# Seismicity Pattern Changes before theM = 4.8 Aeolian Archipelago (Italy) Earthquake of August 16, 2010

Authors: Salvatore Gambino; Antonino Laudani; Salvatore Mangiagli
Journal: The Scientific World Journal
 (2014)

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## Abstract

We investigated the seismicity patterns associated with anM=4.8 earthquake recorded in the Aeolian Archipelago on 16, August, 2010, by means of the region-time-length (RTL) algorithm. This earthquake triggered landslides at Lipari; a rock fall on the flanks of the Vulcano, Lipari, and Salina islands, and some damages to the village of Lipari. The RTL algorithm is widely used for investigating precursory seismicity changes before large and moderate earthquakes. We examined both the spatial and temporal characteristics of seismicity changes in the Aeolian Archipelago region before the M=4.8 earthquake. The results obtained reveal  6-7 months of seismic quiescence which started about 15 months before the earthquake. The spatial distribution shows an extensive area characterized by seismic quiescence that suggests a relationship between quiescence and the Aeolian Archipelago regional tectonics.


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## Body

## 1. Introduction

The quiescence of seismic activity has been defined as the notable decrease in the seismic activity against the average background. Temporal seismic observations have shown trends of seismic quiescence preceding large and moderate events [1, 2]. Successively Sobolev and Tyupkin [3, 4] proposed the region-time-length algorithm (RTL algorithm), a statistical method for the investigation of the seismic activity level preceding large earthquakes.This method may evidence a decrease (quiescence) or an increase (activation) in the seismic activity against the average background [5]. The RTL method has previously been applied to earthquakes in Kamchatka and Caucasus [4, 6, 7], Japan (e.g., [7–9]), China [10, 11], Greece [12], Turkey [13], Taiwan [14], and India [15]. Some moderate Italian earthquakes have been studied by Di Giovanbattista and Tyupkin [16–18], Gentili and Bressan [19], and Gentili [20] by using this technique.The Aeolian Archipelago (Figure1) is located in the Southern Tyrrhenian Sea (Italy) and represents the manifestation of a submarine volcanic arc originating in the central sectors of the Tyrrhenian Sea during the Pliocene and successively migrating towards the southeast.Figure 1
Map of the investigated area with main structural features and seismic network. The largest earthquakes, which occurred in Aeolian Archipelago in the last 50 years, are reported.It can be subdivided into three sectors with a different structural and tectonic evolution [21]. In the western sector, comprising the Alicudi and Filicudi islands, the volcanic activity started at about 1.3 Ma [22] and ended at about 30–40 kyr. At present, the seismicity occurs in the crust along the WNW-ESE Sisifo fault system (Figure 1). The eastern sector, which comprises Panarea and Stromboli islands and where volcanism developed from 0.8 Ma ago and is still active and is affected by a prevailing NE-SW striking fault system. The central sector includes the islands of Salina, Lipari, and Vulcano. Here, the volcanism began at 0.4 Myr [23] and is still active (last eruption 1888–1890) at Lipari and Vulcano (e.g., [24–27]).These volcanoes are aligned along a lithospheric NNW-SSE fault system, the Aeolian-Tindari-Letojanni fault system (Figure1) with right-lateral to oblique kinematics along which the seismicity is roughly aligned (e.g., [28–30]). Earthquakes occur mostly in the upper 20 km of the crust [31]; in particular, the seismicity west of Tindari-Letoianni fault system is distributed in a 7–18 km interval of depth, whereas earthquakes of Lipari-Vulcano eastern area are not deeper than 12-13 km [32].The southern Tyrrhenian area is characterized by seismicity with maximum magnitude in the range of 5-6; in the last 50 years two strong events have been recorded:M=5.5 (15/04/1978) and M=5.7 (28/05/1980) (Figure 1, [33]). These two moderate earthquakes have marked an increase of the regional dynamics that, according to Chiodini et al., 1992 [34], and Montalto, 1996 [35], caused the reactivation of the volcanic system on Vulcano. Moreover the occurrence of an earthquake of regional significance shortly before the last eruption of Vulcano [36] confirms that a moderate seismic event could initiate a rapid magma ascent.The seismicity recorded from 1999 to 2011 comprises events withM<5.0 and the 16, August, 2010 (M=4.8), one represents the event with the highest magnitude recorded. In this study, the region-time-length (RTL) algorithm has been implemented to the catalogue of earthquakes which occurred in the period from 2000 to 2010 and we discuss the phases of seismic activation and quiescence preceding the M=4.8 event in 2010.


## 2. Data

Since the late ‘70s, continuous seismic monitoring activity in the Aeolian Archipelago has been performed by a permanent seismic network made up of a few analogical 3C stations. Starting from the ‘80s, the network was augmented with other stations deployed over the entire Aeolian Archipelago and equipped with short-period seismometers, having a natural frequency of 1 Hz. During 2005 and 2007, almost all the stations were replaced by new digital 24-bit ones, equipped with broadband (40 s) three-component sensors, with a dynamic range of 144 dB. To date, the Aeolian permanent seismic network, managed by INGV-CT (Istituto Nazionale di Geofisica e Vulcanologia-Sezione di Catania), consists of 12 three-component digital seismic stations (Figure1). In order to reduce the azimuthal gap, events location is obtained also using the stations deployed in the Calabro-Peloritan area and on the northern flanks of Mt. Etna (Figure 1). Furthermore, where possible, we added data from the INGV national permanent seismic network.We considered an area of100×80 km with a latitude between 38.00 and 38.85 and a longitude of 14.00 and 15.30. The dataset used in this study comprises 1680 crustal earthquakes recorded from August 1999 to 2011 with magnitude 1.0≤Md≤4.8, whose location, performed for surveillance purposes, is obtained by using the Hypoellipse code [37] (Figure 2). The mean errors of the analytical locations are, respectively, 0.95 km for the epicentral coordinates and 1.15 km for focal depth; the mean root mean square (RMS) is 0.16 s.Figure 2
Seismic activity recorded in the Aeolian Archipelago area during the August 1999–December 2011 period. The dataset comprises 1680 earthquakes recorded from August 1999 to 2011; the red circle shows location of the 16, August, 2010,M=4.8 earthquake.The main event of the catalogue occurred at 12.54 GMT of the 16, August, 2010, when Aeolian Archipelago was shaken by an earthquake of an estimated 4.8 magnitude. The hypocenter of the earthquake was situated 8 km west-south-west of the island of Vulcano at a depth of 13.0 km b.s.l. (Figure1). The earthquake was felt on the northern coast of Sicily and in the cities of Palermo, Catania, and Messina. The earthquake triggered some landslides at Lipari, a rock fall on the flanks of Vulcano Lipari and Salina. In the village of Lipari minor damages to buildings and roads were reported and some beaches were closed for safety reasons.


## 3. Method

The analysis of the earthquake dataset has been performed by using the well-established method known as RTL algorithm [4, 8] which uses three parameters, namely, R (region around the earthquake epicenter), T (time), and L (rupture length). The fundamental idea of RTL algorithm is to assign a weighting RTL value to a given spatiotemporal value (x,y,z,t), which comes from events occurring in a prescribed space-time window within the characteristic distance and time. An RTL parameter is defined as the product of R, T, and L describing the influence weights of location, occurrence time, and magnitude as
(1)R(x,y,z,t)=[∑i:1nexp(-riro)I(ri≤2ro)I(t-ti≤2to)×I(di≤do)I(Mi≥Mmin)∑i:1nexp(-riro)]-Rbk(x,y,z,t),T(x,y,z,t)=[∑i:1nexp(-t-tito)I(ri≤2ro)I(t-ti≤2to)×I(di≤do)I(Mi≥Mmin)∑i:1nexp(-t-tito)]-Tbk(x,y,z,t),L(x,y,z,t)=[∑i:1n(-liri)I(ri≤2ro)I(t-ti≤2to)×I(di≤do)I(Mi≥Mmin)∑i:1nexp(-t-tito)]-Lbk(x,y,z,t),
where li is the rupture dimension (a function of magnitude Mi); ti is the occurrence time of the ith earthquake; ri is the distance from the position (x,y,z) to the epicenter of the ith event; r0 and t0 are the characteristic distance and time associated with the spatiotemporal criteria; do is the cut-off depth; and n is the number of events satisfying the following criterion:M
i
≥
M
min (Mi is the magnitude of ith event and Mmin is the cut-off magnitude ensuring the completeness of the earthquake catalogue); ri≤Rmax=2ro; and t-ti=Tmax=2to.For the rupture dimensionli the following expression is used [16]:
(2)li=exp(0.44*Mi-1.289).Rbk, Tbk, and Lbk are the background values of R, T, and L, respectively, obtained as the expected values in the time interval considered for the analyzed position. RTL parameter describes the deviation from the background level of seismicity and is expressed in units of the standard deviation. A negative RTL value indicates a lower seismicity and a positive RTL value indicates a higher seismicity compared to the background. Clearly, both a temporal and a spatial analysis of RTL can be performed and some authors often use the spatial average value for the RTL parameters calling it Q parameter [11]. The algorithm for the computation of R, T, L, and Q parameters has been implemented in the MATLAB environment (Figure 3), allowing simple management and plotting of the results.Figure 3
Flowchart that documents the algorithm used on Matlab for RTL analyses. The input variable “data” contains all the information about the events to be analyzed.P test and t, are respectively, the position and the time to be studied, whereas IT1 and IT2 individuate the interval of time to be considered for the RTL analysis. Clearly the constants “ref_d,” “ref_t,” “refM,” and “refD” correspond, respectively, to ro, to, Mmin, and do.


## 4. RTL’s Calculation and Results

The RTL analysis needs to be applied to declustered catalogues, where aftershocks are removed [9]. In order to decluster the INGV catalogue, we applied the Reasemberg [38] algorithm implemented in Zmap software [39].The Reasenberg algorithm defines a seismic sequence as a chain of events linked to each other by spatial and temporal windows. The variables arerfact, the factor for the interaction radius of dependent event, τmin, the look-ahead time for un-clustered events in days, τmax, the maximum look-ahead time for clustered events in days, and P, a measure of the confidence that the next event in the sequence is being observed.For declustering we used the default parameters (rfact=10, τmin=1, τmax=10, and P=0.95) obtaining a catalogue of 1324 events.Moreover the magnitude of completeness has been evaluated for the catalogue by using the Gutenberg-Richter relation of earthquake frequency and magnitude.The completeness of the data entries depends on the characteristics of the seismic network. The geometry, sensitivity, and resolution of the seismic network quantify different parts of the region in order to judge the behavior of the seismic regimes based on the representation of minimum magnitude.We applied the Gutenberg-Richter relation to search theMmin, representative magnitude for the present earthquake time series of the Aeolian Archipelago region.The power law of Gutenberg-Richter fits the earthquake energy distribution as a linear plot of recurrence. The bending of the linear plot for the smaller magnitude earthquake gives an indication of incompleteness of the catalogue below a specified magnitude. This specified magnitude is the minimum or the threshold magnitude for the studied area. Figure4 shows the earthquake frequency magnitude plot. It may be noted from here that the data are complete for earthquakes of M=1.8. After removing events with M<1.8 the remaining data comprised 838 events which were used for the present study to estimate the RTL variation.Figure 4
B-value estimation of the complete earthquake dataset (August 1999 to 2011) after removing the aftershocks in the Aeolian Archipelago region.We calculated the RTL andQ parameters [9, 13], that is, the possible time and spatial variation of the seismic quiescence, and to this end we made some choices about the input parameters; if we consider, for example, the M=7.3 earthquake, which occurred in the western region of Tottori prefecture, Japan, on 6, October, 2000, Huang [9] adopted a distance r0=50 km, t0=1 year, and a focal depth (d0) of 30 km.Shashidhar et al. [15], for moderate earthquakes (M=5.0) in a small area (20 km × 30 km), tried different values for parameters adopting the following values: r0=10 km, t0=25 days, and d0=20 km.In order to obtain the RTL, we have considered location of the 16, August, earthquake (M=4.8) and the 1, January, 2008–15, August, 2010 (958 days), period.We set a focal depth of 30 km considering that almost all earthquakes (98.7%) are not more than 30 km deep (Figure5) and we tried different values of r0 and t0 (Figure 6). RTL algorithm does not show large differences between the different curves (Figure 6); we adopted the following model parameters: a characteristic distance r0 = 25 km and t0 = 50 days. Finally, we also ran (Figure 7) the RTL algorithm for the entire 2000–August 2010 period.Figure 5
Cross-section of the selected seismicity catalogue to show depth distribution of all seismicity (grey diamonds) and after removing aftershocks andM<1.8 (purple diamonds).Figure 6
Temporal variation of the RTL at the epicenter of the 16, August, 2010,M=4.8 earthquake. The variation in RTL anomaly is obtained at this location with different values of parameters reported on the left of the graphs. The three values are referred to as ro, to, and do. Starting point is 1, January, 2008 and duration is 958 days. Some examples of seismic activation are indicated by arrows.Figure 7
2000–August 2010 time variation of the RTL at the epicenter of the 16, August, 2010,M=4.8 earthquake by using ro=25, to=50, and do=30 as input parameters. Red diamonds identify the occurrence times of the 3.2≤M≤3.8 earthquakes located nearby (10–15 km) the 16, August, 2010, epicenter.


## 5. Discussion

In many parts of the world, the RTL method has been used for larger regions and longer seismic catalogues, obtaining valid observations on the quiescence phenomenon prior to large earthquakes [11, 40]. In this study, the RTL algorithm has been implemented in the MATLAB environment and tested to a triggered earthquake time series occurring in the Aeolian Archipelago (Italy), a relatively small area (100 km × 80 km) characterized by a moderate seismicity. A phase of seismic quiescence (between the 700th and the 850th day in Figure 6) was detected by the Q parameter around the epicenter of the 16, August, 2010, earthquake. The seismic quiescence spans the June–December 2009 period, ending 8-9 months before the M=4.8 earthquake.Figures6 and 7 show the presence of short-time positive changes (activations) during the 2000–2010 period. These short changes are linked to the occurrence of 3.2≤M≤3.8 earthquakes located nearby (10–15 km) the M=4.8 epicenter. Moreover some modest and rapid negative changes are also visible.All these short-time variations may be related to an imperfect removing of the aftershocks in the catalogue and/or to the adopted parameters.Six-seven-month quiescence ending 8-9 months before the earthquake is in accordance with duration of the quiescence (0.6 to 3 years) and time shift from the end of the quiescence to the earthquake (0 to 2.9 years) was found by Gentili [20] for several Italian sectors.Finally, in order to investigate its possible spatial variation, we calculated theQ parameter in the quiescence period (June–December 2009) for the entire area (Figure 8). To this end, the territory has been divided into 2,500 cells, each one with an area of ca. 4 km2.Figure 8
Spatial variation of RTL in the Aeolian Archipelago area during the observed quiescence period (June–December 2009). The scale on the right corresponds to the RTL value in the units of the standard deviation. The white circle shows location of the 16 August 2010,M=4.8 earthquake.The main area covered by the quiescence (ca. 200 km2) comprises a sector around Vulcano island. The M=4.8 earthquake occurred in this area, which is about 4 km west of the pixel with lower (−3.3) Q value. However, an area between Salina and Filicudi of ca. 80 km2 and a small sector (ca. 40 km2) in the north of Sicily also show negative Q values. Areas covered by the quiescence agree with sectors affected by Sisifo and Tindari-Letojanni fault system.Considering theM=4.8 location (Figures 1 and 8) we would expect an quiescence focussed only on Tindari-Letojanni fault system. As different tectonic zones have different background seismicity [13] our results suggest a continuity between the two structures and a relationship between the quiescence recorded before the M=4.8 and overall Aeolian Archipelago regional tectonics.


## 6. Conclusions

The results obtained reveal a seismic quiescence phase before anM=4.8 earthquake with an extensive (ca. 320 km2) spatial distribution which comprises the triggered zone. However the area covered by the quiescence seems large in order to affirm that the method presented here is an effective tool of improving the significance and reliability of earthquake precursors.These features are consistent with the results obtained by different authors by using RTL worldwide and encourage us to improve RTL analyses on other earthquakes by testing different parameters in order to evaluate the future possibility of moderate earthquake occurrence in this region that could also have an impact on the volcanic system of Vulcano.



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*Source: 531212-2014-01-08.xml*