For example, during the 1992 Nicaragua event (mb= 5.3; Ms= 7.2), the earthquake was not felt in some coastal communities, whose unprepared population was washed away 40 min later, at a cost of 170 casualties (Satake et al. Briggs R.W. It shares the focal geometry of Model 22.1, but features a lower rigidity, and hence an enhanced slip, with a slightly elongated more ‘ribbon-like’ fault geometry. In the case of Event III, all solutions are displaced SSW from the main shock in the vicinity of our relocated solution (19.24°N, 104.34°W), although our confidence ellipses for the three events do intersect. The largest observed earthquake in the region was a magnitude 8.6 in Oaxaca in 1787. Okal & Kirby (2002) and later López & Okal (2006) have shown that this approach can be applied to paper records from historical events. Kanamori′s (1972) original paper was based on two events: the 1896 Sanriku earthquake and the 1946 Aleutian one. (1985) suggested the existence of a Colima seismic gap, which was filled during the later Tecoman earthquake of 2003 January 22 (Yagi et al. This site uses cookies. Among the 29 earthquakes listed on Table 1, we earmark with a a eight events which have generally better locations, as evidenced by smaller confidence ellipses. We conduct a detailed seismological study of the large Colima, Mexico earthquake of 1932 June 3 and of its aftershocks of June 18 and 22. (2008) after the 2007 Solomon Islands earthquake. Event I on 1932 June 3 resulted in severe destruction in Manzanillo and adjoining areas with upwards of 400 casualties. We use Mansinha & Smylie′s (1971) algorithm to compute the field of static displacement of the ocean bottom resulting from the dislocation, which is then taken as the initial condition, for the numerical simulation, of the deformation of the sea surface. We also show, on Fig. Havskov J. Fritz H.M. Pranantyo I.R. As shown on Fig. You do not currently have access to this article. John Bellini, a geophysicist at the USGS National Earthquake Information Center in Golden, Colorado, said it was the strongest quake since an 8.1 temblor struck the western state of Jalisco in 1932. Estimated magnitude: 7.8-8.4. Agriculture & Commerce, Catâlogo de tsunamis (Maremotos) en la Costa Occidental de Mexico [Catalog of tsunamis on the Western coast of Mexico], World Data Center A Pub. Based on the work of Boatwright & Choy (1986), Newman & Okal (1998) have proposed a modern rendition of the mb:Ms discriminant, in the form of the parameter Θ = log10(EE/M0), where EE is the seismic energy radiated into the body waves, estimated without knowledge of focal mechanism and exact depth, and M0 the seismic moment. 2 and can be used to obtain an estimate of the length of rupture of the main shock, their relocated epicentres spreading over 140 km parallel to the coastline. In the case of the 1932 Mexican series, we are limited by the availability of adequate records, in particular because the events predate the development of the broad-band ‘1-90’ instruments (available at Pasadena starting in 1937). 12(b) shows inundation of the land spit separating the ocean from the Cuyutlán lagoons, in accordance with the description reported in local newspapers (El Excelsior 1932) and summarized by Sánchez & Farreras (1993). Earthquake information for europe. The ISS location is shown as a downward triangle at 19.2°N, 104.2°W, whereas GR′s is shown as an upward triangle at 19.5°N, 104.25°W. (a) Field of vertical displacement of the ocean floor, computed using Mansinha & Smylie′s (1971) algorithm. Synolakis C.E. 6 for Event III (Model 22.1). The analysis of the spectral amplitude of mantle surface waves yields low-frequency moments of 24, 5.2 and 4 times 1027 dyn cm, respectively, with Event III featuring a moment growing with period, which expresses the source slowness characteristic of ‘tsunami earthquakes’. Mikumo T. In this respect, the specific hazard inherent in those anomalous events that are treacherous because they do not carry the natural warning of an impending tsunami in the form of intense shaking, should be emphasized globally as part of tsunami education programs. (a) and (b) Same as Fig. Taylor F.W. We conclude that Fukao′s (1979) model involving rupture along a splay fault satisfactorily explains the available data. Tsunamis in Mexico In a total of 24 tidal waves classified as a tsunami since 1732 a total of 91 people died in Mexico. 10 shows that the results are changed only marginally and that it would not predict the reported widespread inundation. This suggests that Event III has a static moment of approximately 4 × 1027 dyn cm and definitely identifies it as an event featuring an anomalously slow source, confirming its nature as a ‘tsunami earthquake’. Because the epicentral distances involved (19.17°, 19.32° and 19.30°, respectively) are significantly shorter than the range of applicability (35° ≤ Δ ≤ 80°) of the distance correction used in the definition of T (Newman & Okal 1998), we use an empirical extension of this correction derived by Ebeling & Okal (2007). This is the exact geometry favoured by Fukao (1979) to explain the Kuril ‘tsunami earthquakes’ of 1963 October 20 and 1975 June 10. Five of those were assigned magnitudes MPAS ≥ 6 by GR. Solid dots form a background of typical values from recent sources. The aftershocks locations, the first motions at MNZ, and the isoseismic maps of the two main shocks strongly suggest that: (a) the 3 June 1932 earthquake initiated NW of but close to MNZ and propagated NW for an estimated length of rupture of 220 km; (b) the 18 June 1932 earthquake nucleated SW of MNZ (offshore) and perhaps ruptured a length of about 60 km; and (c) the width of rupture was approximately 80 km. All these figures are substantially lower than ours, and expectedly so, because the authors worked at higher frequencies, which for this size of source are systematically affected by the destructive interference due to source finiteness (Ben-Menahem 1961; Geller 1976). We conduct a detailed seismological study of the large Colima, Mexico earthquake of 1932 June 3 and of its aftershocks of June 18 and 22. It generated a minor tsunami starting with a leading depression, but which did not rise over 1 m. GR assigned it MPAS= 7.9. 11, but differs from Figs 6-10. Engdahl E.R. All relevant parameters are listed in Table 3. We were able to gather a number of historical seismograms of Events I, II and III for the purpose of computing spectral amplitudes of long-period surface waves and examining the energy contained in teleseismic P waves. This model would predict a smaller, rather than larger, tsunami than for Event I. What controls the lateral variation of large earthquake occurrence along the Japan trench? Search for other works by this author on: We use these geometries to compute focal mechanism corrections to our, Radiation of seismic surface waves from finite moving sources, Rigidity variations with depth along interplate megathrust faults in subduction zones, Teleseismic estimates of the energy radiated by shallow earthquakes, Über die partiellen Differenzengleichungen der mathematischen Physik, Source parameters of large historical (1917-1961) earthquakes, North Island, New Zealand, An extension to short distances of real-time estimators of seismic sources, Seismicity and tectonics of the Rivera Plate and implications for the 1932 Jalisco, Mexico, earthquake, International Earthquake and Engineering Seismology Part A, Seismic moments of large Mexican subduction earthquakes since 1907, Reconnaissance of the 25 October 2010 Mentawai Islands tsunami in Indonesia, Tsunami earthquakes and subduction processes near deep-sea trenches, Scaling relations for earthquake source parameters and magnitudes, Finite difference methods for numerical computations of discontinuous solutions of the equations of fluid dynamics, Seismology microfiche publications from the Caltech archives, Seismicity of the Earth and Associated Phenomena, Turbidity currents and submarine slumps, and the 1929 Grand Banks earthquake, Synthesis of long-period surface waves and its application to earthquake source studies - Kuril Islands earthquake of October 13, 1963, Anomalous earthquake ruptures at shallow depths on subduction zone megathrusts, The Seismogenic Zone of Subduction Thrust Faults, A seismological reassessment of the source of the 1946 Aleutian “tsunami” earthquake, The displacement fields of inclined faults, Teleseismic estimates of radiated seismic energy: the, The 25 October 2010 Mentawai tsunami earthquake, from real-time discriminants, fault rupture, and tsunami excitation, Seismic parameters controlling far-field tsunami amplitudes: a review, Energy-to-moment ratios for damaging intraslab earthquaes: preliminary results on a few case studies, The mechanism of the great Banda Sea earthquake of 01 February 1938: applying the method of preliminary determination of focal mechanism to a historical event, Theoretical comparison of tsunamis from dislocations and landslides, Source discriminants for near-field tsunamis, Split mode evidence for no ultra-slow component to the source of the 2010 Maule, Chile earthquake, Shallow subduction zone earthquakes and their tsunamigenic potential, The Rivera plate: a study in seismology and tectonics, The China Sea earthquake of February 14th, 1934, Seismological Bulletin for 1934 January-June, Dept. Another mechanism for the generation of exceptionally large tsunamis after earthquakes is the triggering of submarine landslides. The relocated epicentre of Event I, at 19.65°N, 104.00°W, is compared on Fig. 1 also shows our relocation of Event II, at 19.58°N, 103.84°W, as well as the other estimates for this source. 7 shows that the simulated tsunami amplitude falls to 1.5 m in Manzanillo, substantially lower than observed. The 1985 earthquake hit near the capital Mexico City, killing thousands and injuring many more. In turn, such events can be treacherous for the local populations who feel them at most as weak tremors and are thus deprived of a natural warning for the impending tsunami. Aftershocks of the 7.8 quake Colima, Mexico, 18 June 1932 10:12 GMT More info Based on its magnitude, the fault that was active during the quake ruptured along a surface of approx. Convers J. Singh S.K. EPA-EFE/JORGE NUÑEZ Emergency Services workers inspect the debris of a … 6(b). Tappin D.R. Please click on the PDF icon to access. Okal E.A. Note significantly lower wave heights. Lee W.H.K. What makes the event truly remarkable is the occurrence, 19 d later, of an aftershock that generated an even more devastating tsunami, despite a clearly smaller conventional magnitude and seismic moment. Our results may help in quantifying seismic potential of tectonically similar areas such as the Juan de Fuca subduction zone in the NW United States. Link to Wikipedia biography This model is particularly suited to the case of ‘tsunami earthquakes’ occurring as aftershocks, where the softer wedge material may have seen a loading by stress transfer from the primary event. Although this model produces larger waves than 22.1 and 22.2, they remain smaller than reported. EMSC (European Mediterranean Seismological Centre) provides real time earthquake information for seismic events with magnitude larger than 5 in the European … MOST has been extensively validated through comparisons with laboratory and field data, per standard international protocols; full details can be found in Synolakis (2003). The latter (Event III) generated a tsunami more devastating than that of the main shock despite much smaller seismic magnitudes, thus qualifying as a so‐called ‘tsunami earthquake’. Fig. 1932-06-03 10:36:56 (UTC) | 19.786°N 103.784°W | 15.0 km depth Previous determinations of Event I′s moment include Espíndola ′s (1981) comparative study of surface waves at Uppsala in the 40-70 σ range (1.0 × 1028 dyn cm), Wang ′s (1982) analysis of 50-s surface waves at three European stations (0.9 × 1028 dyn cm) and Singh ′s (1984) body wave modelling at Uppsala and Stuttgart (0.3 × 1028 dyn cm). S. K. Singh, L. Ponce, S. P. Nishenko; The great Jalisco, Mexico, earthquakes of 1932: Subduction of the Rivera plate. In Model 22.2, we consider a rupture on a splay fault, by changing the dip to 45° whereas maintaining all other parameters, including the rigidity, unchanged. (c) Run-up along coastline, plotted as a function of longitude. It resulted in considerable destruction in the city of Manzanillo and generated a locally damaging tsunami. The latter (Event III) generated a tsunami more devastating than that of the main shock despite much smaller seismic magnitudes, thus qualifying as a so-called ‘tsunami earthquake’. Same as Fig. For Event III, we assume a steeper dip, representative of faulting along a splay fault in the accretionary wedge that will be our preferred model. the development of H. Benioff′s broad-band ‘1-90’ seismometers), the significant difference in size between Events I and III (which can preclude a direct comparison, with Event III hardly emerging from the noise on Wiechert seismograms), and other unfortunate occurrences (the records being changed or the presence of obvious non-linearities). All bathymetry grids are derived from the GEBCO 0.5-min global data set, the finer ones being simply interpolated from the coarser grid. As mentioned by Eissler & McNally (1984), Event I′s entry is missing from the collection of B. Gutenberg′s notepads (Goodstein et al. The diagonal lines feature constant T, the solid one being the theoretical value (-4.90) expected from scaling laws. Dixon T. Records of Events I, II and III on the west-east component of the 6-s Wood-Anderson torsion seismometer at Pasadena. Event II, the largest aftershock on 1932 June 18, caused additional damage, especially in the hinterland locations of Colima and Guadalajara. This is confirmed by a deficient energy-to-moment ratio, as derived from high-frequency P waves recorded at Pasadena. (1991), which includes a Monte Carlo algorithm injecting Gaussian noise into the data set. Note that the ISS did not locate the event, but simply assumed a common epicentre with Event I. In a variation to this model, Bilek & Lay (1999) and Lay & Bilek (2007) have proposed that the slowness of the slip release could be due to the existence of a zone of reduced rigidity along the interplate contact, itself resulting from the ingestion, compaction and dehydration of sediments along its uppermost part. It resulted in considerable destruction in the city of Manzanillo and generated a locally damaging tsunami. 1981; Wang et al. Table 2 lists all the records used in this study. In general, two tectonic contexts have been proposed for the occurrence of ‘tsunami earthquakes’. In 1932, Mexico was hit by the Jalisco earthquake with a magnitude of 8.1. We emphasize that, because Ebeling & Okal′s (2007) regional distance corrections were derived empirically in the absence of a rigorous theoretical framework, these values remain tentative in an absolute sense; however, because the epicentral distance is essentially the same for all three earthquakes, the relative values for the three events are robust. For each event, the estimated energy EE is plotted against the seismic moment M0 in logarithmic units. Its relationship to the main shock fits Fukao′s (1979) model and is particularly reminiscent of that of the Kuril duo on 1963 October 13 and 20. Modern relocations show Event III 48 km from Event I in the azimuth N207°E (EV) or 52 km in the azimuth N219°E (this study). People in southern Mexico woke up when the earth was shaking violently, to find rubble, buildings damaged and without electricity, as a result of the 8.2 magnitude earthquake, which struck at … Bulletin of the Seismological Society of America ; 75 (5): 1301–1313. Rodríguez M. Synolakis C.E. Reexamination of arrival time data for the 1932 Jalisco earthquake yields an epicenter at 19.57°N, 104.42°W, close to the boundary zone inferred from these two earthquakes. 3 regroups our results for all three events. The 1998 tsunami in Papua New Guinea is also generally described as resulting from a landslide triggered by the seismic event with a delay of 13 min (Synolakis et al. Same as Fig. 6 for Event II (Model 18.1). Scenario 22.3 is inspired by Lay & Bilek′s (2007) model of a variable, generally deficient, rigidity along the uppermost part of the subduction interplate. The common scale allows for direct comparison of the three events, clearly exposing Event III′s deficiency in high frequencies. 3, M0 increases regularly and steeply with period on all three available records, gaining close to a factor of 10 between 80 and 200 s. Our empirical regression features a slope of -13.7 logarithmic units per mHz, 2.5 times steeper than for Event I, and clearly shows that the data set transgresses its 2s band. (1985) used a combination of differential S-P and L-P travel times and of first motion polarities at the local station MNZ and the regional stations GUM and TAC (Tacubaya), in support of Eissler & McNally′s (1984) solution. In summary, Model 03.1 best describes the effects of the tsunami on Manzanillo and its vicinity. Borrero J.C. What makes the event truly remarkable is the occurrence, 19 d later, of an aftershock that generated an even more devastating tsunami, despite a clearly smaller conve… Relocation based on published arrival times shows that Event III took place up-dip of the main shock. Classical examples would include the 1929 Grand Banks, Newfoundland and 1934 Luzon events, for which the existence of the landslides was documented during the repair of telegraphic cables severed by the events (Repetti 1934; Heezen & Ewing 1952). Depth: 15 km In this section, we simulate the regional tsunamis generated by Events I, II and III based on models of their ruptures derived from the waveform studies of Section 4. 1, at 19.57°N, 104.42°W. These events have relatively small confidence ellipses and as such help provide an estimate of the dimension of rupture. Earthquake information. 3, does not stray outside of the 2s window shown as the yellow band. For each event, the values of Mc, the mantle magnitude corrected for focal mechanism (Okal & Talandier 1989), are plotted against frequency, with relevant period and moment scales given along the top and right axes. The effects of Events I, II and III and especially of their tsunamis are summarized, for example, by Sánchez & Farreras (1993), based primarily on Mexican newspaper accounts. A study by Mexico's National Seismological Service says Thursday's deadly quake matches the force of a magnitude 8.1 quake that hit the country on June 3, 1932… Kisslinger C. Espíndola J.M. However, a mechanism similar to those used for Events I and II would not modify our main conclusion, namely that Event III features source slowness. 2, the resulting estimate for the fault length relies entirely on their events 1, 22 and 12. 2. By contrast, Event III, on 1932 June 22, that GR assessed at only MPAS= 6.9, generated a catastrophic tsunami that wiped out a 25 km stretch of coastline and in particular, destroyed the resort city of Cuyutlán, killing at least 75 people. As a result, our simulations remain tentative in an absolute sense, but can be used to compare the relative responses of the coastline to different seismic source scenarios. It furthers the University's objective of excellence in research, scholarship, and education by publishing worldwide, This PDF is available to Subscribers Only. Note: This seismic event was followed by a 7.5-8.1 magnitude earthquake in the same general area (the second shock was closer to Colima) on 18 June 1932 at 10:12 UT. Estimated casualties: 600. Two other earthquakes of magnitude 8 or over were recorded in the 20 th century—a magnitude 8.1 in 1932 and a magnitude 8 in 1985. Relocation of Events I (red), II (blue) and III (green). Singh et al. Lay T. You could not be signed in. Fig. With a published moment of 1.6 × 1028 dyn cm (Okal 1992), the great Colima-Jalisco earthquake of 1932 June 3 was one of the largest to strike Mexico since the dawn of instrumental seismology. Search for other works by this author on: Bulletin of the Seismological Society of America (1985) 75 (5): 1301–1313. 9 for preferred Model 22.4, featuring rupture in a weaker material. Even the ISS and GR′s locations (constrained to precisions no better than 0.1° and 1/4°, respectively) exhibit similar trends (33 km, N250°E and 55 km, N205°E, respectively). Those eight ‘major’ aftershocks are plotted with their confidence ellipses on Fig. 2002). A gap of about 60 km remains between the aftershock areas of the 1932 Jalisco and the 1973 Colima earthquakes whose seismic potential is unknown. 1932-06-03 10:36:56 UTC at 10:36 June 03, 1932 UTC Location: Epicenter at 19.786, -103.784 11.2 km from Las Primaveras [Invernadero] (7.2 miles) Michoacan, Mexico. 12(c), run-up at selected locations along the coastline obtained, on initially dry land, as the elevation above sea level of the point of maximum wave inundation. We show on Fig. In particular, we address the question of a Rivera-Cocos boundary.There have been several large historic earthquakes in the coastal areas of the Mexican states Colima and Jalisco, but the last large event was in June 1932 (the 1932 Jalisco earthquake, M s = 8.1). The US Geological Survey reported the earthquake's magnitude as 8.1, making it the biggest earthquake in Mexico since 1932 However, we emphasize the trend, common to all solutions, in the relative locations of Events III and I. Seismic records used in this study. The aftershocks locations, the first motions at MNZ, and the isoseismic maps of the two main shocks strongly suggest that: (a) the 3 June 1932 earthquake initiated NW of but close to MNZ and propagated NW for an estimated length of rupture of 220 km; (b) the 18 June 1932 earthquake nucleated SW of MNZ (offshore) and perhaps ruptured a length of about 60 km; … A third earthquake of 3.0 magnitude occurred in the area at 11:16 a.m. On March 27, four more quakes, including one measured at 3.7 magnitude, occurred in the same area. Epicenters and Locations of the Latest Quakes Near Santa Anita, Jalisco, Mexico 8.0 magnitude and above - Before 1932-06-03 10:36:56 UTC Earthquake … For each event, we use scaling laws (Geller 1976) to interpret the static values of the seismic moment M0 in terms of fault length L, fault width W and seismic slip Δu. Billy D. Yagi Y. A tsunami was reported which destroyed a … Note that Event III is systematically offset about 50 km to the SSW of Event I. 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