al. 1971; Savage and Cockerham 1984; Moran et al. 2011). In addition, forecasting was hindered by the related issue of characterizing background seismicity levels (Wood 1974; Decker 1973). For example, the 1949 eruption of Mauna Loa was preceded by an increase in frequency of earthquakes, but the increase was not sufficiently great, or the pattern sufficiently definite, to make possible a forecast of the eruption (Macdonald 1954). Most early eruption forecasts focused on increases in the number of instrumentally detected discrete events, and indicated only that an eruption was likely, with little or no indication of the timing of the anticipated eruption. An early and rare example is of numerous tremor events that were recorded at Merapi Volcano, Indonesia, in January 1930, with an increase in their occurrence to 25 November. These, together with increased fumarole temperatures, were used to forecast the eruption (BNEIVS 1949; Van Padang 1933; Voight et al. 2000).
Forecasts based on seismic unrest became both more diverse, and more accurate, beginning in the 1960s with the advent of conceptual models, such as those of Minakami (1960, 1974) and the landmark recognition that an increase in B-type (Fig. 4) earthquakes could serve as a short-term precursor. As summarized by Girina (2013), after the first seismic station was installed in 1960 (Tokarev 1981) near Bezymianny Volcano, Russia, earthquake classification led to recognition of reliable patterns of seismic activity leading to phases of lava dome growth and explosive eruptions that could be used to forecast changes in the ongoing eruption (Gorelchik 2001) (Fig. 13). Similarly, the occurrence of volcanic tremor was used to formulate successful short-term (up to 7 days in advance) forecasts of eruptions at Ruapehu, New Zealand (Dibble 1969; Clacy 1972). A notable success occurred at Tolbachik, Russia, in 1976, where a dense network of rapidly deployed seismometers allowed forecasting not only of the time but also the location of the eruption approximately one week in advance (Tokarev 1978). The methods for rapid data analysis developed during these responses provided an early basis for the formalization of the Failure Forecast Method (FFM) later applied at Mount St. Helens in the 1980s (Voight 1988). Additional notable successes in short-term forecasting during these decades also occurred in Iceland at Heimaey in 1973 (Björnsson and Einarsson 1974) and Krafla in 1974 (Einarsson 2018).
Following these efforts between 1960 and 1980, a series of challenges and successes in seismicity-based eruption forecasting continued through the 1980s and 1990s. For example, the start of the 1980–1986 eruption of Mount St. Helens, USA, was successfully forecasted based on earthquakes that began approximately 2 months prior to the major explosive eruption on May 18, 1980 (Endo et al. 1981). Forecasts of subsequent eruptions at Mount St. Helens, based on seismic energy release in combination with observations of tilt and dome expansion, became increasingly precise through the end of the eruptive phase in 1986 (e.g., Swanson et al. 1985; Malone et al. 1981, 1983). In Hawai‘i, an eruption forecast for Mauna Loa, based on 2 years of increased seismicity and deformation, was published in 1983 and was qualitatively correct regarding the timing of the next eruption (Decker et al. 1995). In contrast, although preceded by a detected increase in seismicity almost a year before its cataclysmic eruption in November 1985, Nevado del Ruiz, Colombia ultimately presented a complex situation that resulted in substantial issues with false alarms and communication of warnings (Voight 1996). An eruption at Redoubt Volcano, Alaska, beginning in 1989 led to the formalization of the Real-Time Seismic Amplitude Measurement (RSAM) and Spectral Seismic Amplitude Measurement (SSAM) approaches, which allowed rapid characterization of seismicity levels in multiple frequency bands for forecasting (Endo and Murray 1991; Stephens et al. 1994). RSAM and SSAM soon proved to be critical tools for seismic-based forecasting, as during the 1991 eruption of Pinatubo, Philippines (Pinatubo Volcano Observatory Team 1991; Cornelius and Voight 1994; Power et al. 1994). Regardless of these decades of progress, eruption forecasting based on seismicity continues to be a challenge, particularly for smaller eruptions (Cameron et al. 2018), phreatic eruptions (Roman et al. 2019; Kilgour et al. 2021), and occasional larger eruptions that appear to be preceded only by short and subtle seismic precursors (Johnson et al. 2010).
Volcano infrasound since the 1990s
As reviewed above, volcano acoustics research remained relatively dormant until a significant revival beginning in the 1990s. This revival was facilitated by factors including the availability of new infrasound instrumentation technology and computational capability to perform digital infrasound signal processing and noise discrimination (e.g., Garcés et al. 2003, Matoza et al. 2007; Christie and Campus 2010). Since that time, much progress has been made. The utility of infrasound technology in volcano monitoring is now firmly established, and infrasonic systems are increasingly being implemented as a volcano monitoring tool worldwide. Reviews of various aspects of volcano acoustics are provided in the work by Johnson and Ripepe (2011), Fee and Matoza (2013), Garces et al. (2013), McNutt et al. (2015), Allstadt et al. (2018), Matoza and Fee (2018), Matoza et al. (2019a), Marchetti et al. (2019), Taisne et al. (2019), Ripepe and Marchetti (2019), De Angelis et al. (2019), and Johnson (2019). We here refer the reader to these reviews and do not attempt a comprehensive review of volcano infrasound research since the 1990s, instead limiting the discussion to a highlight of major signals studied and trends in the research progression.
Explosive eruptions are the most obvious volcanic sources producing easily observable high-amplitude infrasound signals. Infrasound signals from explosive eruptions may propagate in the atmosphere over distances of thousands of kilometers under favorable conditions, enabling regional (ranges 15–250 km) and remote (ranges > 250 km) ground-based infrasonic monitoring (e.g., Matoza et al. 2007; Fee et al. 2010a,b; Matoza et al. 2011a; 2018; Ripepe et al. 2018; Lyons et al. 2020). The utility and limitations of infrasound for globally detecting and cataloging Earth’s volcanism is presently under investigation (Dabrowa et al. 2011; Matoza et al. 2017; de Negri et al. 2022). We refer the reader to reviews by Matoza et al. (2019a) and Taisne et al. (2019) for discussions on progress and outstanding challenges in developing global eruption notification and acoustic early warning using regional and global infrasound networks for the time covering up to about 2017 (the time of writing of those reviews).
Even considering only explosive eruption sources, a wide variety of infrasound signals have been observed (Fig. 14), capturing the underlying variety of physical explosion mechanisms and mass flux source-time functions (Johnson 2003; Matoza et al. 2014b; Fee et al. 2017). These signals range between (1) discrete explosion waves with relatively simple waveforms lasting from several to tens of seconds (Fig. 14a, b) (e.g., Firstov and Kravchenko 1996; Ripepe and Marchetti 2002; Johnson 2003; Marchetti et al. 2009, 2013), and (2) sustained, broadband, infrasonic tremor signals lasting from minutes to hours (Fig. 14e, f) (e.g., Vergniolle and Caplan-Auerbach 2006; Matoza et al. 2009a; Fee et al. 2010b; Caplan-Auerbach et al. 2010). The latter signals (2) resemble an infrasonic form of jet noise from flight vehicles and have thus been termed volcanic jet noise (Matoza et al. 2009a; 2013a; Fee et al. 2013a, b; McKee et al. 2017). Intermediate signal types (Fig. 14c–e) consisting of a short-duration impulsive explosion waveform followed by sustained jetting (of variable duration) are commonly observed and appear to be a characteristic feature and behavior of intermediate-composition (andesitic) low-level explosive volcanism, as well as strombolian eruptions (e.g., Ishihara 1985; Ripepe et al. 1996, 2007; Johnson 2007, Johnson et al. 2008b; Sahetapy-Engel et al. 2008; Marchetti et al. 2009; Yokoo et al. 2013; Lopez et al. 2013; Firstov et al. 2013; Taddeucci et al. 2014).
The acoustics of all of these complex explosive eruption sources are currently being investigated through dedicated field studies (e.g., Jolly et al. 2017b; Iezzi et al. 2019a; Wallace et al. 2020; Taddeucci et al. 2021; Matoza et al. 2022a) and in the laboratory (e.g., Médici et al. 2014; Médici and Waite 2016; Swanson et al. 2018; Peña Fernández et al. 2020), as well as through numerical modeling (e.g., Taddeucci et al. 2014; Cerminara et al. 2016; Brogi et al. 2018; Watson et al. 2021). The effects of, especially near-source, topography and atmospheric propagation on shaping the observed signals are being investigated for a variety of scales from local (< 15 km) to remote (> 250 km) (e.g., Fee and Garces 2007; Matoza et al. 2009b; 2011a; Kim and Lees 2011, 2014; Johnson et al. 2012; Assink et al. 2012, 2013; Fee et al. 2013b; Lacanna and Ripepe 2013; Lacanna et al. 2014; Lonzaga et al. 2015; Ortiz et al. 2018, 2021; Sabatini et al. 2019; Iezzi et al. 2019a,b; Waxler and Assink 2019; Ishii et al. 2020; Martire et al. 2022; Maher et al. 2021). Non-linearity in source and propagation is also being examined in observations and by numerical simulation (Marchetti et al. 2013; Fee et al. 2013a; Maher et al. 2020, 2022; Watson et al. 2021). Complex explosive processes and signals from eruptions in partially water-submerged (marine, or crater lake) settings have been documented (e.g., Green et al. 2013; Lyons et al. 2019; Fee et al. 2020; Park et al. 2021; Rose and Matoza 2021).
As reviewed above, infrasonic source resonance signatures in the long-period band, e.g., infrasonic harmonic tremor (e.g., Sakai et al. 1996; Garces et al. 1998; Lyons et al 2013) and seismo-acoustic expressions of LP events (Yamasato 1998; Johnson et al. 2008b; Matoza et al. 2009b) were noted early and observations of these signals have progressively expanded to cover a range of magma compositions and eruption styles. Effusive eruptions, lava flows, lava flowing in tubes, and convecting lava lakes have been observed to produce near-continuous broadband and/or harmonic infrasound (Garces et al. 2003; Cannata et al. 2009; Matoza et al. 2010; Fee et al. 2010c; Ulivieri et al. 2013; Patrick et al. 2016, 2019; Spina et al. 2017; Valade et al. 2018; Barrière et al. 2018; Lyons et al. 2021) as well as seismicity (Harris et al. 2005; Jones et al. 2006). Eruptions sites at Kīlauea, for example, have produced prodigious broadband and harmonic infrasonic tremor associated with effusive and degassing activity and occasional short-duration explosions (e.g., Garces et al. 2003; Matoza et al. 2010; Fee et al. 2010c; Patrick et al. 2016, 2019; Lyons et al. 2021). Overpressurized degassing (gas puffing) also has its own infrasonic signature (Ripepe et al. 2002, 2007; Harris and Ripepe 2007b). Cavities and gas-filled conduits above degassing magma appear to significantly influence the infrasonic signature (Matoza et al. 2010; Fee et al. 2010c; Goto and Johnson 2011; Richardson et al. 2014; Spina et al. 2015; Johnson et al. 2018). In a series of papers, Buckingham and Garcés (1996), Garcés and McNutt (1997), and Garcés (2000) developed a canonical model, deriving an analytic solution for the upgoing sound field (i.e., the airborne Green’s function) from a resonant magma or gas-filled conduit. In these conduit resonance models (Buckingham and Garcés 1996), the geometrical idealization of the conduit was similar to that of Chouet (1985), with the exception that the “radiator” was then a diaphragm-like motion of the magma surface radiating sound into the atmosphere. This formulation demonstrated that high-frequency (> 50 Hz) acoustic energy is propagated preferentially in a narrow beam of sound vertically above a conduit, while infrasonic frequencies (< 10 Hz) diffract spherically from the conduit opening (vent), partially explaining why these frequencies are more readily recorded with ground-based sensors. The formulation of Garcés (2000) considered the resonant properties of a tube of fluid connected to the atmosphere with arbitrary variable cross-sectional area that may also be moving at high velocity relative to the sound speed of the flow (i.e., at a high Mach number). More recent work by Watson et al. (2019, 2020) has developed an analytic solution for the shallow crater resonance signature. Similarly to Garces (2000), the Watson et al. (2019, 2020) formulation is axisymmetric and permits a variable cross-sectional area with depth.
A variety of surficial mass movements have now been shown to generate infrasound (Allstadt et al. 2018, and references therein). For example, infrasound signals have been documented from lava dome collapse (Green and Neuberg 2005), pyroclastic flows (Yamasato 1997; Ripepe et al. 2009, 2010; Delle Donne et al. 2014), debris avalanches (Toney et al. 2021), rockfalls (Moran et al. 2008c; Johnson and Ronan 2015), lahars (Johnson and Palma 2015), and explosive blowout of gas-charged blocks impacting the ground (Oshima and Maekawa 2001). As reviewed by Allstadt et al., (2018), this represents significant potential in augmenting monitoring capability for hazardous surficial mass movements. However, much more work is required to quantify the seismo-acoustic source mechanisms from these sources (e.g., Moretti et al. 2012; Allstadt 2013; Farin et al. 2019; Coco et al. 2021; Brosch et al. 2021; Toney et al. 2021) and develop signal processing strategies to identify robustly the sometimes low-amplitude signals of surficial mass movements within realistic persistent and variable background noise (Matoza et al. 2013b) including from (but not limited to) background fluvial infrasound from drainages through which lahars may propagate (Sanderson et al. 2021), distant storms (microbaroms) (Landès et al. 2012), and, in coastal locations, surf infrasound (Garcés et al. 2006).
Future trends
In the first section of this review, we provided a brief snapshot of the current state of volcano seismology and acoustics (also termed seismo-acoustics). One hundred years of advances amounts to a vast amount of progress and changes in instrumentation, analysis and inversion methodologies, as well as in our quantitative understanding of seismic and acoustic sources in volcanic systems. Despite this progress, major questions remain regarding source processes, patterns of volcano-seismic unrest, internal volcanic structure, and the relationship between seismic unrest and volcanic processes. We refer the reader to two recent papers by Thelen et al. (2022) and Watson et al. (2022) published in the Bulletin of Volcanology Special Issue, “Looking Backwards and Forwards in Volcanology: A Collection of Perspectives on the Trajectory of a Science”. These two short perspective papers summarize recent progress and look to the future of volcano seismology and acoustics, speculating on advances to come based on current trajectories and trends.
Conclusions
Over the past hundred years, volcano seismology and acoustics have advanced profoundly. By 1919, the basic recognizable components of these fields were already in place, with early instrumental waveform capture of volcanic seismicity and atmospheric pressure waves on seismographs and barographs demonstrating that geophysical monitoring could help track eruption progression and mitigate hazards. Technological advances during the past hundred years have seen the toolkit of volcano seismology advance from smoked paper drum records to robust continuous digital waveform streams, with increasingly sensitive and wider band instrumentation and denser networks capturing new signals and phenomena. The measurement of atmospheric pressure waves (acoustic-gravity waves) from explosive eruptions was a prominent feature of early volcano seismology and volcanology studies through 1919, but advances in volcano seismology rapidly outpaced those in atmospheric acoustics until about the 1990s. Infrasound technology has since become increasingly integrated into volcano-seismic monitoring operations. Regional (15–250 km distance) and remote (at > 250 km) infrasound detection and explosive eruption notification systems are now in operation and undergoing testing and refinement. Computational and quantitative volcano seismological approaches, beginning in the 1970s, have also led to major progressions in understanding of source mechanisms and their relation to volcanic processes. Geophysical monitoring is an essential component of societal resilience to volcanic hazards. Quantitative volcano seismology and acoustics are indispensable for robust volcano monitoring and should continue to provide progressively sharper insights into how volcanoes work.
Postscript: January 2022 eruption of Hunga, Tonga
While this manuscript was in a final editorial stage, the climactic eruption of Hunga volcano, Tonga occurred on 15 January 2022. This event produced atmospheric waves unprecedented in the modern geophysical record and has resulted in exceptional multi-technology observations of rarely captured physical phenomena (e.g., Amores et al. 2022; Astafyeva et al. 2022; Carr et al. 2022; Carvajal et al. 2022; Ern et al. 2022; Harding et al. 2022; Harrison 2022; Kubota et al. 2022; Kulichkov et al. 2022; Lin et al. 2022; Liu et al. 2022; Le et al. 2022; Matoza et al. 2022b; Omira et al. 2022; Otsuka 2022; Poli and Shapiro 2022; Ramírez-Herrera et al. 2022; Saito 2022; Schnepf et al. 2022; Themens et al. 2022; Vergoz et al. 2022; Wright et al. 2022; Yamazaki et al. 2022; Yuen et al. 2022). The prominent Lamb wave was observed propagating around the Earth for the same number of passages (four plus three antipodal) as the historic 1883 Krakatau eruption (Matoza et al. 2022b). As measured by the Lamb wave amplitudes, the Hunga explosion was comparable in size to that of the 1883 Krakatau eruption and over an order of magnitude greater than that of the 1980 Mount St. Helens eruption (Matoza et al. 2022b). As we have reviewed herein, the time from the 1883 eruption of Krakatau (Scott 1883; LeConte 1884; Strachey 1888) to the 2022 eruption of Hunga represents more than a century of remarkable advances in the instrumental recording, technology, analyses, and understanding of seismic and atmospheric waves produced by volcanic eruptions.
References
Agnew DC (2002) History of seismology. In: IASPEI international handbook of earthquake and engineering seismology. Academic Press, San Diego, pp 3–13. https://doi.org/10.1016/s0074-6142(02)80203-0
Ágústsdóttir T, Woods J, Greenfield T, Green RG, White RS, Winder T, Brandsdóttir B, Steinthórsson S, Soosalu H (2016) Strike-slip faulting during the 2014 Bárdarbunga-Holuhraun dike intrusion, central Iceland. Geophys Res Lett 43(4):1495–1503. https://doi.org/10.1002/2015GL067423
Aki K, Koyanagi R (1981) Deep volcanic tremor and magma ascent mechanism under Kilauea, Hawaii. J Geophys Res 86(B8):7095–7109. https://doi.org/10.1029/JB086iB08p07095
Aki K, Fehler M, Das S (1977) Source mechanism of volcanic tremor: fluid driven crack models and their application to the 1963 Kilauea eruption. J Volcanol Geotherm Res 2:259–287. https://doi.org/10.1016/0377-0273(77)90003-8
Aki K, Chouet B, Fehler M, Zandt G, Koyanagi R, Colp J, Hay RG (1978) Seismic properties of a shallow magma reservoir in Kilauea Iki by active and passive experiments. J Geophys Res 83:2273–2282. https://doi.org/10.1029/JB083iB05p02273
Aki K, Ferrazzini V (2000) Seismic monitoring and modeling of an active volcano for prediction. J Geophys Res 105( B7):16617–16640, https://doi.org/10.1029/2000JB900033
Aki K (1992) "State of the art in volcanic seismology." Volcanic Seismology, 3–10
Alcaraz A, Abad LF, Quema JC (1952) Hibok-Hibok volcano, Philippines Islands, and its activity since 1948. The Volcano Letter 516:1–6
Allstadt K (2013) Extracting source characteristics and dynamics of the August 2010 Mount Meager landslide from broadband seismograms. J Geophys Res Earth Surf 118(3):1472–1490
Allstadt KE, Matoza RS, Lockhart AB, Moran S, Caplan-Auerbach J, Haney MM, Thelen W, Malone SD (2018) Seismic and acoustic signatures of surficial mass movements at volcanoes. J Volcanol Geotherm Res 364:76–106. https://doi.org/10.1016/j.jvolgeores.2018.09.007
Almendros J, Chouet B, Dawson P (2001) Spatial extent of a hydrothermal system at Kilauea Volcano, Hawaii, determined from array analyses of shallow long-period seismicity 2. Results. J Geophys Res 106:13581–13597
Alparone S, Cannata A, Gambino S, Gresta S, Milluzzo V, Montalto P (2010) Time-space variation of volcano-seismic events at La Fossa (Vulcano, Aeolian Islands, Italy): new insights into seismic sources in a hydrothermal system. Bull Volcanol 72:803–816
Alvarado A, Ruiz M, Mothes P, Yepes H, Segovia M, Vaca M, Ramos C, Enríquez W, Ponce G, Jarrín P, Aguilar J, Acero W, Vaca S, Singaucho JC, Pacheco D, Córdova A (2018) Seismic, volcanic, and geodetic networks in Ecuador: building capacity for monitoring and research. Seismol Res Lett 89(2A):432–439. https://doi.org/10.1785/0220170229
Alvizuri CR, Matoza RS, Okubo PG (2021) Earthquake collapse mechanisms and periodic, migrating seismicity during the 2018 summit collapse at Kilauea caldera. Earth Planet Sci Lett 562:116819. https://doi.org/10.1016/j.epsl.2021.116819
Ammon CJ, Velasco AA, Lay T, Wallace TC (2020) Foundations of modern global seismology. Academic Press
Amores A, Monserrat S, Marcos M, Argüeso D, Villalonga J, Jordà G, Gomis D (2022) Numerical simulation of atmospheric Lamb waves generated by the 2022 Hunga‐Tonga Volcanic Eruption. Geophys Res Lett 49(6), e2022GL098240
Anderson K, Lisowski M, Segall P (2010) Cyclic ground tilt associated with the 2004–2008 eruption of Mount St. Helens. J Geophys Res 115:B11201, https://doi.org/10.1029/2009JB007102
Anderson T, Flett JS (1903) Report on the eruptions of the Soufrière, in St. Vincent, in 1902, and on a visit to Montagne Pelée, in Martinique - Part I. Phil Trans Royal Soc Lon A 200:353–553
Apple RA (1987) Thomas A. Jaggar, Jr., and the Hawaiian Volcano Observatory. In: Decker RW, Wright TL, Stauffer PH (eds), Volcanism in Hawaii. US Geol Surv Prof Pap 1350(2), pp 1619–1644. https://doi.org/10.1016/0198-0254(87)91119-8
Arciniega-Ceballos A, Chouet BA, Dawson P (1999) Very-long-period signals associated with Vulcanian explosions at Popocatepetl Volcano, Mexico. Geophys Res Lett 26:3013–3016. https://doi.org/10.1029/1999GL005390
Arciniega-Ceballos A, Chouet B, Dawson P, Asch G (2008) Broadband seismic measurements of degassing activity associated with lava effusion at Popocatépetl Volcano, Mexico. J Volcanol Geoth Res 170:12–23
Arciniega-Ceballos A, Dawson P, Chouet BA (2012) Long-period seismic source characterization at Popocatépetl Volcano, Mexico. Geophys Res Lett 39(2012):L20307. https://doi.org/10.1029/2012GL053494
Arciniega-Ceballos A, Alatorre-Ibargüengoitia M, Scheu B, Dingwell DB (2015) Analysis of source characteristics of experimental gas burst and fragmentation explosions generated by rapid decompression of volcanic rocks. J Geophys Res 120:5104–5116. https://doi.org/10.1002/2014JB011810
Arrowsmith SJ, Johnson JB, Drob DP, Hedlin MA (2010) The seismoacoustic wavefield: A new paradigm in studying geophysical phenomena. Rev Geophys 48(4). https://doi.org/10.1029/2010RG000335
Arrowsmith S, Euler G, Marcillo O, Blom P, Whitaker R, Randall G (2015) Development of a robust and automated infrasound event catalogue using the International Monitoring System. Geophys J Int 200(3):1411–1422. https://doi.org/10.1093/gji/ggu486
Aspinall WP, Miller AD, Lynch LL, Latchman JL, Stewart RC, White RA, Power JA (1998) Soufrière Hills eruption, Montserrat, 1995–1997: volcanic earthquake locations and fault plane solutions. Geophys Res Lett 25(18):3397–3400. https://doi.org/10.1029/98GL00858
Assink JD, Waxler R, Drob D (2012) On the sensitivity of infrasonic traveltimes in the equatorial region to the atmospheric tides. J Geophys Res Atmospheres 117:D01110. https://doi.org/10.1029/2011JD016107
Assink JD, Waxler R, Frazier WG, Lonzaga J (2013) The estimation of upper atmospheric wind model updates from infrasound data. J Geophys Res: Atmospheres 118(19):10–707
Astafyeva E, Maletckii B, Mikesell TD, Munaibari E, Ravanelli M, Coïsson P, Manta F. Rolland L (2022) The 15 January 2022 Hunga Tonga eruption history as inferred from ionospheric observations. Geophys Res Lett, p.e2022GL098827
Aster R, MacIntosh W, Kyle P, Esser R, Bartel B, Dunbar N, Johnson J, Karstens R, Kurnik C, McGowan M, McNamara S (2004) Real-time data received from Mount Erebus volcano, Antarctica. EOS Trans Am Geophys Union 85(10):97–101
Aster R, Beaudoin B, Hole J, Fouch M, Fowler J, James D (2005) IRIS Seismology Program marks 20 years of discovery. EOS Trans Am Geophys Union 86(17):171–172
Balmforth NJ, Craster RV, Rust AC (2005) Instability in flow through elastic conduits and volcanic tremor. J Fluid Mech 527:353–377. https://doi.org/10.1017/S0022112004002800
Bame D, Fehler M (1986) Observations of long period earthquakes accompanying hydraulic fracturing. Geophys Res Lett 13:149–152. https://doi.org/10.1029/GL013i002p00149
Barker SE, Malone SD (1991) Magmatic system geometry at Mount St. Helens modeled from the stress field associated with posteruptive earthquakes. J Geophys Res 96(B7): 11883–11894. https://doi.org/10.1029/91JB00430
Barrientos S, National Seismological Center (CSN) Team (2018) The Seismic Network of Chile. Seismolo Res Lett 89(2A):467-474https://doi.org/10.1785/0220160195
Barrière J, Nicolas d'Oreye, Adrien Oth, Halldor Geirsson, Niche Mashagiro, Jeffrey B. Johnson, Benoît Smets, Sergey Samsonov, and François Kervyn (2018) Single-station seismo-acoustic monitoring of Nyiragongo's lava lake activity (DR Congo). Front Earth Sci 82.
Battaglia J, Métaxian JP, Garaebiti E (2016a) Families of similar events and modes of oscillation of the conduit at Yasur volcano (Vanuatu). J Volcanol Geoth Res 322:196–211
Battaglia J, Métaxian JP, Garaebiti E (2016b) Short term precursors of strombolian explosions at Yasur volcano (Vanuatu). Geophys Res Lett 43(5):1960–1965. Chicago
Bautista MLP, Bautista BC (2004) The Philippine historical earthquake catalog: its development, current state and future directions. Annal Geophys 47: 2/3. https://doi.org/10.4401/ag-3307
Bean CJ, De Barros L, Lokmer I, Métaxian JP, O’Brien G, Murphy S (2014) Long-period seismicity in the shallow volcanic edifice formed from slow-rupture earthquakes. Nature Geosci 7(1):71–75. https://doi.org/10.1038/ngeo2027
Bean C, Lokmer I, O'Brien G (2008) Influence of near‐surface volcanic structure on long‐period seismic signals and on moment tensor inversions: simulated examples from Mount Etna. J Geophys Res 113(B8). https://doi.org/10.1029/2007JB005468
Bedard AJ, Georges TM (2000) Atmospheric infrasound. Phys Today 53(3):32–37. https://doi.org/10.1063/1.883019
Bell AF, Hernandez S, Gaunt HE, Mothes P, Ruiz M, Sierra D, Aguaiza S (2017) The rise and fall of periodic ‘drumbeat’ seismicity at Tungurahua volcano, Ecuador. Earth Planet Sci Lett 475:58–70
Bell AF, La Femina PC, Ruiz M, Amelung F, Bagnardi M, Bean CJ, Bernard B, Ebinger C, Gleeson M, Grannell J, Hernandez S, Higgins M, Liorzou C, Lundgren P, Meier N, Molloff M, Oliva S-J, Ruiz AG, Stock MJ (2021) Caldera resurgence during the 2018 eruption of Sierra Negra volcano, Galápagos Islands. Nature Comm 12:1397. https://doi.org/10.1038/s41467-021-21596-4
Benítez C, Ramírez J, Segura JC, Rubio A, Ibañez JM, Almendros J, García-Yeguas A, Cortés G (2007) Continuous HMM-based seismic event classification at Deception Island. Antarctica IEEE Trans Geosci Remotesens 45(1):138–147
Ben-Menahem A (1995) A concise history of mainstream seismology: origins, legacy, and perspectives. Bull Seismol Soc Am 85(4):1202–1225. https://doi.org/10.1785/BSSA0850041202
Benoit JP, Mcnutt SR (1997) New constraints on source processes of volcanic tremor at Arenal Volcano, Costa Rica, using broadband seismic data. Geophys Res Lett 24(4):449–452
Biot MA (1952) Propagation of elastic waves in a cylindrical bore containing a fluid. J Appl Phys 23:997–1005. https://doi.org/10.1063/1.1702365
Björnsson S, Einarsson P (1974) Seismicity of Iceland. In: Geodynamics of Iceland and the North Atlantic area. Springer, Dordrecht, pp 225–239. https://doi.org/10.1007/978-94-010-2271-2_16
BNEIVS, Bull. Netherlands East Indian Volcanol. Surv., 1927–1935, no.1–72; also Bull. Netherlands Indies Volcanol. Surv., 1935–1940, no. 73–94, 1941 (pub. 1949) no. 95–98.
Bogiatzis P, Ishii M (2016) Digitseis: a new digitization software for analog seismograms. Seismol Res Lett 87(3):726–736
Borgstrom S, De Lucia M, Nave R (1999) Luigi Palmieri: first scientific bases for geophysical surveillance in Mt. Vesuvius area. Annal Geophys 42(3). https://doi.org/10.4401/ag-3741
Boschi E, Giardini D, Morelli A (1991) MedNet: the very broad-band seismic network for the Mediterranean. Il Nuovo Cimento C 14:79–99. https://doi.org/10.1007/BF02509260
Braun T, Ripepe M (1993) Interaction of seismic and air waves as recorded at Stromboli volcano. Geophys Res Lett 20:65–68. https://doi.org/10.1029/92GL02543
Brenner JC (1911) The seismologic service of Chile. Bull Seismol Soc Am 1:25–26. https://doi.org/10.1785/BSSA0010010025B
Bretherton FP (1969) Lamb waves in a nearly isothermal atmosphere. Q J R Meteorol Soc 95(406):754–757
Brogi F, Ripepe M, Bonadonna C (2018) Lattice Boltzmann modeling to explain volcano acoustic source. Sci Rep 8(1):1–8. https://doi.org/10.1038/s41598-018-27387-0
Brosch E, Lube G, Cerminara M, Esposti-Ongaro T, Breard EC, Dufek J, Sovilla B, Fullard L (2021) Destructiveness of pyroclastic surges controlled by turbulent fluctuations. Nat Commun 12(1):1–12
Buckingham MJ, Garcés MA (1996) Canonical model of volcano acoustics. J Geophys Res 101(B4):8129–8151. https://doi.org/10.1029/95JB01680
Busby RW, Aderhold K (2020) The Alaska transportable array: as built. Seismological Society of America 91(6):3017–3027
Busby RW, Woodward RL, Hafner KA, Vernon FL, Frassetto AM (2018) The design and implementation of EarthScope's USArray Transportable Array in the Conterminous United States and Southern Canada. http://www.usarray.org/researchers/obs/transportable/l48_ta_report. Accessed 21 March 2022
Butcher S, Bell AF, Hernandez S, Ruiz M (2021) Evolution of seismicity during a stalled episode of reawakening at Cayambe Volcano, Ecuador. Front Earth Sci 9:464
Buurman H, West ME (2010) Seismic precursors to volcanic explosions during the 2006 eruption of Augustine Volcano (2010), in J.A. Power, M.L. Coombs, J.T. Freymueller (Eds.), The 2006 Eruption of Augustine Volcano, Alaska, U.S. Geological Survey Prof. Pap. 1769, pp. 41–57 (Ch. 2)
Cameron CE, Prejean SG, Coombs ML, Wallace KL, Power JA, Roman DC (2018) Alaska volcano observatory alert and forecasting timeliness: 1989–2017. Front Ear Sci 6:86. https://doi.org/10.3389/feart.2018.00086
Campus P, Christie DR (2010) Worldwide observations of infrasonic waves. In Infrasound monitoring for atmospheric studies (pp. 185–234). Springer, Dordrecht
Cannata A, Diliberto IS, Alparone S et al (2012) Multiparametric approach in investigating volcano-hydrothermal systems: the case study of Vulcano (Aeolian Islands, Italy). Pure Appl Geophys 169:167–182. https://doi.org/10.1007/s00024-011-0297-z
Cannata A, Montalto P, Privitera E, Russo G, Gresta S (2009) Tracking eruptive phenomena by infrasound: May 13, 2008 eruption at Mt. Etna. Geophys Res Lett 36(5)
Cao H, Nakagawa S, Askari R (2021) Laboratory measurements of the impact of fracture and fluid properties on the propagation of Krauklis waves. J Geophys Res 126: e2020JB021593. https://doi.org/10.1029/2020JB021593
Caplan-Auerbach J, Bellesiles A, Fernandes JK (2010) Estimates of eruption velocity and plume height from infrasonic recordings of the 2006 eruption of Augustine Volcano, Alaska. J Volcanol Geoth Res 189(1):12–18. https://doi.org/10.1016/j.jvolgeores.2009.10.002
Caplan-Auerbach J, Dziak RP, Haxel J, Bohnenstiehl DR, Garcia C (2017) Explosive processes during the 2015 eruption of Axial Seamount, as recorded by seafloor hydrophones. Geochem Geophys Geosys 18(4):1761–1774. https://doi.org/10.1002/2016GC006734
Caplan-Auerbach J, Duennebier F (2001) Seismic and acoustic signals detected at Lo'ihi Seamount by the Hawai'i Undersea Geo-Observatory. Geochemistry, Geophysics, Geosystems, 2(5).
Carn SA, Fioletov VE, McLinden CA, Li C, Krotkov NA (2017) A decade of global volcanic SO2 emissions measured from space. Sci Rep 7(1):1–12
Carniel R, Guzmán SR (2021) Machine learning in volcanology: a review. In: Nemeth K (ed) Updates in volcanology - transdisciplinary nature of volcano science. IntechOpen. https://doi.org/10.5772/intechopen.94217
Carr JL, Horváth Á, Wu DL, Friberg MD (2022) Stereo plume height and motion retrievals for the record-setting Hunga Tonga-Hunga Ha'apai eruption of 15 January 2022. Geophys Res Lett 49:e2022GL098131. https://doi.org/10.1029/2022GL098131
Carvajal M, Sepúlveda I, Gubler A, Garreaud R (2022) Worldwide signature of the 2022 Tonga volcanic tsunami. Geophys Res Lett 49(6), e2022GL098153
Cas RA (2022) The centenary of IAVCEI 1919–2019 and beyond: origins and evolution of the International Association of Volcanology and Chemistry of the Earth’s Interior. Bull Volcanol 84:15. https://doi.org/10.1007/s00445-021-01509-5
Castellano M, Buonocunto C, Capello M, La Rocca M (2002) Seismic surveillance of active volcanoes: the Osservatorio Vesuviano Seismic Network (OVSN, southern Italy). Seismol Res Lett 73(2):177–184. https://doi.org/10.1785/gssrl.73.2.177
Caudron C, Lecocq T, Syahbana DK, McCausland W, Watlet A, Camelbeeck T, Bernard A (2015) Stress and mass changes at a “wet” volcano: example during the 2011–2012 volcanic unrest at Kawah Ijen volcano (Indonesia). J Geophys Res: Solid Earth 120(7):5117–5134
Ceranna L, Matoza R, Hupe P, Le Pichon A, Landès M (2019) Systematic array processing of a decade of global IMS infrasound data, in "Infrasound monitoring for atmospheric studies: challenges in middle-atmosphere dynamics and societal benefits", ed. A. Le Pichon, E. Blanc, and A. Hauchecorne, Ch 13, pp 471–482, Springer, Cham, https://doi.org/10.1007/978-3-319-75140-5_13, ISBN:978–3–319–75140–5
Cerminara M, Ongaro TE, Neri A (2016) Large eddy simulation of gas–particle kinematic decoupling and turbulent entrainment in volcanic plumes. J Volcanol Geotherm Res 326:143–171. https://doi.org/10.1016/j.jvolgeores.2016.06.018
Chadwick WW, Cashman KV, Embley RW, Matsumoto H, Dziak RP, de Ronde CEJ, Lau TK, Deardorff ND, Merle SG (2008) Direct video and hydrophone observations of submarine explosive eruptions at NW Rota-1 volcano, Mariana Arc. J Geophys Res 113(8):1–23. https://doi.org/10.1029/2007JB005215
Chadwick WW, Dziak RP, Haxel JH, Embley RW, Matsumoto H (2012) Submarine landslide triggered by volcanic eruption recorded by in situ hydrophone. Geology 40(1):51–54. https://doi.org/10.1130/G32495.1
Chouet B (1979) Sources of seismic events in the cooling lava lake of Kilauea Iki, Hawaii. J Geophys Res 84:2315–2330. https://doi.org/10.1029/JB084iB05p02315
Chouet B (1981) Ground motion in the near field of a fluid-driven crack and its interpretation in the study of shallow volcanic tremor. J Geophys Res 86(B7):5985–6016. https://doi.org/10.1029/JB086iB07p05985
Chouet B (1982) Free surface displacements in the near field of a tensile crack expanding in three dimensions. J Geophys Res 87:3868–3872. https://doi.org/10.1029/JB087iB05p03868
Chouet B (1983) Ground motion near an expanding preexisting crack. J Volcanol Geotherm Res 19:367–379. https://doi.org/10.1016/0377-0273(83)90119-1
Chouet B (1985) Excitation of a buried magmatic pipe: a seismic source model for volcanic tremor. J Geophys Res 90:1881–1893. https://doi.org/10.1029/JB090iB02p01881
Chouet B (1986) Dynamics of a fluid-driven crack in three dimensions by the finite difference method. J Geophys Res 91:13967–13992. https://doi.org/10.1029/JB091iB14p13967
Chouet B (1988) Resonance of a fluid-driven crack: radiation properties and implications for the source of long-period events and harmonic tremor. J Geophys Res 93:4375–4400. https://doi.org/10.1029/JB093iB05p04375
Chouet BA (1996a) Long-period volcano seismicity: its source and use in eruption forecasting. Nature 380:309–316. https://doi.org/10.1038/380309a0
Chouet B (2003) Volcano seismology. Pure Appl Geophys 160:739–788. https://doi.org/10.1007/PL00012556
Chouet B, Dawson P (2011) Shallow conduit system at Kilauea Volcano, Hawaii, revealed by seismic signals associated with degassing bursts. J Geophys Res 116:B12317. https://doi.org/10.1029/2011JB008677
Chouet B, Dawson P (2015) Seismic source dynamics of gas-piston activity at Kilauea Volcano, Hawai’i. J Geophys Res 120(4):2525–2560. https://doi.org/10.1002/2014JB011789
Chouet BA, Dawson PB (2016) Origin of the pulse-like signature of shallow long-period volcano seismicity. J Geophys Res 121(8):5931–5941. https://doi.org/10.1002/2016JB013152
Chouet B, Julian BR (1985) Dynamics of an expanding fluid-filled crack. J Geophys Res 90:11187–11198. https://doi.org/10.1029/JB090iB13p11187
Chouet BA, Matoza RS (2013) A multi-decadal view of seismic methods for detecting precursors of magma movement and eruption. J Volcanol Geotherm Res 252:108–175. https://doi.org/10.1016/j.jvolgeores.2012.11.013
Chouet B, Shaw HR (1991) Fractal properties of tremor and gas piston events observed at Kilauea Volcano, Hawaii. J Geophys Res 96(B6):10177–10189
Chouet BA, Page RA, Stephens CD, Lahr JC, Power JA (1994) Precursory swarms of long-period events at Redoubt Volcano (1989–1990), Alaska: their origin and use as a forecasting tool. J Volcanol Geotherm Res 62:95–135. https://doi.org/10.1016/0377-0273(94)90030-2
Chouet B, Saccorotti G, Martini M, Dawson P, De Luca G, Milana G, Scarpa R (1997) Source and path effects in the wave fields of tremor and explosions at Stromboli Volcano, Italy. J Geophys Res 102(B7):15129–15150. https://doi.org/10.1029/97JB00953
Chouet B, Dawson P, Ohminato T, Martini M, Saccorotti G, Giudicepietro F, Luca GD, Milana G, Scarpa R (2003) Source mechanisms of explosions at Stromboli Volcano, Italy, determined from moment tensor inversions of very-long-period data. J Geophys Res 108:2019. https://doi.org/10.1029/2002JB001919
Chouet B, Dawson P, Arciniega-Ceballos A (2005) Source mechanism of Vulcanian degassing at Popocatepetl Volcano, Mexico, determined from waveform inversions of very long period signals. J Geophys Res 110:B070301. https://doi.org/10.1029/2004JB003524
Chouet B (1976) Source, scattering and attenuation effects on high frequency seismic waves. Dissertation, Massachusetts Institute of Technology.
Chouet B (1992) A seismic model for the source of long-period events and harmonic tremor. In: Gasparini P, Scarpa R, Aki K (Eds) Volcanic Seismology. Springer-Verlag, Berlin, pp. 133–156. https://doi.org/10.1007/978-3-642-77008-1_11
Chouet BA (1996b) New methods and future trends in seismological volcano monitoring. In: Scarpa R, Tilling RI (Eds) Monitoring and mitigation of volcano hazards. Springer-Verlag, New York, pp 23–97. https://doi.org/10.1007/978-3-642-80087-0_2
Christie D, Campus P (2010) The IMS infrasound network: design and establishment of infrasound stations. In: Pichon AL, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. chap. 2. Springer, Netherlands, pp 29–75
Clacy GRT (1972) Analysis of seismic events recorded with a slow motion tape recorder near Chateau Tongariro, New Zealand during February 18, 1966 to December 31, 1966. Bull Volcanol 36(1):20–28. https://doi.org/10.1007/BF02596980
Coco M, Marchetti E, Morandi O (2021) Numerical modeling of infrasound energy radiation by debris flow events. Pure Appl Geophys 178:1–13. https://doi.org/10.1007/s00024-021-02759-2
Commander KW, Prosperetti A (1989) Linear pressure waves in bubbly liquids: comparison between theory and experiments. J Acoustic Soc Am 85:732–746. https://doi.org/10.1121/1.397599
Cooley JW, Lewis PAW, Welch PD (1969) The fast Fourier transform and its applications. IEEE Trans Education 12(1):27–34. https://doi.org/10.1109/TE.1969.4320436
Cooley JW, Tukey JW (1965) An algorithm for the machine calculation of complex Fourier series. Math Computation 19(90):297–301. https://doi.org/10.2307/2003354
Coombs ML, Wech AG, Haney MM, Lyons JL, Schneider DJ, Schwaiger HF, Wallace KL, Fee D, Freymueller JT, Schaefer JR et al (2018) Short-term forecasting and detection of explosions during the 2016–2017 eruption of Bogoslof Volcano, Alaska. Front Earth Sci 6. https://doi.org/10.3389/feart.2018.00122
Cornelius RR, Voight B (1994) Seismological aspects of the 1989–1990 eruption at Redoubt Volcano, Alaska: The Materials Failure Forecast Method (FFM) with RSAM and SSAM seismic data. J Volcanol Geotherm Res 62(1–4):469–498. https://doi.org/10.1016/0377-0273(94)90048-5
Cusano P, Petrosino S, Saccorotti G (2008) Hydrothermal origin for sustained long-period (LP) activity at Campi Flegrei Volcanic Complex, Italy. J Volcanol Geoth Res 177(4):1035–1044
Dabrowa AL, Green DN, Rust AC, Phillips JC (2011) A global study of volcanic infrasound characteristics and the potential for long-range monitoring. Earth Planet Sci Lett 310:369–379. https://doi.org/10.1016/j.epsl.2011.08.027
D’Auria L, Giudicepietro F, Aquino I, Borriello G, Del Gaudio C, Lo Bascio D, Martini M, Ricciardi GP, Ricciolino P, Ricco C (2011) Repeated fluid-transfer episodes as a mechanism for the recent dynamics of Campi Flegrei caldera (1989–2010). J Geophys Res 116:B04313. https://doi.org/10.1029/2010JB007837
D’Auria L, Barrancos J, Padilla GD, Pérez NM, Hernández PA, Melián G, Padrón E, Asensio-Ramos M, García-Hernández R (2019) The 2016 Tenerife (Canary Islands) long-period seismic swarm. J Geophys Res: Solid Earth 124(8):8739–8752
Davi R, O’Brien GS, De Barros L, Lokmer I, Bean CJ, Lesage P, Mora MM, Soto GJ (2012) Seismic source mechanisms of tremor recorded on Arenal volcano, Costa Rica, retrieved by waveform inversion. J Volcanol Geoth Res 213–214:1–13
Davison C (1924) Fusakichi Omori and his work on earthquakes. Bull Seismol Soc Am 14(4):240–255. https://doi.org/10.1785/BSSA0140040240
Dawson P, Chouet B (2019) Long period seismicity at Mammoth Mountain, California. J Geophys Res: Solid Earth 124:6751–6778. https://doi.org/10.1029/2019JB017580
Dawson PB, Benítez MC, Chouet BA, Wilson D, Okubo PG (2010) Monitoring very-long-period seismicity at Kilauea Volcano, Hawaii. Geophys Res Lett 37:L18306. https://doi.org/10.1029/2010GL044418
Dawson PB, Chouet BA, Power J (2011) Determining the seismic source mechanism and location for an explosive eruption with limited observational data: Augustine Volcano. Alaska Geophys Res Lett 38:L0330. https://doi.org/10.1029/2010GL045977
Dawson PB, Benítez MC, Lowenstern JB, Chouet BA (2012) Identifying bubble collapse in a hydrothermal system using hidden Markov models. Geophys Res Lett 39:L01304. https://doi.org/10.1029/2011GL049901
Dawson PB, Dietel C, Chouet BA, Honma K, Ohminato T, Okubo P (1998) A digitally telemetered broadband seismic network at Kilauea Volcano, Hawaii US Geol Surv Open-File Rep 98–108 https://doi.org/10.3133/ofr98108
De Angelis S, Henton SM (2011) On the feasibility of magma fracture within volcanic conduits: constraints from earthquake data and empirical modeling of magma viscosity. Geophys Res Lett 38:L19310. https://doi.org/10.1029/2011GL049297
De Angelis S, Fee D, Haney M, Schneider D (2012) Detecting hidden volcanic explosions from Mt. Cleveland Volcano, Alaska with infrasound and ground-coupled airwaves. Geophys Res Lett 39: L21312. https://doi.org/10.1029/2012GL053635
De Angelis S, Diaz-Moreno A, Zuccarello L (2019) Recent developments and applications of acoustic infrasound to monitor volcanic emissions. Remote Sensing 11(11):1302. https://doi.org/10.3390/rs11111302
De Barros L, Lokmer I, Bean CJ, O’Brien GS, Saccorotti G, Métaxian J-P, Zuccarello L, Patanè D (2011) Source mechanism of long-period events recorded by a high-density seismic network during the 2008 eruption on Mount Etna. J Geophys Res 116:B01304. https://doi.org/10.1029/2010JB007629
De Cesare W, Orazi M, Peluso R, Scarpato G, Caputo A, D’Auria L, Giudicepietro F, Martini M, Buonocunto C, Capello M, Esposito AM (2009) The broadband seismic network of Stromboli volcano, Italy. Seismol Res Lett 80(3):435–439. https://doi.org/10.1785/gssrl.80.3.435
de Jong Boers BB (1995) Mount Tambora in 1815: a volcanic eruption in Indonesia and its aftermath. Indonesia 60:37–60. https://doi.org/10.2307/3351140
De la Cruz-Reyna S, Siebe C (1997) The giant Popocatépetl stirs. Nature 388:227. https://doi.org/10.1038/40749
De Lauro E, De Martino S, Falanga M, Palo M (2011) Self-sustained vibrations in volcanic areas extracted by Independent Component Analysis: a review and new results. Nonlin Processes Geophys 18:925–940. https://doi.org/10.5194/npg-18-925-2011
De Lauro E, Falanga M, Petrosino S (2012) Study on the long-period source mechanism at Campi Flegrei (Italy) by a multi-parametric analysis. Phys Earth Planet Inter 206:16–30
De Negri RS, Rose KM, Matoza RS, Hupe P, Ceranna L (2022) Long-range multi-year infrasonic detection of eruptive activity at Mount Michael volcano, South Sandwich Islands. Geophys Res Lett 49:e2021GL096061 https://doi.org/10.1029/2021GL096061
Decker RW (1973) State-of-the-art in volcano forecasting. Bull Volcanol 37(3):372–393. https://doi.org/10.1007/BF02597635
Decker RW, Klein FW, Okamura AT, Okubo PG (1995) Forecasting eruptions of Mauna Loa Volcano, Hawaii. AGU Geophys Monogr Ser 92:337–348. https://doi.org/10.1029/GM092p0337
Delclos C, Blanc E, Broche P, Glangeaud F, Lacoume JL (1990) Processing and interpretation of microbarograph signals generated by the explosion of Mount St. Helens. J Geophys Res Atmos 95(D5):5485–5494. https://doi.org/10.1029/JD095iD05p05485
Delle Donne D, Ripepe M, De Angelis S, Cole PD, Lacanna G, Poggi P, Stewart R (2014) Thermal, acoustic and seismic signals from pyroclastic density currents and Vulcanian explosions at Soufrière Hills Volcano, Montserrat. Geolo Soc Lon Mem 39(1):169–178. https://doi.org/10.1144/M39.9
Delle Donne D, Ripepe M, Lacanna G, Tamburello G, Bitetto M, Aiuppa A (2016) Gas mass derived by infrasound and UV cameras: implications for mass flow rate. J Volcanol Geoth Res 325:169–178
Dempsey DE, Cronin SJ, Mei S, Kempa-Liehr AW (2020) Automatic precursor recognition and real-time forecasting of sudden explosive volcanic eruptions at Whakaari, New Zealand. Nat Commun 11(1):3562. https://doi.org/10.1038/s41467-020-17375-2
Dewey K, Byerly P (1969) The early history of seismometry (to 1900). Bull Seismol Soc Am 59(1):183–227. https://doi.org/10.1785/BSSA0590010183
Dibble RR (1969) Seismic power recordings during hydrothermal eruptions from Ruapehu Crater Lake in April 1968. J Geophys Res 74(27):6545–6551. https://doi.org/10.1029/JB074i027p06545
Dibble RR, Kienle J, Kyle PR, Shibuya K (1984) Geophysical studies of Erebus Volcano, Antarctica, from 1974 December to 1982 January. New Zealand J Geol Geophys 27(4):425–455. https://doi.org/10.1080/00288306.1984.10422264
Drob D (2019) Meteorology, climatology, and upper atmospheric composition for infrasound propagation modeling. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Cham, pp 485–508. https://doi.org/10.1007/978-3-319-75140-5_14
Dunham EM, Ogden DE (2012) Guided waves along fluid-filled cracks in elastic solids and instability at high flow rates. J Appl Mech 79(3):031020. https://doi.org/10.1115/1.4005961
Dziak RP, Park M, Matsumoto H, Byun SK (2005) Hydroacoustic records and a numerical model of the source mechanism from the first historical eruption of Anatahan Volcano, Mariana Islands. J Volcanol Geotherm Res 146:86–101. https://doi.org/10.1016/j.jvolgeores.2004.12.009
Dziak R, Hammond S, Fox C (2011) A 20-year hydroacoustic time series of seismic and volcanic events in the Northeast Pacific Ocean. Oceanography 24(3):280–293. https://doi.org/10.5670/oceanog.2011.79
Eaton JP (1977) Frequency response of the USGS short period telemetered seismic system and its suitability for network studies of local earthquakes. US Geol Surv Open File Rep 77844:145. https://doi.org/10.3133/ofr77844
Einarsson P (2018) Short-term seismic precursors to Icelandic eruptions 1973–2014. Front Ear Sci 6:45. https://doi.org/10.3389/feart.2018.00045
Endo ET, Murray T (1991) Real-time seismic amplitude measurement (RSAM): a volcano monitoring and prediction tool. Bull Volcanol 53(7):533–545. https://doi.org/10.1007/BF00298154
Endo ET, Malone SD, Noson LL, Weaver CJ (1981) Locations, magnitudes and statistics of the March 20–May 18 earthquake sequence. USGS Prof Pap 1250:93–108. https://doi.org/10.3133/pp1250
Ern M, Hoffmann L, Rhode S, Preusse P (2022) The mesoscale gravity wave response to the 2022 Tonga volcanic eruption: AIRS and MLS satellite observations and source backtracing. Geophys Res Lett 49:e2022GL098626. https://doi.org/10.1029/2022GL098626
Evers LG, Haak HW (2005) The detectability of infrasound in the Netherlands from the Italian volcano Mt. Etna. J Atmos Sol Terr Phys 67(3):259–268. https://doi.org/10.1016/j.jastp.2004.09.002
Evers LG, Haak HW (2010) The characteristics of infrasound, its propagation and some early history. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Dordrecht, pp 3–27. https://doi.org/10.1007/978-1-4020-9508-5_1
Ewert JW, Swanson DA (1992) Monitoring volcanoes: techniques and strategies used by the staff of the Cascades Volcano Observatory, 1980–90. USGS Bull 1966 https://doi.org/10.3133/b1966_1992
Falsaperla S, Graziani S, Nunnari G, Spampinato S (1996) Automatic classification of volcanic earthquakes by using multi-layered neural networks. Nat Haz 13(3):205–228. https://doi.org/10.1007/BF00215816
Falsaperla SE, Privitera BC, Dawson P (2002) Analysis of long-period events recorded at Mount Etna (Italy) in 1992, and their relationship to eruptive activity. J Volcanol Geoth Res 114:419–440
Farin M, Tsai VC, Lamb MP, Allstadt KE (2019) A physical model of the high-frequency seismic signal generated by debris flows. Earth Surf Proc Land 44(13):2529–2543
Fedotov SA, Feofilaktov VD, Gordeev EI, Gavrilov VA, Chebrov VN (1987) The development of seismometric observations in Kamchatka. Vulkanol Seis 6:11–28
Fee D, Matoza RS (2013) An overview of volcano infrasound: from Hawaiian to Plinian, local to global. J Volcanol Geotherm Res 249:123–139. https://doi.org/10.1016/j.jvolgeores.2012.09.002
Fee D, Garces M, Steffke A (2010b) Infrasound from Tungurahua Volcano 2006–2008: Strombolian to Plinian eruptive activity. J Volcanol Geotherm Res 193:67–81. https://doi.org/10.1016/j.jvolgeores.2010.03.006
Fee D, Garcés M, Patrick M, Chouet B, Dawson P, Swanson D (2010c) Infrasonic harmonic tremor and degassing bursts from Halema’uma’u Crater, Kilauea Volcano, Hawaii. J Geophys Res 115:B11316. https://doi.org/10.1029/2010JB007642
Fee D, Matoza RS, Gee KL, Neilsen TB, Ogden DE (2013a) Infrasonic crackle and supersonic jet noise from the eruption of Nabro Volcano, Eritrea. Geophys Res Lett 40:1–5. https://doi.org/10.1002/grl.50827
Fee D, McNutt SR, Lopez TM, Arnoult KM, Szuberla CA, Olson JV (2013b) Combining local and remote infrasound recordings from the 2009 Redoubt Volcano eruption. J Volcanol Geoth Res 259:100–114
Fee D, Haney M, Matoza R, Szuberla C, Lyons J, Waythomas C (2016) Seismic envelope-based detection and location of ground-coupled airwaves from volcanoes in Alaska. Bull Seismol Soc Am 106(3):1024–1035. https://doi.org/10.1785/0120150244
Fee D, Izbekov P, Kim K, Yokoo A, Lopez T, Prata F, Kazahaya R, Nakamichi H, Iguchi M (2017) Eruption mass estimation using infrasound waveform inversion and ash and gas measurements: evaluation at Sakurajima Volcano, Japan. Earth Planet Sci Lett 480:42–52. https://doi.org/10.1016/j.epsl.2017.09.043
Fee D, Lyons J, Haney M, Wech A, Waythomas C, Diefenbach AK, Lopez T, Van Eaton A, Schneider D (2020) Seismo-acoustic evidence for vent drying during shallow submarine eruptions at Bogoslof volcano, Alaska. Bull Volcanol 82(1):1–14. https://doi.org/10.1007/s00445-019-1326-5
Fee D, Garcés M (2007) Infrasonic tremor in the diffraction zone. Geophys Res Lett 34(16)
Fee D, Steffke A, Garces M (2010a) Characterization of the 2008 Kasatochi and Okmok eruptions using remote infrasound arrays. J Geophys Res: Atmospheres, 115(D2).
Fehler M (1983) Observations of volcanic tremor at Mount St. Helens Volcano. J Geophys Res 88:3476–3484. https://doi.org/10.1029/JB088iB04p03476
Fehler M, Chouet B (1982) Operation of a digital seismic network on Mount St. Helens volcano and observations of long period seismic events that originate under the volcano. Geophys Res Lett 9:1017–1020. https://doi.org/10.1029/GL009i009p01017
Fernández J, Pepe A, Poland MP, Sigmundsson F (2017) Volcano geodesy: recent developments and future challenges. J Volcanol Geoth Res 344:1–12
Fernández JP, Cigala V, Kueppers U, Sesterhenn J (2020) Acoustic analysis of starting jets in an anechoic chamber: implications for volcano monitoring. Sci Rep 10(1):1–12
Ferrazzini V, Aki K (1987) Slow waves trapped in a fluid-filled infinite crack: implication for volcanic tremor. J Geophys Res 92(B9):9215–9223. https://doi.org/10.1029/JB092iB09p09215
Ferrick MG, Qamar A, St Lawrence WF (1982) Source mechanism of volcanic tremor. J Geophys Res 87(B10):8675–8683. https://doi.org/10.1029/JB087iB10p08675
Filson J, Simkin T, Leu LK (1973) Seismicity of a caldera collapse: Galapagos Islands 1968. J Geophys Res 78(35):8591–8622. https://doi.org/10.1029/JB078i035p08591
Finch RH (1949) Volcanic tremor (Part I). Bull Seismol Soc Am 39(2):73–78. https://doi.org/10.1785/BSSA0390020073
Firstov PP, Kravchenko NM (1996) Estimation of the amount of explosive gas released in volcanic eruptions using air waves. Volcanol Seismol 17:547–560
Firstov PP, Fee D, Makhmudov ER (2013) The explosive activity of Karymskii Volcano, Kamchatka: acoustic and seismic observations. J Volcanol Seismol 7(4):252–264. https://doi.org/10.1134/S0742046313040039
Fischer TP, Morrissey MM, Lucia Calvache VM, Diego Gomez M, Roberto Torres C, Stix J, Williams SN (1994) Correlations between SO2 flux and long-period seismicity at Galeras volcano. Nature 368(6467):135–137
Fisher NH (1940) Note on the vulcanological observatory at Rabaul. Bull Volcanol 6(1):185–187. https://doi.org/10.1007/BF02994879
Francis TJG (1974) A new interpretation of the 1968 Fernandina caldera collapse and its implications for the mid-oceanic ridges. Geophys J Int 39(2):301–318. https://doi.org/10.1111/j.1365-246X.1974.tb05456.x
Frank WB, Shapiro NM, Gusev AA (2018) Progressive reactivation of the volcanic plumbing system beneath Tolbachik volcano (Kamchatka, Russia) revealed by long-period seismicity. Earth Planet Sci Lett 493:47–56
Frehner M (2014) Krauklis wave initiation in fluid-filled fractures by seismic body waves. Geophys 79(1):T27–T35. https://doi.org/10.1190/geo2013-0093.1
Gabrielson T (2010) Krakatoa and the Royal Society: the Krakatoa explosion of 1883. Acoustics Today 6(2):14–19
Garcés MA (2000) Theory of acoustic propagation in a multi-phase stratified liquid flowing within an elastic-walled conduit of varying cross-sectional area. J Volcanol Geotherm Res 101(1):1–17. https://doi.org/10.1016/S0377-0273(00)00155-4
Garcés MA, McNutt SR (1997) Theory of the airborne sound field generated in a resonant magma conduit. J Volcanol Geotherm Res 78:155–178. https://doi.org/10.1016/S0377-0273(97)00018-8
Garcés MA, Hagerty MT, Schwartz SY (1998) Magma acoustics and time-varying melt properties at Arenal Volcano, Costa Rica. Geophys Res Lett 25(13):2293–2296. https://doi.org/10.1029/98GL01511
Garcés M, Harris A, Hetzer C, Johnson J, Rowland S, Marchetti E, Okubo P (2003) Infrasonic tremor observed at Kīlauea Volcano, Hawai’i. Geophys Res Lett 30(20):2023. https://doi.org/10.1029/2003GL018038
Garcés M, Fee D, McCormack D, Servranckx R, Bass H, Hetzer C, Hedlin M, Matoza R, Yepes H, Ramon P (2008) Capturing the acoustic fingerprint of stratospheric ash injection. EOS Trans AGU 89(40):377–379. https://doi.org/10.1029/2008EO400001
Garces M, Hetzer C (2006) Characterization of the infrasound field in the central Pacific, Defense Threat Reduction Agency Technical Report. https://apps.dtic.mil/sti/citations/ADA456663
Garcés M, Aucan J, Fee D, Caron P, Merrifield M, Gibson R, Bhattacharyya J, Shah S (2006) Infrasound from large surf. Geophys Res Lett 33(5)
Garcés MA, Fee D, Matoza R (2013) Volcano Acoustics. In: Fagents SA, Gregg TKP, Lopes RMC (eds) Modeling volcanic processes: the physics and mathematics of volcanism. Cambridge University Press, Cambridge, pp 359–383. https://doi.org/10.1017/cbo9781139021562.016
Gasparini P, Scarpa R, Aki K (1992) Preface. In: Gasparini P, Scarpa R (eds), Monitoring and mitigation of volcano hazards. Springer-Verlag, Berlin, pp V-VIII. https://doi.org/10.1007/978-3-642-80087-0
Geller R (1974) "POSEIDON Project-Its application to the better understanding of the nature of interplate earthquakes." In: Second International Tsunami Workshop on the Technical Aspects of Tsunami Warning Systems, Tsunami Analysis, Preparedness, Observation and Instrumentation, 4:99
Gil Cruz F, Chouet BA (1997) Long-period events, the most characteristic seismicity accompanying the emplacement and extrusion of a lava dome in Galeras Volcano, Colombia, in 1991. J Volcanol Geoth Res 77:121–158
Gil-Cruz F (1999) Observations of two special kinds of tremor at Galeras volcano, Colombia (1989–1991). Ann Geophys 42(3). https://doi.org/10.4401/ag-3727
Girina OA (2013) Chronology of Bezymianny volcano activity, 1956–2010. J Volcanol Geotherm Res 263:22–41. https://doi.org/10.1016/j.jvolgeores.2013.05.002
Giudicepietro F, Orazi M, Scarpato G, Peluso R, D’Auria L, Ricciolino P, Lo Bascio D, Esposito AM, Borriello G, Capello M, Caputo A (2010) Seismological monitoring of Mount Vesuvius (Italy): more than a century of observations. Seismol Res Lett 81(4):625–634. https://doi.org/10.1785/gssrl.81.4.625
Glasgow ME, Schmandt B, Hansen SM (2018) Upper crustal low-frequency seismicity at Mount St. Helens detected with a dense geophone array. J Volcanol Geotherm Res 358:329–341. https://doi.org/10.1016/j.jvolgeores.2018.06.006
Goerke VH, Young JM, Cook RK (1965) Infrasonic observations of the May 16, 1963, volcanic explosion on the Island of Bali. J Geophys Res 70(24):6017–6022. https://doi.org/10.1029/JZ070i024p06017
Goldstein P, Chouet B (1994) Array measurements and modeling of sources of shallow volcanic tremor at Kilauea Volcano, Hawaii. J Geophys Res 99(B2):2637–2652. https://doi.org/10.1029/93JB02639
Gordeev EI, Saltykov VA, Sinitsyn VI, Chebrov VN (1990) Temporal and spatial characteristics of volcanic tremor wave fields. J Volcanol Geotherm Res 40(1):89–101. https://doi.org/10.1016/0377-0273(90)90108-R
Gordeev EI, Chebrov VN, Levina VI, Senyukov S, Shevchenko YV, Yashchuk V (2006) The system of seismological observation in Kamchatka. Vulkanol Seismol 3:6–27
Gorelchik VI (2001) By the history of development of seismic investigations of Kamchatkan volcanoes. In: Geodynamics and Volcanism of the Kurile-Kamchatka Island-Arc System. IVGG FED RAS, Petropavlovsk-Kamchatsky, Russia, pp 341–351
Gorshkov GS (1960) Determination of the explosion energy in some volcanoes according to barograms. Bull Volcanol 23:141–144. https://doi.org/10.1007/BF02596639
Gossard EE, Hooke WH (1975) Waves in the atmosphere: atmospheric infrasound and gravity waves: their generation and propagation. Elsevier, Amsterdam
Goto A (1999) A new model for volcanic earthquake at Unzen Volcano: melt rupture. Geophys Res Lett 26(16):2541–2544
Goto A, Johnson JB (2011) Monotonic infrasound and Helmholtz resonance at Volcan Villarrica (Chile). Geophys Res Lett 38(6):L06301. https://doi.org/10.1029/2011gl046858
Green DN, Neuberg J (2005) Seismic and infrasonic signals associated with an unusual collapse event at the Soufrière Hills volcano, Montserrat. Geophys Res Lett 32(7):L07308. https://doi.org/10.1029/2004GL022265
Green DN, Neuberg J (2006) Waveform classification of volcanic low-frequency earthquake swarms and its implication at Soufrière Hills Volcano, Montserrat. J Volcanol Geotherm Res 153(1–2):51–63. https://doi.org/10.1016/j.jvolgeores.2005.08.003
Green DN, Neuberg J, Cayol V (2006) Shear stress along the conduit wall as a plausible source of tilt at Soufrière Hills volcano, Montserrat. Geophys Res Lett 33:L10306. https://doi.org/10.1029/2006GL025890
Green DN, Evers LG, Fee D, Matoza RS, Snellen M, Smets P, Simons D (2013) Hydroacoustic, infrasonic and seismic monitoring of the submarine eruptive activity and sub-aerial plume generation at South Sarigan, May 2010. J Volcanol Geotherm Res 257:31–43. https://doi.org/10.1016/j.jvolgeores.2013.03.006
Gresse M, Uyeshima M, Koyama T, Hase H, Aizawa K, Yamaya Y, Morita Y, Weller D, Rung‐Arunwan T, Kaneko T, Sasai Y (2021) Hydrothermal and magmatic system of a volcanic island inferred from magnetotellurics, seismicity, self‐potential, and thermal image: an example of Miyakejima (Japan). J Geophys Res: Solid Earth 126(6):e2021JB022034
Gudmundsson MT, Pedersen R, Vogfjörd K, Thorbjarnardóttir B, Jakobsdóttir S, Roberts MJ (2010) Eruptions of Eyjafjallajökull Volcano, Iceland. Eos Trans AGU 91(21):190–191. https://doi.org/10.1029/2010EO210002
Hagerty MT, Schwartz SY, Protti M, Garces M, Dixon T (1997) Observations at Costa Rican volcano offer clues to causes of eruptions. Eos Trans AGU 78(49):565–580. https://doi.org/10.1029/97EO00337
Hagerty MT, Schwartz SY, Garces MA, Protti M (2000) Analysis of seismic and acoustic observations at Arenal Volcano, Costa Rica, 1995–1997. J Volcanol Geotherm Res 101(1–2):27–65. https://doi.org/10.1016/S0377-0273(00)00162-1
Haney MM, Matoza RS, Fee D, Aldridge DF (2018) Seismic equivalents of volcanic jet scaling laws and multipoles in acoustics. Geophys J Int 213:623–636. https://doi.org/10.1093/gji/ggx554
Harding BJ, Wu Y.-JJ, Alken P, Yamazaki Y, Triplett CC, Immel TJ, et al. (2022). Impacts of the January 2022 Tonga volcanic eruption on the ionospheric dynamo: ICON-MIGHTI and Swarm observations of extreme neutral winds and currents. Geophys Res Lett 49:e2022GL098577. https://doi.org/10.1029/2022GL098577
Harkrider DG (1964) Theoretical and observed acoustic-gravity waves from explosive sources in the atmosphere. J Geophys Res 69(24):5295–5321. https://doi.org/10.1029/JZ069i024p05295
Harkrider D, Press F (1967) The Krakatoa air-sea waves: an example of pulse propagation in coupled systems. Geophys J Int 13(1–3):149–159. https://doi.org/10.1111/j.1365-246X.1967.tb02150.x
Harlow DH, Power JA, Laguerta EP, Ambubuyog G, White RA, Hoblitt RP (1996) Precursory seismicity and forecasting of the June 15, 1991, eruption of Mount Pinatubo. In: Newhall CG, Punongbayan S (eds) Fire and Mud. University of Washington Press, pp 223–247
Harris AJ, Carniel R, Jones J (2005) Identification of variable convective regimes at Erta Ale Lava Lake. J Volcanol Geotherm Res 142(3–4):207–223
Harris A, Ripepe M (2007a) Synergy of multiple geophysical approaches to unravel explosive eruption conduit and source dynamics – a case study from Stromboli. Geochemistry 67:1–35. https://doi.org/10.1016/j.chemer.2007.01.003
Harris A, Alparone S, Bonforte A, Dehn J, Gambino S, Lodato L, Spampinato L (2012) Vent temperature trends at the Vulcano Fossa fumarole field: the role of permeability. Bull Volcanol 74(6):1293–1311
Harris A, Ripepe M (2007b) Temperature and dynamics of degassing at Stromboli. J Geophys Res: Solid Earth, 112(B3)
Harrison G (2022) Pressure anomalies from the January 2022 Hunga Tonga-Hunga Ha’apai eruption. Weather 77:87–90. https://doi.org/10.1002/wea.4170
Havskov J, De la Cruz-Reyna S, Singh SK, Medina F, Gutierrez C (1983) Seismic activity related to the March–April, 1982 eruptions of El Chichon Volcano, Chiapas, Mexico. Geophys Res Lett 10:293–296
Hawaiian Volcano Observatory (2001) Volcano Watch — Professor Fusakichi Omori—an instrumental person at HVO, MARCH 15, 2001. https://www.usgs.gov/center-news/volcano-watch-professor-fusakichi-omori-instrumental-person-hvo. Accessed 21 March 2022
Hedlin MA, Raspet R (2003) Infrasonic wind-noise reduction by barriers and spatial filters. J Acoust Soc Am 114(3):1379–1386
Hedlin MAH, Garces M, Bass H, Hayward C, Herrin G, Olson J, Wilson C (2002) Listening to the secret sounds of Earth’s atmosphere. EOS Trans AGU 83:557–565. https://doi.org/10.1029/2002EO000383
Heiken G (2013) From Kilauea Iki 1959 to Eyjafiallajökull 2010: How volcanology has changed! in The Web of Geological Sciences: Advances, Impacts, and Interactions, edited by M. E. Bickford, The Geological Society of America Special Paper 500, 33.
Helz RT (1980) Crystallization history of Kilauea Iki lava lake as seen in drill core recovered in 1967–1979. Bulletin Volcanologique 43(4):675–701
Helz RT, Thornber CR (1987) Geothermometry of Kilauea Iki lava lake, Hawaii. Bull Volcanology 49(5):651–668
Helz RT (1993) Drilling report and core logs for the 1988 drilling of Kilauea Iki lava lake, Kilauea Volcano, Hawaii, with summary descriptions of the occurrence of foundered crust and fractures in the drill core, USGS Professional Paper 93–15 https://doi.org/10.3133/ofr9315
Hill DP (1977) A model for earthquake swarms. J Geophys Res 82(8):1347–1352. https://doi.org/10.1029/JB082i008p01347
Hill DP (1984) Monitoring unrest in a large silicic caldera, the Long Valley-Inyo Craters volcanic complex in east-central California. Bull Volcanol 47:371–395. https://doi.org/10.1007/BF01961568
Hirn A, Girardin N, Viodé JP, Eschenbrenner S (1987) Shallow seismicity at Montagne Pelée volcano, Martinique, Lesser Antilles. Bull Volcanol 49(6):723–728. https://doi.org/10.1007/BF01079823
Hotovec AJ, Prejean SG, Vidale JE, Gomberg J (2013) Strongly gliding harmonic tremor during the 2009 eruption of Redoubt Volcano. J Volcanol Geotherm Res 259:89–99. https://doi.org/10.1016/j.jvolgeores.2012.01.001
Howell BF (1989) Seismic instrumentation: history. In: Geophysics. Encyclopedia of Earth Science, Springer, Boston. https://doi.org/10.1007/0-387-30752-4_126
Hutko AR, Bahavar M, Trabant C, Weekly RT, Fossen MV, Ahern T (2017) Data products at the IRIS-DMC: Growth and usage. Seismol Res Lett 88(3):892–903
Hwang LJ, Ahern T, Ebinger CJ, Ellsworth WL, Euler GG, Okal EA, Okubo PG, Walter WR (2020) Rescuing legacy seismic data FAIR’ly. Seismol Res Lett 91(3):1339–1340. https://doi.org/10.1785/0220200027
Ibáñez JM, Alejandro Díaz-Moreno, Janire Prudencio, Patené D, Luciano Zuccarello, Ornella Cocina, Lühr B et al (2016) TOMO-ETNA experiment at Etna volcano: activities on land. Ann Geophys 59:4
Ibáñez JM, Benítez C, Gutiérrez LA, Cortés G, García-Yeguas A, Alguacil G (2009) The classification of seismo-volcanic signals using Hidden Markov Models as applied to the Stromboli and Etna volcanoes. J Volcanol Geotherm Res 187(3–4):218–226. https://doi.org/10.1016/j.jvolgeores.2009.09.002
Ichihara M, Takeo M, Yokoo A, Oikawa J, Ohminato T (2012) Monitoring volcanic activity using correlation patterns between infrasound and ground motion. Geophys Res Lett 39:L04304. https://doi.org/10.1029/2011GL050542
Ichihara M, Yamakawa K, Muramatsu D (2021) A simple method to evaluate the air-to-ground coupling efficiency: a tool helping the assessment of seismic/infrasonic energy partitioning during an eruption. Earth Planets Space 73:180. https://doi.org/10.1186/s40623-021-01510-4
Iezzi AM, Fee D, Kim K, Jolly AD, Matoza RS (2019a) Three-dimensional acoustic multipole waveform inversion at Yasur volcano, Vanuatu. J Geophys Res 124:8679–8703. https://doi.org/10.1029/2018JB017073
Iezzi AM, Schwaiger HF, Fee D, Haney MM (2019b) Application of an updated atmospheric model to explore volcano infrasound propagation and detection in Alaska. J Volcanol Geoth Res 371:192–205
Iezzi AM, Matoza RS, Fee D, Kim K, Jolly AD (2022) Synthetic evaluation of infrasonic multipole waveform inversion. J Geophys Res: Solid Earth 127(1):e2021JB023223
Iguchi M (2016) Method for real-time evaluation of discharge rate of volcanic ash–case study on intermittent eruptions at the Sakurajima volcano, Japan–. J Disaster Res 11(1):4–14
Iguchi M, Ishihara K (1990) Comparison of earthquakes and airshocks accompanied with explosive eruptions at Sakurajima and Suwanosejima volcanoes. Annu Disas Prev Res Inst Kyoto Univ 33B–1:1–11
Iguchi M (2013) Magma movement from the deep to shallow Sakurajima Volcano as revealed by geophysical observations (Sakurajima Special Issue). Bull Volcanol Soc Japan 58(1): 1–18. https://doi.org/10.18940/kazan.58.1_1
Imbò G (1949) L’Osservatorio Vesuviano e la sua attività nel primo secolo di vita. Annali Osservatorio Vesuviano , V serie, volume unico, 9–64
Ishihara K (1985) Dynamical analysis of volcanic explosion. J Geodyn 3:327–349. https://doi.org/10.1016/0264-3707(85)90041-9
Ishii K, Yokoo A, Iguchi M, Fujita E (2020) Utilizing the solution of sound diffraction by a thin screen to evaluate infrasound waves attenuated around volcano topography. J Volcanol Geoth Res 402:106983
Jaggar TA (1920) Seismometric investigation of the Hawaiian lava column. Bull Seismol Soc Am 10(4):155–275. https://doi.org/10.1785/BSSA0100040155
Jaggar TA (1956) My experiments with volcanoes. Hawaiian Volcano Research Association, Honolulu.
James MR, Lane SJ, Chouet B, Gilbert JS (2004) Pressure changes associated with the ascent and bursting of gas slugs in liquid-filled vertical and inclined conduits. J Volcanol Geotherm Res 129:61–82. https://doi.org/10.1016/S0377-0273(03)00232-4
Johnson JB (2003) Generation and propagation of infrasonic airwaves from volcanic explosions. J Volcanol Geotherm Res 121(1):1–14. https://doi.org/10.1016/S0377-0273(02)00408-0
Johnson JB (2007) On the relation between infrasound, seismicity, and small pyroclastic explosions at Karymsky Volcano. J Geophys Res 112:B08203. https://doi.org/10.1029/2006JB004654
Johnson JB, Ripepe M (2011) Volcano infrasound: a review. J Volcanol Geotherm Res 206(3–4):61–69. https://doi.org/10.1016/j.jvolgeores.2011.06.006
Johnson JB, Lees JM, Gordeev EI (1998) Degassing explosions at Karymsky volcano, Kamchatka. Geophys Res Lett 25(21):3999–4002. https://doi.org/10.1029/1998GL900102
Johnson JB, Ruiz MC, Lees JM, Ramon P (2005) Poor scaling between elastic energy release and eruption intensity at Tungurahua Volcano, Ecuador. Geophys Res Lett 32(15):L15304. https://doi.org/10.1029/2005GL022847
Johnson J, Aster R, Jones KR, Kyle P, McIntosh B (2008a) Acoustic source characterization of impulsive Strombolian eruptions from the Mount Erebus lava lake. J Volcanol Geoth Res 177(3):673–686. https://doi.org/10.1016/j.jvolgeores.2008.06.028
Johnson JB, Lees JM, Gerst A, Sahagian D, Varley N (2008b) Long-period earthquakes and co-eruptive dome inflation seen with particle image velocimetry. Nature 456(7220):377–381. https://doi.org/10.1038/nature07429
Johnson JB, Ruiz MC, Ortiz HD, Watson LM, Viracucha G, Ramon P, Almeida M (2018) Infrasound tornillos produced by Volcán Cotopaxi’s deep crater. Geophys Res Lett 45:5436–5444. https://doi.org/10.1029/2018GL077766
Johnson JB, Palma JL (2015) Lahar infrasound associated with Volcán Villarrica's 3 March 2015 eruption. Geophys Res Lett 42: 2015GL065024. https://doi.org/10.1002/2015GL065024
Johnson JB, Ronan TJ (2015) Infrasound from volcanic rockfalls. J Geophys Res 120: 2015JB012436. https://doi.org/10.1002/2015JB012436
Johnson JH, Prejean S, Savage MK, Townend J (2010) Anisotropy, repeating earthquakes, and seismicity associated with the 2008 eruption of Okmok volcano, Alaska. J Geophys Res 115(B9): B00B04. https://doi.org/10.1029/2009JB006991
Johnson JB, Anderson J, Marcillo O, Arrowsmith S (2012) Probing local wind and temperature structure using infrasound from Volcan Villarrica (Chile). J Geophys Res: Atmospheres, 117(D17).
Johnson J (2019) Local volcano infrasound monitoring. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Cham, pp 989–1022. https://doi.org/10.1007/978-3-319-75140-5_32
Jolly AD, Lokmer I, Thun J, Salichon J, Fry B, Chardot L (2017a) Insights into fluid transport mechanisms at White Island from analysis of coupled very long-period (VLP), long-period (LP) and high-frequency (HF) earthquakes. J Volcanol Geotherm Res 343:75–94. https://doi.org/10.1016/j.jvolgeores.2017.06.006
Jolly AD, Matoza RS, Fee D, Kennedy BM, Iezzi AM, Fitzgerald RH, Austin AC, Johnson R (2017b) Capturing the acoustic radiation pattern of strombolian eruptions using infrasound sensors aboard a tethered aerostat, Yasur volcano, Vanuatu. Geophys Res Lett 44:9672–9680. https://doi.org/10.1002/2017GL074971
Jones J, Carniel R, Harris AJ, Malone S (2006) Seismic characteristics of variable convection at Erta ʻAle lava lake, Ethiopia. J Volcanol Geotherm Res 153(1–2):64–79
Jousset P, Neuberg J, Sturton S (2003) Modelling the time-dependent frequency content of low-frequency volcanic earthquakes. J Volcanol Geotherm Res 128:201–223. https://doi.org/10.1016/S0377-0273(03)00255-5
Jousset P, Neuberg J, Jolly A (2004) Modelling low-frequency volcanic earthquakes in a viscoelastic medium with topography. Geophys J Int 159:776–802. https://doi.org/10.1111/j.1365-246X.2004.02411.x
Jousset P, Budi-Santoso A, Jolly AD, Boichu M, Dwiyono S, Sumarti S, Hidayati S, Thierry P (2013) Signs of magma ascent in LP and VLP seismic events and link to degassing: an example from the 2010 explosive eruption at Merapi volcano, Indonesia. J Volcanol Geoth Res 261:171–192
Julian BR (1994) Volcanic tremor: nonlinear excitation by fluid flow. J Geophys Res 99(1994):11859–11877
Kamo K, Ishihara K, Tahira M (1994) Infrasonic and seismic detection of explosive eruptions at Sakurajima volcano, Japan, and the PEGASAS-VE early-warning system. In: Casadevall TJ (ed) Proceedings of the First International Symposium on Volcanic Ash and Aviation Safety. US Geol Surv Bull 2047: 357–365. https://doi.org/10.3133/b2047
Kaneshima S, Kawakatsu H, Matsubayashi H, Sudo Y, Tsutsui T, Ohminato T, Ito H, Uhira K, Yamasato H, Oikawa J, Takeo M, Iidaka T (1996) Mechanism of phreatic eruptions at Aso Volcano inferred from near-field broadband seismic observations. Science 273:642–645. https://doi.org/10.1126/science.273.5275.642
Kato A, Terakawa T, Yamanaka Y et al (2015) Preparatory and precursory processes leading up to the 2014 phreatic eruption of Mount Ontake, Japan. Earth Planet Sp 67:111. https://doi.org/10.1186/s40623-015-0288-x
Kauahikaua J, Poland M (2012) One hundred years of volcano monitoring in Hawaii. EOS Trans Am Geophys Union 93(3):29–30
Kawakatsu H, Ohminato T, Ito H, Kuwahara Y (1992) Broadband seismic observation at Sakurajima Volcano, Japan. Geophys Res Lett 19:1959–1962. https://doi.org/10.1029/92GL01964
Kawakatsu H, Kaneshima S, Matsubayashi H, Ohminato T, Sudo Y, Tsutsui T, Uhira K, Yamasato H, Ito H, Legrand D (2000) Aso94: Aso seismic observation with broadband instruments. J Volcanol Geotherm Res 101:129–154. https://doi.org/10.1016/S0377-0273(00)00166-9
Kawakatsu H, Yamamoto M (2015) Volcano seismology. In: Treatise on geophysics. Elsevier. pp 389–419. https://doi.org/10.1016/B978-0-444-53802-4.00081-6
Kieffer SW (1977) Sound speed in liquid-gas mixtures: water-air and water-steam. J Geophys Res 82(20):2895–2904
Kilgour G, Kennedy B, Scott B, Christenson B, Jolly A, Asher C, Rosenberg M, Saunders K (2021) Whakaari/White Island: a review of New Zealand’s most active volcano. New Zealand J Geol Geophys 64(2–3):273–295. https://doi.org/10.1080/00288306.2021.1918186
Kim K, Lees JM (2011) Finite-difference time-domain modeling of transient infrasonic wavefields excited by volcanic explosions. Geophys Res Lett 38:L06804. https://doi.org/10.1029/2010GL046615
Kim K, Lees JM (2014) Local volcano infrasound and source localization investigated by 3D simulation. Seismol Res Lett 85(6):1177–1186. https://doi.org/10.1785/0220140029
Kim K, Lees JM, Ruiz M (2012) Acoustic multipole source model for volcanic explosions and inversion for source parameters. Geophys J Int 191(3):1192–1204. https://doi.org/10.1111/j.1365-246X.2012.05696.x
Kim K, Fee D, Yokoo A, Lees JM (2015) Acoustic source inversion to estimate volume flux from volcanic explosions. Geophys Res Lett 42:5243–5249. https://doi.org/10.1002/2015GL064466
Kiser E, Palomeras I, Levander A, Zelt C, Harder S, Schmandt B, Hansen S, Creager K. Ulberg C (2016) Magma reservoirs from the upper crust to the Moho inferred from high-resolution Vp and Vs models beneath Mount St. Helens, Washington State, USA. Geology 44(6):411–414
Klein FW, Koyanagi RY (1980) Hawaiian Volcano Observatory seismic network history, 1950–1979. US Geol Surv Open-File Rep 80–302 https://doi.org/10.3133/ofr80302
Klein FW, Koyanagi RY, Nakata J, Tanigawa WR (1987) The seismicity of Kilauea's magma system. US Geol Surv Prof Pap 1350: 1019–1185. https://pubs.usgs.gov/pp/1987/1350/
Konstantinou KI, Schlindwein V (2003) Nature, wavefield properties and source mechanism of volcanic tremor: a review. J Volcanol Geotherm Res 119(1–4):161–187. https://doi.org/10.1016/S0377-0273(02)00311-6
Korneev V (2008) Slow waves in fractures filled with viscous fluid. Geophysics 73(1):N1–N7. https://doi.org/10.1190/1.2802174
Korneev VA (2011) Krauklis wave in a stack of alternating fluid-elastic layers. Geophysics 76(6):N47–N53. https://doi.org/10.1190/geo2011-0086.1
Koulakov I, Shapiro N (2021) Seismic tomography of volcanoes. In: Encyclopedia of earthquake engineering: vol. d (pp. 1–18). Springer Berlin Heidelberg. https://doi.org/10.1007/978-3-642-36197-5_51-1
Krauklis PV (1962) On some low-frequency vibrations of a liquid layer in an elastic medium. J Appl Math Mech 26(6):1685–1692. https://doi.org/10.1016/0021-8928(62)90203-4
Krauklis PV, Krauklis LA (1998) Excitation of a tube wave in a borehole by a slow wave propagating in a fluid layer. J Math Sci 91:2776–2781. https://doi.org/10.1007/BF02433993
Kubota T, Saito T, Nishida K (2022) Global fast-traveling tsunamis driven by atmospheric Lamb waves on the 2022 Tonga eruption. Science, eabo4364
Kubotera A (1974) Volcanic tremors at Aso volcano. In: Civetta L, Gasparini P, Luongo G, Rapolla A (eds) Physical volcanology. Elsevier, New York, pp 29–48. https://doi.org/10.1016/b978-0-444-41141-9.50008-5
Kulichkov SN, Chunchuzov IP, Popov OE, Gorchakov GI, Mishenin AA, PerepelkinVG, Bush GA, et al. (2022) Acoustic-gravity Lamb waves from the eruption of the Hunga-Tonga-Hunga-Hapai Volcano, its energy release and impact on aerosol concentrations and tsunami. Pure Appl Geophys : 1–16
Kumagai H (2006) Temporal evolution of a magmatic dike system inferred from the complex frequencies of very long period seismic signals. J Geophys Res 111:B06201. https://doi.org/10.1029/2005JB003881
Kumagai H, Chouet BA (1999) The complex frequencies of long-period seismic events as probes of fluid composition beneath volcanoes. Geophys J Int 138:F7–F12. https://doi.org/10.1046/j.1365-246X.1999.00911.x
Kumagai H, Chouet BA (2000) Acoustic properties of a crack containing magmatic or hydrothermal fluids. J Geophys Res 105(B11):25493–25512. https://doi.org/10.1029/2000JB900273
Kumagai H, Chouet BA (2001) The dependence of acoustic properties of a crack on the resonance mode and geometry. Geophys Res Lett 28:3325–3328. https://doi.org/10.1029/2001GL013025
Kumagai H, Chouet BA, Nakano M (2002a) Waveform inversion of oscillatory signatures in long-period events beneath volcanoes. J Geophys Res 107:2301. https://doi.org/10.1029/2001JB001704
Kumagai H, Miyakawa K, Negishi H, Inoue H, Obara K, Suetsugu D (2003) Magmatic dyke resonances inferred from very-long-period seismic signals. Science 299:2058–2061
Kumagai H, Chouet BA, Nakano M (2002b) Temporal evolution of a hydrothermal system in Kusatsu-Shirane Volcano, Japan, inferred from the complex frequencies of long-period events. J Geophys Res 107(B10):2236. https://doi.org/10.1029/2001JB000653
Kumagai H (2009) Source quantification of volcano seismic signals, in: Meyers RA (ed) Encyclopedia of complexity and systems science. Springer-Verlag, New York, pp. 9899–9932. https://doi.org/10.1007/978-0-387-30440-3_583
Kumazawa M, Imanishi Y, Fukao Y, Furumoto M, Yamamoto A (1990) A theory of spectral analysis based on the characteristic property of a linear dynamic system. Geophys J Int 101:613–630. https://doi.org/10.1111/j.1365-246X.1990.tb05574.x
Kuno H (1958) Bull. Volcan., Vol. 19, p. 58 — Contribution in the discussion in Signore, F. XIe assemblée générale de l’Union Géodésique et Géophysique internationale à Toronto, Ontario, Canada 3–14 Septembre 1957. Bull Volcanol 19, 3–84 (1958). https://doi.org/10.1007/BF02596598
Lacanna G, Ripepe M (2013) Influence of near-source volcano topography on the acoustic wavefield and implication for source modeling. J Volcanol Geotherm Res 250:9–18. https://doi.org/10.1016/j.jvolgeores.2012.10.005
Lacanna G, Ichihara M, Iwakuni M, Takeo M, Iguchi M, Ripepe M (2014) Influence of atmospheric structure and topography on infrasonic wave propagation. J Geophys Res 119:2988–3005. https://doi.org/10.1002/2013JB010827
Lacroix A (1904) La Montagne Pelée et ses éruptions. Masson, Paris. https://www.worldcat.org/title/montagne-pelee-et-ses-eruptions/oclc/875356663
Lahr JC, Chouet BA, Stephens CD, Power JA, Page RA (1994) Earthquake classification, location and error analysis in a volcanic environment: implications for the magmatic system of the 1989–1990 eruptions at Redoubt Volcano, Alaska. J Volcanol Geotherm Res 62:137–151. https://doi.org/10.1016/0377-0273(94)90031-0
Lamb H (1911) On atmospheric oscillations. Proc Royal Soc Lon A 84(574):551–572. https://doi.org/10.1098/rspa.1911.0008
Lamb OD, De Angelis S, Lavallée Y (2015) Using infrasound to constrain ash plume rise. J Appl Volcanol 4(1):1
Landès M, Ceranna L, Le Pichon A, Matoza RS (2012) Localization of microbarom sources using the IMS infrasound network. J Geophys Res 117:D06102. https://doi.org/10.1029/2011JD016684
Lane SJ, James MR (2009) Explosive volcanic eruptions: experimental insights. In: Meyers RA (ed) Encyclopedia of complexity and systems science. Springer-Verlag, New York, pp 9784–9830. https://doi.org/10.1007/978-0-387-30440-3_579
Langer H, Falsaperla S, Thompson G (2003) Application of artificial neural networks for the classification of the seismic transients at Soufriere Hills volcano, Montserrat. Geophys Res Lett 30(21)
Latter JH (1981) Volcanic earthquakes, and their relationship to eruptions at Ruapehu and Ngauruhoe volcanoes. J Volcanol Geoth Res 9:293–309
Latter JH (1979) Volcanological observations at Tongariro National Park, 2, types and classification of volcanic earthquakes, 1976–1978. NZ Dep Sci Ind Res Geophy. Div Wellington Rep 150
Lavallée Y, Meredith PG, Dingwell DB, Hess K-U, Wassermann J, Cordonnier B, Gerik A, Kruhl JH (2008) Seismogenic lavas and explosive eruption forecasting. Nature 453:507–510. https://doi.org/10.1038/nature06980
Lawrence WS, Qamar A (1979) Hydraulic transients: a seismic source in volcanoes and glaciers. Science 203:654–656. https://doi.org/10.1126/science.203.4381.654
Le Bras R, Arora N, Kushida N, Mialle P, Bondár I, Tomuta E, Alamneh FK, Feitio P, Villarroel M, Vera B, Sudakov A (2021) NET-VISA from cradle to adulthood. A machine-learning tool for seismo-acoustic automatic association. Pure Appl Geophys 178(7):2437–2458
Le G, Liu G, Yizengaw E, Englert CR (2022) Intense equatorial electrojet and counter electrojet caused by the 15 January 2022 Tonga volcanic eruption: space- and ground-based observations. Geophysical Research Letters 49:e2022GL099002. https://doi.org/10.1029/2022GL099002
Le Pichon A, Pilger C, Ceranna L, Marchetti E, Lacanna G, Souty V, Vergoz J, Listowski C, Hernandez B, Mazet-Roux G, Dupont A (2021) Using dense seismo-acoustic network to provide timely warning of the 2019 paroxysmal Stromboli eruptions. Sci Rep 11(1):1–12. https://doi.org/10.1038/s41598-021-93942-x
Le Pichon A, Blanc E, Drob D, Lambotte S, Dessa JX, Lardy M, Bani P, Vergniolle S (2005) Infrasound monitoring of volcanoes to probe high‐altitude winds. J Geophys Res: Atmospheres 110:D13
LeConte J (1884) Atmospheric waves from Krakatoa. Science 3(71): 701–702. https://www.jstor.org/stable/1758846
Lee T, Ishii M, Okubo P (2020) Relative time corrections for historical analog seismograms using the single-day ambient noise correlation function. Bull Seismol Soc Am 110(6):3185–3195. https://doi.org/10.1785/0120190313
Lees JM (2007) Seismic tomography of magmatic systems. J Volcanol Geotherm Res 167(1–4):37–56. https://doi.org/10.1016/j.jvolgeores.2007.06.008
Lees JM, Gordeev EI, Ripepe M (2004) Explosions and periodic tremor at Karymsky volcano, Kamchatka, Russia. Geophys J Int 158(3):1151–1167
Leet RC (1988) Saturated and subcooled hydrothermal boiling in groundwater-flow channels as a source of harmonic tremor. J Geophys Res 93:4835–4849
Lesage P, Mora MM, Alvarado GE, Pacheco J, Metaxian JP (2006) Complex behavior and source model of the tremor at Arenal volcano, Costa Rica. J Volcanol Geotherm Res 157:49–59. https://doi.org/10.1016/j.jvolgeores.2006.03.047
Lin CH, Konstantinou KI, Liang WT, Pu HC, Lin YM, You SH, Huang YP (2005) Preliminary analysis of volcanoseismic signals recorded at the Tatun Volcano Group, northern Taiwan. Geophys Res Lett 32(10)
Lin JT, Rajesh PK, Lin CC, Chou MY, Liu JY, Yue J, Hsiao TY, Tsai HF, Chao HM, Kung MM (2022) Rapid conjugate appearance of the giant ionospheric Lamb Wave signatures in the Northern Hemisphere after Hunga‐Tonga Volcano eruptions. Geophys Res Lett 49(8):e2022GL098222
Lipovsky BP, Dunham EM (2015) Vibrational modes of hydraulic fractures: inference of fracture geometry from resonant frequencies and attenuation. J Geophys Res 120:1080–1107. https://doi.org/10.1002/2014JB011286
Liszka L, Garces MA (2002) Infrasonic observations of the Hekla eruption of February 26, 2000. J Low Freq Noise Vibration and Active Control 21(1):1–8
Liu X, Xu J, Yue J, Kogure M (2022). Strong gravity waves associated with Tonga volcano eruption revealed by SABER observations. Geophys Res Lett 49:e2022GL098339. https://doi.org/10.1029/2022GL098339
Lockhart AB, Murray TL, Furukawa BT (1992) Operating low-power telemetry networks in severe environments. In: Monitoring volcanoes: techniques and strategies used by the staff of the Cascades Volcano Observatory, 1980–90. USGS Bull 1966. https://doi.org/10.3133/b1966_1992
Lockhart AB, Marcial S, Ambubuyog G, Laguerta EP, Power JA, Newhall CG, Punongbayan RS (1996) Installation, operation, and technical specifications of the first Mount Pinatubo telemetered seismic network. In: Newhall CG, Punongbayan S (eds) Fire and mud. University of Washington Press, pp 215-223
Lonzaga JB, Waxler RM, Assink JD, Talmadge CL (2015) Modelling waveforms of infrasound arrivals from impulsive sources using weakly non-linear ray theory. Geophys J Int 200(3):1347–1361
Lopez T, Fee D, Prata F, Dehn J (2013) Characterization and interpretation of volcanic activity at Karymsky Volcano, Kamchatka, Russia, using observations of infrasound, volcanic emissions, and thermal imagery. Geochem Geophys Geosyst 14(12):5106–5127. https://doi.org/10.1002/2013GC004817
Lyons JJ, Ichihara M, Kurokawa A, Lees JM (2013) Switching between seismic and seismo-acoustic harmonic tremor simulated in the laboratory: insights into the role of open degassing channels and magma viscosity. J Geophys Res Solid Earth 118:277–289. https://doi.org/10.1002/jgrb.50067
Lyons JJ, Haney MM, Werner C, Kelly P, Patrick M, Kern C, Trusdell F (2016) Long period seismicity and very long period infrasound driven by shallow magmatic degassing at Mount Pagan, Mariana Islands. J Geophys Res 121:188–209. https://doi.org/10.1002/2015JB012490
Lyons JJ, Haney MM, Fee D, Wech AG, Waythomas CF (2019) Infrasound from giant bubbles during explosive submarine eruptions. Nature Geo 12(11):952–958. https://doi.org/10.1038/s41561-019-0461-0
Lyons JJ, Iezzi AM, Fee D, Schwaiger HF, Wech AG, Haney MM (2020) Infrasound generated by the 2016–2017 shallow submarine eruption of Bogoslof volcano. Alaska Bull Volcanol 82(2):1–14. https://doi.org/10.1007/s00445-019-1355-0
Lyons JJ, Dietterich HR, Patrick MP, Fee D (2021) High-speed lava flow infrasound from Kīlauea’s fissure 8 and its utility in monitoring effusion rate. Bull Volcanol 83(11):1–12
Macdonald GA (1954) Activity of Hawaiian volcanoes during the years 1940–1950. Bull Volcanol 15(1):119–179. https://doi.org/10.1007/BF02596001
MacGregor AG (1949) Prediction in relation to seismo-volcanic phenomena in the Caribbean volcanic arc. Bull Volcanol 8(1):69–86. https://doi.org/10.1007/BF02596780
Maeda Y, Kumagai H (2013) An analytical formula for the longitudinal resonance frequencies of a fluid-filled crack. Geophys Res Lett 40(19):5108–5112. https://doi.org/10.1002/grl.51002
Maeda Y, Kumagai H (2017) A generalized equation for the resonance frequencies of a fluid-filled crack. Geophys J Int 209(1):192–201. https://doi.org/10.1093/gji/ggx019
Maeda Y, Takeo M, Ohminato T (2011) A waveform inversion including tilt: method and simple tests. Geophys J Int 184:907–918. https://doi.org/10.1111/j.1365-246X.2010.04892.x
Maeda Y, Kumagai H, Lacson R Jr, Figueroa MS, Yamashina T (2013) Source process of long-period seismic events at Taal volcano, Philippines: vapor transportation and condensation in a shallow hydrothermal fissure. J Geophys Res: Solid Earth 118(6):2832–2846
Maeda Y, Kato A, Yamanaka Y (2017) Modeling the dynamics of a phreatic eruption based on a tilt observation: barrier breakage leading to the 2014 eruption of Mount Ontake, Japan. J Geophys Res 122:1007–1024. https://doi.org/10.1002/2016JB013739
Maher SP, Matoza RS, de Groot-Hedlin C, Kim K, Gee KL (2021) Evaluating the applicability of a screen diffraction approximation to local volcano infrasound. Volcanica 4(1):67–85. https://doi.org/10.30909/vol.04.01.6785
Maher SP, Matoza RS, Jolly A, de Groot-Hedlin C, Gee KL, Fee D, Iezzi AM (2022) Evidence for near-source nonlinear propagation of volcano infrasound from Strombolian explosions at Yasur volcano, Vanuatu. Bull Volcanol 84:41. https://doi.org/10.1007/s00445-022-01552-w
Maher SP, Matoza RS, de Groot‐Hedlin CD, Gee KL, Fee D, Yokoo A (2020) Investigating spectral distortion of local volcano infrasound by nonlinear propagation at Sakurajima Volcano, Japan. J Geophys Res 125: e2019JB018284. https://doi.org/10.1029/2019JB018284
Malfante M, Dalla Mura M, Métaxian JP, Mars JI, Macedo O, Inza A (2018) Machine learning for volcano-seismic signals: challenges and perspectives. IEEE Signal Process Mag 35(2):20–30
Malone S (1995) Seismology and the information super-highway. Seismol Res Lett 66(1):28–30
Malone SD (2020) Recovering analog-tape seismograms from the 1980 Mount St. Helens pre-eruption period. Seismol Res Lett 91(3):1430–1440. https://doi.org/10.1785/0220190327
Malone SD, Endo ET, Weaver CJ, Ramey JW (1981) Seismic monitoring for eruption prediction. USGS Prof Pap 1250:803–814. https://doi.org/10.3133/pp1250
Malone SD, Boyko C, Weaver CS (1983) Seismic precursors to the Mount St. Helens eruptions in 1981 and 1982. Science 221(4618): 1376–1378. https://doi.org/10.1126/science.221.4618.1376
Malone SD, Buland R, Presgrave B, Ellsworth W, Michael A, Ahern T (1993) Rapid exchange of seismic data between international, national and regional networks using the Internet. EOSV74 N 16:216
Malone SD (1983) Volcanic earthquakes: examples from Mount St. Helens. Earthquakes: Observations, Theory and Interpretation. In: Kanamori H, Boschi E (eds) Earthquakes - observation, theory and interpretation, Pro Int School Phys "Enrico Fermi," Course 85, North Holland Publishing Co, New York, pp 436-455
Malone SD (1990) Mount St. Helens, the 1980 re-awakening and continuing seismic activity. Geoscience Canada, 17(3). Retrieved from https://journals.lib.unb.ca/index.php/GC/article/view/3667
Manga M, Brodsky E (2006) Seismic triggering of eruptions in the far field: volcanoes and geysers. Annu Rev Earth Planet Sci 34:263–291
Marchetti E, Ripepe M, Harris AJL, Delle Donne D (2009) Tracing the differences between Vulcanian and Strombolian explosions using infrasonic and thermal radiation energy. Earth Planet Sci Lett 279(3):273–281. https://doi.org/10.1016/j.epsl.2009.01.004
Marchetti E, Ripepe M, Delle Donne D, Genco R, Finizola A, Garaebiti E (2013) Blast waves from violent explosive activity at Yasur Volcano. Vanuatu Geophys Res Lett 40(22):5838–5843. https://doi.org/10.1002/2013GL057900
Marchetti E, Ripepe M, Campus P, Le Pichon A, Brachet N, Blanc E, Gaillard P, Mialle P, Husson P (2019) Infrasound monitoring of volcanic eruptions and contribution of ARISE to the volcanic ash advisory centers. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies, 2nd edn. Springer, Dordrecht, pp 1141–1162. https://doi.org/10.1007/978-3-319-75140-5_36
Martini M, Giannini L, Capaccioni B (1991) Geochemical and seismic precursors to volcanic activity. Acta Volcanol 1:7–11
Martini M, Giudicepietro F, D’Auria L, Esposito AM, Caputo T, Curciotti R, De Cesare W, Orazi M, Scarpato G, Caputo A (2007) Seismological monitoring of the February 2007 effusive eruption of the Stromboli volcano. Ann Geophys 50(6):775–788. https://doi.org/10.4401/ag-3056
Martire L, Martin R, Brissaud Q, Garcia RF (2022) SPECFEM2D-DG, an open source software modeling mechanical waves in coupled solid-fluid systems: the Linearised Navier-Stokes approach. Geophys J Int 228(1):664–697. https://doi.org/10.1093/gji/ggab308
Marty J (2019) The IMS Infrasound Network: current status and technological developments. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Cham, 3–62. https://doi.org/10.1007/978-3-319-75140-5_1
Matoza RS (2020) Seismicity from the deep magma system. Science 368(6492):708–709. https://doi.org/10.1126/science.abc2452
Matoza RS, Fee D (2014) Infrasonic component of volcano-seismic eruption tremor. Geophys Res Lett 41:1964–1970. https://doi.org/10.1002/2014GL059301
Matoza RS, Fee D (2018) The inaudible rumble of volcanic eruptions. Acoust Today 14(1):17–25
Matoza RS, Hedlin MAH, Garces MA (2007) An infrasound array study of Mount St. Helens. J Volcanol Geotherm Res 160:249–262. https://doi.org/10.1016/j.jvolgeores.2006.10.006
Matoza RS, Fee D, Garces MA, Seiner JM, Ramon PA, Hedlin MAH (2009a) Infrasonic jet noise from volcanic eruptions. Geophys Res Lett 36:L08303. https://doi.org/10.1029/2008GL036486
Matoza RS, Garces MA, Chouet BA, D’Auria L, Hedlin MAH, De Groot-Hedlin C, Waite GP (2009b) The source of infrasound associated with long-period events at Mount St. Helens. J Geophys Res 114:B04305. https://doi.org/10.1029/2008JB006128
Matoza RS, Fee D, Garces MA (2010) Infrasonic tremor wavefield of the Pu`u O`o crater complex and lava tube system, Hawaii, in April 2007. J Geophys Res 115:B12312. https://doi.org/10.1029/2009JB007192
Matoza RS, Le Pichon A, Vergoz J, Herry P, Lalande J, Lee H, Che I, Rybin A (2011a) Infrasonic observations of the June 2009 Sarychev Peak eruption, Kuril Islands: implications for infrasonic monitoring of remote explosive volcanism. J Volcanol Geotherm Res 200:35–48. https://doi.org/10.1016/j.jvolgeores.2010.11.022
Matoza RS, Vergoz J, Le Pichon A, Ceranna L, Green DN, Evers LG, Ripepe M, Campus P, Liszka L, Kvaerna T, Kjartansson E, Hoskuldsson A (2011b) Long-range acoustic observations of the Eyjafjallajökull eruption, Iceland, April–May 2010. Geophys Res Lett 38:L06308. https://doi.org/10.1029/2011GL047019
Matoza RS, Fee D, Neilsen TB, Gee KL, Ogden DE (2013a) Aeroacoustics of volcanic jets: acoustic power estimation and jet velocity dependence. J Geophys Res 118:6269–6284. https://doi.org/10.1002/2013JB010303
Matoza RS, Landès M, Le Pichon A, Ceranna L, Brown D (2013b) Coherent ambient infrasound recorded by the International Monitoring System. Geophys Res Lett 40:429–433. https://doi.org/10.1029/2012GL054329
Matoza RS, Shearer PM, Okubo PG (2014a) High-precision relocation of long-period events beneath the summit region of Kilauea Volcano, Hawai`i, from 1986 to 2009. Geophys Res Lett 41:3413–3421. https://doi.org/10.1002/2014GL059819
Matoza RS, Fee D, Lopez TM (2014b) Acoustic characterization of explosion complexity at Sakurajima, Karymsky, and Tungurahua Volcanoes. Seismol Res Lett 85(6):1187–1199. https://doi.org/10.1785/0220140110
Matoza RS, Chouet BA, Dawson PB, Shearer PM, Haney MM, Waite GP, Moran SC, Mikesell TD (2015) Source mechanism of small long-period events at Mount St. Helens in July 2005 using template matching, phase-weighted stacking, and full-waveform inversion. J Geophys Res 120:6351–6364. https://doi.org/10.1002/2015JB012279
Matoza RS, Green DN, Le Pichon A, Shearer PM, Fee D, Mialle P, Ceranna L (2017) Automated detection and cataloging of global explosive volcanism using the International Monitoring System infrasound network. J Geophys Res 122:2946–2971. https://doi.org/10.1002/2016JB013356
Matoza RS, Fee D, Green DN, Le Pichon A, Vergoz J, Haney MM, Mikesell TD, Franco L, Valderrama OA, Kelley MR, McKee K, Ceranna L (2018) Local, regional, and remote seismo-acoustic observations of the April 2015 VEI 4 eruption of Calbuco volcano, Chile. J Geophys Res 123:3814–3827. https://doi.org/10.1002/2017JB015182
Matoza RS, Arciniega-Ceballos A, Sanderson RW, Mendo-Pérez G, Rosado-Fuentes A, Chouet BA (2019b) High-broadband seismoacoustic signature of Vulcanian explosions at Popocatépetl volcano, Mexico. Geophys Res Lett 46:148–157. https://doi.org/10.1029/2018GL080802
Matoza RS, Chouet BA, Jolly AD, Dawson PB, Fitzgerald RH, Kennedy BM, Fee D, Iezzi AM, Kilgour GN, Garaebiti E, Cevuard S (2022a) High-rate very-long-period seismicity at Yasur volcano, Vanuatu: source mechanism and decoupling from surficial explosions and infrasound. Geophys J Int 230(1):392–426. https://doi.org/10.1093/gji/ggab533
Matoza RS, Fee D, Assink JD, Iezzi AM, Green DN, Kim K, Toney L, Lecocq T, Krishnamoorthy S, Lalande J-M, Nishida K, Gee KL, Haney MM, Ortiz HD, Brissaud Q, Martire L, Rolland L, Vergados P, Nippress A, Park J, Shani-Kadmiel S, Witsil A, Arrowsmith S, Caudron C, Watada S, Perttu AB, Taisne B, Mialle P, Le Pichon A, Vergoz J, Hupe P, Blom PS, Waxler R, De Angelis S, Snively JB, Ringler AT, Anthony RE, Jolly AD, Kilgour G, Averbuch G, Ripepe M, Ichihara M, Arciniega-Ceballos A, Astafyeva E, Ceranna L, Cevuard S, Che I-Y, De Negri R, Ebeling CW, Evers LG, Franco-Marin LE, Gabrielson TB, Hafner K, Harrison RG, Komjathy A, Lacanna G, Lyons J, Macpherson KA, Marchetti E, McKee KF, Mellors RJ, Mendo-Pérez G, Mikesell TD, Munaibari E, Oyola-Merced M, Park I, Pilger C, Ramos C, Ruiz MC, Sabatini R, Schwaiger HF, Tailpied D, Talmadge C, Vidot J, Webster J, Wilson DC (2022b) Atmospheric waves and global seismoacoustic observations of the January 2022 Hunga eruption, Tonga. Science 377(6601):95-100. https://doi.org/10.1126/science.abo7063
Matoza RS, Chouet BA (2010), Subevents of long-period seismicity: implications for hydrothermal dynamics during the 2004–2008 eruption of Mount St. Helens. J Geophys Res 115:B12206. https://doi.org/10.1029/2010JB007839
Matoza R, Fee D, Green D, Mialle P (2019a) Volcano infrasound and the International Monitoring System. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies, 2nd edn. Springer, Dordrecht, pp 1023–1077. https://doi.org/10.1007/978-3-319-75140-5_33
Matoza RS, Okubo PG, Shearer PM (2021) Comprehensive high-precision relocation of seismicity on the Island of Hawai'i 1986–2018. Ear Space Sci 8: e2020EA001253. https://doi.org/10.1029/2020EA001253
Matsuzawa T (1953) Feldtheorie der Erdbeben. Bull Earthquake Res Inst Tokyo Univ 31:179–201
Mattia M, Palano M, Aloisi M, Bruno V, Bock Y (2008) High rate GPS data on active volcanoes: an application to the 2005–2006 Mt. Augustine (Alaska, USA) eruption. Terra Nova 20(2): 134–140. https://doi.org/10.1111/j.1365-3121.2008.00798.x
Mauk FJ (1983) Utilization of seismically recorded infrasonic-acoustic signals to monitor volcanic explosions: The El Chichon Sequence 1982–A case study. J Geophys Res 88(B12):10385–10401. https://doi.org/10.1029/JB088iB12p10385
McCormack D, Bass H, Garcés M, Yepes H (2005) Acoustic surveillance for hazardous eruptions (ASHE). J Acous Soc Am 117(4):2419–2419. https://doi.org/10.1121/1.4786426
McKee K, Fee D, Yokoo A, Matoza RS, Kim K (2017) Analysis of gas jetting and fumarole acoustics at Aso Volcano, Japan. J Volcanol Geotherm Res 340:16–29. https://doi.org/10.1016/j.jvolgeores.2017.03.029
McKee K, Smith C, Reath K, Snee E, Maher S, Matoza RS, Carn S, Mastin L, Anderson K, Damby D, Roman D, Degterev A, Rybin A, Chibisova M, Assink J, de Negri LR, Perttu A (2021) Evaluating the state-of-the-art in remote volcanic eruption characterization Part I: Raikoke volcano, Kuril Islands. J Volcanol Geotherm Res 419:107354. https://doi.org/10.1016/j.jvolgeores.2021.107354
McNutt SR (2005) Volcanic seismology. Annu Rev Ear Plan Sci 32:461–491. https://doi.org/10.1146/annurev.earth.33.092203.122459
McNutt SR, Nishimura T (2008) Volcanic tremor during eruptions: temporal characteristics, scaling and constraints on conduit size and processes. J Volcanol Geotherm Res 178:10–18. https://doi.org/10.1016/j.jvolgeores.2008.03.010
McNutt SR, Williams ER (2010) Volcanic lightning: global observations and constraints on source mechanisms. Bull Volcanol 72:1153–1167. https://doi.org/10.1007/s00445-010-0393-4
McNutt SR, Roman DC (2015) Volcanic seismicity. In: The encyclopedia of volcanoes. Academic Press, Chicago, pp 1011–1034. https://doi.org/10.1016/b978-0-12-385938-9.00059-6
McNutt SR, Thompson G, Johnson J, De Angelis S, Fee D (2015) Seismic and infrasonic monitoring. In: The encyclopedia of volcanoes. Academic Press, Chicago, pp 1071–1099. https://doi.org/10.1016/b978-0-12-385938-9.00063-8
McNutt SR (1992) Volcanic tremor. In: Nierenberg WA (ed) Encyclopedia of earth system science 4. Academic Press, San Diego, pp 417–425
McNutt SR (1996) Seismic monitoring and eruption forecasting of volcanoes: a review of the state-of-the-art and case histories. In: Scarpa R, Tilling RI (Eds) Monitoring and mitigation of volcano hazards. Springer-Verlag, New York, pp 99–146
Médici EF, Waite GP (2016) Experimental laboratory study on the formation of multiple shock waves observed during volcanic eruptions. Geophys Res Lett 43(1):85–92
Médici EF, Allen JS, Waite GP (2014) Modeling shock waves generated by explosive volcanic eruptions. Geophys Res Lett 41(2):414–421
Metz D, Watts AB, Grevemeyer I, Rodgers M, Paulatto M (2016) Ultra-long-range hydroacoustic observations of submarine volcanic activity at Monowai, Kermadec Arc. Geophys Res Lett 43(4):1529–1536. https://doi.org/10.1002/2015GL067259
Metz D, Grevemeyer I (2018) Hydroacoustic measurements of the 2014 eruption at Ahyi volcano, 20.4°N Mariana Arc. Geophys Res Lett 45, 11,050– 11,058. https://doi.org/10.1029/2018GL079983
Minakami T (1950) On explosive activities of andesitic volcanoes and their forerunning phenomena. Bull Volcanol 10:59–87. https://doi.org/10.1007/BF02596077
Minakami T (1960) Fundamental research for predicting volcanic eruptions, Part I. Bull Earthquake Res Inst Tokyo Univ 38:497–544
Minakami T (1961) Study of eruptions and earthquakes originating from volcanoes (part 1 of 3). Statistical relations between eruptions and earthquakes of Asama volcano. Int Geol Rev 3(8):712–719
Minakami T (1974) Seismology of volcanoes in Japan. Develop Solid Ear Geophys 6:1–27. https://doi.org/10.1016/b978-0-444-41141-9.50007-3
Mogi K (1962) Study of elastic shocks caused by the fracture of heterogeneous materials and its relations to earthquake phenomena. Bull Earthquake Res Inst Tokyo Univ 40(125):196
Molina I, Kumagai H, Yepes H (2004) Resonances of volcanic conduit triggered by repeated injections of ash-laden gas. Geophys Res Lett 31:L03603. https://doi.org/10.1029/2003GL018934
Moore SV, Hutt CR, Anthony RE, Ringler AT, Alejandro ACB, Wilson DC (2018) A collection of historic seismic instrumentation photographs at the Albuquerque Seismological Laboratory. Seismol Res Lett 90(2A):765–773. https://doi.org/10.1785/0220180267
Moran SC, Newhall C, Roman DC (2011) Failed magmatic eruptions: late-stage cessation of magma ascent. Bull Volcanol 73(2):115–122. https://doi.org/10.1007/s00445-010-0444-x
Moran SC, Freymueller JT, LaHusen RG, McGee KA, Poland MP, Power JA, Schmidt DA, Schneider DJ, Stephens G, Werner CA, White RA (2008a) Instrumentation recommendations for volcano monitoring at US volcanoes under the National Volcano Early Warning System. US Geol Surv Sci Investig Rep 5114. https://doi.org/10.3133/sir20085114
Moran SC, Malone SD, Qamar AI, Thelen W, Wright AK, Caplan-Auerbach J (2008b) 2004–2005 seismicity associated with the renewed dome-building eruption of Mount St. Helens. In: Sherrod DR, Scott WE, Stauffer PF (eds) A volcano rekindled: the renewed eruption of Mount St. Helens, 2004–2006, US Geol Surv Prof Pap 1750:27–60. https://doi.org/10.3133/pp17502
Moran SC, Matoza RS, Garces MA, Hedlin MAH, Bowers D, Scott WE, Sherrod DR, Vallance JW (2008c) Seismic and acoustic recordings of an unusually large rockfall at Mount St. Helens, Washington. Geophys Res Lett 35:L19302. https://doi.org/10.1029/2008GL035176
Moretti L, Mangeney A, Capdeville Y, Stutzmann E, Huggel C, Schneider D, Bouchut F (2012) Numerical modeling of the Mount Steller landslide flow history and of the generated long period seismic waves. Geophys Res Lett 39:L16402. https://doi.org/10.1029/2012GL052511.
Morrissey MM, Chouet BA (1997) Burst conditions of explosive volcanic eruptions recorded on microbarographs. Science 275(5304):1290–1293. https://doi.org/10.1126/science.275.5304.1290
Morrissey MM, Chouet BA (2001) Trends in long-period seismicity related to magmatic fluid compositions. J Volcanol Geotherm Res 108:265–281. https://doi.org/10.1016/S0377-0273(00)00290-0
Murray TL (1992) A low-data-rate digital telemetry system, in Monitoring volcanoes: techniques and strategies used by the staff of the Cascades Volcano Observatory, 1980–90. USGS Bull 1966 https://doi.org/10.3133/b1966_1992
Nakamichi H, Kumagai H, Nakano M, Okubo M, Kimata F, Ito Y, Obara K (2009) Source mechanism of very-long-period event at Mt Ontake, Central Japan: Response of a hydrothermal system to magma intrusion beneath the summit. J Volcanol Geotherm Res 187:167–177
Nakano M, Kumagai H (2005) Waveform inversion of volcano-seismic signals assuming possible source geometries. Geophys Res Lett 32:L12302. https://doi.org/10.1029/2005GL022666
Nakano M, Kumagai H, Kumazawa M, Yamaoka K, Chouet BA (1998) The excitation and characteristic frequency of the long-period volcanic event: an approach based on an inhomogeneous autoregressive model of a linear dynamic system. J Geophys Res 103:10031–10046. https://doi.org/10.1029/98JB00387
Nakano M, Kumagai H, Chouet BA (2003) Source mechanism of long-period events at Kusatsu-Shirane Volcano, Japan, inferred from waveform inversion of the effective excitation functions. J Volcanol Geotherm Res 122:149–164. https://doi.org/10.1016/S0377-0273(02)00499-7
Narváez ML, Torres CRA, Gómez MDM, Cortés JGP, Cepeda VH, Stix J (1997) ‘Tornillo’-type seismic signals at Galeras volcano, Colombia, 1992–1993. J Volcanol Geoth Res 77(1–4):159 171
National Academies of Sciences, Engineering, and Medicine (2017) Volcanic eruptions and their repose, unrest, precursors, and timing. The National Academies Press, Washington, DC. https://doi.org/10.17226/24650
Neal CA, Brantley SR, Antolik L, Babb JL, Burgess M, Calles K, Cappos M, Chang JC, Conway S, Desmither L, Dotray P et al (2019) The 2018 rift eruption and summit collapse of Kīlauea Volcano. Science 363(6425):367–374
Neuberg J, Luckett R, Ripepe M, Braun T (1994) Highlights from a seismic broadband array on Stromboli Volcano. Geophys Res Lett 21:749–752. https://doi.org/10.1029/94GL00377
Neuberg J, Baptie B, Luckett R, Stewart R (1998) Results from the broadband seismic network on Montserrat. Geophys Res Lett 25(19):3661–3664. https://doi.org/10.1029/98GL01441
Neuberg J, Luckett R, Baptie B, Olsen K (2000) Models of tremor and low-frequency earthquake swarms on Montserrat. J Volcanol Geotherm Res 101:83–104. https://doi.org/10.1016/S0377-0273(00)00169-4
Neuberg JW, Tuffen H, Collier L, Green D, Powell T, Dingwell D (2006) The trigger mechanism of low-frequency earthquakes on Montserrat. J Volcanol Geoth Res 153:37–50
Neuberg JW, Taisne B, Burton M, Ryan GA, Calder E, Fournier N, Collinson ASD (2022) A review of tectonic, elastic and visco-elastic models exploring the deformation patterns throughout the eruption of Soufrière Hills volcano on Montserrat, West Indies. J Volcanol Geoth Res 425:107518
Neuberg JW (2011) Earthquakes, volcanogenic. In: Gupta, H.K., et al. (Ed.), Encyclopedia of Solid Earth Geophysics. Springer, pp. 261–269
Newhall CG, Self S (1982) The volcanic explosivity index (VEI) an estimate of explosive magnitude for historical volcanism. J Geophys Res 87(C2):1231–1238. https://doi.org/10.1029/JC087iC02p01231
Nief G, Talmadge C, Rothman J, Gabrielson T (2019) New generations of infrasound sensors: technological developments and calibration. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Cham. Pp 63–89. https://doi.org/10.1007/978-3-319-75140-5_2
Nishida K, Ichihara M (2016) Real-time infrasonic monitoring of the eruption at a remote island volcano using seismoacoustic cross correlation. Geophysical Journal International, 204(2):748–752 https://doi.org/10.1093/gji/ggv478
Nishimura T, Nakamichi H, Tanaka S, Sato M, Kobayashi T, Ueki S, Hamaguchi H, Ohtake M, Sato H (2000) Source process of very long period seismic events associated with the 1998 activity of Iwate Volcano, northeastern Japan. J Geophys Res 105:19135–19147
Nishimura T, Iguchi M (2011) Volcanic earthquakes and tremor in Japan. Kyoto University Press, Kyoto
Nishimura T, Fujiwara S, Murakami M, Tobita M, Nakagawa H, Sagiya T, Tada T (2001) The M6.1 earthquake triggered by volcanic inflation of Iwate volcano, northern Japan, observed by satellite radar interferometry. Geophys Res Lett 28(4): 635–638. https://doi.org/10.1029/2000GL012022
Norris RD (1991) The Cascade volcanoes: monitoring history and current land management. US Geol Surv Open-File Rep 91-31.https://doi.org/10.3133/ofr9131
Obermann A, Lupi M, Mordret A, Jakobsdóttir SS, Miller SA (2016) 3D-ambient noise Rayleigh wave tomography of Snæfellsjökull volcano, Iceland. J Volcanol Geotherm Res 317:42–52. https://doi.org/10.1016/j.jvolgeores.2016.02.013
Manila Observatory (2016) Manila observatory exhibition: discoveries (1865–1945). http://www.observatory.ph/2016/02/26/manila-observatory-exhibition-discoveries-1865-1945/. Accessed 21 March 2022
Ohminato T (2006) Characteristics and source modeling of broadband seismic signals associated with the hydrothermal system at Satsuma-Iwojima volcano, Japan. J Volcanol Geoth Res 158:467–490
Ohminato T, Chouet BA, Dawson PB, Kedar S (1998a) Waveform inversion of very-long-period impulsive signals associated with magmatic injection beneath Kilauea Volcano, Hawaii. J Geophys Res 103:23839–23862
Ohminato T, Chouet BA, Dawson PB, Kedar S (1998b) Waveform inversion of very-long-period impulsive signals associated with magmatic injection beneath Kilauea Volcano, Hawaii. J Geophys Res 103:23839–23862. https://doi.org/10.1029/98JB01122
Okubo PG, Nakata JS, Koyanagi RY, Poland MP, Takahashi TJ, Landowski CM (2014) The evolution of seismic monitoring systems at the Hawaiian Volcano Observatory. US Geol Surv Prof Pap 1801:67–94. https://doi.org/10.3133/pp18012
Omer GC (1950) Volcanic tremor (Part two: the theory of volcanic tremor). Bull Seismol Soc Am 40:175–194. https://doi.org/10.1785/BSSA0400030175
Omira R, Ramalho RS, Kim J, González PJ, Kadri U, Miranda JM, Carrilho F, Baptista MA (2022) Global Tonga tsunami explained by a fast-moving atmospheric source. Nature : 1–2
Omori F (1894) On after-shocks of earthquakes. J Coll Sci Imp Univ Tokyo 7:111–200
Omori F (1899) Horizontal pendulums for the mechanical registration of seismic and other earth movements. J Coll Sci Imp Univ Tokyo 11(3):121–145
Omori F (1908) On micro-tremors, Bull Imp Earthq Inv Comm 2(1): 1–6. https://ci.nii.ac.jp/naid/110006606464/
Omori F (1911) The Usu-san eruption and earthquake and elevation phenomena. Bull Imp Earthq Inv Comm 5: 1–38. https://ci.nii.ac.jp/naid/10011105255/
Omori F (1912) The eruptions and earthquakes of the Asama-Yama. Bull Imp Earthq Inv Comm 6(3): 227–257. https://ci.nii.ac.jp/naid/110006606508/
Omori F (1914) Remarks on the seismographical observations of the Asama-Yama eruptions at Yuno-Taira, Ashino-Taira, and the Asama pasture ground (the eruptions and earthquakes of the Asama-Yama IV, [Strong Asama-yama Outbursts, Dec. 1912 to May 1914]). Bull Imp Earthq Inv Comm 7(1): 133–158. https://ci.nii.ac.jp/naid/110006606517
Omori F (1916) The Sakura-Jima eruptions and earthquakes, II. Bull Imp Earthq Inv Comm 8: 5–152. https://ci.nii.ac.jp/naid/10003670193/
Orazi M, D’Auria L, Tramelli A, Buonocunto C, Capello M, Caputo A, De Cesare W, Giudicepietro F, Martini M, Peluso R, Scarpato G (2013) The seismic monitoring network of Mt. Vesuvius. Ann Geophys 56(4):S0450–S0450
Ortiz H, Johnson J, Ramón P, Ruiz M (2018) Using infrasound waves to monitor tropospheric weather and crater morphology changes at Tungurahua Volcano, Ecuador. J Volcanol Geoth Res 349:205–2016. https://doi.org/10.1016/j.jvolgeores.2017.11.001
Ortiz H, Matoza R, Johnson J, Hernandez S, Anzieta J, Ruiz M (2021) Autocorrelation infrasound interferometry. J Geophys Res: Solid Earth, 126, e2020JB020513. https://doi.org/10.1029/2020JB020513
Oshima H, Maekawa T (2001) Excitation process of infrasonic waves associated with Merapi-type pyroclastic flow as revealed by a new recording system. Geophys Res Lett 28:1099–1102. https://doi.org/10.1029/1999GL010954
Otsuka S (2022) Visualizing Lamb waves from a volcanic eruption using meteorological satellite Himawari‐8. Geophys Res Lett 49(8):e2022GL098324
Padrón E, Hernández PA, Carmona E, Pérez NM, Melián G, Sumino H, Almendros J, Kusakabe M, Wakita H, Padilla GD (2015) Geochemical evidence of different sources of long-period seismic events at Deception volcano, South Shetland Islands. Antarctica Antarctic Science 27(6):557–565
Pallister JS, Cashman KV, Hagstrum JT, Beeler NM, Moran SC, Denlinger RP (2012) Faulting within the Mount St. Helens conduit and implications for volcanic earthquakes. Geol Soc Am Bull 125(3–4): 359–376. https://doi.org/10.1130/B30716.1
Palmieri L (1859) Origine e presenti condizioni dell’Osservatorio. Capitolo Primo, Annali del Reale Osservatorio Meteorologico Vesuviano anno I. Napoli: Capitolo, 9–23.
Palo M, Ibanez JM, Cisneros M, Bretón M, Del Pezzo E, Ocana E, Orozco-Rojas J, Posadas AM (2009) Analysis of the seismic wavefield properties of volcanic explosions at Volcan de Colima, Mexico: insights into the source mechanism. Geophys J Int 177:1383–1398
Park I, Jolly A, Kim KY, Kennedy B (2019) Temporal variations of repeating low frequency volcanic earthquakes at Ngauruhoe Volcano, New Zealand. J Volcanol Geoth Res 373:108–119
Park I, Jolly A, Matoza RS, Kennedy B, Kilgour G, Johnson R, Garaebiti E, Cevuard S (2021) Seismo-acoustic characterization of the 2018 Ambae (Manaro Voui) eruption, Vanuatu. Bull Volcanol 83:60. https://doi.org/10.1007/s00445-021-01474-z
Patanè D, Di Grazia G, Cannata A, Montalto P, Boschi E (2008) Shallow magma pathway geometry at Mt. Etna volcano. Geochem Geophys Geosystem 9:Q12021. https://doi.org/10.1029/2008GC002131
Patrick MR, Smellie JL (2013) Synthesis A spaceborne inventory of volcanic activity in Antarctica and southern oceans, 2000–10. Antarct Sci 25(4):475–500
Patrick MR, Orr T, Sutton AJ, Lev E, Thelen W, Fee D (2016) Shallowly driven fluctuations in lava lake outgassing (gas pistoning), Kīlauea Volcano. Earth Planet Sci Lett 433:326–338
Patrick MR, Dietterich HR, Lyons JJ, Diefenbach AK, Parcheta C, Anderson KR, Namiki A, Sumita I, Shiro B, Kauahikaua JP (2019) Cyclic lava effusion during the 2018 eruption of Kīlauea Volcano. Science, 366(6470):eaay9070
Pekeris CL (1939) The propagation of a pulse in the atmosphere. Proc Roy Soc Lon A 171(947):434–449. https://doi.org/10.1098/rspa.1939.0076
Pérez-Campos X, Espíndola VH, Pérez J, Estrada JA, Monroy CC, Bello D, González-López A, Ávila DG, Esparza MGCR, Maldonado R, Tan Y (2018) The Mexican national seismological service: an overview. Seismol Res Lett 89(2A):318–323. https://doi.org/10.1785/0220170186
Pérez-Campos X, Armendáriz-Sánchez S, Espíndola VH, Castro-Escamilla M, Perez P, Manuel Casiano L, Rodriguez Rasilla I, Cárdenas Monroy C, Cárdenas A (2020) Preservation and reuse of historical seismic data in Mexico: SISMOMex and the Online “National Seismogram Library.” Seismol Res Lett 91(3):1482–1487. https://doi.org/10.1785/0220190340
Perret FA (1939) The volcano-seismic crises at Montserrat, 1933–1937. Carnegie Inst Wash Publ 512, Washington DC.
Perret FA (1950) Volcanological observations. Carnegie Inst Wash Publ 549, Washington DC.
Perttu A, Corentin Caudron JD, Assink D, Metz D, Tailpied B, Perttu CH et al (2020a) Reconstruction of the 2018 tsunamigenic flank collapse and eruptive activity at Anak Krakatau based on eyewitness reports, seismo-acoustic and satellite observations. Earth Planet Sci Lett 541:116268
Perttu A, Taisne B, De Angelis S, Assink JD, Tailpied D, Williams RA (2020b) Estimates of plume height from infrasound for regional volcano monitoring. J Volcanol Geoth Res 402:106997
Petersen T, McNutt SR (2007) Seismo-acoustic signals associated with degassing explosions recorded at Shishaldin Volcano, Alaska, 2003–2004. Bull Volcanol 69:527–536. https://doi.org/10.1007/s00445-006-0088-z
Philippine Geodetic & Geophysical Institute (1952) A preliminary report on the recent eruptions of Hibok-Hibok volcano, Camiguin Island, Philippines. Bull Volcanol 12:215–225. https://doi.org/10.1007/BF02596023
Pierce AD (1963) Propagation of acoustic-gravity waves from a small source above the ground in an isothermal atmosphere. J Acoust Soc Am 35(11):1798–1807. https://doi.org/10.1121/1.1918824
Pierce, A.D. (1981) Acoustics: an introduction to its physical principles and applications. The Acoustical Society of America.
Pinatubo Volcano Observatory Team (1991) Lessons from a major eruption: Mt. Pinatubo, Philippines. Eos Trans AGU 72(49):545–555. https://doi.org/10.1029/90EO00386
Poland MP, Carbone D (2018) Continuous gravity and tilt reveal anomalous pressure and density changes associated with gas pistoning within the summit lava lake of Kīlauea Volcano, Hawai‘i. Geophys Res Lett 45:2319–2327. https://doi.org/10.1002/2017GL076936
Poland MP, de Zeeuw-van DE, Bagnardi M, Johanson IA (2019) Post-collapse gravity increase at the summit of Kīlauea Volcano, Hawaiʻi. Geophys Res Lett 46:14430–14439. https://doi.org/10.1029/2019GL084901
Poland MP, Lopez T, Wright R et al (2020) Forecasting, detecting, and tracking volcanic eruptions from space. Remote Sens Earth Syst Sci 3:55–94. https://doi.org/10.1007/s41976-020-00034-x
Poland M (2015) Volcano monitoring from space. Global volcanic hazards and risk; Loughlin, SC, Sparks, RSJ, Brown, SK, Jenkins, SF, Vye-Brown, C., Eds, 311–316.
Poli P, Shapiro NM (2022) Rapid characterization of large volcanic eruptions: measuring the impulse of the Hunga Tonga Ha’apai explosion from teleseismic waves. Geophys Res Lett 49(8):e2022GL098123
Pollard DD (1987) Elementary fracture mechanics applied to the structural interpretation of dykes. In Mafic dyke swarms 34:5–24
Ponceau D, Bosca L (2010) Low-noise broadband microbarometers. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Dordrecht, pp 119–140. https://doi.org/10.1007/978-1-4020-9508-5_4
Powell CF (1938) The Royal Society expedition to Montserrat, B. W. I. Final Report. Phil Trans Roy Soc Lond A 237:1–34. https://doi.org/10.1098/rsta.1938.0002
Powell TW, Neuberg J (2003) Time dependent features in tremor spectra. J Volcanol Geotherm Res 128:177–185. https://doi.org/10.1016/S0377-0273(03)00253-1
Power JA, Lahr JC, Page RA, Chouet BA, Stephens CD, Harlow DH, Murray TL, Davies JN (1994) Seismic evolution of the 1989–1990 eruption sequence of Redoubt Volcano, Alaska. J Volcanol Geotherm Res 62(1–4):69–94. https://doi.org/10.1016/0377-0273(94)90029-9
Power JA, Haney MM, Botnick SM, Dixon JP, Fee D, Kaufman AM, Ketner DM, Lyons JJ, Parker T, Paskievitch JF, Read CW (2020) Goals and development of the Alaska Volcano Observatory Seismic Network and application to forecasting and detecting volcanic eruptions. Seismol Res Lett 91(2A):647–659. https://doi.org/10.1785/0220190216
Power JA, Lalla DJ (2010) Seismic observations of Augustine Volcano, 1970–2007. In: Power JA, Coombs ML, Freymueller JT (eds) The 2006 eruption of Augustine Volcano, Alaska, USGS Prof Pap 1769–1, pp 3–40. https://doi.org/10.3133/pp17691
Power JA, Jolly AD, Page RA, McNutt SR (1995) Seismicity and forecasting of the 1992 eruptions of Crater Peak vent, Mount Spurr Volcano, Alaska: an overview. In: Keith TEC (ed) The 1992 eruptions of Crater Peak Vent, Mount Spurr, Alaska. US Geol Surv Bull 2139, 149–160. https://doi.org/10.3133/b2139
Prata AJ (2009) Satellite detection of hazardous volcanic clouds and the risk to global air traffic. Nat Hazards 51(2):303–324
Press F, Harkrider D (1962) Propagation of acoustic-gravity waves in the atmosphere. J Geophys Res 67(10):3889–3908. https://doi.org/10.1029/JZ067i010p03889
Press F, Harkrider D (1966) Air-sea waves from the explosion of Krakatoa. Science 154(3754):1325–1327. https://doi.org/10.1126/science.154.3754.1325
Proceedings of the first Pan-Pacific Scientific Conference: Under auspices of the Pan-Pacific Union, Honolulu, Hawaii, August 2 to 20, 1920, Honolulu, Hawaii (1921). Bernice P. Bishop Museum Special Pub 7(1).
Punongbayan RS, Newhall CG (1999) Early warning for the 1991 eruptions of Pinatubo volcano - success story, Proceedings of the WMO/UNESCO Sub-Forum on Science and Technology in support of Natural Disaster Reduction, Geneva, pp 140–149
Quinteros J, Strollo A, Evans PL, Hanka W, Heinloo A, Hemmleb S, Hillmann L, Jaeckel K-H, Kind R, Saul J, Zieke T, Tilmann F (2021) The GEOFON Program in 2020. Seismol Res Lett 92(3):1610–1622. https://doi.org/10.1785/0220200415
Raga AC, Raga GB, Cantó J, Alfonso L (2002) Atmospheric expansion wave simulations of Popocatepetl explosions. J Geophys Res 107(D16): ACL-9. https://doi.org/10.1029/2001JD000693
Ramírez-Herrera MT, Coca O, Vargas-Espinosa V (2022) Tsunami effects on the coast of Mexico by the Hunga Tonga-Hunga Ha’apai Volcano Eruption, Tonga. Pure Appl Geophys 179:1117–1137. https://doi.org/10.1007/s00024-022-03017-9
Ramos EG, Hamburger MW, Pavlis GL, Laguerta EP (1999) The low-frequency earthquake swarms at Mount Pinatubo, Philippines: implications for magma dynamics. J Volcanol Geotherm Res 92(3–4):295–320. https://doi.org/10.1016/S0377-0273(99)00091-8
Ramos EG, Laguerta EP, Hamburger MW (1996) Seismicity and magmatic resurgence at Mount Pinatubo in 1992. In: Newhall CG, Punongbayan S (eds) Fire and mud. University of Washington Press, pp 387-406
Ramsey MS, Harris AJ (2013) Volcanology 2020: how will thermal remote sensing of volcanic surface activity evolve over the next decade? J Volcanol Geoth Res 249:217–233
Rasmussen DJ, Plank TA, Roman DC, Power JA, Bodnar RJ, Hauri EH (2018) When does eruption run-up begin? Multidisciplinary insight from the 1999 eruption of Shishaldin volcano. Earth Planet Sci Lett 486:1–14. https://doi.org/10.1016/j.epsl.2018.01.001
Raspet R, Abbott J-P, Webster J, Yu J, Talmadge C, Alberts II K, Collier S, Noble J (2019) New systems for wind noise reduction for infrasonic measurements. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound Monitoring for Atmospheric Studies. Springer, Cham. Pp 91–124. https://doi.org/10.1007/978-3-319-75140-5_3
Ratdomopurbo A, Poupinet G (2000) An overview of the seismicity of Merapi volcano (Java, Indonesia), 1983–1994. J Volcanol Geotherm Res 100(1–4):193–214. https://doi.org/10.1016/S0377-0273(00)00137-2
Rawson DE (1960) Drilling into molten lava in the Kilauea Iki volcanic crater, Hawaii. Nature 188(4754):930–931
Reed JW (1987) Air-pressure waves from Mount St. Helens eruptions. J Geophys Res Atm 92(D10):11979–11992. https://doi.org/10.1029/JD092iD10p11979
Reid HF (1929) The forces and movements at the earthquake-focus. Eos Trans AGU 10–11(1):43–46. https://doi.org/10.1029/TR010i001p00043
Repetti WC (1946) Seventy-five years of seismology in the Manila Observatory. Eos Trans AGU 27(1):15–18. https://doi.org/10.1029/TR027i001p00015
Repetti WC (1948) The Manila Observatory. Manila Philippines. Edwards Bros, Washington DC
Richards AF (1963) Volcanic sounds, investigation and analysis. J Geophys Res 68:919–928. https://doi.org/10.1029/JZ068i003p00919
Richards PG, Hellweg M (2020) Challenges and opportunities in turning large U.S. archives of analog seismograms into a modern usable resource. Seismol Res Lett 91(3): 1531–1541. https://doi.org/10.1785/0220200053
Richardson JP, Waite GP, Palma JL (2014) Varying seismic-acoustic properties of the fluctuating lava lake at Villarrica volcano, Chile. J Geophys Res 119(7):5560–5573. https://doi.org/10.1002/2014JB011002
Richter, D.H., J.P. Eaton, K.J. Murata, W.U. Ault, and H.L. Krivoy (1970), Chronological narrative of the 1959–60 eruption of Kilauea Volcano, Hawaii, USGS Professional Paper 537-E, doi:https://doi.org/10.3133/pp537E
Ripepe M, Marchetti E (2002) Array tracking of infrasonic sources at Stromboli volcano. Geophys Res Lett 29(22):33–41. https://doi.org/10.1029/2002GL015452
Ripepe M, Poggi P, Braun T, Gordeev E (1996) Infrasonic waves and volcanic tremor at Stromboli. Geophys Res Lett 23(2):181–184. https://doi.org/10.1029/95GL03662
Ripepe M, Ciliberto S, Della Schiava M (2001) Time constraints for modeling source dynamics of volcanic explosions at Stromboli. J Geophys Res 106(B5):8713–8727. https://doi.org/10.1029/2000JB900374
Ripepe M, Harris AJ, Carniel R (2002) Thermal, seismic and infrasonic evidences of variable degassing rates at Stromboli volcano. J Volcanol Geoth Res 118(3–4):285–297
Ripepe M, Marchetti E, Ulivieri G (2007) Infrasonic monitoring at Stromboli volcano during the 2003 effusive eruption: Insights on the explosive and degassing process of an open conduit system. J Geophys Res 112:B09207. https://doi.org/10.1029/2006JB004613
Ripepe M, De Angelis S, Lacanna G, Poggi P, Williams C, Marchetti E, Donne DD, Ulivieri G (2009) Tracking pyroclastic flows at Soufrière Hills Volcano. Eos Trans AGU 90(27):229–230. https://doi.org/10.1029/2009EO270001
Ripepe M, Bonadonna C, Folch A, Delle Donne D, Lacanna G, Marchetti E, Höskuldsson A (2013) Ash-plume dynamics and eruption source parameters by infrasound and thermal imagery: the 2010 Eyjafjallajökull eruption. Earth Planet Sci Lett 366:112–121
Ripepe M, Marchetti E, Delle Donne D, Genco R, Innocenti L, Lacanna G, Valade S (2018) Infrasonic early warning system for explosive eruptions. J Geophys Res 123:9570–9585. https://doi.org/10.1029/2018JB015561
Ripepe M, Marchetti E (2019) Infrasound monitoring of volcano-related hazards for civil protection. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Cham. pp 1107–1140. https://doi.org/10.1007/978-3-319-75140-5_35
Ripepe M, De Angelis S, Lacanna G, Voight B (2010) Observation of infrasonic and gravity waves at Soufrière Hills Volcano, Montserrat. Geophys Res Lett 37: L00E14. https://doi.org/10.1029/2010gl042557
Rodgers M, Roman DC, Geirsson H, LaFemina P, Muñoz A, Guzman C, Tenorio V (2013) Seismicity accompanying the 1999 eruptive episode at Telica Volcano, Nicaragua. J Volcanol Geoth Res 265:39–51
Rodgers M, Rodgers S, Roman DC (2015a) Peakmatch: a Java program for multiplet analysis of large seismic datasets. Seismol Res Lett 86:1208–1218. https://doi.org/10.1785/0220140160
Rodgers M, Roman DC, Geirsson H, LaFemina P, McNutt SR, Muñoz A, Tenorio V (2015b) Stable and unstable phases of elevated seismic activity at the persistently restless Telica Volcano, Nicaragua. J Volcanol Geoth Res 290:63–74
Roman DC, Cashman KV (2006) The origin of volcano-tectonic earthquake swarms. Geology 34(6):457–460. https://doi.org/10.1130/G22269.1
Roman DC, De Angelis S, Latchman JL, White R (2008) Patterns of volcanotectonic seismicity and stress during the ongoing eruption of the Soufrière Hills Volcano, Montserrat (1995–2007). J Volcanol Geotherm Res 173(3–4):230–244. https://doi.org/10.1016/j.jvolgeores.2008.01.014
Roman DC, LaFemina PC, Bussard R, Stephens K, Wauthier C, Higgins M, Feineman M, Arellano S, de Moor JM, Avard G, Martinez Cruz M, Burton M, Varnam M, Saballos A, Ibarra M, Strauch W, Tenorio V (2019) Mechanisms of unrest and eruption at persistently restless volcanoes: insights from the 2015 eruption of Telica Volcano, Nicaragua. Geochem Geophys Geosyst 20(8):4162–4183. https://doi.org/10.1029/2019GC008450
Roman DC, Soldati A, Dingwell DB, Houghton BF, Shiro BR (2021) Earthquakes indicated magma viscosity during Kīlauea’s 2018 eruption. Nature 592(7853):237–241. https://doi.org/10.1038/s41586-021-03400-x
Rose KM, Matoza RS (2021) Remote hydroacoustic-infrasonic detection and characterization of Anak Krakatau eruptive activity leading to, during, and following the December 2018 flank collapse and tsunami. Bull Volcanol 83:50. https://doi.org/10.1007/s00445-021-01468-x
Roult G, Montagner J-P, Romanowicz B, Cara M, Rouland D, Pillet R, Karczewski J-F, Rivera L, Stutzmann E, Maggi A, the GEOSCOPE team, (2010) The GEOSCOPE Program: progress and challenges during the past 30 years. Seismol Res Lett 81(3):427–452. https://doi.org/10.1785/gssrl.81.3.427
Rowe C, Thurber RCH, White RA (2004) Dome growth behavior at Soufriere Hills Volcano, Montserrat, revealed by relocation of volcanic event swarms, 1995–1996. J Volcanol Geoth Res 134:199–221
Rubin AM (1995) Propagation of magma-filled cracks. Ann Rev Ear Plan Sci 23(1):287–336. https://doi.org/10.1146/annurev.ea.23.050195.001443
Rubin AM (1993) Tensile fracture of rock at high confining pressure: implications for dike propagation. J. Geophys. Res. 98: 15,9 19–35
Ruiz MC, Lees JM, Johnson JB (2006) Source constraints of Tungurahua volcano explosion events. Bull Volcanol 68:480–490. https://doi.org/10.1007/s00445-005-0023-8
Ruiz MC, Yepes HA, Steele A, Segovia M, Vaca S, Cordova A, Enriquez W, Vaca M, Ramos C, Arrais S, Tapa I (2013) Permanent infrasound monitoring of active volcanoes in Ecuador. In AGU Fall Meeting Abstracts 2013:S23B–2497
Rust AC, Balmforth NJ, Mandre S (2008) The feasibility of generating low-frequency volcano seismicity by flow through a deformable channel. In: Lane SJ, Gilbert JS (eds) Fluid motions in volcanic conduits: a source of seismic and acoustic signals. Geol Soc London Spec Pub 307, pp 45–56. https://doi.org/10.1144/sp307.4
Sabatini R, Marsden O, Bailly C, Gainville O (2019) Three-dimensional direct numerical simulation of infrasound propagation in the Earth’s atmosphere. J Fluid Mech 859:754–789. https://doi.org/10.1017/jfm.2018.816
Sabit JP, Pigtain RC, De la Cruz EG (1996) The west-side story: observations of the 1991 Mount Pinatubo eruptions from the west. In: Newhall CG, Punongbayan S (eds) Fire and mud. University of Washington Press, pp 445–455
Saccorotti G, Chouet B, Dawson P (2001) Wavefield properties of a shallow long-period event and tremor at Kilauea Volcano, Hawaii. J Volcanol Geotherm Res 109(1–3):163–189
Saccorotti G, Lokmer I, Bean CJ, Di Grazia G, Patane D (2007) Analysis of sustained long-period activity at Etna Volcano, Italy. J Volcanol Geoth Res 160(3-4):340–354
Saccorotti G, Lokmer I (2021) A review of seismic methods for monitoring and understanding active volcanoes. In: Papale P (ed) Forecasting and planning for volcanic hazards, risks, and disasters. Elsevier, Amsterdam, pp 25–73. https://doi.org/10.1016/b978-0-12-818082-2.00002-0
Saderra Masó M (1919) Recent eruptions of volcanos in the Philippine Islands. Bull Seismol Soc Am 9(2):35–37. https://doi.org/10.1785/BSSA0090020035
Saderra Masó M (1904) Volcanoes and seismic centers of the Philippine Archipelago (Vol. 3). Department of Commerce and Labor, Bureau of the Census.
Saderra Masó M (1911a) The eruption of Taal volcano January 30, 1911a. Department of the Interior, Weather Bureau, Manila Bureau of Printing, Manila.
Saderra Masó M (1911b) Volcanic eruptions in the Philippines in relation to earthquakes and subterranean noises, to rainfall and atmospheric pressure, In: Seismological Bulletin for July, 1911b, Department of the Interior, Weather Bureau, Manila Central Observatory, Manila, pp. 238–249.
Saderra Masó M (1913) The new seismic station near Taal Volcano. Bull Seismol Soc Am 3(2):49–50. https://doi.org/10.1785/BSSA0030020049
Sahetapy-Engel ST, Harris AJ, Marchetti E (2008) Thermal, seismic and infrasound observations of persistent explosive activity and conduit dynamics at Santiaguito lava dome, Guatemala. J Volcanol Geoth Res 173(1):1–14. https://doi.org/10.1016/j.jvolgeores.2007.11.026
Saito S (2022) Ionospheric disturbances observed over Japan following the eruption of Hunga Tonga-Hunga Ha’apai on 15 January 2022. Earth Planet Space 74(1):1–9
Sakai T, Yamasato H, Uhira K (1996) Infrasound accompanying C-type tremor at Sakurajima volcano. Bull Volcanol Soc Japan 41(4): 181–185. https://doi.org/10.18940/kazan.41.4_181
Sanderson RW, Matoza RS, Haymon RM, Steidl JH (2021) A pilot experiment on infrasonic lahar detection at Mount Adams, Cascades: Ambient infrasound and wind-noise characterization at a quiescent stratovolcano. Seismol Res Lett 92:3065–3086. https://doi.org/10.1785/0220200361
Sanderson RW, Matoza RS, Fee D, Haney MM, Lyons JJ (2020) Remote detection and location of explosive volcanism in Alaska with the EarthScope Transportable Array. J Geophys Res 125: e2019JB018347. https://doi.org/10.1029/2019JB018347
Sassa K (1935) Volcanic micro-tremors and eruption-earthquakes: (Part I of the Geophysical Studies on the Volcano Aso). Mem Coll Sci Kyoto Imp Univ A 18(5):255–293
Sassa K (1936) Micro-seismometric study on eruptions of the Volcano Aso: (Part II of the Geophysical Studies on the Volcano Aso). Mem Coll Sci Kyoto Imp Univ A 19(1):11–56
Saunders K, Blundy J, Dohmen R, Cashman K (2012) Linking petrology and seismology at an active volcano. Science 336(6084):1023–1027
Savage JC, Cockerham RS (1984) Earthquake swarm in Long Valley caldera, California, January 1983: evidence for dike inflation. J Geophys Res 89(B10):8315–8324. https://doi.org/10.1029/JB089iB10p08315
Sayyadi S, Einarsson P, Gudmundsson MT (2021) Seismic activity associated with the 1963–1967 Surtsey eruption off the coast of South Iceland. Bull Volcanol 83:54. https://doi.org/10.1007/s00445-021-01481-0
Scandone R, Malone SD (1985) Magma supply, magma discharge and readjustment of the feeding system of Mount St. Helens during 1980. J Volcanol Geotherm Res 23:239–262. https://doi.org/10.1016/0377-0273(85)90036-8
Scarpetta S, Giudicepietro F, Ezin EC, Petrosino S, Del Pezzo E, Martini M, Marinaro M (2005). Automatic classification of seismic signals at Mt. Vesuvius volcano, Italy, using neural networks. Bull Seismol Soc Am 95(1):185–196
Schnepf NR, Minami T, Toh H, Nair MC (2022) Magnetic signatures of the January 15 2022 Hunga Tonga–Hunga Ha‘apai volcanic eruption. Geophys Res Lett e2022GL098454
Schwaiger HF, Iezzi AM, Fee D (2019) AVO-G2S: a modified, open-source ground-to-space atmospheric specification for infrasound modeling. Comp Geosci 125:90–97. https://doi.org/10.1016/j.cageo.2018.12.013
Scott RH (1883) Note on a series of barometrical disturbances which passed over Europe between the 27th and the 31st of August, 1883. Proc Roy Soc Lon 36:139–143. https://doi.org/10.1098/rspl.1883.0087
Scott BJ, Travers J (2009) Volcano monitoring in NZ and links to SW Pacific via the Wellington VAAC. Nat Haz 51(2):263–273. https://doi.org/10.1007/s11069-009-9354-7
Scrope GP (1825) Considerations on volcanoes: the probable causes of their phenomena, the laws which determine their march, the disposition of their products, and their connexion with the present state and past history of the globe; leading to the establishment of a new theory of the Earth. W Phillips, London
Segall P (2013) Volcano deformation and eruption forecasting. Geological Society, London, Special Publications 380(1):85–106
Segall P, Anderson K (2021) Repeating caldera collapse events constrain fault friction at the kilometer scale. Proc Natl Acad Sci 118(30):e2101469118
Seidl D, Kirbani SB, Brüstle W (1990) Maximum entropy spectral analysis of volcanic tremor using data from Etna (Sicily) and Merapi (central Java). Bull Volcanol 52:460–474. https://doi.org/10.1007/BF00268926
Senyukov SL, Droznina SY, Nuzhdina IN, Garbuzova VT, Kozhevnikova TY (2009) Studies in the activity of Klyuchevskoi volcano by remote sensing techniques between January 1, 2001 and July 31. J Volcanol Seismol 3(3):191–199. https://doi.org/10.1134/S0742046309030051
Sgattoni G, Jeddi Z, Gudmundsson O, Einarsson P, Tryggvason A, Lund B, Lucchi F (2016) Long-period seismic events with strikingly regular temporal patterns on Katla volcano’s south flank (Iceland). J Volcanol Geoth Res 324:28–40
Shen H, Shen Y (2021) Array-based convolutional neural networks for automatic detection and 4D localization of earthquakes in Hawai‘i. Seismol Res Lett 92(5):2961–2971. https://doi.org/10.1785/0220200419
Shepherd JB, Tomblin JF, Woo DA (1971) Volcano-seismic crisis in Montserrat, West Indies, 1966–67. Bull Volcanol 35(1):143–162. https://doi.org/10.1007/BF02596813
Shima M (1958) On the second volcanic micro-tremor at volcano Aso. Bull Disaster Prev Res Inst Kyoto Univ 22:1–6
Shimazaki K, Miyatake T, Tsuboi S, Takano K, Abe K, Takeo M (1992) Planning of the POSEIDON Data Center. Progr Abstr Seism Soc Jpn l:120
Shimozuru D (1961) Volcanic microseisms - discussion on the origin. Bull Volcanol Soc Japan 5:154–162
Shiro BR, Zoeller MH, Kamibayashi K, Johanson IA, Parcheta C, Patrick MR, Nadeau P, Lee L, Miklius A (2021) Monitoring network changes during the 2018 Kīlauea volcano eruption. Seismol Res Lett 92(1):102–118
Sigurdsson H, Cashdollar S, Sparks SRJ (1982) The eruption of Vesuvius in A. D. 79: reconstruction from historical and volcanological evidence. Am J Archaeol 86(1):39–51 https://doi.org/10.2307/504292
Smith SW (1987) IRIS—a university consortium for seismology. Reviews of Geophysics, 25(6), 1203–1207. Chicago
Snodgrass JM, Richards AF (1956) Observations of underwater volcanic acoustics at Barcena volcano, San Benedicto Island, Mexico, and in Shelikof Strait, Alaska. EOS Trans AGU 37:97–104. https://doi.org/10.1029/TR037i001p00097
Soubestre J, Shapiro NM, Seydoux L, de Rosny J, Droznin DV, Droznina SY, Senyukov SL, Gordeev EI (2018) Network-based detection and classification of seismovolcanic tremors: example from the Klyuchevskoy volcanic group in Kamchatka. J Geophys Res: Solid Earth 123(1):564–582
Soubestre J, Chouet B, Dawson P (2021) Sources of volcanic tremor associated with the summit caldera collapse during the 2018 east rift eruption of Kīlauea Volcano, Hawai'i. J Geophys Res 126: e2020JB021572. https://doi.org/10.1029/2020JB021572
Sparks RSJ (2003) Forecasting volcanic eruptions. Earth Planet Sci Lett 210(1–2):1–15. https://doi.org/10.1016/S0012-821X(03)00124-9
Sparks RSJ, Young SR (2002) The eruption of Soufrière Hills Volcano, Montserrat (1995–1999): overview of scientific results. Geological Society, London, Memoirs 21(1):45–69
Spina L, Taddeucci J, Cannata A, Sciotto M, Del Bello E, Scarlato P, Kueppers U, Andronico D, Privitera E, Ricci T, Pena-Fernandez J (2017) Time-series analysis of fissure-fed multi-vent activity: a snapshot from the July 2014 eruption of Etna volcano (Italy). Bull Volcanol 79(7):1–12
Spina L, Morgavi D, Cannata A, Campeggi C, Perugini D (2018) An experimental device for characterizing degassing processes and related elastic fingerprints: analog volcano seismo-acoustic observations. Rev Sci Instrum 89(5):055102. https://doi.org/10.1063/1.5020004
Spina L, Cannata A, Privitera E, Vergniolle S, Ferlito C, Gresta S, Montalto P, Sciotto M (2015) Insights into Mt. Etna’s shallow plumbing system from the analysis of infrasound signals, August 2007–December 2009. Pure Appl Geophys 172(2):473–490
Stammler K, Bischoff M, Brüstle A, Ceranna L, Donner S, Fischer K, Gaebler P, Friederich W, Funke S, Hartmann G, Homuth B (2021) German seismic and infrasound networks contributing to the European integrated data archive (EIDA). Seismol Res Lett 92(3):1854–1875
Steinberg GS, Steinberg AS (1975) On possible causes of volcanic tremor. J Geophys Res 80:1600–1604. https://doi.org/10.1029/JB080i011p01600
Stephens CD, Chouet BA, Page RA, Lahr JC, Power JA (1994) Seismological aspects of the 1989–1990 eruptions at Redoubt Volcano, Alaska: the SSAM perspective. J Volcanol Geotherm Res 62(1–4):153–182. https://doi.org/10.1016/0377-0273(94)90032-9
Stoneley R (1926) The effect of the ocean on Rayleigh waves. Geophysical Supplements to the Monthly Notices of the Royal Astronomical Society 1(7):349–356
Strachey RH (1884) Note on the foregoing paper. Proc Roy Soc Lon 36:143–151. https://doi.org/10.1098/rspl.1883.0088
Strachey RH (1888) On the air waves and sounds caused by the eruption of Krakatoa in August 1883. In: Symons GJ (ed) The eruption of Krakatoa and subsequent phenomena. Report of the Krakatoa Committee of the Royal Society, Trübner and Co, London, II. https://doi.org/10.1002/qj.4970146809
Sturkell E, Einarsson P, Roberts MJ, Geirsson H, Gudmundsson MT, Sigmundsson F, Pinel V, Guðmundsson GB, Ólafsson H, Stefánsson R (2008) Seismic and geodetic insights into magma accumulation at Katla subglacial volcano, Iceland: 1999 to 2005. J Geophys Res 113:B03212. https://doi.org/10.1029/2006JB004851
Suárez G, Pérez-Campos X (2020) 110th Anniversary of the Mexican National Seismological Service: an account of its early contributions. Seismol Res Lett 91(5):2904–2911. https://doi.org/10.1785/0220200157
Suwa A (1980) The surveillance and prediction of volcanic activities in Japan. GeoJ 4:153–159. https://doi.org/10.1007/BF00705522
Suzuki Z (1959) A statistical study on the occurrence of small earthquakes (fourth paper). Sci Rep Tohoku Univ Ser. 5, Geophysics 11(1): 10–54
Swanson DA (1972) Magma supply rate at Kilauea Volcano, 1952–1971. Sci 175(4018):169–170. https://doi.org/10.1126/science.175.4018.169
Swanson DA, Casadevall TJ, Dzurisin D, Holcomb RT, Newhall CG, Malone SD, Weaver CS (1985) Forecasts and predictions of eruptive activity at Mount St. Helens, USA: 1975–1984. J Geodyn 3:397–423. https://doi.org/10.1016/0264-3707(85)90044-4
Swanson E, Theunissen R, Rust A, Green D, Phillips J (2018) An experimental study of the flow structure and acoustics of jets: implications for volcano infrasound. J Volcanol Geotherm Res 363:10–22. https://doi.org/10.1016/j.jvolgeores.2018.08.005
Syahbana DK, Caudron C, Jousset P, Lecocq T, Camelbeeck T, Bernard A (2014) Fluid dynamics inside a “wet” volcano inferred from the complex frequencies of long-period (LP) events: an example from Papandayan volcano, West Java, Indonesia, during the 2011 seismic unrest. J Volcanol Geoth Res 280:76–89
Taddeucci J, Sesterhenn J, Scarlato P, Stampka K, Del Bello E, Pena Fernandez JJ, Gaudin D (2014) High-speed imaging, acoustic features, and aeroacoustic computations of jet noise from Strombolian (and Vulcanian) explosions. Geophys Res Lett 41(9): 2014GL059925. https://doi.org/10.1002/2014gl059925
Taddeucci J, Peña Fernández JJ, Cigala V, Kueppers U, Scarlato P, Del Bello E, et al. (2021) Volcanic vortex rings: axial dynamics, acoustic features, and their link to vent diameter and supersonic jet flow. Geophys Res Lett 48:e2021GL092899. https://doi.org/10.1029/2021GL092899
Taguchi K, Kumagai H, Maeda Y, Torres R (2018) Source properties and triggering processes of long-period events beneath volcanoes inferred from an analytical formula for crack resonance frequencies. J Geophys Res 123:7550–7565. https://doi.org/10.1029/2018JB015866
Taguchi K, Kumagai H, Maeda Y, Torres R (2021) Empirical formula for the quality factors of crack resonances and its application to the estimation of source properties of long-period seismic events at active volcanoes. Geophys J Int 224(3):2131–2148. https://doi.org/10.1093/gji/ggaa519
Tahira M (1982) A study of the infrasonic wave in the atmosphere: (II) Infrasonic waves generated by the explosions of the volcano Sakurajima. J Meteorol Soc Japan 60(3):896–907. https://doi.org/10.2151/jmsj1965.60.3_896
Tahira M, Nomura M, Sawada Y, Kamo K (1996) Infrasonic and acoustic-gravity waves generated by the Mount Pinatubo eruption of June 15, 1991. In: Newhall CG, Punongbayan S (eds) Fire and mud. University of Washington Press, pp 601–614
Tailpied D, Le Pichon A, Marchetti E, Ripepe M, Kallel M, Ceranna L, Brachet N (2013) Remote infrasound monitoring of Mount Etna: observed and predicted network detection capability. InfraMatics 2(1):1–11. https://doi.org/10.4236/inframatics.2013.21001
Tailpied D, Pichon AL, Marchetti E, Assink J, Vergniolle S (2016) Assessing and optimizing the performance of infrasound networks to monitor volcanic eruptions. Geophysical Journal International, ggw400.
Taisne B, Perttu A, Tailpied D, Caudron C, Simonini L (2019) Atmospheric controls on ground- and space-based remote detection of volcanic ash injection into the atmosphere, and link to early warning systems for aviation hazard mitigation. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Cham, pp 1079–1105. https://doi.org/10.1007/978-3-319-75140-5_34
Takahashi TJ (1988) Early HVO Bulletins collected, published. Eos Trans AGU 69(19):579–579. https://doi.org/10.1029/88EO00167
Takeo M (2021) Harmonic tremor model during the 2011 Shinmoe-dake eruption, Japan. Geophys J Int 224(3):2100–2120
Talandier J, Okal EA (1987) Seismic detection of underwater volcanism: the example of French Polynesia. Pure Appl Geophys 125(6):919–950
Talandier J, Hyvernaud O, Hébert H, Maury RC, Allgeyer S (2020) Seismic and hydroacoustic effects of the May 29, 2010 submarine South Sarigan volcanic explosion: energy release and interpretation. J Volcanol Geoth Res 394:106819. https://doi.org/10.1016/j.jvolgeores.2020.106819
Tayag JC, Punongbayan RS (1994) Volcanic disaster mitigation in the Philippines: experience from Mt. Pinatubo. Disast 18(1):1–15. https://doi.org/10.1111/j.1467-7717.1994.tb00281.x
Taylor GI (1929) Waves and tides in the atmosphere. Proc Roy Soc Lon A 126(800):169–183. https://doi.org/10.1098/rspa.1929.0213
Taylor GI (1936) The oscillations of the atmosphere. Proc Roy Soc Lon A 156(888):318–326. https://doi.org/10.1098/rspa.1936.0150
Temkin S, Dobbins RA (1966) Attenuation and dispersion of sound by particulate-relaxation processes. J Acoust Soc Am 40(2):317–324
Tepp G, Dziak RP (2021) The seismo-acoustics of submarine volcanic eruptions. J Geophys Res 126: e2020JB020912. https://doi.org/10.1029/2020JB020912
Tepp G, Chadwick WW, Haney MM, Lyons JJ, Dziak RP, Merle SG, Butterfield DA, Young CW (2019) Hydroacoustic, seismic, and bathymetric observations of the 2014 submarine eruption at Ahyi Seamount, Mariana Arc. Geochemistry Geophys Geosystems 3608–3627https://doi.org/10.1029/2019gc008311
Tepp G, Dziak RP, Haney MM, Lyons JJ, Searcy C, Matsumoto H, Haxel J (2020) Seismic and hydroacoustic observations of the 2016–17 Bogoslof eruption. Bull Volcanol 82(1). https://doi.org/10.1007/s00445-019-1344-3
Thelen W, Matoza RS, Hotovec-Ellis A (2022) Trends in volcano seismology: 2010 to 2020 and beyond. Bull Volcanol 84:26. https://doi.org/10.1007/s00445-022-01530-2
Themens DR, Watson C, Žagar N, Vasylkevych S, Elvidge S, McCaffrey A, et al. (2022) Global propagation of ionospheric disturbances associated with the 2022 Tonga volcanic eruption. Geophys Res Lett 49:e2022GL098158. https://doi.org/10.1029/2022GL098158
Thomas ME, Neuberg J (2012) What makes a volcano tick — a first explanation of deep multiple seismic sources in ascending magma. Geology 40(4):351–354
Thomas JE, Pierce AD, Flinn EA, Craine LB (1971) Bibliography on infrasonic waves. Geophys J Int 26(1–4):399–426
Thompson G, Power JA, Braunmiller J, Lockhart AB, Lynch L, McCausland W, Rowe CA, Shea T, White RA, Breithaupt CI (2020) Capturing, preserving, and digitizing legacy seismic data from the Montserrat Volcano Observatory Analog Seismic Network, July 1995–December 2004. Seismol Res Lett 91:2127–2140. https://doi.org/10.1785/0220200012
Thompson G (2015) Seismic monitoring of volcanoes. In: Beer M, Kougioumtzoglou IA, Patelli E, Au SK (eds) Encyclopedia of earthquake engineering. Springer, Berlin, Heidelberg, 978–3. https://doi.org/10.1007/978-3-642-35344-4_41
Toda S, Stein RS, Sagiya T (2002) Evidence from the AD 2000 Izu islands earthquake swarm that stressing rate governs seismicity. Nature 419:58–61. https://doi.org/10.1038/nature00997
Tokarev PI (1963) On a possibility of forecasting of Bezymianny volcano eruptions according to seismic data. Bull Volcanol 26(1):379–386. https://doi.org/10.1007/BF02597299
Tokarev PI (1966) Eruptions and seismic activity of Klyuchevskaya Group Volcanoes. Nauka, Moscow
Tokarev PI (1978) Prediction and characteristics of the 1975 eruption of Tolbachik volcano. Kamchatka Bull Volcanol 41(3):251–258. https://doi.org/10.1007/BF02597226
Tokarev PI (1981) Volcanic earthquakes of Kamchatka. Nauka, Moscow
Toney L, Fee D, Allstadt K, Haney M, Matoza RS (2021) Reconstructing the dynamics of the highly-similar May 2016 and June 2019 Iliamna Volcano, Alaska ice-rock avalanches from seismoacoustic data. Earth Surf Dynam 9:271–293. https://doi.org/10.5194/esurf-9-271-2021
Torres R, Kumagai H, Taguchi K (2021) Source models of long-period seismic events at Galeras volcano, Colombia. Geophys J Int 227(3):2137–2155. https://doi.org/10.1093/gji/ggab325
Traversa PO, Lengliné O, Macedo JP, Metaxian JR, Grasso A, Inza ET (2011) Short term forecasting of explosions at Ubinas Volcano, Perú. J Geophys Res 116:B11301. https://doi.org/10.1029/2010JB008180
Tuffen H, Dingwell D (2005) Fault textures in volcanic conduits: evidence for seismic trigger mechanisms during silicic eruptions. Bull Volcanol 67:370–387. https://doi.org/10.1007/s00445-004-0383-5
Tuffen H, Dingwell DB, Pinkerton H (2003) Repeated fracture and healing of silicic magma generates flow banding and earthquakes? Geology 31:1089–1092
Udías A, Stauder W (1996) The Jesuit contribution to seismology. Seismol Res Lett 67(3):10–19. https://doi.org/10.1785/gssrl.67.3.10
Uffen RJ (1959) On the origin of rock magma. J Geophys Res 64(1):117–122. https://doi.org/10.1029/JZ064i001p00117
Uffen RJ, Jessop AM (1963) The stress release hypothesis of magma formation. Bull Volcanol 26:57–66. https://doi.org/10.1007/BF02597274
Ulberg CW, Creager KC, Moran SC, Abers GA, Thelen WA, Levander A, Kiser E, Schmandt B, Hansen SM, Crosson RS (2020) Local source VP and VS tomography in the Mount St. Helens region with the iMUSH broadband array. Geochem Geophys Geosyst 21(3):e2019GC008888. https://doi.org/10.1029/2019GC008888
Ulivieri G, Ripepe M, Marchetti E (2013) Infrasound reveals transition to oscillatory discharge regime during lava fountaining: implication for early warning. Geophys Res Lett 40(12):3008–3013
Umakoshi K, Takamura N, Shinzato N, Uchida K, Matsuwo N, Shimizu H (2008) Seismicity associated with the 1991–1995 dome growth at Unzen Volcano, Japan. J Volcanol Geotherm Res 175(1–2):91–99. https://doi.org/10.1016/j.jvolgeores.2008.03.030
Unglert K, Radić V, Jellinek AM (2016) Principal component analysis vs. self-organizing maps combined with hierarchical clustering for pattern recognition in volcano seismic spectra. J Volcanol Geoth Res 320:58–74
Unwin HE, Tuffen H, Phillips E, Wadsworth FB, James MR (2021) Pressure-driven opening and filling of a volcanic hydrofracture recorded by tuffisite at Húsafell, Iceland: a potential seismic source. Front Ear Sci 9:347. https://doi.org/10.3389/feart.2021.668058
Valade S, Ripepe M, Giuffrida G, Karume K, Tedesco D (2018) Dynamics of Mount Nyiragongo lava lake inferred from thermal imaging and infrasound array. Earth Planet Sci Lett 500:192–204
van van Eck T, Dost B (1999) ORFEUS, a European initiative in broadband seismology: status and future plans. Phys Earth Planet Inter 113(1–4):45–55
van Driel M, Wassermann J, Pelties C, Schiemenz A, Igel H (2015) Tilt effects on moment tensor inversion in the near field of active volcanoes. Geophys J Int 202(3):1711–1721. https://doi.org/10.1093/gji/ggv209
Van Padang N (1933) Die uitbarsting van den Merapi (Midden Java) in de jaren 1930–1931. Vulkanol En Seism Med 12:1–117
Van Eaton AR, Amigo Á, Bertin D, Mastin LG, Giacosa RE, González J et al (2016) Volcanic lightning and plume behavior reveal evolving hazards during the April 2015 eruption of Calbuco volcano, Chile. Geophys Res Lett 43:3563–3571. https://doi.org/10.1002/2016GL068076
Vargas CA, Caneva A, Monsalve H, Salcedo E, Mora H (2018) Geophysical networks in Colombia. Seismol Res Lett 89(2A):440–445. https://doi.org/10.1785/0220170168
Verbeek RDM (1884) The Krakatoa eruption. Nature 30(757):10–15. https://doi.org/10.1038/030010a0
Vergniolle S, Brandeis G (1994) Origin of the sound generated by Strombolian explosions. Geophys Res Lett 21:1959–1962. https://doi.org/10.1029/94GL01286
Vergniolle S, Caplan-Auerbach J (2006) Basaltic thermals and subplinian plumes: constraints from acoustic measurements at Shishaldin volcano, Alaska. Bull Volcanol 68(7–8):611–630. https://doi.org/10.1007/s00445-005-0035-4
Vergniolle S, Brandeis G, Mareschal JC (1996) Strombolian explosions: 2. Eruption dynamics determined from acoustic measurements. J Geophys Res Solid Earth 101(B9):20449–20466
Vergoz J, Hupe P, Listowski C, Le Pichon A, Garcés MA, Marchetti E, Labazuy P, Ceranna L, Pilger C, Gaebler P, Näsholm SP (2022) IMS observations of infrasound and acoustic-gravity waves produced by the January 2022 volcanic eruption of Hunga, Tonga: a global analysis. Earth Planet Sci Lett 591:117639
Voight B (1988) A method for prediction of volcanic eruptions. Nature 332(6160):125–130. https://doi.org/10.1038/332125a0
Voight B, Constantine EK, Siswowidjoyo S, Torley R (2000) Historical eruptions of Merapi volcano, central Java, Indonesia, 1768–1998. J Volcanol Geotherm Res 100(1–4):69–138. https://doi.org/10.1016/S0377-0273(00)00134-7
Voight B (1996) The management of volcano emergencies: Nevado del Ruiz. In: Scarpa R, Tilling RI (eds) Monitoring and mitigation of volcano hazards. Springer, Berlin, Heidelberg, pp 719–769. https://doi.org/10.1007/978-3-642-80087-0_22
Wada T, Sudo Y (1967) Focal mechanism of volcanic earthquake of the volcano Aso. Special Contrib Geophy Inst Kyoto Univ 7:151–160
Wada T, Kamo K, Ono H (1963) Note on volcanic explosion earthquakes of the volcano Sakurajima. Special Contrib Geophy Inst Kyoto Univ 3:293–296
Waite GP, Chouet BA, Dawson PB (2008) Eruption dynamics at Mount St. Helens imaged from broadband seismic waveforms: interaction of the shallow magmatic and hydrothermal systems. J Geophys Res 113: B02305. https://doi.org/10.1029/2007JB005259
Waite GP, Lanza F (2016) Nonlinear inversion of tilt-affected very long period records of explosive eruptions at Fuego volcano. J Geophys Res 121:7284–7297. https://doi.org/10.1002/2016JB013287
Walker KT, Hedlin MAH (2010) A review of wind-noise reduction methodologies. In: Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies. Springer, Netherlands, pp 141–182. https://doi.org/10.1007/978-1-4020-9508-5_5
Wallace PA, Lamb OD, De Angelis S, Kendrick JE, Hornby AJ, Díaz-Moreno A, González PJ, von Aulock FW, Lamur A, Utley JE, Rietbrock A (2020) Integrated constraints on explosive eruption intensification at Santiaguito dome complex, Guatemala. Ear Plan Sci Lett 536:116–139. https://doi.org/10.1016/j.epsl.2020.116139
Wang Y, Lin F-C, Schmandt B, Farrell J (2017) Ambient noise tomography across Mount St. Helens using a dense seismic array. J Geophys Res 122:4492–4508. https://doi.org/10.1002/2016JB013769
Ward PL, Gregersen S (1973) Comparison of earthquake locations determined with data from a network of stations and small tripartite arrays on Kilauea volcano, Hawaii. Bull Seismol Soc Am 63(2):679–711. https://doi.org/10.1785/BSSA0630020679
Warren NW, Latham GV (1970) An experimental study of thermally induced microfracturing and its relation to volcanic seismicity. J Geophys Res 75(23):4455–4464. https://doi.org/10.1029/JB075i023p04455
Wassermann J (2012) Volcano seismology. In: New manual of seismological observatory practice 2 (NMSOP-2) (pp. 1–77). Deutsches GeoForschungsZentrum GFZ.
Watson LM, Dunham EM, Johnson JB (2019) Simulation and inversion of harmonic infrasound from open-vent volcanoes using an efficient quasi-1D crater model. J Volcanol Geotherm Res 380:64–79. https://doi.org/10.1016/j.jvolgeores.2019.05.007
Watson L, Iezzi AM, Toney L, Maher SP, Fee D, McKee K, Ortiz HD, Matoza RS, Gestrich JE, Bishop JW, Witsil AJC, Anderson JF, Johnson JB (2022) Volcano infrasound: progress and future directions. Bull Volcanol 84:44. https://doi.org/10.1007/s00445-022-01544-w
Watson LM, Johnson JB, Sciotto M, Cannata A (2020) Changes in crater geometry revealed by inversion of harmonic infrasound observations: 24 December 2018 eruption of Mount Etna, Italy. Geophys Res Lett 47(19): e2020GL088077. https://doi.org/10.1029/2020GL088077
Watson LM, Dunham EM, Mohaddes D, Labahn J, Jaravel T, Ihme M (2021) Infrasound radiation from impulsive volcanic eruptions: Nonlinear aeroacoustic 2D simulations. J Geophys Res 126: e2021JB021940. https://doi.org/10.1029/2021JB021940
Wauthier C, Roman DC, Poland MP (2013) Moderate-magnitude earthquakes induced by magma reservoir inflation at Kīlauea Volcano, Hawai ‘i. Geophys Res Lett 40(20):5366–5370. https://doi.org/10.1002/2013GL058082
Wauthier C, Roman DC, Poland MP (2016) Joint analysis of geodetic and earthquake fault-plane solution data to constrain magmatic sources: a case study from Kīlauea Volcano. Earth Planet Sci Lett 455:38–48
Waxler R, Assink J (2019) Propagation modeling through realistic atmosphere and benchmarking. Le Pichon A, Blanc E, Hauchecorne A (eds) Infrasound monitoring for atmospheric studies, 2nd edn. Springer, Dordrecht, pp 509–549. https://doi.org/10.1007/978-3-319-75140-5_15
Weaver CS, Norris RD, Jonientz-Trisler C (1990) Results of seismological monitoring in the Cascade Range, 1962–1989: earthquakes, eruptions, avalanches, and other curiosities. Geosci Canada 17(3):158–162
Webb SL, Dingwell DB (1990) Non-Newtonian rheology of igneous melts at high stresses and strain rates: experimental results for rhyolite, andesite, basalt, and nephelinite. J Geophys Res 95(B10):15695–15701
Webley P, Mastin L (2009) Improved prediction and tracking of volcanic ash clouds. J Volcanol Geotherm Res 186(1–2):1–9. https://doi.org/10.1016/j.jvolgeores.2008.10.022
White R, McCausland W (2016) Volcano-tectonic earthquakes: A new tool for estimating intrusive volumes and forecasting eruptions. J Volcanol Geotherm Res 309:139–155
Wilson CR, Forbes RB (1969) Infrasonic waves from Alaskan volcanic eruptions. J Geophys Res 74:4511–4522. https://doi.org/10.1029/JC074i018p04511
Wilson CR, Nichparenko S, Forbes RB (1966) Evidence of two sound channels in the polar atmosphere from infrasonic observations of the eruption of an Alaskan volcano. Nature 211:163–165. https://doi.org/10.1038/211163a0
Wood HO (1913) The Hawaiian Volcano Observatory. Bull Seismol Soc Am 3(1):14–19. https://doi.org/10.1785/BSSA0030010014
Wood R (1974) Microearthquakes at central American volcanoes. Bull Seismol Soc Am 64(1):275–277
Wood HO (1912) Review of “Volcanic Eruptions in the Philippines in Relation to Earthquakes and Subterranean Noises, to Rainfall and Atmospheric Pressure By Rev. Miguel Saderra Maso, S. J., Assistant Director of the Weather Bureau. Bulletin of the Weather Bureau, July 1911. (Philippine Weather Service.)”. Bull Seismol Soc Am 2(3): 213–215. https://doi.org/10.1785/BSSA0020030213
Woulff G, McGetchin TR (1976) Acoustic noise from volcanoes: theory and experiment. Geophys J Int 45:601–616. https://doi.org/10.1111/j.1365-246X.1976.tb06913.x
Wright T, Takahashi T (1998) Hawaii Bibliographic Database. Bull Volcanol 59:276–280. https://doi.org/10.1007/s004450050191
Wright R, Flynn LP, Garbeil H, Harris AJ, Pilger E (2004) MODVOLC: near-real-time thermal monitoring of global volcanism. J Volcanol Geoth Res 135(1–2):29–49
Wright CJ, Hindley NP, Alexander MJ et al (2022) Surface-to-space atmospheric waves from Hunga Tonga-Hunga Ha’apai eruption. Nature. https://doi.org/10.1038/s41586-022-05012-5
Wright TL, Takahashi TJ (1989) Observations and interpretation of Hawaiian volcanism and seismicity, 1779–1955: an annotated bibliography and subject index. University of Hawaii Press.
Wright TL, Peck DL, Shaw HR (1976) Kilauea lava lakes: natural laboratories for the study of cooling, crystallization, and differentiation of basaltic magma. In: Sutton GH, Manghnani MH, Moberly R (eds) The geophysics of the Pacific Ocean basin and its margin. Geophys Monogr Ser 19, pp 375–390. https://doi.org/10.1029/gm019p0375
Wu S.-M, Ward KM, Farrell J, Lin F.-C, Karplus M, Smith RB (2017) Anatomy of Old Faithful from subsurface seismic imaging of the Yellowstone Upper Geyser Basin. Geophys Res Lett 44:10,240– 10,247. https://doi.org/10.1002/2017GL075255
Yamasato H (1997) Quantitative analysis of pyroclastic flows using infrasonic and seismic data at Unzen volcano. Japan J Phys Ear 45(6):397–416. https://doi.org/10.4294/jpe1952.45.397
Yamasato H, Hamada N, McCreery CS, Oliveira FJ, Walker DA, Talandier J (1993) T waves associated with submarine volcanic eruptions in the Marianas observed by ocean bottom seismographs. J Phys Earth 41(2):57–74. https://doi.org/10.4294/jpe1952.41.57
Yamasato H (1998) Nature of infrasonic pulse accompanying low frequency earthquake at Unzen Volcano, Japan. Bull Volcanol Soc Japan 43(1): 1–13. https://doi.org/10.18940/kazan.43.1_1
Yamasato H (2005) Modern history of volcano observation in Japan - especially volcano surveillance of Japan Meteorological Agency. Bull Volcanol Soc Japan 50: S7-S18. https://doi.org/10.18940/kazan.50.Special_S7
Yamazaki Y, Soares G, Matzka J (2022) Geomagnetic detection of the atmospheric acoustic resonance at 3.8 mHz during the Hunga Tonga eruption event on January 15, 2022. J Geophys Res: Space Physics, 127:e2022JA030540. https://doi.org/10.1029/2022JA030540
Yeh KC, Liu CH (1974) Acoustic-gravity waves in the upper atmosphere. Rev Geophys 12(2):193–216. https://doi.org/10.1029/RG012i002p00193
Yoder HS Jr (1952) Change of melting point of diopside with pressure. J Geol 60(4):364–374. https://doi.org/10.1086/625984
Yokoo A, Ishii K, Ohkura T et al (2019) Monochromatic infrasound waves observed during the 2014–2015 eruption of Aso volcano. Japan Earth Planets Space 71:12. https://doi.org/10.1186/s40623-019-0993-y
Yokoo A, Iguchi M, Tameguri T, Yamamoto K (2013) Processes prior to outbursts of vulcanian eruption at Showa crater of Sakurajima volcano. Bull Volcanol Soc Japan 58(1): 163–181. https://doi.org/10.18940/kazan.58.1_163
Yokoyama I, De la Cruz-Reyna S (1990) Precursory earthquakes of the 1943 eruption of Paricutin volcano, Michoacan, Mexico. J Volcanol Geotherm Res 44(3–4):265–281. https://doi.org/10.1016/0377-0273(90)90021-7
Yokoyama I (2001) The largest magnitudes of earthquakes associated with some historical volcanic eruptions and their volcanological significance. Annals Geophys 44(5–6). https://doi.org/10.4401/ag-3553
Yuen DA, Scruggs MA, Spera FJ, Zheng Y, Hu H, McNutt SR, Thompson G, Mandli K, Keller BR, Wei SS, Peng Z (2022) Under the surface: pressure-induced planetary-scale waves, volcanic lightning, and gaseous clouds caused by the submarine eruption of Hunga Tonga-Hunga Ha'apai volcano. Earthquake Res Adv, p.100134
Zobin VM (1971) Mechanism of volcanic earthquakes of the Sheveluch volcano, Kamchatka. Bull Volcanol 35(1):225–229. https://doi.org/10.1007/BF02596819
Zobin V (2016) Introduction to volcanic seismology (third edition). Elsevier, Amsterdam
Acknowledgements
R.S.M. acknowledges NSF grants EAR-1446543 and EAR-1847736. R.S.M. thanks Annie Platoff, UC Santa Barbara Library for assistance with tracking down references. We thank Bernard Chouet, two anonymous reviewers, and editor Andrew Harris for their helpful comments and additional perspective.
Figure 2 Reproduced from Omori (1912) and Omori (1916). Figure 3 Reproduced from Saderra Masó (1911a). Figure 4 Reproduced from Minakami (1960). Figure 5 (left) Reproduced from Okubo et al. (2014). Figure 5 (right) Reprinted from Matoza et al. (2021), with permission from Wiley. Figure 6(a) Reprinted from Chouet (1979), with permission from Wiley. Figure 6(b and c) Reprinted from Fehler (1983), with permission from Wiley. Figure 7(a) Reprinted from Kawakatsu et al. (1992), with permission from Wiley. Figure 7(b) Reprinted from Neuberg et al. (1994), with permission from Wiley. Figure 7(c) Figure from Kaneshima et al. (1996) reprinted with permission from AAAS. Figure 8(a) Reprinted from Ripepe et al. (1996), with permission from Wiley. Figure 8(b) Reprinted from Vergniolle and Brandeis (1994), with permission from Wiley. Figure 8(c) Reprinted from Sakai et al. (1996). Figure 8(d) Reprinted from Garces et al. (1998), with permission from Wiley. Figure 9 Reproduced from Gil-Cruz (1999). Figure 10(a and b) Reproduced from Finch (1949). Figure 10(c) Reprinted from Developments in Solid Earth Geophysics Book series, Physical Volcanology, Edited by L. Civetta, P. Gasparini, G. Luongo, A. Rapolla, Author: Akira Kubotera, Chapter 2 - Volcanic tremors at Aso volcano, Volume 6, 1974, Pages 29–47, with permission from Elsevier. Figure 11(a) Reprinted from Aki et al. (1977), with permission from Elsevier. Figure 11(b) Reprinted from Chouet (1985), with permission from Wiley. Figure 11(c) Reprinted from Chouet (1988), with permission from Wiley. Figure 11(d) Reprinted from Kumagai and Chouet (2000), with permission from Wiley. Figure 12 Reprinted from Developments in Solid Earth Geophysics Book series, Physical Volcanology, Edited by L. Civetta, P. Gasparini, G. Luongo, A. Rapolla, Author: Takeshi Minakami, Chapter 1 - Seismology of Volcanoes in Japan, Volume 6, 1974, Pages 1-27, with permission from Elsevier. Figure 13 Figure from Tokarev (1978), reprinted by permission from Springer Nature.
Author information
Authors and Affiliations
Corresponding author
Additional information
Editorial responsibility: R.Sulpizio
This paper constitutes part of a topical collection: IAVCEI 1919-2019: One hundred years of international outreach and scientific advances in Volcanology
Rights and permissions
Open Access This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons licence, and indicate if changes were made. The images or other third party material in this article are included in the article's Creative Commons licence, unless indicated otherwise in a credit line to the material. If material is not included in the article's Creative Commons licence and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this licence, visit http://creativecommons.org/licenses/by/4.0/.
About this article
Cite this article
Matoza, R.S., Roman, D.C. One hundred years of advances in volcano seismology and acoustics. Bull Volcanol 84, 86 (2022). https://doi.org/10.1007/s00445-022-01586-0
Received:
Accepted:
Published:
DOI: https://doi.org/10.1007/s00445-022-01586-0