Coupling Between Magmatic Degassing and Volcanic Tremor in Basaltic Volcanism

Magmatic degassing, typically measured as SO2 flux, plays a key role in controlling volcanic eruption style and is one of the key parameters used by volcano observatories to assess volcanic unrest and detect eruption precursors. Volcanic tremor, the integrated amplitude of seismic energy release over a range of frequencies, is also a key parameter in volcano monitoring. A connection between volcanic degassing and tremor has been inferred through correlations between the signals which are often, but not always, observed during periods of unrest or eruption. However, data are often equivocal and our understanding of the physical processes, which couple degassing with tremor are still evolving. New insights into degassing-tremor coupling can be made by investigation of the long-term relationship between degassing and tremor, focussing on the frequency-dependence of tremor and passive degassing behaviour. In this study, we examine how long-term SO2 emission rates and volcanic tremor on Mt. Etna, track rapid variability in eruptive dynamics. Correlations between SO2 flux and tremor are explored in both quiescent and eruptive periods, comparing the two parameters at both long and short time-scales (<< 1 day) for ~2 years. Our analysis reveals that over month-long timescales passive degassing of SO2 and tremor tend to be well-correlated, but these correlations are lost over shorter timescales. This reflects a coupling process between passive degassing and tremor, produced by a combination of gas flow through permeable magma and the convective flow of magma within the conduit. Short-term correlations are lost because variations in the continuous degassing process are relatively small compared with the overall degassing rate and fall below measurement noise..During eruptive periods strong correlations are observed between degassing and tremor, with a greater contribution of higher frequency signal in tremor, controlled by eruptive style. These observations suggest that in sin-eruptive periods the tremor source is dominated by the coupling between the eruption column and the ground through infrasonic waves, rather than conduit processes. Our results demonstrate the importance of high quality long-term observations and offer new insights into the physical mechanisms which couple degassing and volcanic tremor at active volcanoes.

Volcanic tremor is observed at volcanoes as background seismic radiation in quiescent stages and as peaks in amplitudes during eruptive episodes such as explosive eruptions (e.g., Alparone et al., 2003;Patanè et al., 2013). Dominant frequency ranges between 0.1 and 10 Hz and episodes of high amplitude tremor may persist for months (e.g., Kubotera, 1974;McNutt, 1992;Zobin, 2003). Physical processes generating volcanic tremor are thought to be associated with unsteady mass transport-flow of magma dynamically coupled with the surrounding rocks (Steinberg and Steinberg, 1975;Schick and Mugiono, 1991;Neuberg and Pointer, 2000;Battaglia et al., 2005). However, several other mechanisms (e.g., Gordeev, 1993;Benoit and McNutt, 1997) and models have been proposed as potential sources of tremor (e.g., Aki et al., 1977;Chouet et al., 1987) depending on individual volcanoes and eruption style (Konstantinou and Schlindwein, 2002;Matoza and Fee, 2014). In particular, a review of the engineering literature associated with studies of two phase fluid flow induced vibration in pipes was recently published (Miwa et al., 2015), focusing on the hydrodynamic force produced by flows that generate potentially destructive vibrations in industrial machines and infrastructure. The review highlighted the impact of different flow patterns, turbulence and pipe geometry, producing a fluctuation force magnitude spectrum with a frequency range similar to that observed for tremor in volcanic settings when velocities were in the range of magma flow during quiescent degassing ∼0.6 ms −1 (Burton et al., 2007).
Persistent degassing from active volcanoes is widely associated with volcanic tremor (e.g., Williams-Jones et al., 2001;Konstantinou and Schlindwein, 2002;McNutt, 2002). Evidence of coupling between the two parameters has been discussed at different volcanic systems (e.g., Mt. Etna: Gresta et al., 1991, Bruno et al., 1995Patanè et al., 2013;Zuccarello et al., 2013;Soufrière Hills: Miller et al., 1998;Edmonds et al., 2003b;Piton de la Fournaise: Battaglia et al., 2005;Colima: Vargas-Bracamontes et al., 2009). Increases in tremor amplitude were observed prior to and during effusive eruptions and synchronous with explosive activity (e.g., Usu: Omori, 1911;Pavlof: McNutt, 1986;Hekla: Brandsdóttir and Einarsson, 1992;Galeras: Fischer et al., 1994;Mt. Etna: Cannata et al., 2008;Bonaccorso et al., 2011b;Kilauea: Nadeau et al., 2015). Changes in the dominant tremor frequency have been commonly associated with changes in the regime and style of eruptive activity (e.g., Ereditato and Luongo, 1994;Thompson et al., 2002;Alparone et al., 2003;Bryan and Sherburn, 2003;Cannata et al., 2018). At Mt. Etna, Leonardi et al. (2000a) studied the relationship between volcanic tremor and SO 2 flux in the period between 1987 and 1992 by cross-correlation analysis. Their results indicated that, in the case of eruptive activity, the two signals strongly correlated. The authors proposed that such as behavior might have resulted from common physical mechanisms related to magma dynamics. Similarly, at Soufrière Hills, Montserrat, Young et al. (2003) found systematic and direct correlation between SO 2 flux and tremor analyzing data between December 1999 and January 2000, with gas flux lagging behind the tremor signal. Similar correlations between SO 2 outgassing and seismic amplitude were observed also at Villarrica (Palma et al., 2008), Yasur (Bani and Lardy, 2007), Fuego (Nadeau et al., 2011), and Kilauea (Nadeau et al., 2015). Volcanic tremor has also shown good correlation with other geochemical parameters. For instance, Alparone et al. (2005) carried out a statistical analysis on radon emissions from the soil and reduced displacement of volcanic tremor both recorded during paroxysmal explosive phases of Mt. Etna's summit craters. Their studies revealed increase in radon concentrations ∼58 ± 12 h prior to changes in volcanic tremor. More recently, investigating the relationship between CO 2 flux and volcanic tremor at Mt. Etna, Cannata et al. (2009a) found that variations in the geochemical signal preceded those of volcanic tremor of ∼50 days. Nevertheless, in some cases contradictory or/and lack of relationship between eruptive activity and tremor amplitude has been observed. Doukas and Gerlach (1995), observed an episode of inverse correlation between SO 2 flux and volcanic tremor at Mount Spurr, Alaska during the 1991-1993 eruptive activity, interpreting the gas declined as a result of SO 2 absorption by the hydrothermal system. Similarly, inverse correlations between CO 2 flux and volcanic tremor were observed at Stromboli (Aiuppa et al., 2009). At Soufrière hills volcano, Watson et al. (2000) reported that high rates of SO 2 were associated with enhanced seismicity and ground deformation a month before the 1997 dome collapse. However, previous observations by Young et al. (1998) showed that the enhanced long-period seismicity at Soufrière Hills did not relate to increases in SO 2 flux. This indicates that, though tremor and degassing are somewhat coupled, the nature of their relationship, as well as the source mechanism for tremor, are still poorly understood. It is likely that several processes are involved in the generation of volcanic tremor from gas and magma flows, making the unraveling of the tremor and degassing relationship challenging.
Here, we focus on three mechanisms by which volcanic tremor may be coupled with degassing: (1) flow of gas through permeable magma (e.g., Burton et al., 2007;La Spina et al., 2017), (2) magma flow within a conduit (e.g., Kazahaya et al., 1994;Beckett et al., 2014), and (3) coupling of eruptive processes to ground seismicity through infrasound during explosive activity (Matoza and Fee, 2014). The links between these processes and magmatic degassing are explored on Mt. Etna by comparing seismic tremor measured with the INGV seismic network with SO 2 flux measurements collected with INGV FLAME network. Long-and short-timescale comparisons of the two parameters for six case studies selected between 2007 and 2008 were carried out by correlation analysis to investigate whether the correlation holds across different timescales.

ERUPTIVE ACTIVITY BETWEEN 2007 AND 2008
Mt. Etna is the most active volcano in Europe characterized by extensive quiescent and active degassing activity that occurs at the main craters (North-East Crater: NEC, South-East Crater: SEC, and central craters Voragine: VOR, and Bocca Nuova: BN, Figure 1; e.g., Allard, 1997;Aiuppa et al., 2008). Between 2007 and 2008, eruptive activity at Mt. Etna resumed after a quiescent period following the 2006 eruption (Bonaccorso et al., 2011a). Activity was vigorous and characterized by a series of relatively short explosive episodes and long-lasting lava effusion both occurring from the eastern flank of SEC. (Andronico et al., 2008;Corsaro and Miraglia, 2009;Bonaccorso et al., 2011a). This period is divided into two main phases, firstly the period January 2007 to early May 2008 characterized by intermittent lava fountains and the period May-December 2008, characterized by effusive activity (Figure 2). The first stage, from January 2007 to early May 2008, consisted of sporadic violent strombolian and lava fountaining episodes accompanied by short-lasting lava effusion (e.g., Andronico et al., 2008;Di Grazia et al., 2009;Bonaccorso et al., 2011a,b;Behncke et al., 2016). Paroxysms exhibited recurrent features consisting on increasing strombolian activity at first, lava flow output, and transition from strombolian to lava fountaining (Aloisi et al., 2009;Di Grazia et al., 2009;Langer et al., 2010). This activity was similar to the lava fountain sequences observed at SEC in 2000 (e.g., Alparone et al., 2003;Allard et al., 2005;La Spina et al., 2015), and between 2011 and 2015 (e.g., Calvari et al., 2011;Patanè et al., 2013;Corsaro et al., 2017). The effusion phase, between 13 May and December 2008, started 3 days after the 10 May paroxysm (Aloisi et al., 2009;James et al., 2011), and was dominated by lava effusion occasionally accompanied between May and early September 2008 with strombolian activity from the eruptive fissure (Cannata et al., 2009b;Bonaccorso et al., 2011a;Currenti et al., 2011).

DATA ACQUISITION AND ANALYSIS
All data presented here were acquired by the continuous geochemical and geophysical monitoring system of Istituto Nazionale di Geofisica e Vulcanologia, Osservatorio Etneo (INGV-OE).

SO 2 Flux
The bulk SO 2 flux from the summit craters and eruptive fissure of Mt. Etna was measured automatically by the FLAME scanning spectrometer network (Salerno et al., 2009b;Calvari et al., 2011). The network consists of ten ultraviolet scanning spectrometer stations spaced ∼7 km apart and installed at an altitude of ∼900 m above sea level (a.s.l.) on the flanks of Mt. Etna (Calvari et al., 2011). Recorded UV spectra were retrieved in SO 2 column amounts using the DOAS method (e.g., Platt and Stutz, 2008), and applying a modeled background reference spectrum Salerno et al., 2009a). Retrieved SO 2 data were transmitted to INGV-OE where they were converted into mass flux rate. Each flux datum was time corrected to account for the travel time of the plume from the summit craters to the scanning plane of each scanner of the network (∼14 km). Uncertainty in computed SO 2 flux depends to an extent on plume velocity, because at very low velocities the absolute velocity error becomes a larger proportion of the relative error in calculated flux. Assumptions on plume height are made based on observations of the relationship between plume velocity and height, and light scattering effects also contribute to the flux error budget (e.g., Campion et al., 2015). Salerno et al. (2009b) estimates uncertainty in SO 2 flux by stationary automatic scanning array between −22 + 36%, but error can vary to greater than 100% depending on conditions.

Seismic Data
The permanent seismic network of INGV comprises 45 threecomponent broadband (40 s) digital stations with continuous data acquisition and transmission at a sampling frequency of 100 Hz (Figure 1; e.g., Di Grazia et al., 2006;Patanè et al., 2008). In this work, we use data from the Etna Cratere del Piano (ECPN) station, which is set up on the southern flank of the volcano at an altitude of 2900 m a.s.l. and ∼1 km from the summit craters (Figure 1). The ECPN station was chosen as it offers the longest data continuity provided during the studied period, the best signal to noise ratio and its proximity to the summit craters makes it especially sensitive to eruptive activity. Volcanic tremor spectral amplitude was calculated using the root mean square (RMS expressed in arbitrary unit) of the seismic signal recorded on the vertical component. In this study, the daily RMS at overall spectral amplitude (OSA) was used for long-term characterization of volcanic tremor and to explore its relationship with daily SO 2 flux. In order to inspect the shortterm relationship between SO 2 flux and tremor and identify if any and which frequency components correlated most strongly with degassing rates, seismic amplitude was decomposed into separate frequency bands (e.g., Gresta et al., 1987;Thompson et al., 2002;Di Grazia et al., 2009). RMS spectral amplitude was calculated for several frequency bands of 1 Hz width in the frequency range 0.025-10.5 Hz, and tremor amplitude was obtained by averaging the RMS values with a 5 min time window. This time window was chosen according Cannata et al. (2009a), who report that time windows of this length are a good compromise between the stability of the signal and the opportunity of observing details of the evolution of the parameter during eruptions. Uncertainties affecting RMS depends on the dispersion of the averaged RMS time window; it ranges between 10% for the short-5 min intraday study and up to mean 25%, enveloped between a minimum of 6% and maximum of 77%, for the long-temporal daily averaged RMS.

Data Analysis
To investigate the relationship between the SO 2 flux and volcanic tremor, we apply the correlation analysis, which expresses the strength of linkage or co-occurrence between two variables in a single value ranging from −1 to +1, i.e.,−1 ≤ r ≤ +1 (e.g., Davis, 1986;McKillup and Dyar, 2010). Usually for evaluating dependences between two parameters, the conventional Pearson's correlation analysis is used. However, this method requires normal distribution of the parameter samples. Since both SO 2 flux and volcanic tremor data were characterized by non-Gaussian distribution (mean skewness and kurtosis are 1.1 and 0.9, and 1.2 and 1.1, respectively; Table 1 and Supplementary Figure S1) and the SO 2 flux sample sizes were small (maximum 120 daily-light observations), the non-parametric Spearman's Rank correlation analysis was applied (e.g., Zar, 1972;Davis, 1986;Swan and Sandilands, 1995). Compared to the Pearson's correlation analysis, the Spearman's correlation method does not require continuous-level data (interval or ratio), as it uses ranks instead of assumptions on the distributions of two variables. This allows analysis of the association between variables of ordinal measurement levels. Mathematically, Spearman's and Pearson's correlations are very similar in the way that they use different measurements to calculate the strength of association of two parameters. Pearson's correlation applies standard deviations, while Spearman's the difference in ranks (Davis, 1986;Swan and Sandilands, 1995). Figure 2 reports the weekly averaged SO 2 flux and the daily OSA of the volcanic tremor RMS for long-term observation between 2007 and 2008. Over the investigated period, tremor and SO 2 flux show common changes at different temporal and magnitude scales associated in both stages of quiescentpassive degassing and eruptive activity (Figure 2). During the intermittent paroxysmal phase, preceding the opening of the eruptive fissure on May 13, 2008, the SO 2 rates and tremor behaved in a similar manner showing marked oscillations in correspondence to the explosive activity. These waxing-waning trends have higher amplitudes starting from the end of July 2007 until the opening of the 2008-2009 eruptive fissure ( Table 1). Note that in Figure 2, volcanic tremor RMS is plotted in logarithmic scale to allow for better comparison with SO 2 flux, and values are expressed in arbitrary units. Short-term intraday comparison between SO 2 flux-volcanic tremor patterns were long time window can be splitted into two phases according to the eruptive activity observed at the surface. The first phase relates to an intermittent paroxysmal phase consisting of ash emission (black square), strombolian activity (green-square), lava fountaining (gray-square), and lava emission (red-square), the second phase refer to a period characterized by persistent lava emission and irregular moderate strombolian explosions and ash emissions along the 2008-09 eruptive fissure. Uncertainty in SO 2 flux by stationary array arise from several sources, such as wind-plume transport speed, plume height and radiative transfer, these parameters maybe highly variable being the flux affected by and uncertainty that may ranges between -22 and 36, up to 100% in challenging condition. Uncertainty in daily RMS depends on the intraday variability of the seismic averaged signal and it ranges between 10% for the intraday study and mean of 25% for the daily long-term investigation.

RESULTS
carried out to explore potential correlation between the two signals on a scale of minutes (Figure 3). Of the seven lava fountain episodes of the intermittent paroxysmal phase and of the strombolian activity fed by the eruptive fissure on 14 May, only 6 days could be analyzed ( Table 1). The other episodes had to be excluded due to eruptive events at night (when UV spectroscopy was not possible) or on days when the plume was blown to the northern and western flanks of the volcano beyond the coverage of the FLAME network. In addition, some of the eruptive episodes were also excluded from the analysis due to the limited number of SO 2 scans on the given days. Figure 3 shows the intraday SO 2 flux and volcanic tremor data for the six case studies. In each of the six graphs, SO 2 flux is plotted together with RMS at a dominant frequency, i.e., that has shown the highest SO 2 flux-volcanic tremor correlation coefficient between 0.025 and 10.5 Hz; likewise correlation analysis was also performed considering the OSA (Table 1; Figure 4). Signals display simultaneous changes in both magnitude and temporal scale repeatedly over the course of the measurements and persist over time scales ranging from 6 to 12 h. This correlation occurs during both stage of onset and waning phase of strombolian activity (case 1 and 2) and transition from strombolian to lava fountaining (case 3), both eruptive styles superimposed on short-lived and persistent lava flow output (4-6; Table 1). SO 2 flux was strongly correlated with seismic tremor between 2.5 and 6.5 Hz during explosive eruptions and between 0.025 and 2.5 Hz (case studies 1-3, and in 4-6, respectively; Table 1), isolated anticorrelation were also observed for cases 1, 2, and 4, when SO 2 emission rates increased while RMS decreased.
Analysis of the source depth of seismic tremor demonstrates that the entire shallow conduit is a tremor source (e.g., Patanè et al., 2008;Cannata et al., 2013), consistent with our frictional flow hypothesis, with a peak in energy at a depth of 2-3 km, perhaps due to the lower viscosity of magma at this depth permitting a maximum ascent rate (e.g., Burton et al., 2007). There are two main regimes of magma flow, firstly as a result of effusive eruption, in which magma degasses and crystallizes during ascent before erupting, and secondly due to the convective overturn of magma during quiescent degassing (Kazahaya et al., 1994;Beckett et al., 2014) which is required to sustain the persistent degassing flux of Mt. Etna (e.g., Allard, 1997). This flow transports magma from below 3 km depth (from the volcano summit) to nearsurface, which is the principle pressure regime where sulfur and water exsolution takes place at Mt. Etna (Metrich et al., 2004;Spilliaert et al., 2006;Wallace and Edmonds, 2011). Convective overturn leads to permanent burial of degassed magma in the roots of the plumbing system, revealed as a voluminous plutonic body in seismic tomography observations (Patanè et al., 2006;Díaz-Moreno et al., 2018). We tentatively propose that periods of weak correlation between SO 2 flux and tremor, such as that observed in early 2007, are produced when magmatic overturn slows down, and degassing becomes dominated by permeable gas flow from depth. A further related process, which could play a key role, is the level and condition of magma in the conduit, as a lower magma level together with magma viscosity, gas and crystal content may attenuate the tremor amplitude (e.g., Collier et al., 2006). These processes will be investigated in future work through examination of CO 2 /SO 2 and ground deformation time series. Short-term correlations on the scale of a day between gas flux and tremor during quiescent periods are not observed clearly, perhaps because variations in the continuous degassing process are relatively small compared with the overall degassing rate and fall below measurement noise. Future improvements in the precision and accuracy of SO 2 flux quantifications are required to reveal any short-term correlations during passive degassing.
In order to characterize the main oscillations of both intermittent paroxysmal and 2008-2009 eruptive phases, corresponding to the more intense explosive episodes of the study period, an inspection at daylight intraday scale was carried out. Tremor was decomposed to its spectral components between 0.025 and 10.5 Hz signal, and then each volcanic tremor frequency was compared with SO 2 flux using correlation analysis. This decomposition allowed statistical identification on the best correlation between SO 2 flux and volcanic tremor frequency, and highlights that in different eruptive contexts the geochemical signal correlated with tremor at different dominant frequencies (Figure 4). We found that SO 2 flux correlated strongly with volcanic tremor with high frequencies during the most explosive activity. This is consistent with the observation of coupling via infrasound between explosive volcanic activity and the ground, producing a high frequency tremor source (Matoza and Fee, 2014). In the six case studies investigated here, the first three of them, i.e., those falling within the intermittent paroxysmal phase (Figure 2) showed the highest SO 2 flux/tremor correlation coefficients at frequencies of 2.5-6.5 Hz (Table 1;  Figure 4). Conversely, the case studies pertaining to the 2008-2009 eruptive fissure activity displayed the highest correlations at lower frequencies, i.e., from 0.025 to 2.5 Hz (Table 1; Figure 4). The fact that the two parameters correlated at different tremor frequencies, and that the frequency depended on the intensity of the associated eruptive phenomenon, suggests that on long time scales, some of the signal features could be masked or missed if the RMS is calculated for all frequencies. Falsaperla et al. (2005) analyzed amplitude and frequency content of the seismic FIGURE 3 | Intraday SO 2 flux and volcanic tremor amplitude for the selected case studies ( Table 1). In the six cases, tremor mirrored SO 2 outgassing in different eruptive style and transition. SO 2 flux (red line) was strongly correlated with volcanic tremor at frequency band with max correlation clustered in two groups of high (black line) and medium-low frequency (gray, green, cyan, and blue lines).
signal of the 2001 Mt. Etna's flank eruption finding considerable changes in the volcanic tremor associated with different styles of eruptive activity. In particular, they observed that the dominant frequency of the signal decreased from ∼5 Hz to 3 Hz during lava fountaining, and further decreased to ∼2 Hz during intense lava emissions, supporting the infrasound-coupling hypothesis as the source of seismic tremor during more explosive activity. There were also periods where SO 2 flux and tremor appear anticorrelated on short timescale, resulting from time shifts of the two parameters. Shifts were identified in cases 1, 2, and 4, with gas lagging behind seismic energy release. This behavior, which has also been observed on long-time scales by Leonardi et al., 2000b, has been interpreted as due to increasing pressurization of the volcano's shallow feeder system, which simultaneously increases tremor but with a lag time before gas release at the onset of eruptive activity (e.g., Young et al., 2003;Nadeau et al., 2011). A further process might rely on the turbulent magma-flow rate in the upper conduit triggered by gas-slug dynamics during ongoing eruptive events (e.g., Parfitt, 2004) coupled with instability of magma column (Bercovici et al., 2013).
These results underline that though the strong association between magmatic degassing and tremor, several process are involved in generating seismic energy. Their mutual behavior might change depending on the physical mechanism of magma flow regime and gas/melt separation in the conduit, revealing the gas-tremor study puzzling. Although further efforts are required to advance our understating in magmatic degassing -seismic tremor release relationship, the strong correlation observed in this study between the two parameters, indicates that degassing generates seismic tremor, and that gas flux might thereby provide a proxy for eruptive style and intensity and short-term warning for impeding eruptions.
FIGURE 4 | Correlation coefficient of SO 2 flux vs. volcanic tremor in the six intraday case studies investigated at frequency bands between 0.025 and 10.5 Hz and OSA. Overall, the two parameters show reliable correlation between 0.6 and 0.9 Hz (Leonardi et al., 2000b). In each of the six histograms, the yellow bin represents the maximum correlation between the SO 2 flux and volcanic tremor. In detail, case studies 1, 2, and 5 (except for the frequency below 0.5 Hz) show good correlation at almost all frequencies. Case studies 3 and 6 display bimodal distribution of the correlation coefficients with dominant frequencies centered at 3 and 1 Hz in case study 3 and 6, respectively. Case study 4 is characterized by both positive and negative correlation coefficient values. The positive maximum value corresponds to below 0.5 Hz. The negative bars indicate the frequencies at which SO 2 flux and volcanic tremor anticorrelated CONCLUSION Both explosive and effusive eruptions are believed to be largely controlled by volatile content and magma flow rate (e.g., Woods and Cardoso, 1997), and by their mutual modulation within the shallow conduit (e.g., Jaupart and Vergniolle, 1988). Likewise, seismic tremor varies with volcanic activity and is considered originated by fluids dynamic process in volcanic conduit (e.g., Chouet, 1996). Results achieved in this study provide strong evidence that for extended periods the volcanic tremor and SO 2 flux signals on Mt. Etna are strongly correlated. The mutual relationship rely on a physical mechanism of magma flow, which through friction between magma and conduit walls produces a tremor signal with frequency dominated between 0.025 and 2.5 Hz. This magma flow provides the source of SO 2 emitted persistently at the summit craters during passive degassing and the eruptive vents during effusive activity, through exsolution and transport of SO 2 during magma ascent. We tentatively attribute periods of low correlation between tremor and SO 2 flux to a different degassing regime, dominated by fluxing of gas from depth, and this hypothesis will be tested in future work. Our examination of explosive activity demonstrates that the best correlation is achieved between high frequency tremor (2.5-6.5 Hz) and SO 2 flux, which we attribute to a process of coupling through infrasound between the explosive activity in the atmosphere and the surface, creating high frequency tremor. Our results underline the clear link between the geochemical and the geophysical signals. Their common behavior during both quiescent and eruptive stages, and during transitions between eruptive regimes, emphasizes that magmatic degassing produces volcanic tremor, and that both originate from a common physical mechanism of magma dynamics in the shallow conduit. This study provides a framework for the interpretation of tremor and SO 2 degassing to other persistently active basaltic systems worldwide, which will assist in the understanding of the processes and mechanisms controlling unrest and pre-eruptive activity.

AUTHOR CONTRIBUTIONS
GS and MB coordinated the research and mainly wrote the manuscript with the substantial, direct, and intellectual contribution to the work from all authors.

ACKNOWLEDGMENTS
We greatly acknowledge F. Murè and V. Longo for their technical assistance in the FLAME network. We thank Dr. L. Spampinato for useful discussions. We are also grateful to the two reviewers for helpful comments and suggestions.