One of the most effective approaches to identifying possible precursors of eruptions is the analysis of seismicity patterns recorded at volcanoes. Accurate locations of the seismicity and the estimate of source mechanisms can resolve fault systems and track fluid migrations through volcanoes. We analysed the six main swarms recorded at Campi Flegrei since 2000, using them as a proxy of the processes involved in the long-term-unrest of this densely populated caldera. We re-located the earthquakes comprised in these swarms and estimated the focal mechanisms, which appear in agreement with the fault systems of the caldera and with tomographic images. The focal mechanisms are in agreement with the tensional stress induced by the caldera uplift. Most of the swarms and remaining seismicity delineate a highly fractured volume extending vertically below the Solfatara/Pisciarelli vents, where gases find preferential paths to the surface triggering earthquakes. The main swarms are located below this volume where the presence of a rigid caprock is still debated. We interpreted the current unrest in term of a gradual increment in the activity of a wide hydrothermal system whose most evident manifestation is the enlargement of the fumarolic-field of Pisciarelli and the increment of the earthquakes occurrence rate.
The Campi Flegrei caldera, southern Italy, is one of the most populated active volcanoes on the Earth. Its ground suffers repeated vertical uplifts and subsidence phases; since 1950, four episodes of uplift (bradyseism crises) that raised the coastal town of Pozzuoli by up to 4 m1,2 are reported. The uplift episodes are believed to be governed by overpressure of the shallow hydrothermal system3,4,5, magma movement through the crust6 or by both the phenomena7,8. The seismicity which characterizes the area is shallow, low in magnitude (up to Md = 4.0 on March 14, 1984) and mainly located below the area of Solfatara/Pisciarelli5,9,10,11,12.
Few LP events were identified during the bradiseismic crises of 1982–8413. In 2000, when the last phase of subsidence stopped, a swarm of hybrid events was recorded in the area South of Solfatara at a depth of almost 3 km. These events showed a dominant frequency around 1–3 Hz and a clear S-wave onset, placing them in the hybrid category13. In October 2006, a shallow LP activity accompanied by a VT swarm13,14 lasted for 1 week.
During the last bradiseismic crisis, in 1982–84, more than 16,000 earthquakes accompanied an uplift of almost 1.8 m. In this period, seismic swarms have been identified which correlate in space and time with possible fluid injection from a deep hot source15. The swarms’ locations, compared with the attenuation topography images, were interpreted in terms of fluid migration. The fluids moved from a volume located 3–4 km below Pozzuoli toward a shallower aseismic volume below Solfatara, identified as the ground deformation source, reaching the area of the last eruption (Mt. Nuovo, 1538) at the end of the crisis15. During this crisis an offshore WNW-ESE seismogenic structure southwest of Pozzuoli was identifies13. After 1984, the caldera had subsided continuously, except for occasional minor uplift episodes, until 2000 when the trend slightly reversed1,13. At that time two swarms (the hybrid events mentioned above and one comprising exclusively VT earthquakes) were recorded after a prolonged aseismic period. The seismicity recorded since 2000 was located mostly onshore and concentrates at Solfatara/Pisciarelli9. Very few events occured offshore and the WNW-ESE structure that was identified in the previous crisis (1982–84) was practically aseismic.
After the eruption of the Neapolitan Yellow Tuff (about 15 ky B.P.), Campi Flegrei caldera was affected by variable vertical movements of disjointed blocks with fault and fracture systems mainly trending NE–SW and NW–SE16. Many vents active over the past 15,000 years have been identified within the caldera17. Their areal distribution with time is a good tracer of the active structures which have favoured magma movement towards the surface7,18. In the recent eruptive history of Campi Flegrei, stress changes, due to topographic, bathymetric and density variations between the caldera centre and periphery and to the inflating central source, favoured the magma movement towards different faults reaching the surface in different areas within the caldera19.
The ground deformations recorded during the last bradiseismic crises have been associated to both magmatic or hydrothermal sources and their location, depth, shape and density have been constrained thanks to gravimetric (20 and references therein), seismological (e.g.6), pore pressure21, geochemical or petrological measurements22. A deep magmatic source is usually invoked as the source for magma movements towards the surface (e.g.23) or to justify the movement of shallow hydrothermal fluids. Fluid movements were evidenced during the 1982–1984 crisis (e.g.15) and also during the current unrest (e.g.11,24,25) and their intrusion were linked to the characteristic of the caprock present at 2–3 km depth26.
We investigated the swarm seismicity recorded at Campi Flegrei in the last 20 years to obtain information on faults, stress regimes and fluid movements that are mainly involved during the current uplift phase and to draw considerations on the possible preferential routes for fluids and magma movements towards the surface.
Figure 1B shows the monthly seismicity and the earthquake magnitudes recorded at Campi Flegrei from 2000 to March 2021 by the seismic network of Osservatorio Vesuviano, INGV. As evidenced by Tramelli et al.4 the occurrence rate of earthquakes increased with time since 2000 and the hypocentral depth is decreasing. We analysed 6 main swarms (black vertical lines in Fig. 1, summary in Table 1) and described their locations and focal mechanisms in the context of the whole seismicity, the vertical movement of the ground, the known faults and fractures and the subsoil structure.
August 22, 2000
A swarm of VT events was recorded on August 22, 2000, a month after a swarm of hybrid events that lasted a week (July 2–7)14. 90 events with magnitudes between -0.5 and 2.1 were recorded within 7 h. Due to the number and position of the seismic stations at that time only 6 of those events were located. The hypocenters resulted below the Solfatara crater at a depth of about 2 km. To understand the sensitivity of the seismic network at that time, a detailed analysis is presented in Tramelli et al.4. The events occurred during a period of uplift started a couple of months before. The relocation of the earthquakes with both methods, NLLoc and HypoDD, shows a sub-vertical structure, which slightly tends to East with decreasing depth, extending between 2.6 and 1.9 km below Sofatara/Pisciarelli (Fig. 2). Since these events are very old and being complicated to find all the traces, we considered just the well located ones: horizontal and vertical location errors ≤ 100 m. The focal mechanism of the highest-magnitude earthquake is associable to a normal fault trending N-NE.
September 7, 2012
The quasi-quiescence of the volcano between 2000 and 2012 was interrupted in October 2006 by a seismic swarm of LP events14, which we do not take into consideration here. After this LP swarm, on September 7, 2012 more than 180 low-magnitude earthquakes occurred within a time window of almost 3 h; two of them had the maximum magnitude of Md = 1.7. This was the largest swarm in terms of energy released and number of recorded earthquakes since the end of the bradiseismic crisis of 1982–84. The swarm occurred at the end of a period of almost 2 months of increment in the ground uplift rate, which passed from 0.4–0.5 cm/year to 1–1.6 cm/month in the central part of the caldera. Immediately after the swarm the ground uplift slowed down.
This swarm was located North to the area of the maximum uplift (port of Pozzuoli), differently from the seismicity recorded after 198413, which is located close to the Solfatara/Pisciarelli area (NE to the maximum uplift area) (Fig. 3).
We relocated 64 earthquakes of the swarm in a very narrow volume of 2 × 2 km2 extending between 2.2 and 4.2 km of depth (Fig. 3). The mean location error was 150 m for the horizontal and less than 100 m for the vertical. The differences between the locations obtained with NLLoc and with HypoDD are not appreciable. The focal mechanisms are all normal and generally trending NE-SW.
October 7, 2015
33 low magnitude earthquakes were recoded within a time window of almost 2 h in the area East to the Sofatara border on October 7, 2015. The swarm started at 7:20 and the maximum magnitude earthquake, Md = 2.5, was recorded at 9:10 almost at the end of the swarm. Also in this case, the swarm was recorded at the end of a period of increment in the velocity uplift (~ 1.5 cm/month), which started almost 1 month before (at the beginning of September).
The relocation of the earthquakes evidences an almost vertical structure extending below Solfatara/Pisciarelli at a depth of 1.2–3.9 km (Fig. 4); the mean horizontal and vertical location errors are < 350 m. The double difference location evidences a restricted hypocentral volume of ~ 1 km3. The focal mechanism solutions confirm the extensional field for the slipping fault.
March 12, 2018
Between 13:33 and 15:35 of March 12, 2018, 42 seismic events were recorded by the seismic network of Osservatorio Vesuviano in the area of Solfatara-Pisciarelli. The maximum magnitude recorded was Md = 2.4, corresponding to the deepest earthquake of the swarm recorded at 14:09. Differently from the previous ones, this swarm occurred during a period of stable uplift, without any evidence of variation in the uplift rate which was almost 0.7 cm/month since middle 2017. Since 2014 the total uplift recorded at the GPS station located at the Pozzuoli harbor was almost 26 cm.
We relocated 35 earthquakes of the swarm. Using the program NLLoc the events result located in an area of almost 3 × 3 km2 between 0 and 3.2 km depth; with mean horizontal and vertical error of 100 m. The hypocentral volume is highly reduced using the double difference location resulting in a flattened shape of 0.5 × 0.5 km2 extending between 2 and 3 km of depth. The solutions of the focal mechanisms are all normal and trending primarily NE-SW (Fig. 5).
December 5–6, 2019
34 earthquakes with maximum magnitude Md = 3.1 were recorded in the area of Solfatara/Pisciarelli between 24:51 of December 5 and 2:24 of December 6, 2019. The hypocenters were located between depths of 0.9 and 2.3 km. The uplift mean velocity showed an increment between the end of November and the beginning of December, passing from almost 7 mm/month to about 1 cm/month and moved back to the values of 7 mm/month after the swarm. At that time, the total uplift recorded in the center of the caldera since 2005 was 65 cm.
We relocated 18 earthquakes of the swarm and plot the results in Fig. 6. The locations obtained with NLLoc are spread in an area of ~ 2 × 3 km2 extending between 1 and 2.7 km depth with a mean horizontal and vertical error of 80 m. When applying the double-differences approach, the earthquakes of the swarm concentrate within a very small volume but is still visible a structure vertically elongated below Solfatare/Pisciarelli. The focal mechanisms are normal trending NE-SW.
April 26, 2020
A seismic swarm was recorded between 1:26 and 5:23 of April 26, 2020. 81 earthquakes with low magnitude (max Md = 3.3) were identified. The most energetic event was recorded at 2:59 and was located below the Solfatara/Pisciarelli area at the depth of 2.6 km. This earthquake is the highest magnitude recorded from the end of the bradiseismic crises of 1982–84 until the end of 2021. The vertical uplift recorded at the center of the caldera had an increment between the end of November and the beginning of December 2019, when the previous swarm was recorded, but it come back to values of 6–7 mm/month before this swarm. No anomalies in the vertical displacement can be directly associated with this swarm. From 2005 to April 2020 a total uplift of almost 70 cm was recorded at the Pozzuoli harbor.
We relocated 46 earthquakes of the swarm and the results are shown in Fig. 7. The locations and focal mechanisms are similar to those comprised in previous swarms. Also in this case the hypocentral volume estimated using the absolute locations obtained with NLLoc is wider than the one estimated using HypoDD. The mean horizontal and vertical location errors obtained with the Bayesian approach are ~ 100 m.
The focal mechanisms
We analyzed the focal mechanisms of the earthquakes of the most significant swarms recorded since 2000 to evidence any variation in the local stress. We showed beach balls for earthquakes with sufficient azimuthal coverage and with adequate signal-to-noise ratios (usually Md ≥ 1). The rapid occurrence of earthquakes within a swarm sometimes obscures the first arrivals also for magnitudes higher than 1.5 and increases the picking errors.
The obtained focal mechanisms are all congruent (see supplementary Table 1): normal and oriented mostly NE-SW confirming the local extensional trend of the caldera, which is suffering a persistent uplift in its central part. The obtained results confirm what founded by La Rocca and Galluzzo28 for the events of the seismic catalogue of Campi Flegrei between 2005 and 2019. The earthquakes belonging to the swarms are all located below the area of Solfatara/Pisciarelli at 2–4 km, except for the 2012 swarm. This swarm was located North of the area of maximum uplift at a depth of almost 3 km. Furthermore, the location of the earthquakes belonging to the 2012 swarm evidence a NS direction and a squashed hypocentral volume. After this swarm, this volume was not involved anymore in the seismicity of the caldera.
Changes in the differential stress between the caldera centre and periphery, due to topographic, bathymetric and density variations31, make a correlation between the stress induced by the inflating of the central part of the caldera and the orientation of the focal mechanisms largely ineffective. Pepe et al.32 inferred that stress, seismicity and secondary deformation are likely modulated by shallow structures, located at a depth of ~ 1 km, under the eastern sector of the caldera. In the same paper, the authors also evidenced that shallow structures are able to channel fluids in the Solfatara/Pisciarelli area. Regional stress33 and pre-existing tectonic structures play, indeed, an important role on the modulation of the stress distribution34. More efficient is the comparison of the direction of the mechanisms with the known faults system distributed within the caldera. We plotted the relocated swarms on a simplified map of the faults and fractures presented by Vilardo et al.29 (Fig. 8A) to evidence any alignment. All the earthquakes of the swarms occurred along the faults that cut the Solfatara/Pisciarelli area with SW-NE orientation and on the orthogonal ones. The focal mechanisms are congruent with the SW-NE orientation. Again, the only exception is the 2012 swarm. In this case the earthquake locations follow the N-S fault that cuts the caldera from the South of San Vito area to the port of Pozzuoli (Fig. 8). The focal mechanisms are oriented NE-SW and the hypocenters are the deepest recorded at Campi Flegrei since 2000.
The swarms in the context of the whole seismicity
The relocation of the whole seismicity and of the main swarms with a 3D velocity model27 and a Bayesian approach showed a vertical extension of the hypocenters enlightening the presence of sub-vertical structures, which allow the movement of the fluids towards the surface10,11. Within the swarms, we cannot identify any relation between number of recorded earthquakes and the maximum magnitude of the earthquakes in the swarm. On the other hand, considering the entire seismic catalog, the plot of the magnitude vs time shows that the seismicity is increasing both in terms of magnitude and rate (Fig. 1). In Fig. 1 we used the completeness magnitude Mc = 0.2 as found by Tramelli et al.4; this value can be considered constant since 2010 in the central part of the caldera.
The seismicity in the context of the subsoil characteristics
We plotted the relocated earthquakes recorded between 2000 and the end of 2020 on the slices of the S-waves attenuation and Vp/Vs tomographyes obtained by Calò and Tramelly36 (Fig. 9 and supplementary Figure 1) and on the MT slice, ~ 5500 m long, cutting the central part of the caldera from SW to NE (Fig. 8, see30 for details). We choose these quantities as they can be associated to gas and/or fluid presence within the analyzed medium.
The Qs and Vp/Vs tomographic slices here represented cut the caldera from West to East with an azimuth of 110°. We distinguish a U shape area extending down to 2 km characterized by high attenuation (low Qs) that extends from the Pozzuoli harbor to the Solfatara/Pisciarelli area. Only the Eastern arm of this U, which extends below Solfatara/Pisciarelli, hosts earthquakes. The other arm is almost aseismic. These two arms have similar attenuation but different Vp/Vs: the eastern arm, where the seismicity lies, has low Vp/Vs values. This same trend is evidenced also by the Qc tomography described by Akande et al.37. The analyzed swarms border the bottom of this area and are placed almost at the interface between high and low Vp/Vs. The comparison of earthquake locations with the MT tomography performed by Siniscalchi et al.30 shows that the swarms are located at the bottom of the high resistivity vertical body extending below Solfatara/Pisciarelli (Fig. 8B). The remaining seismicity is mainly located along this high resistivity volume.
Discussion and conclusions
The focal mechanism, which are consistent with normal, high-angle or nearly vertical faults, obtained for all the analysed earthquakes well fit with the uplift of the central part of the caldera in the analysed period.
In regions particularly enriched in water5, molten rocks33 or both of them22 we can assume that the faults activation is induced by the reduction of the normal stress caused by hot hydrothermal uprising fluids, as modelled by Akande et al.37. As a consequence, swarms and earthquakes locations can be uses to monitor fluid movements. Until 2014, a correlation between the main swarms and peaks in the geochemical signal (CO2/CH4 recorded within Solfatara crater) has indeed been reported by Chiodini et al.38, finding a delay of ~ 200 days.
Within fluid saturated media, as we expect for the hydrothermal system of Campi Flegrei, the temperature variations affect mostly the velocity of the P waves, modifying the fluid compressibility26. As a consequence, low Vp/Vs typically characterizes gas bearing rocks whereas high Vp/Vs characterizes liquid-bearing formation with low fluid compressibility26. In the area where the seismicity concentrates below Solfatara/Pisciarelli, Calò and Tramelli36 found low Vp/Vs and high attenuation (confirmed also by De Siena et al.39) that can be interpreted as a vertically elongated highly fractured rock matrix40 filled with vapor that feeds the large gas emission of Solfatara/Pisciarelli. Swarms with the higher magnitude earthquakes mainly occur in tiny volumes below this area where the presence of a rigid caprock acting as a barrier for fluids coming from a deeper magmatic source was evidenced by different authors (e.g.41,39,36). This layer is quite thin (~ 0.5 km36) and its bottom edge is characterized by high contrasts in the mechanical properties.
This interpretation is corroborated also by the comparison of earthquakes location with the MT profile proposed by Siniscalchi et al.30. The high resistivity vertical body extending below Solfatara/Pisciarelli between 0.5 and 2 km (Fig. 8B) was interpreted by the authors as the main upraising pathway of magmatic gases coming from the feeding reservoir located below the caprock. The earthquakes belonging to the analyzed swarms are located within or at the border of this rigid structure.
During the bradiseismic crises of 1982–84 the seismicity was spread over the caldera inner portion with two wide preferential volumes: one below Solfatara and the other extending offshore and oriented NW–SE13,15 To the contrary, the seismicity is currently shallower and mainly concentrated in a vertically elongated volume below the Solfatara/Pisciarelli area, even if the location of the 2012 swarm indicates that the current long-term unrest involves the entire system of the Campi Flegrei caldera. The 2012 swarm contains the deepest events and is located where the caprock should flex down36.
In volcanic environments, where the activation of pre-existing seismogenic sources may be the first consequence of renewed volcanic activity, it is critical to monitor the seismicity behaviour in terms of location and stress conditions. Geophysical studies performed on the 1982–84 bradiseismic crisis (e.g.15,9) evidenced a correlation between seismicity and variations of the pressure of the hydrothermal system. Anyway, hydrothermal instability alone cannot explain 1982–84 inflation because the densities of the estimated intrusions are greater than aqueous fluids (20 and references therein). A sill-like expansion source (at ~ 4 km depth) seems to be the main cause of 1970–2013 ground deformation episodes whereas the presence of a shallow hydrothermal system justifies the post 1984 mini-uplift episodes (20 and references therein). However, the mechanism feeding this hydrothermal reservoir is still under debate (e.g.3,38,41). The seismicity recorded from 2000 to 2021 is mainly located within the hydrothermal system that extends below Solfatara/Pisciarelli25,30,36,39, except for the main swarms that are located below this volume where the presence of a rigid caprock is regulating the injection of gases in the system above10. The injection of deep magmatic fluid seems to regulate the occurrence of main swarms fracturing the caprock that constitute a barrier for the magmatic fluids38 coming from the deep source, which feeds the shallow hydrothermal system22.
Analysing the seismicity recorded since 2000 in Campi Flegrei, Chiodini et al.25 distinguished two populations corresponding to events occurring during swarms and the background seismicity. With the same catalogue, Tramelli et al.4 calculated the clustering degree that is always > 1 concluding that the seismicity occurs with swarms that are becoming denser in time. To evidence the swarms of Campi Flegrei, Bellucci Sessa et al.42 used the operative definition inferred by the OV seismologists, which is used locally for the surveillance activities in agreement with the Italian Department of Civil Defence. Since there is not a generally accepted quantitative definition of an earthquake swarms, except for the qualitative definition of seismic sequences with earthquakes of similar magnitude occurring close in space and time43, we used a method based on earthquakes rate variation44 to identify the main swarms. We analysed the earthquake catalogue of Campi Flegrei from 2000 to the end of 2020 using Mc = 0.24. In Fig. 1C we plot the function f(t) defined as the difference between the number of recorded earthquakes at a certain time, N(t), and the expected number, which is calculated as the rate of earthquakes (R) times the time elapsed since the beginning of the analysed catalogue:
The rate is estimated as the total number of earthquakes occurred in a time window divided by the window length.
As the rate of occurrence of earthquakes in Campi Flegrei increased with time since 20004 we divided the catalogue into three time-series where the rate has been considered constant: [01/01/2000–13/09/2017]; [13/09/2017–07/07/2020] and [07/07/2020–31/12/2020]. These functions (black curves Fig. 1C) have been compared with the expected trends (dashed lines Fig. 1C) and the cumulative number of earthquakes (grey curve Fig. 1C). We identified 9 possible swarms and we selected 6 of them that were most significant in terms of number of events, magnitude and moment of occurrence with respect to the volcano dynamic; therefore, they were suitable for analysis. The three discarded swarms are: the swarm of October 2006 (dashed vertical line Fig. 1C), a mainly LP swarm accompanied by low magnitude earthquakes13,14; the September 9, 2014 swarm (first arrow Fig. 1C) composed by 9 recorded earthquakes with Mmax = 1.0 located between Solfatara and Pozzuoli harbour and the October 12, 2018 swarm (second arrow Fig. 1C) composed by 13 recorded earthquakes with one earthquake of M = 2.0 and the others with magnitude lower than 1.1. We analysed the 6 swarms (black vertical lines in Fig. 1, summary in Table 1) focusing on their locations and focal mechanisms with respect to the seismic36 and MT30 tomographies and to the faults and fractures system29 to investigate the evolution of the long-term unrest which is currently taking place in the caldera.
For each swarm we relocated the earthquakes using the NLLoc program45 with a 3D velocity model27 to define the hypocentral position and for the highest magnitude earthquakes we resolved the focal mechanism using the FPFit program46. We reported the focal mechanisms with their misfits in the supplementary. Finally, we relocated the earthquakes using the HypoDD software47 which allows to define an improved position of hypocenters with respect to the others in the swarms. This allows to image possible structures involved in the swarm.
Seismic waveforms, locations and magnitudes of Campi Flegrei earthquakes since 2016 are available at https://terremoti.ov.ingv.it/gossip/flegrei. Previous catalogue, without waveforms, is available at http://sismolab.ov.ingv.it/sismo/index.php?PAGE=SISMO/last&area=Flegrei. Waveforms prior to 2015 are currently available upon request at email@example.com.
Del Gaudio, C., Aquino, I., Ricciardi, G., Ricco, C. & Scandone, R. Unrest episodes at Campi Flegrei: A reconstruction of verticalground movements during 1905–2009. J. Volcanol. Geoth. Res. 195(1), 48–56 (2010).
De Martino, P., Tammaro, U. & Obrizzo, F. Ps time series at Campi Flegrei caldera (2000–2013). Ann. Geophys. 57(2), 0213 (2014).
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. Solid Earth 117(B8), B08209 (2012).
Tramelli, A. et al. Statistics of seismicity to investigate the Campi Flegrei caldera unrest. Sci. Rep. 11(1), 1–10 (2021).
Chiodini, G. et al. Hydrothermal pressure-temperature control on CO2 emissions and seismicity at Campi Flegrei (Italy). J. Volcanol. Geotherm. Res. 414, 107245 (2021).
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(1), 1–11 (2015).
Giudicepietro, F., Macedonio, G. & Martini, M. A physical model of sill expansion to explain the dynamics of unrest at calderas with application to Campi Flegrei. Front. Earth Sci. 5, 54 (2017).
Macedonio, G., Giudicepietro, F., D’auria, L. & Martini, M. Sill intrusion as a source mechanism of unrest at volcanic calderas. J. Geophys. Res. Solid Earth 119(5), 3986–4000 (2014).
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(18), 7498–7506 (2015).
Giudicepietro, F. et al. Tracking episodes of seismicity and gas transport in Campi Flegrei caldera through seismic, geophysical, and geochemical measurements. Seismol. Soc. Am. 92(2A), 965–975 (2021).
Giudicepietro, F. et al. Campi Flegrei, Vesuvius and Ischia seismicity in the context of the Neapolitan volcanic area. Front. Earth Sci. 9, 512 (2021).
Tramelli, A., Troise, C., De Natale, G. & Orazi, M. A new method for optimization and testing of microseismic networks: An application to Campi Flegrei (Southern Italy). Bull. Seismol. Soc. Am. 103(3), 1679–1691 (2013).
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. Solid Earth 116(B4), B04313 (2011).
Saccorotti, G. et al. Seismicity associated with the 2004–2006 renewed ground uplift at Campi Flegrei Caldera, Italy. Phys. Earth Planet. Inter. 165(1–2), 14–24 (2007).
De Siena, L. et al. Source and dynamics of a volcanic caldera unrest: Campi Flegrei, 1983–84. Sci. Rep. 7(1), 1–13 (2017).
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. J. Volcanol. Geoth. Res. 91(2–4), 415–451 (1999).
Smith, V. C., Isaia, R. & Pearce, N. J. G. Tephrostratigraphy and glass compositions of post-15 kyr Campi Flegrei eruptions: implications for eruption history and chronostratigraphic markers. Quatern. Sci. Rev. 30(25–26), 3638–3660 (2011).
Giudicepietro, F., Macedonio, G., D’Auria, L. & Martini, M. Insight into vent opening probability in volcanic calderas in the light of a sill intrusion model. Pure Appl. Geophys. 173(5), 1703–1720 (2016).
Di Vito, M. A. et al. Volcanism and deformation since 12,000 years at the Campi Flegrei caldera (Italy). J. Volcanol. Geoth. Res. 91(2–4), 221–246 (1999).
Bonafede, M. et al. Source Modelling from Ground Deformation and Gravity Changes at Campi Flegrei Caldera (Springer, 2022).
Nespoli, M., Belardinelli, M. E. & Bonafede, M. Stress and deformation induced in layered media by cylindrical thermo-poro-elastic sources: An application to Campi Flegrei (Italy). J. Volcanol. Geotherm. Res. 415, 1269 (2021).
Pappalardo, L., & Buono, G. Insights into processes and timescales of magma storage and ascent from textural and geochemical investigations: case studies from high-risk Neapolitan volcanoes (Italy). in Crustal Magmatic System Evolution: Anatomy, Architecture, and Physico-Chemical Processes 213–235 (2021).
Amoruso, A., Crescentini, L. & Berrino, G. Simultaneous inversion of deformation and gravity changes in a horizontally layered half-space: Evidences for magma intrusion during the 1982–1984 unrest at Campi Flegrei caldera (Italy). Earth Planet. Sci. Lett. 272(1–2), 181–188 (2008).
Petrosino, S. & De Siena, L. Fluid migrations and volcanic earthquakes from depolarized ambient noise. Nat. Commun. 12(6656), 1–8 (2021).
Chiodini, G. et al. Clues on the origin of post-2000 earthquakes at Campi Flegrei caldera (Italy). Sci. Rep. 7(1), 1–10 (2017).
Vanorio, T., Virieux, J., Capuano, P. & Russo, G. Three-dimensional seismic tomography from P wave and S wave microearthquake travel times and rock physics characterization of the Campi Flegrei Caldera. J. Geophys. Res. Solid Earth 110(B3), B03201 (2005).
Battaglia, J., Zollo, A., Virieux, J. & Iacono, D. D. Merging active and passive data sets in traveltime tomography: The case study of Campi Flegrei caldera (Southern Italy). Geophys. Prospect. 56(4), 555–573 (2008).
La Rocca, M. & Galluzzo, D. Focal mechanisms of recent seismicity at Campi Flegrei, Italy. J. Volcanol. Geotherm. Res. 388, 106687 (2019).
Vilardo, G., Isaia, R., Ventura, G., De Martino, P. & Terranova, C. InSAR Permanent Scatterer analysis reveals fault re-activation during inflation and deflation episodes at Campi Flegrei caldera. Remote Sens. Environ. 114(10), 2373–2383 (2010).
Siniscalchi, A. et al. Reservoir structure and hydraulic properties of the Campi Flegrei geothermal system inferred by audiomagnetotelluric, geochemical, and seismicity study. J. Geophys. Res. Solid Earth 124(6), 5336–5356 (2019).
Di Vito, M. A. et al. Magma transfer at Campi Flegrei caldera (Italy) before the 1538 AD eruption. Sci. Rep. 6(1), 1–9 (2016).
Pepe, S. et al. Volcanic structures investigation through SAR and seismic interferometric methods: The 2011–2013 Campi Flegrei unrest episode. Remote Sens. Environ. 234, 111440 (2019).
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. 172(11), 3247–3263 (2015).
Isaia, R. et al. Volcano-tectonic setting of the Pisciarelli fumarole field, Campi Flegrei caldera, southern Italy: Insights into fluid circulation patterns and hazard scenarios. Tectonics 40(5), e2020TC006227 (2021).
Giudicepietro, F. et al. Insight into Campi Flegrei caldera unrest through seismic tremor measurements at Pisciarelli fumarolic field. Geochem. Geophys. Geosyst. 20(11), 5544–5555 (2019).
Calò, M. & Tramelli, A. Anatomy of the Campi Flegrei caldera using enhanced seismic tomography models. Sci. Rep. 8(1), 1–12 (2018).
Akande, W. G., De Siena, L. & Gan, Q. Three-dimensional kernel-based coda attenuation imaging of caldera structures controlling the 1982–84 Campi Flegrei unrest. J. Volcanol. Geotherm. Res. 381, 273–283 (2019).
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 (2015).
De Siena, L. et al. Space-weighted seismic attenuation mapping of the aseismic source of Campi Flegrei 1983–1984 unrest. Geophys. Res. Lett. 44(4), 1740–1748 (2017).
Carlino, S. et al. Field-scale permeability and temperature of volcanic crust from borehole data: Campi Flegrei, southern Italy. J. Volcanol. Geotherm. Res. 357, 276–286 (2018).
Vanorio, T. & Kanitpanyacharoen, W. Rock physics of fibrous rocks akin to Roman concrete explains uplifts at Campi Flegrei Caldera. Science 349(6248), 617–621 (2015).
Bellucci Sessa, E., Castellano, M. & Ricciolino, P. GIS applications in volcano monitoring: the study of seismic swarms at the Campi Flegrei volcanic complex, Italy. Adv. Geosci. 52, 131–144 (2021).
Chouet, B. Volcano seismology. Pure Appl. Geophys. 160(3), 739–788 (2003).
Jacobs, K. M., Smith, E. G., Savage, M. K. & Zhuang, J. Cumulative rate analysis (CURATE): A clustering algorithm for swarm dominated catalogs. J. Geophys. Res. Solid Earth 118(2), 553–569 (2013).
Lomax, A., Virieux, J., Volant, P., & Berge-Thierry, C. (2000). Probabilistic earthquake location in 3D and layered models. In Advances in seismic event location (pp. 101–134). Springer, Dordrecht.
Reasenberg, P., and Oppenheimer D. FPFIT, FPPLOT and FPPAGE; Fortran computer programs for calculating and displaying earthquake fault-plane solutions; OFR; 85–739 (1985).
Waldhauser, F. & Ellsworth, W. L. A double-difference earthquake location algorithm: Method and application to the northern Hayward fault, California. Bull. Seismol. Soc. Am. 90(6), 1353–1368 (2000).
The authors were partially supported by the MIUR project PRIN-2017 WZFT2p “Stochastic forecasting in complex systems” and by the project Progetto Strategico Dipartimentale INGV 2019 “Linking surface Observables to sub–Volcanic plumbing-system: A multidisciplinary approach for Eruption forecasting at Campi Flegrei caldera (Italy)”, LOVE-CF. The authors wish to thank all the many colleagues who have contributed to the monitoring effort on Campi Flegrei. The data used in this study were provided by the Istituto Nazionale di Geofisica e Vulcanologia (Osservatorio Vesuviano). The authors are also grateful to the Italian Presidenza del Consiglio dei Ministri-Dipartimento della Protezione Civile (DPC) for supporting the monitoring activities at Campi Flegrei. This article does not necessarily represent DPC official opinion and policies.
The authors declare no competing interests.
Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
About this article
Cite this article
Tramelli, A., Giudicepietro, F., Ricciolino, P. et al. The seismicity of Campi Flegrei in the contest of an evolving long term unrest. Sci Rep 12, 2900 (2022). https://doi.org/10.1038/s41598-022-06928-8