et al. Sediment input, fluid pressure, temperature, roughness and faulting of the subducting plate affect the frictional properties of the plate interface (e.g. M. Kobayashi At the Japan subduction zone, Suito et al. The Middle America Trench (MAT) marks the boundary where the Cocos Plate subducts under the Caribbean Plate at rates ranging from 67 mm yr−1 at the latitude of Guatemala to 77 mm yr−1 offshore the Nicoya peninsula, Costa Rica (DeMets et al.2010) (Fig. S5) fit the coseismic displacements reasonably well (χ2 = 132). Chadwell 6d). S2). Kanamori In order to define what are aftershocks versus the background rate of seismicity, it is important to consider what the rate of previous seismicity was for the same fault segment. They provide a unique way for us to listen to the vibration of the Earth that is otherwise inaudible to us, and to decipher the complicated earthquake physics and triggering processes. We analyze seismograms from a dense network to characterize the source of this earthquake. Notes. [3], The 2012 earthquake's epicenter was located within the Indo-Australian Plate, which is divided into two sub- or proto-plates: the Indian, and Australian. Watkins [32][33] Since the initial magnitude 8.6 earthquake, there have been 111 aftershocks over magnitude 4.0 according to USGS, including a magnitude 6.2 on 15 April 2012. We only display the results from the coastline inland. et al. Smaller checkers then shown here (i.e. Correa-Mora The mechanism of great Banda Sea earthquake of 1 February 1938: applying the method of preliminary determination of focal mechanism to a historical event. (2013) estimate approximately 1 m of maximum slip and long duration for the earthquake. In 1982, a 4.7 magnitude earthquake centered in Laconia, N.H. shook homes and rattled shelves. At their boundary, the Indian and Australian Plates converge at 11 mm (0.4 in) per year in a NNW–SSE direction. The pattern of coseismic displacements for the 2012 August 27 earthquake points towards the USGS NEIC epicentre (Fig. To estimate the magnitude and spatial variation in the afterslip distribution, we inverted cumulative post-seismic displacements from sites in El Salvador (AIES, SSIA, SNJE, and VMIG) and Nicaragua (CHIN, CN22, LEME and TELN) from 100, 200, 300, 400 and 500 d following the 2012 El Salvador earthquake (Fig. White Sykes Consequently, the Cocos—CAFA convergence is 76 mm yr−1 in a direction N29° offshore El Salvador (Kobayashi et al.2014). Solid vertical lines at 100, 200, 300, 400 and 500 d after the earthquake, show times used for estimating post-seismic deformation. Hesaneh Mohammadi1, Mohammadreza Gheitanchi2* 1M.Sc. Smith 8. (f) Slip modelled as a single 2-D Gaussian function on the thrust interface (model v). Surface projection of estimates of cumulative post-seismic slip distribution after 100, 200, 300, 400 and 500 d after the main shock (a–e, respectively). Each section is 10 km long along-dip and 150 km along-strike. Black arrows show residual displacements (model subtracted from observations; observations and model vectors are shown in Fig. An alternative explanation of large post-seismic deformation lies in the geometry of the subduction zone. GPS time-series for the north component of cGPS stations in El Salvador. Banerjee Checkerboard resolution tests. 6f). Model (iii) predicts somewhat deeper slip than model (i) (Fig. R.L. If the frictional and mechanical characteristics that facilitate tsunami earthquakes are the same for regions of afterslip, we can speculate that relatively large post-seismic deformation should in general follow tsunami earthquakes. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. Johnson [37] A seismologist from the British Geological Survey[38] said that the "tearing earthquake" displaced relatively little water and was therefore unlikely to cause a significant tsunami. M. The colour scale is chosen such that no colour (white) is applied where slip is less than 1 per cent of the maximum slip on the scale. Considerable post-seismic deformation following the 2012 August 27 earthquake is observed at the cGPS stations in El Salvador (Figs 3 and 4). For the parameter optimization we employ sequential simulated annealing and grid search, minimizing the sum of weighted residuals, χ2 = Σ[(O − E)/σ]2, where O are the observations with uncertainties σ, and E are the model predictions. T. P. Hernandez D.J. 7). We test viscosities between 1 × 1017 and 1 × 1020 Pa s for each of the viscoelastic layers in order to estimate what viscosities would be needed to explain the post-seismic deformation if the observations are dominantly caused by viscoelastic relaxation. Dashed grey lines show 10 km depth contours of the plate interface as defined by Hayes et al. 6a; Tables S2–S8). Table S9. The degree to which a plate boundary fault is coupled can have profound effects on its seismogenic behaviour. (d) Slip distribution estimated as Gaussian functions along each downdip profile (model iii). (a) Linear trend estimated from the time period 2005.0–2012.6 has been removed; (b) Linear trend and annual and semi-annual signals estimated from the time period 2005.0–2012.6 have been removed. Below we discuss slip localization in relation to aftershock locations, large post-seismic deformation at other margins and tectonic settings, and how interseismic strain may accumulate offshore El Salvador. B. Black vectors show interseismic GPS-site velocities relative to the Caribbean Plate (from Kobayashi et al.2014). 226‐227. (2004), then the afterslip, and hence geodetic moments we estimate for the afterslip above would be 25 per cent less. The strongest earthquakes of this sequence occurred on May 29, 2012, with Ml 5.8 and Ml 5.3, recorded at 9:00 and 12:55 local time, respectively. This entry was posted in Journal and tagged Koper. The most poorly fit coseismic offset for any of the models is that for eGPS site CH15 (Figs 4 and 6). W. G.P. et al. Georgia Institute of Technology. 2), suggests that the co- and post-seismic slip distributions affect similar areas of the subduction interface. On 26 February 2012, an inland M L 6.4 earthquake occurred near Wutai Township in Pingtung County, Taiwan and caused massive shaking in southern Taiwan. [54], "The 2012 Mw 8.6 Sumatra earthquake: Evidence of westward sequential seismic ruptures associated to the reactivation of a N–S ocean fabric" by C. Satriano, E. Kiraly, P. Bernard, and J.-P. Vilotte, Indian National Centre for Ocean Information Services, Indonesian Agency for Meteorology, Climatology and Geophysics, "Modeling the 2012 Wharton Basin earthquakes off-Sumatra: Complete Lithospheric failure", "Magnitude 8.6 – OFF THE WEST COAST OF NORTHERN SUMATRA", "Why April 11 quake was caused by a strike-slip fault", "M8.6 - off the west coast of northern Sumatra", "Indian Ocean tsunami alert cancelled after two strong quakes hit off Sumatra, Indonesia", "Huge quake strikes off Indonesia, tsunami warning issued", "An integrated global model of present-day plate motions and plate boundary deformation", "Ridge torques and continental collision in the Indian-Australian plate", 10.1130/0091-7613(1995)023<0653:RTACCI>2.3.CO;2, "April Sumatra quakes signal Indian ocean plate break-up", "Indian Ocean on tsunami alert after quakes", "Scientists: Magnitude-8.6 Indonesia jolt was unusually large for a strike-slip quake; Winnipeg Free Press", "Explained: What is a slip-strike quake, and why there was no tsunami - World - DNA", "Poster of the M8.6 Northern Sumatra, Earthquake of 11 April 2012", "Supershear rupture on multiple faults for the Mw 8.6 Off Northern Sumatra, Indonesia earthquake of April 11, 2012", "Earthquake in a Maze: Compressional Rupture Branching During the 2012 Mw 8.6 Sumatra Earthquake", "Séismes au large de Sumatra mercredi 11 avril 2012", "Massive earthquake strikes Indonesia, tremors felt in India", "Strong Indonesian quakes cause panic, not tsunami", "Indian Ocean tsunami alert lifted after Aceh quake", "Strong earthquake in Sumatra slightly felt in Yangon – Xinhua | English.news.cn", "News : Tremors across eastern coast; people evacuated from Andamans", "8.6 earthquake hits Aceh, tsunami alert issued (Update) | theSundaily", "Large Aceh quake triggers Indian Ocean tsunami warning – Tremor felt in Colombo | Independent Television Network News", "8.2-magnitude aftershock hits off Sumatra", "M8.2 – off the west coast of northern Sumatra", "Latest Earthquakes M5.0+ in the World – Past 7 days", "Magnitude 6.2 - off the West Coast of Northern Sumatra", "Indonesia earthquake: No damage to ocean basin, India withdraws tsunami warning", "Pacific Tsunami Warning Center/NOAA/NWS: Tsunami bulletin number 003", "Staff Profile of Dr Roger Musson | British Geological Survey", "Watch: Indonesia Reacts to 8.7 Magnitude Earthquake", "Indonesia earthquake: India issues tsunami warning for Andaman and Nicobars", "Earthquake in Indonesia: How India responded", "Earthquake in Indonesia: India withdraws tsunami warning", "8.6 magnitude quake in Aceh triggers tsunami fears in India", "Tsunami warning in South and East | Top Story", "Trains stopped, power to be disconnected | Breaking News", "Expressway free of charge | Breaking News", "Private buses stop in coastal areas | Breaking News", "Small tsunami reaches Thailand after huge quake", "Strong Indonesian quakes cause panic across Asia, not tsunami", "Update: Indonesia Lifts Tsunami Warning, Residents Return Home", "Terrified Indonesian island survives quake – Yahoo!7", Massive earthquake hits Indonesia, no tsunami risk, Preliminary source parameters obtained by automatic analysis - 2012/04/11 08:38 Off West Coast of Northern Sumatra, After major earthquake, silence: Dynamic stressing of a global system of faults results in rare seismic silence, Rare great earthquake in April triggers large aftershocks all over the globe, https://en.wikipedia.org/w/index.php?title=2012_Indian_Ocean_earthquakes&oldid=1010177927, Earthquake clusters, swarms, and sequences, Articles with dead external links from September 2018, Articles with permanently dead external links, Articles with unsourced statements from April 2012, Creative Commons Attribution-ShareAlike License, This page was last edited on 4 March 2021, at 04:49. The maximum slip (Sx), resulting moment magnitude (Mw), and χ2 are given for each model. Alessandro Amato, an earthquake expert at the Rome-based National Institute of Geophysics and Volcanology (INGV) told Sky Italia television that the epicenter was found in what is known as the Padania plains, an area that had not been noted as a potentially dangerous spot on the seismographically sensitive Italian peninsula. ‘c’ stands for a continuous GPS site and indicates no delay. strongly coupled) up to at least 2 km depth during the interseismic period. Fernández On 27 August 2012 (04:37 UTC, 26 August 10:37 p.m. local time) a magnitude M w = 7.3 earthquake occurred off the coast of El Salvador and generated surprisingly large local tsunami. 5) demonstrates that motion of those sites is dominated by post-seismic deformation from the El Salvador earthquake rather than the Nicoya earthquake because otherwise the deformation would be more south- or southeastward towards the Nicoya epicentre (e.g. [24] Indonesian authorities also issued a statement saying that the likelihood of a tsunami was low. The ratios of the post- to coseismic moments for these events, based on geodetic inversions, are 1.8, 3.6 and 3.1, respectively. To explain the entire observed post-seismic deformation signal as a viscoelastic response, viscosities of 1017 and 1017–1018 Pa s are required for the upper mantle and lower crust, respectively (Fig. The coseismic offsets and subsequent post-seismic deformation are most pronounced in the north component of the GPS time-series (Fig. In fact, shallow strike slip events along the CAFA–Caribbean Plate boundary have caused much localized damage and are a serious seismic hazard in the region. 5). There was a strong correlation between the fault rupture pattern and the distribution of the aftershocks. This earthquake had an overall relatively slow rupture speed, although the speed was above the S-wave velocity in some fault segments. Results of viscoelastic modelling for the north component of station SSIA for a range of upper mantle and lower crust viscosities. The coseismic displacements are equally well fit by either large slip (maximum slip greater than 4 m) over a small area (Figs 6b and c) or low slip (maximum slip as low as ∼0.2 m) over a larger area (e.g. Estimates of the motion of the CAFA microplate relative to the Caribbean Plate from earthquake slip vectors and GPS data range from 10 to 16 mm yr−1 towards the northwest (DeMets 2001; Turner et al.2007; Correa-Mora et al.2009; LaFemina et al.2009; Kobayashi et al.2014). et al. 6e). We considered only earthquakes of magnitude 3 or greater and removed upper-crustal earthquakes along the CAFA–Caribbean boundary. Wang Japan's scientists say the magnitude-7.4 earthquake that hit the Fukushima and Miyagi prefectures on Tuesday was a strong aftershock of the massive Fukushima quake in 2011. The 2012 earthquake's epicenter was located within the Indo-Australian Plate, which is divided into two sub- or proto-plates: the Indian, and Australian. 55, The 2010–2011 Canterbury earthquake sequence, pp. Epicentral location of the 2012 August 27 El Salvador earthquake from USGS–NEIC is shown with a star. Simeulue is an island of fishing villages 150 km (93 mi) off the west coast of Sumatra. E. Mora D. Strauch [11], As part of a risk mitigation measure, the Ceylon Electricity Board disconnected power supplies to coastal areas and railway control rooms. Slip distribution for best-fitting model of coseismic deformation. The data were processed using the GIPSY/ASIS II software in precise-point-positioning mode for kinematic data using loose constraints on the solutions. This is, however, not the case for the eGPS measurements, where the post-seismic contamination depends on the time between the earthquake and the measurement (Table 1) and the extent and amplitude of the post-seismic deformation (see next section). Each station is detrended using its mean velocity during 2005–2012. 4b) show a generally decaying trend of post-seismic motion. Large post-seismic deformation has also been observed at other subduction zones. GPS time-series from selected stations in El Salvador and Nicaragua in east, north, and vertical components. A.P. [7], The Indo–Australian Plate was formed after the amalgamation of the Indian Plate and the Australian Plate some 45 million years ago. The highest was 80 cm (31 in), at Meulaboh. Published by Oxford University Press on behalf of The Royal Astronomical Society. 9). We find that the Mw7.3 2012 August 27 El Salvador tsunami earthquake occurred on shallow parts of the plate interface and was followed by significant afterslip, causing the observed post-seismic deformation to exceed the coseismic deformation in less than 1 yr. Upper crustal earthquakes along the forearc-Caribbean Plate boundary in El Salvador and Nicaragua have been removed from the data set. P. A. At least 600 people died, mainly due to collapsing buildings. Table S8. 3, where we have estimated and removed the pre-seismic average velocity for each site. After the 2010 M L 6.4 Jiasian earthquake caused extensive damage in southern Taiwan, deep, complicated structures were revealed. 8) indicate that slip was focused near the epicentral area during the first 100 d, then progressed further downdip (maximum slip at ∼50 km depth) for the remainder of the transient period. We use the TDEFNODE software (McCaffrey 2009) to invert the geodetically estimated coseismic offsets for displacement on the megathrust. Rupture characteristics of the 2012 earthquake doublet in Ahar-Varzagan region using the Empirical Green Function method . In our interpretation, these observations of seismic and aseismic slip following the 2012 August 27 earthquake signify weak coupling and conditionally stable friction on the subduction interface offshore El Salvador and Nicaragua. Because of the seasonal signals we estimate linear, annual, and semi-annual parameters for each of the cGPS time-series components from pre-seismic data (2005 or later, depending on data availability) and apply these to the entire time-series to remove steady-state (i.e. Figure S8. The maximum observed coseismic displacement is 17 mm at eGPS site JUCU in eastern El Salvador. Listening to the 9. M. 4). The earthquake was followed by a tsunami with a maximum run-up of 2 m near Imperia, Italy. MANA). Hayes For example, Hill et al. As mentioned above, we cannot fully separate the co- and post-seismic deformation at the eGPS sites. Ruptures associated with tsunami earthquakes may propagate up-dip into or through the sediments (Polet & Kanamori 2000). Bock 2Professor, Earth Physics Department, Institute of Geophysics, University of Tehran, Iran Episodic GPS site CHIN (Nicaragua) was occupied continuously from 2012 September 2 onwards. Imakiire In the inverse model we start with zero slip on all nodes and invert the signal calculated from the forward model, using model setup ‘i’ (see Section 3.1). there is low or no coupling between the plates (Correa-Mora et al.2009; LaFemina et al.2009; Kobayashi et al.2014)]. The cGPS sites in El Salvador record post-seismic motion approximately towards the epicentral region (Fig. [49] This caused criticism on the internet, although it was muted by a lèse majesté law. Figures were prepared using the GMT software (Wessel & Smith 1998). S.E. As Fig. Although this depth corresponds to a band of persistent seismicity (boxes 2 and 3 in Fig. In January 2009 a series of low‐intensity seismic movements began to shake the Abruzzo region and its capital, L'Aquila. Wdowinski [11], In Kolkata, underground Metro Railways services were stopped and tall office buildings and shopping malls were evacuated. The initial quake was not expected to affect Sri Lanka, but aftershocks were being monitored. Table S4. There is a fivefold increase in the rate, R, of shallowglobal M$5.5 events for several days following the 2012 mainshock (Fig. We estimate an oblique reverse faulting mechanism, moment magnitude of 5.2 and a shallow hypocenter (4.6 km), at only 5.5 km epicentral distance from the city center. The largest event in the region occurred on 14 November 1981 (M 5.3), 20 km beneath the Wadi Kalabsha embayment, a westward extension of the Lake Aswan. 3), because the measurements were not made instantaneously after the earthquake (Table 1). [42] Prabkhakar Rao of the disaster control room in Port Blair said that there could be tsunamis as high as 1.5 m (4.9 ft) at Port Blair and 3.9 m (12.8 ft) at Campbell Bay. Lin et al.2013). The best-fitting slip distributions for the cumulative post-seismic displacements (Fig. Hill H. (2005) used seafloor-geodetic observations offshore Peru, a sediment-starved margin, to verify that the subduction zone in that location was not slipping (i.e. D.E. Earthquake magnitude and cumulative number of earthquakes for data within boxes 1–4 in (a) and (b) are shown in (c) to (f). Here we solved for the centre, spread, and slip amplitude of the Gaussian function along each set of downdip nodes; (iv) Slip modelled as a single rectangular patch with uniform slip and gradual tapering (Fig. 5). Slip distribution for best-fitting model of cumulative postseismic deformation for the first 100 d. Format follows TDEFNODE conventions for .nod files (see TDEFNODE manual). The maximum slip (Sx), moment magnitude (Mw), and χ2 are given for each model. The rupture of these earthquakes occurred on multiple, almost orthogonal faults. Projected tsunami landfall times in GMT were: 8:38 for Indonesia, 11:38 for Sri Lanka, 14:38 for the Seychelles, 17:38 for Madagascar and 20:38 for South Africa. Figure S5. Displacements from four different sections of the thrust interface as a function of distance from the trench. Map of estimated coseismic displacements (black vectors) with 1σ uncertainties at our geodetic GPS network sites. These events thus indicate that large post-seismic deformation compared to coseismic deformation is not a unique characteristic of weakly coupled margins, but may also be characteristic of areas that straddle the transition from strong interseismic locking to aseismic creep. We reran a subset of our models excluding site CH15 and found that while the χ2 value drops from 88 to 64 (model i), the overall slip distribution or fit to other sites did not change significantly (Figs 6g and h). (2004) for offshore Nicaragua: a 16 km thick elastic upper crust (30 GPa shear modulus), a Maxwell-viscoelastic lower crust between 16 and 30 km, and a Maxwell viscoelastic half-space (upper mantle) below 30 km depth. In this study, we use global positioning system (GPS) data and earthquake locations to investigate the co- and post-seismic deformation associated with this event and discuss our results in terms of the strain accumulation and slip characteristics of the weakly coupled subduction zone offshore El Salvador and Nicaragua. At one end of the spectrum, earthquakes represent near-instantaneous high-strain rate events, whereas at the other end of the spectrum episodic slow-slip events and transient afterslip following intermediate to large magnitude earthquakes represent low strain rate events that may occur over weeks to years. et al. Hill [15], These earthquakes have a complex rupture process. We assume in the following section that the post-seismic deformation is solely caused by afterslip, but discuss later the effects that viscoelastic relaxation may have on our interpretation. The seismic model of Ye et al. Historical accounts of earthquake damage (White et al.2004) and tsunamis (Fernández et al.2004), and instrumental records (Ambraseys & Adams 1996) indicate that the last earthquake to rupture the southern segment of the El Salvadoran subduction zone occurred in 1919 or earlier. (2012), and coloured dashes mark the location of each of the sections we calculate displacement for. Sites TEG2 and CN22 trend to the south or southeast; however, both TEG2 and CN22 have short (1.5 and 0.5 yr, respectively) time-series for estimation of the pre-seismic velocities, which can degrade the estimation of the post-seismic deformation. 4 × 4 nodes and below) are poorly recovered. The mainshock was preceded a few hours before by a Mw 4.3 shock, and it was followed by a dozen Ml >4 aftershocks in May and June, amongst which 11 had Ml ≥4.5. Oxford University Press is a department of the University of Oxford. Cumulative post-seismic displacements at 100, 200, 300, 400 and 500 d after the 2012 El Salvador earthquake. Nishimura Slip distribution for best-fitting model of cumulative post-seismic deformation for the first 200 d. Format follows TDEFNODE conventions for .nod files (see TDEFNODE manual). 6d). E.M. F. Lin M. tectonic motion) and annually cyclic movements. Subduction zones exhibit variable degrees of interseismic coupling as resolved by inversions of geodetic data and analyses of seismic energy release. (2011) note rapid afterslip following the 2010 Mw7.8 Mentawai earthquake, where post-seismic displacements nearly equal the coseismic displacements after 8 months. Fig. This model (with maximum slip at 25–30 km) gives a lower bound for the total post-seismic moment release, assuming that no viscoelastic deformation occurred. [19] The quake prompted people in Indonesia, Thailand and India to leave their homes and offices in fear of tsunamis. 8; Table S9). Black arrows show residual displacements. Here we solve for the centre location, slip amplitude, and along-strike and downdip width of the rectangular patch; (v) Slip modelled as a single 2-D Gaussian distribution on the slab interface (Fig. In the case that viscous relaxation plays an important role, the main effect is that the total moment we estimate for the afterslip would be less. DeMets An interesting aspect of tsunami earthquakes is that they rupture the shallowest part of the subduction interface (<20 km depth), which has been suggested to be generally unable to accumulate large amounts of strain (e.g. M.R. We suggest that the excessive post-seismic motion is characteristic for the El Salvador–Nicaragua segment of the Central American margin and may be a characteristic of margins hosting tsunami earthquakes. This causes a bias in the coseismic estimates because some of the post-seismic deformation will be incorporated into the coseismic displacement estimates. B.J. N. S6). We did not observe any significant post-seismic deformation in the vertical component. Grey circles show location of M > 3 earthquakes from 2012 August 27, to 2014 June 30, from the Nicaraguan seismic network. Heflin The earthquake and the largest aftershock had a fault displacement of 21.3 m (70 ft). The 2012 Indian Ocean earthquake is associated to the reactivation of the NNE-striking sea floor fabric. slip versus no slip) for rectangular patches larger than approximately 100 km by 100 km, the slip amplitudes are not well recovered. This earthquake occurred 292 d after the 2012 August 27 El Salvador earthquake and thus does not affect our post-seismic displacement estimates at 200 d after the El Salvador earthquake. The earthquake, which the United States Geological Survey said had a magnitude of 6.0, crumbled church roofs and Renaissance-era towers, according to Italian television reports. 6c); (iii) Slip modelled as a Gaussian function of depth, using a grid consisting of 25 along-strike and 18 downdip nodes (Fig. Slip distribution for best-fitting model of cumulative post-seismic deformation for the first 500 d. Format follows TDEFNODE conventions for .nod files (see TDEFNODE manual). The 0.1 m of slip gives deformation on the same order of magnitude as for our coseismic deformation at the station locations. [51][52] The Indonesian Agency for Meteorology, Climatology and Geophysics said three small tsunamis struck the Aceh coast. J. Kinematic analysis of 30-s GPS data from stations AIES, VMIG and SSIA. 1). However, if the afterslip is located at even shallower depths (<5 km), then the post-seismic moment release needs to be higher, 6.0 × 1020 Nm (Mw7.8) for the first 500 d, to match the displacements. We thank everyone contributing to collection of episodic and continuous GPS data in the study area. Y. Bilek 1), located about 250 km southeast of the 2012 El Salvador earthquake at cGPS station MANA, where post-seismic displacements exceeded coseismic by a factor of 2 (Fig. Earthquake activity offshore El Salvador and Nicaragua during 2010–2014. With … [9][10], The magnitude 8.6 (Mw) earthquake occurred about 610 km (379 mi) southwest of Banda Aceh, Indonesia at 08:38 UTC on 11 April 2012. [17] The rupture was caused by ductile shear heating instability which is different from frictional failure and operates between 600–800 °C (1,112–1,472 °F), which corresponds to about the depths of 40–60 km (25–37 mi). Annals of Geophysics, the former Annali di Geofisica, published its latest issue today, dedicated to the 2012 Northern Italy earthquakes: Vol 55, No 4 (2012): The Emilia (northern Italy) seismic sequence of May-June, 2012: preliminary data and results.On 20 May 2012 an earthquake with a magnitude of Mw6.1 hit Finale Emilia, on 29 May an Mw5.8 event followed. We thank INETER, Nicaragua, for field support.
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