The inter-arrival times of the post 2000 seismicity at Campi Flegrei caldera are statistically distributed into different populations. The low inter-arrival times population represents swarm events, while the high inter-arrival times population marks background seismicity. Here, we show that the background seismicity is increasing at the same rate of (1) the ground uplift and (2) the concentration of the fumarolic gas specie more sensitive to temperature. The seismic temporal increase is strongly correlated with the results of recent simulations, modelling injection of magmatic fluids in the Campi Flegrei hydrothermal system. These concurrent variations point to a unique process of temperature-pressure increase of the hydrothermal system controlling geophysical and geochemical signals at the caldera. Our results thus show that the occurrence of background seismicity is an excellent parameter to monitor the current unrest of the caldera.
Forecasting the evolution of a volcano in unrest requires interpretation on earthquakes, ground deformation, and volcanic degassing processes1, 2. When dealing with restless calderas, this interpretation is challenging. While eruptions do not always follow clear signs of unrest, calderas can erupt with little warning, preceded only by small unrest signals3, 4. Due to this complex behaviour and the hazard associated to their large-scale eruption
s, calderas are generally considered the most dangerous types of volcanoes.
Starting from 1950’s, Campi Flegrei caldera (CFc) has shown clear signs of reawakening5. Since then, a series of inflation episodes of short duration (1–2 years) and abrupt intensity (1.8 m ground uplift in 1983–1984) has interrupted the long deflation phase started after the last eruption (Monte Nuovo eruption, A.D. 1538; ref. 6). This pattern changed at the beginning of the new millennium, when a long, still ongoing period of semi-continuous and accelerating ground uplift has worked in parallel with large variations in the composition of the main fumaroles, and changes in seismicity patterns7,8,9.
In this work, the CFc seismicity is discussed in combination with the other monitoring parameters, i.e. ground deformation data and the compositions of the main fumaroles located inside Solfatara, the most active zone of the caldera (Fig. 1).
Since 2000 the earthquake occurrence rate and seismic energy release have increased relatively in time, even if both parameters remain low10,11,12 (e.g. max duration magnitude 2.5). Despite the low intensity of earthquakes, the low rate of earthquake occurrence, and the rarity of Long Period (LP) and tremor events many studies have tried to model the mechanisms of the recent CFc seismicity9, 13,14,15,16,17. However, the interpretation of the current processes leading to CFc post-2005 activity is mainly based both on ground deformation data18,19,20 and on the evolution of the hydrothermal activity (fluxes and fumarolic compositions21, 22). Ground deformation data and measured geochemical parameters show in fact remarkable time-dependent variations7, 8, 18.
Our aim is to investigate if and how the source of the current seismicity at CFc is associated with the ground deformation and geochemical signals. Deformations and geochemistry, on the one side, suggest the occurrence of magmatic intrusions18, 23 and/or the injection of large amounts of magmatic fluids7. On the other side, the ongoing shallow, low-magnitude seismicity of CFc is hardly associated with any magma movement. This is the opinion of the scientists involved in recent elicitation experiments, whose conclusion is that earthquakes at CFc may reveal magma movements only if either deep (>3500 m depth) or energetic (M > 2.5–3) (ref. 24; http://bet.bo.ingv.it/elicitazione/public/). Assessing this type of “correlations - not correlations” among different monitoring parameters has important consequences on the quantification of short-term volcanic hazard25,26,27.
In this work, we first extract earthquake swarms (or seismic clusters) from the seismic catalogue, yielding what we name “background seismicity” of CFc. The background seismicity is then compared with ground deformation and gas geochemical indicators from the monitoring system of the Osservatorio Vesuviano-INGV (Fig. 1, see Methods). Finally, the background seismicity is compared with the results of a recently-published thermo-fluid-dynamic model that simulates the effects of repeated injections of magmatic fluids into the CFc hydrothermal system feeding the fumaroles7.
Statistics of earthquake sequences: swarm and background events
The 2000–2016 CFc seismicity is mainly characterized by swarm-type occurrence of low-magnitude volcanic quakes (Volcano-tectonic – VT and Long period – LP). The most common events are VT events that show duration-magnitudes lower than 2.5. Almost all VT epicenters are clustered inside a 2500 m radius circle centered at Solfatara crater (Fig. 1) and above the depth of 2000 m. Swarms of LP events occur only occasionally15, 17 and are characterized by extremely (and not easily quantifiable) low energy. They are localized (when possible due to the low signal-to-noise ratio) in very small volumes (of the order of 200 m side15). On the 30th of January 2015, a short duration (of the order of hours) tremor episode has been detected using small aperture arrays (Fig. 1) and attributed to shallow hydrothermal sources12, 28.
In this work, we focus only on VT events because, also due to their small energy, adding LP’s to the used seismic catalogue would have produced some difficulty into the completeness determination. On the other hand, again due to their low energy and to the much lower numbers of LP swarms with respect to the VT events, the bias introduced in neglecting them is inessential for our aims. In particular, we focus on VT events with duration magnitude Md > −0.5 (the catalogue in the years 2000 – to the present is reasonably complete for Md > −1, see supplementary information). Petrosino and coauthors (ref. 29) revised the VT Md scale at CFc using improved path and site transfer functions.The authors calculated moment-magnitudes and Wood-Anderson equivalent magnitudes, finding out a bias (underestimation) of the local scale of the order of a factor 0.6 for the lowest magnitude events. Despite this bias, we use in the present paper the magnitude values routinely calculated and still in use at CFc for sake of continuity with past literature. It is noteworthy that the obtained results do not depend on this choice, because they are dependent on the inter-arrival time of VT events and not on their magnitude.
While most of the VT events are clustered in space and time (swarms of few hours duration and hundreds of meters lateral extension), a significant number of single events are spatially sparse in time. A bimodal distribution roughly fits the histograms of the earthquake log inter-arrival times at CFc between 2000 and 2016 at all magnitudes (Fig. 2a). The modal values of the two populations are (1) less than 15 minutes for the low inter-arrival time population and (2) more than 3 days for the high inter-arrival time population (Fig. 2a). The two populations correspond to (1) events occurring during volcanic seismic swarms (swarm events) and (2) the sum of seismic swarms plus isolated events that hereafter will be referred as background seismicity. In each of the histograms of Fig. 2a the two populations are roughly divided by a time-interval of approximately 1 day. Practically, the 1-day threshold filters all swarm events out of the CFc earthquake catalogue. The remaining events are what we call background seismicity; their cumulative distribution, which simply corresponds to the sum of the days in which at least one earthquake has occurred, will be referred as CB1.
To separate the swarm events from the background events we applied also a technique originally developed for geochemical data30 and more recently used to investigate different populations in soil CO2 fluxes31. The method is based on plotting the data in a lognormal probability plot (Fig. 2b). A single (n = 1) lognormal population would be plotted as a straight line, while n overlapping lognormal populations would result in a curve characterized by n − 1 inflection points. The observed log inter-arrival times pattern (expressed in log day unit) shows a curve with two inflection points, which describes the theoretical distribution of three (n = 3) overlapping lognormal populations (Fig. 2b). A Monte Carlo approach provides the relevant parameters of the three lognormal populations, i.e. the fraction of each population (f), the mean (μ), and the standard deviation (σ). The results of this test indicate that the observed distribution is given by the overlapping of two low inter-arrival times population L1 and L2 with a high inter-arrival times population H. The estimated parameters μ, σ and f (Table 1) adequately fit the data (Fig. 2b) and were used to compute the probability that each event belongs to the low inter-arrival time populations (either L1 or L2) or to the high inter-arrival times population H by applying the Bayes theorem: Pr(C|x) = (Pr(x|C) Pr(C))/Pr(x). Here C is the population of fraction Pr(C) = f and x is each event log inter-arrival time. Pr(C|x) is computed assuming that C follows a log-normal distribution, while Pr(x) is computed from the sum of the log-normal data. Finally, Pr(C|x) is the desired probability that x belongs to C. In the following, the cumulative of the probabilities that each event belongs to the H population (i.e. the background seismicity) is named CB2.
The third and last approach used to estimate the cumulative distribution of high inter-arrival events is that proposed by ref. 32 for de-clustering seismic catalogues. The method models the rate of earthquakes λ(t) as the sum of the rate v(t) of aftershocks (here swarms) triggered by previous earthquakes (from Omori-Utsu’s and productivity laws33) and the rate μ(t) of events triggered by other processes (here background seismicity). The rate μ(t) can be evaluated by subtracting the modelled rate of aftershocks v(t) from the observed rate λ(t). An iterative Expectation-Maximization approach allows to compute, for each earthquake i, the background probability as ωi = μ(ti)/λ(ti). The aftershock rate v(t) is estimated by optimizing a parameterized model made of a combination of both the Omori-Utsu’s and the productivity laws. The approach requires a temporal smoothing of the background probability time series ωi to determine μ(t). We optimize this smoothing parameter by using the Akaike Information Criterion34 for several such parameters (for a full description of the method, see ref. 32). The cumulative sum of the background probability ωi will be referred as CB3.
CB1, CB2 and CB3 are plotted in Fig. 3 together with the cumulative number of events. The three background curves (CB1, CB2, and CB3) are very similar, and their trend differs from that of the cumulative number of events. It is noteworthy that similar results can be obtained also by standard de-clustering techniques based on the space-time event distribution and not just the time distribution as in the present case35.
Background seismicity, ground deformation and gas geoindicators
Here, the background seismicity expressed as the CB1 function is compared with ground deformation and the fumarolic composition time patterns in 2000–2016 (Fig. 4). We used CB1 because this function is the simplest to measure being the cumulative of the events with inter-arrival times higher than 1 day, and because very similar results, practically the same, are obtained substituting CB1 with CB2 or CB3, given the similarity between the curves (Fig. 3).
The chronograms show that CB1 follows the same time pattern of ground deformation (Fig. 4a) and CO/CO2 ratio (Fig. 4b). Notably, background seismicity correlates much better to the other observations than other parameters derived from the VT catalogue (e.g. total number of events, swarm events, seismic energy). In particular, since 2008 ground deformation and CB1 are basically identical (Fig. 4c, R2 = 0.99). The chronogram (Fig. 4a) indicates that an acceleration has started in 2006, and has been followed by a ~6-years-long period (until 2012–2013) when the signals seem to follow a power-law type curve. The culmination of such period was interpreted as caused by magma intrusion at shallow depth23. After one year characterized by no ground deformation and almost null seismicity, both uplift and seismicity drastically increase starting from 2014. Overall, since 2005, the uplift and CB1 signals increase exponentially7.
CB1 displays a similar positive correlation with the fumarolic CO/CO2 ratio (Fig. 4b,d) that is the most sensitive gas-geothermometer for hydrothermal systems36, 37. The points are more scattered in both the chronogram (Fig. 4b) and the binary plot (Fig. 4d) than the vertical displacement. This is likely due to higher analytical uncertainties of the CO/CO2 ratio and, possibly, to the occurrence of minor seasonal variations that during the wet seasons cause a cooling of the shallowest parts of the hydrothermal system because of the arrival of cold water. By considering the annual mean (magenta dots) point scattering practically disappears and the seismic and geochemical signal show high correlation in both figures (Fig. 4b,d R2 = 0.97). This high correlation between background seismicity and compositional parameter of the fumaroles suggests that the increase of CB1 (and thus the corresponding uplift rates, Fig. 4a) proceeds concurrently with a temperature increase in the subsurface.
Simulation of the hydrothermal system and background seismicity
At Solfatara, large zones of soil diffuse degassing and fumarolic vents emit an impressive amount of hydrothermal vapour, composed mainly by steam and CO2, releasing thermal energy in the order of 100 MW38. Recently, a TOUGH2 model39 of the hydrothermal processes occurring within the feeding system of Solfatara, possibly controlling the current unrest at CFc, has been proposed7. Here we refer to the results of this model whose details are given in the cited reference7. Briefly, we used the TOUGH2 geothermal simulator to model the multiphase (gas and liquid) and multi-component (H2O and CO2) hydrothermal fluid circulation of the system feeding Solfatara fumaroles. The simulations are performed considering a 2D-radial domain (2500 m radius) of 2000 m thick (Fig. 5a), composed of rocks having homogeneous properties. Hydrothermal fluids enter the domain from the bottom (2000 m), in correspondence with the axis of symmetry, and until reaching steady state conditions. The system is then perturbed by injections of high amount of magmatic fluids. The observed CO2/CH4 and He/CH4, which are good indicators of the arrival of a magmatic component at fumaroles40, have constrained the timing of 14 episodes of magmatic fluid injections from 1983 to 20147. The magnitude and the CO2-H2O magmatic composition of each injection were constrained by the measured fumarolic CO2/H2O and N2/He molar ratios, respectively7.
Here, results of interest are the cumulative mass of magmatic fluids injected into the hydrothermal system (CMFCO2-H2O-CH4-N2-He Mt), and the temperature (TCO2-H2O-CH4-N2-He °C) of the rocks above the injection zone (Fig. 5a) simulated in the 2000–2014 period. The simulated absolute values of CMFCO2-H2O-CH4-N2-He and TCO2-H2O-CH4-N2-He partially depend on the initial steady state conditions (i.e. initial flux and composition of the hydrothermal fluids, rock properties, boundary conditions), however their temporal evolution during the simulation is a complex function of the fumarolic CO2-H2O-CH4-N2-He composition only, because these variables constrained the simulation while rock properties and boundary conditions have remained unchanged. Considering that no geophysical data were involved to constrain the simulation, the similarity of the temporal evolutions of CB1, TCO2-H2O-CH4-N2-He, and CMFCO2-H2O-CH4-N2-He (Fig. 6a,b), shown here by the high correlation of the seismic and geochemically derived signals (Fig. 6c,d; R2 = 0.98 and R2 = 0.99, respectively), is thus independent of the input of the model. This correspondence suggests an intimate relation between background seismicity and hydrothermal circulation and supports the reliability of the conceptual model of repeated magmatic fluid injections as the engine of the ongoing crisis of CFc.
Discussions and Conclusions
Ground deformations, seismicity, and geochemical variations are independent observations, but show the same temporal pattern. They thus point to a unique process controlling the ongoing crisis at CFc. Each observation, and in particular the seismic signal, is in strong correlation with the results (mass of injected fluids and temperature) of a thermo-fluid-dynamic model of repeated injections of high temperature magmatic fluids into the hydrothermal system feeding the fumaroles of Solfatara. These correlations are relevant and robust, as seismic data, geodetic data, and CO/CO2 ratios were not used to constrain the numerical model. They indicate that the observed patterns are all likely controlled by the pressure and temperature increase of the hydrothermal system due to repeated, impulsive transfers of high amount of magmatic gases from depth. This control is unsurprising considering that, since 2000, the cumulative seismic energy (~5 × 109 J) is orders of magnitude lower than the thermal energy released by fluid expulsion just at Solfatara (~5 × 1016 J assuming a thermal release of 100 MW38), and without accounting for the portion of energy lost in heating of the rocks in the subsurface.
In our interpretation, one of the reasons of the coincidence between background seismicity and geochemical simulations is that the computational domain of the model, centered at Solfatara (green circle in Fig 1 and Fig 5a) and 2000 m thick, practically coincides with the volume of rocks affected by the post-2000 seismicity (Figs 1 and 5b). This volume comprises on map a low-attenuation circular area obtained via seismic coda-wave attenuation imaging using the earthquake data accompanying the 1983–84 1.80 m uplift event41. The anomaly has a 500 m radius and includes the areas of maximum deformation during the 1983–84 and 2011–2013 unrests. Its centre is located 1000 m SW of the centre of our model and extends at a depth of ~2250 m, thus at the bottom or just below the seismogenic volume (Fig. 5). The anomaly is similar in shape and nature to those associated with ancient magma chambers and/or active intrusions found in other volcanoes. According to general considerations about fluid movements in the magmatic-epithermal environment42, the low-attenuation anomaly could correspond to a self-sealed zone of relatively impermeable material. A recent study43 discusses the formation of fibrous minerals by intertwining filaments, which may partly concur in the formation of the low attenuation zone evidenced by coda wave tomography. This zone would separate the brittle rocks hosting the hydrothermal circulation from the pressurized plastic region where gases either separated by crystallizing magma44, 45 or released by fresh magma accumulate. Episodically, major breaches of the self-sealing zone caused by the increase of magmatic fluid pressure into the plastic zone, would allow the injection of the magmatic gases into the hydrothermal system, exerting a major control on the dynamic of CFc44,45,46. The earthquake-depth histogram shows a maximum earthquake density between 1000 m and 2000 m (Fig. 5b), i.e. at depths compatible with the portion of the computational domain above the zone of magmatic fluids injections (Fig. 1c). Only the 25% of the earthquakes occur instead below the depth of 2000 m, possibly suggesting a progressive transition from brittle to plastic behavior of the rocks associated with very high temperatures9. The overlying self-sealed low attenuation zone would separate this deep almost aseismic portion of the caldera from the shallower seismic domain. Here, the temperature and fluid pressure increase caused by magmatic fluid injections would generate sufficient thermo-elastic stress to originate the background VT earthquakes, in accordance with the mechanisms proposed for their origin47.
Recently, based solely on mechanical considerations in an elastic-brittle deformation regime, the VT earthquake occurrence at CFc was associated to the brittle partial response of the caldera to the magmatic input48. It was proposed that the whole sequence of Campi Flegrei unrests since 1950 belongs to a single, long-term evolutionary trend of accumulating stress and crustal damage, and that the continuation of the trend will favor the progressive approach to eruptive conditions48. In this framework, the surprisingly high correlations that we find among independent observations and simulations highlight an additional role of temperature and pressure increase of the hydrothermal system on the process of crustal damage at CFc. In agreement with this interpretation, previous seismological studies suggested the recent occurrence of a transition from elastic to plastic behavior due to fluid saturation and heating of the rocks in the hydrothermal reservoir9. Furthermore, a recent analysis of the seismic noise49 has discovered a long timescale (2011–2014) decrease of seismic wave velocities in the central part of CFc that is likely related to heating and pressurization. All these evidences point to an increase in the release of H2O-rich gases from a depressurizing magmatic system, and the consequent heating of the hydrothermal system7. It is worth to note that heating at CFc can be particularly efficient in reducing the rock tensile strength due to the presence of thermally unstable zeolites50.
The results of this work have important consequences for the volcanic surveillance of CFc. We show that the occurrence of background seismicity can be considered an excellent parameter to monitor the current unrest of the caldera, since it is highly correlated with ground deformations and geochemical indicators, but simpler to detect. At the same time, any future significant deviation among these parameters may imply significant changes from the current unrest dynamics. These findings must be considered in the framework of recent literature, showing (1) the occurrence of potential recent magmatic intrusions23, (2) the increase in magma degassing, pointing to a critical pressure value7, and (3) the progressive approach to eruption of the caldera48. The need of updating all the short-term forecasting tools presently applied to Campi Flegrei is thus self-evident. This can be done in the framework of new group discussions and consequent elicitations, as those within the updating scheme discussed in ref. 24.
Noteworthy, our new analysis based on the extraction from seismic catalogues of the background seismicity and its comparison with other signals (i.e. ground deformation and gas compositions) can find general applications in understanding the causes of unrest at any volcano, and particularly at calderas.
In this section, the data used in the study are briefly illustrated. The data are obtained from the monitoring system of the Osservatorio Vesuviano-INGV (OV). The system consists of several permanent networks, which provide geodetic, seismological and geochemical data, and systematic surveys for gas composition of the fumaroles in the Solfatara crater (Fig. 1, lower right panel).
The current permanent seismic network of CFc (Fig. 1, black diamonds) is composed of 18 broadband three-component digital stations, 2 short-period three-components analog stations and three short-period single-component analog ones, for a total of 23 stations. Data transmission in real time to the OV Monitoring Center is realized by different systems such as UHF, Wi-Fi radio links, TCP/IP client-server applications. The CFc earthquake catalog used in this work (supplementary dataset 1) contains a data set of about 1800 VT earthquakes recorded between 2000 and July 2016, with magnitude ranging between −2.5 and 2.5. In 2000, the permanent seismic network of CFc was composed of 8 short-period analog stations and 1 broadband digital one, for a total of 9 stations. Seven of these stations have operated continuously until today and represent the initial core of the present network (Fig. 1). In particular, the STH station is adopted as reference station for CFc seismicity because of its closeness to the Solfatara area where the post-2000 seismicity concentrates. Starting from 2005, more stations were added to the CFc seismic network increasing the number of broadband digital stations and covering a more wide area, reaching the present configuration. The network development has improved the hypocenter locations quality but did not add significant effects on the detection capability because the stations distribution provided, already in the early 2000, an appropriate coverage of the area interested by 2000–2016 seismicity.
Ground deformations are monitored through the NeVoCGPS (Neapolitan Volcanoes Continuous GPS) network. The network provides measurements of the 3D time changes in the position of 36 permanent stations, located in the Neapolitan volcanic district and surrounding area51, 52. At present, 20 of these continuous GPS (CGPS) stations are operating at CFc (Fig. 1). A full description of CGPS network and of processing strategies, as well as the 2000–2013 complete database are reported in a previous work51. The supplementary dataset 2 reports the updated data to July 2016 of the vertical displacement at RITE GPS station. The RITE GPS station (Fig. 1) is commonly adopted as reference station for CFc because it is closest to the zone of maximum vertical displacement. Here, we assume this station as representative of the time pattern of ground deformations at CFc. We note, however, that the temporal pattern of the vertical deformation is very similar at all the GPS stations51.
Chemical composition of fumaroles
In the last ten years, time series of chemical compositions of Solfatara fumaroles (BG, BN and Pisciarelli, Fig. 1) were published in different works (e.g. ref. 7). Analytical methodologies and uncertainties are described in ref. 53. Here, we consider the time series of the CO/CO2 ratio measured at BG and BN fumaroles updated to July 2016. This ratio is an excellent indicator of the temperature variations at depth36.
All relevant data are available from the authors.
Aiuppa, A. et al. Forecasting Etna eruptions by real-time observation of volcanic gas composition. Geology 35(12), 1115–1118, l, doi:10.1130/G24149A.1l (2007).
Pallister, J., McNutt S. R. & Chapter 66 - 2015. In (Second Edition), e. b., Academic Press, Amsterdam, Pages 1151-. Synthesis of Volcano Monitoring. in The Encyclopedia of Volcanoes (ed. Sigurdsson, H.) (2015).
Newhall, C. G. & Dzurisin, D. Historical Unrest at Large Calderas of the World., 1108 US Geological Survey Bulletin 1855l (1988).
Acocella, V., Di Lorenzo, R., Newhall, C. & Scandone, R. An overview of recent (1988 to 2014) caldera unrest: Knowledge and perspectives. Rev. Geophys. 53, 896–955,l, doi:10.1002/2015RG000492.l (2015).
Del Gaudio, C., Aquino, I., Ricciardi, G. P., Ricco, C. & Scandone, R. Unrest episodes at Campi Flegrei: A reconstruction of vertical ground movements during 1905–2009. J. Volcanol. Geotherm. Res. 195(1), 48–56,l, doi:10.1016/j.jvolgeores.2010.05.014.l (2010).
Orsi, G. et al. Short-term ground deformations and seismicity in the resurgent Campi Flegrei caldera (Italy): an example of active block- resurgence in a densely populated area. Journal of Volcanology and Geothermal Research 91, 415–451l (1999).
Chiodini, G. et al. Magmas near the critical degassing pressure drive volcanic unrest towards a critical state. Nature Communications,l doi:10.1038/ncomms13712l (2016).
D’Auria, L., Giudicepietro, F., Martini, M. & Lanari, R. The 4D imaging of the source of ground deformation at Campi Flegrei caldera (southern Italy). J. Geophys. Res. 117, B08209,l, doi:10.1029/2012JB009181l (2012).
Di Luccio, F., Pino, N. A., Piscini, A. & Ventura, G. Significance of the 1982-2014 Campi Flegrei seismicity: Preexisting structures, hydrothermal processes, and hazard assessment. Geophys. Res. Lett. 42, 7498–7506,l, doi:10.1002/2015GL064962.l (2015).
Battaglia, J., Zollo, A. & Got, J. L. Rates of Similar Micro-Earthquakes: Comparison Between Campi Flegrei (Southern Italy) and Other Volcanic Areas. J. Volc. Geotherm. Res 200, 62–74l (2010).
Del Pezzo, E. et al. Detection of Seismic Signals From Background Noise in the Area of Campi Flegrei: Limits of the Present Seismic Monitoring. Seismological Research Letters 84, 190–98,l, doi:10.1785/0220120062l (2013).
La Rocca, M. & Galluzzo, D. A Seismic Array in the Town of Pozzuoli in Campi Flegrei (Italy). Seismological Research Letters 83, 86–96,l, doi:10.1785/gssrl.83.1.86l (2012).
Bianco, F., Del Pezzo, E., Saccorotti, G. & Ventura, G. The role of hydrothermal fluids in triggering the July-August 2000 seismic swarm at Campi Flegrei, Italy; evidence from seismological and mesostructural data. J. Volcanol. Geotherm. Res 133, 229–246l (2004).
D’Auria, L. et al. Retrieving the Stress Field Within the Campi Flegrei Caldera (Southern Italy) Through an Integrated Geodetical and Seismological Approach. Pure Appl. Geophys.,l, doi:10.1007/s00024-014-1004-7l (2014).
D’Auria, L. et al. Repeated fluid-transfer episodes as a mechanism for the recent dynamics of Campi Flegrei Caldera (1989–2010). J. Geophys Res. 116, no. B4, B04313,l doi:10.1029/2010JB007837l (2011).
Falanga, M. & Petrosino, S. Inferences on the source of long-period seismicity at Campi Flegrei from polarization analysis and reconstruction of the asymptotic dynamics. Bull. Volcanol. 74, 1537,l, doi:10.1007/s00445-012-0612-2l (2012).
Saccorotti, G. et al. Seismicity associated with the 2004-2006 renewed ground uplift at Campi Flegrei caldera. Italy. Physics Earth Planet. Inter. 165, 14–24l (2007).
Amoruso, A. et al. Clues to the cause of the 2011-2013 Campi Flegrei caldera unrest, Italy, from cGPS data. Geophys. Res. Lett.,l doi:10.1002/2014GL059539l (2014).
Rinaldi, A. P., Todesco, M. & Bonafede, M. Hydrothermal instability and ground displacement at the Campi Flegrei caldera. Physics of The Earth and Planetary Interiors 178, 155–161,l, doi:10.1016/j.pepi.2009.09.005l (2010).
Trasatti, E., Polcari, M., Bonafede, M. & Stramondo, S. Geodetic constraints to the source mechanism of the 2011-2013 unrest at Campi Flegrei (Italy) caldera. Geophys. Res. Lett. 42, 3847–3854,l, doi:10.1002/2015GL063621l (2015).
Aiuppa, A. et al. First observations of the fumarolic gas output from a restless caldera: Implications for the current period of unrest (2005–2013) at Campi Flegrei. Geochemistry Geophysics Geosystems 14, 4153–4169,l, doi:10.1002/ggge.20261l (2013).
Chiodini, G. et al. &. Evidence of thermal driven processes triggering the 2005–2014 unrest at Campi Flegrei caldera. Earth Planet. Sci. Lett. 414, 58–67,l, doi:10.1016/j.epsl.2015.01.012l (2015).
D’Auria, L. et al. Magma injection beneath the urban area of Naples: a new mechanism for the 2012–2013 volcanic unrest at Campi Flegrei caldera. Sci. Rep. 5, 13100,l, doi:10.1038/srep13100l (2015).
Selva, J., Marzocchi, W., Papale, P. & Sandri, L. Operational eruption forecasting at high-risk volcanoes: the case of Campi Flegrei, Naples. Journal of Applied Volcanology 1, 5,l, doi:10.1186/2191-5040-1-5l (2012).
Aspinall, W. P., Woo, G., Voight, B. & Baxter, P. J. Evidence-based volcanology: Application to eruption crises. j. Volc. Geotherm. Res 128, 273–285,l, doi:10.1016/S0377-0273(03)00260-9.l (2003).
Marzocchi, W. & Bebbington, M. Probabilistic eruption forecasting at short and long time scales. Bull. Volcanol. 74, 1777–1805l (2012).
Marzocchi, W., Sandri, L. & Selva, J. BET_EF: a probabilistic tool for long- and short-term eruption forecasting. Bull. Volcanol. 70, 623–632,l, doi:10.1007/s00445-007-0157-yl (2008).
Galluzzo, D. & La Rocca, M. In 35mo Convegno Nazionale GNGTS (Lecce, 22-24 Novembre 2016).
Petrosino, S., De Siena, L. & Del Pezzo, E. Recalibration of the Magnitude Scales at Campi Flegrei, Italy, on the Basis of Measured Path and Site and Transfer Functions. Bulletin of the Seismological Society of America 98, 1964–74,l, doi:10.1785/0120070131l (2008).
Sinclair, A. J. Selection of threshold values in geochemical data using probability graphs. Journal of Geochemical Exploration 3, 129–149l (1974).
Cardellini, C., Chiodini, G. & Frondini, F. Application of stochastic simulation to CO (sub 2) flux from soil; mapping and quantification of gas release. J. Geophys. Res. 108(B9), 2425,l, doi:10.1029/2002JB002165l (2003).
Marsan, D., Prono, E. & Helmstetter, A. Monitoring Aseismic Forcing in Fault Zones Using Earthquake Time Series. Bull. Seism. Soc. Am. 103, 169–179,l, doi:10.1785/0120110304l (2013).
Helmstetter, A., Kagan, Y. Y. & Jackson, D. D. Importance of small earthquakes for stress transfers and earthquake triggering. J. Geophys. Res. 110, B05S08l (2005).
Akaike, H. A new look at the statistical model identification. IEEE Transactions on Automatic Control 19, 716–723l (1974).
Reasenberg, P. Second Order moment of central California seismicity, 1969–1982. J. Geophys. Res. 90(B7), 5479–5495l (1985).
Chiodini, G. & Marini, L. Hydrothermal gas equilibria: The H2O-H2-CO2-CO-CH4 system. Geochim. Cosmochim. Acta 62, 2673–2687l (1998).
Giggenbach, W. F. Redox processes governing the chemistry of fumarolic gas discharges from White Island, New Zealand. Appl. Geochem. 2, 143–161l (1987).
Chiodini, G. et al. CO2 degassing and energy release at Solfatara volcano, Campi Flegrei, Italy. J. Geophys. Res. 106, 16213–16221l (2001).
Pruess, K. The TOUGH codes-A family of simulation tools for multiphase flow and transport processes in permeable media. Vadose Zone Journal 3, 738–746,l, doi:10.2113/3.3.738l (2004).
Chiodini, G. CO2/CH4 ratio in fumaroles a powerful tool to detect magma degassing episodes at quiescent volcanoes. Geophys. Res. Lett. 36, L02302,l, doi:10.1029/2008GL036347l (2009).
De Siena, L. et al. Space-weighted seismic attenuation mapping of the aseismic source of Campi Flegrei 1983-1984 unrest. Geophys. Res. Lett. 44,l doi:10.1002/2017GL072507l (2017).
Fournier, R. O. Hydrothermal processes related to movement of fluid from plastic into brittle rock in the magmatic- epithermal environment. Economic Geology 94, 1193–1212l (1999).
Vanorio, T. & Kanitpanyacharoen, W. Rock physics of fibrous rocks akin to Roman concrete explains uplifts at Campi Flegrei Caldera. Science 349, 617–621,l, doi:10.1126/science.aab1292l (2015).
Bodnar, R., Cannatelli, C., De Vivo, B. L. A. & Belkin, H. E. Quantitative model for magma degassing and ground deformation (bradyseism) at Campi Flegrei, Italy: Implications for future eruptions. Geology 35(9), 791–794,l, doi:10.1130/G23653A.1l (2007).
Lima, A. et al. Thermodynamic model for uplift and deflation episodes (bradyseism) associated with magmatic-hydrothermal activity at the Campi Flegrei (Italy). Earth-Science Reviews 97, 44l (2009).
Chiodini, G. et al. Magma degassing as a trigger of bradyseismic events; the case of Phlegrean Fields (Italy). Geophysical Research Letters 30, 1434,l, doi:10.1029/2002GL016790l (2003).
Chouet, B. Volcano Seismology. Pure Appl. Geophys. 160, 739–788l (2003).
Kilburn, C., De Natale, G. & Carlino, S. Progressive approach to eruption at Campi Flegrei caldera in southern Italy. Nature Communications (in press: doi:10.1038/ncomms15312) (2017).
Zaccarelli, L. & Bianco, F. Noise-based seismic monitoring of the Campi Flegrei caldera. Geophys. Res. Lett. 44,l doi:10.1002/2016GL072477l (2017).
Heap, M. J., Baud, P., Meredith, P. G., Vinciguerra, S. & Reuschlé, T. The permeability and elastic moduli of tuff from Campi Flegrei, Italy: implications for ground deformation modelling. Solid Earth 5, 1–20,l, doi:10.5194/se-5-1-2014ll (2014).
De Martino, P., Tammaro, U. & Obrizo, F. GPS time series at Campi Flegrei caldera (2000–2013). Annals of Geophysics 57, S0213,l, doi:10.4401/ag-6431l (2014).
Tammaro, U. et al. Somma Vesuvius volcano: ground deformations from CGPS observations (2001–2012). Annals of Geophysics 56, S0456,l, doi:10.4401/ag-6462l (2013).
Caliro, S. et al. The origin of the fumaroles of La Solfatara (Campi Flegrei, South Italy). Geochimica et Cosmochimica Acta 71, 3040–3055,l, doi:10.1016/j.gca.2007.04.007l (2007).
Tarquini, S. et al. TINITALY/01: a new Triangular Irregular Network of Italy. Annals of Geophysicsl (2007).
We thank the INGV-OV staff involved in the management and maintenance of the seismic and GPS networks and Francesca Di Luccio for the data of the best located earthquakes. We acknowledge Valerio Acocella and an anonymous reviewer for the helpful comments that improved the clarity of the manuscript.This study has benefited from funding provided by INGV (project COHESO) by the Italian Presidenza del Consiglio dei Ministri Dipartimento della Protezione Civile (DPC), INGV-DPC Research Agreement 2012–2014, Progetto V2 “Precursori di eruzioni”. This paper does not necessarily represent DPC official opinion and policies. EdP has been partly supported by Spanish Project Ephestos, CGL2011-29499-C02-01 and KNOWAVES, TEC2015-68752. We wish to acknowledge the former contribution of Lorenzo Casertano, Oliveri del Castillo and Maria Teresa Quagliariello, who, in an early paper published on Nature in 1976, first discussed the importance of fluids in the dynamics of Campi Flegrei Caldera.
The authors declare that they have no competing interests.
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Chiodini, G., Selva, J., Del Pezzo, E. et al. Clues on the origin of post-2000 earthquakes at Campi Flegrei caldera (Italy). Sci Rep 7, 4472 (2017). https://doi.org/10.1038/s41598-017-04845-9
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