2002). This estimate is half the 280 km proposed by Singh et al. However, we emphasize the trend, common to all solutions, in the relative locations of Events III and I. Frohlich C. Kisslinger C. Espíndola J.M. In 1932, Mexico was hit by the Jalisco earthquake with a magnitude of 8.1. Also a comparison of seismograms of 1932 and 1995 earthquakes show great differences. On their Fig. 7 shows that the simulated tsunami amplitude falls to 1.5 m in Manzanillo, substantially lower than observed. This content is PDF only. 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. The resulting values of T (-6.37 and -6.43, respectively) are typical of recent tsunami earthquakes (e.g. 6 for Event III (Model 22.1). The paper was significantly improved by the comments of two anonymous reviewers. We relocated systematically the main shock and all 28 apparent aftershocks occurring in 1932, using the data listed by the International Seismological Summary (ISS) and the interactive iterative method of Wysession et al. Singh S.K. 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. Seismic records used in this study. 1981; Wang et al. These events have relatively small confidence ellipses and as such help provide an estimate of the dimension of rupture. 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. For full access to this pdf, sign in to an existing account, or purchase an annual subscription. SE-50, U.S. Dept. Kanamori H. 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). Relocation based on published arrival times … Tsunamis in Mexico In a total of 24 tidal waves classified as a tsunami since 1732 a total of 91 people died in Mexico. All this evidence strongly suggests that Event III occurred about 50 km seawards of the main shock, in a geometry which would be compatible with rupturing either at the very top of the interplate contact, or along a splay fault located in an accretionary wedge inside the North American Plate. It seems that the 1995 event is not a repeat of either June 3 or June 18, 1932 earthquakes. 8.1 magnitude earthquake. For each event, the estimated energy EE is plotted against the seismic moment M0 in logarithmic units. Borrero J.C. Near-field hydrodynamic simulations show that the effects of the main shock′s tsunami are well modelled by a standard seismic source, whereas the stronger tsunami from Event III can be modelled by rupture along a splay fault in a mechanically deficient material. Summary of energy-to-moment ratios for a data set of large recent earthquakes (adapted from Newman & Okal 1998; López & Okal 2006; Okal et al. We note that these authors did not carry out a full relocation based on worldwide travel times but rather used a limited number of differential times, such as S-P at regional distances. These authors used Richter′s (1958) algorithm based on the variation of P-wave residuals with azimuth to derive their own relocation, shown as the square on Fig. 1). S. K. Singh, L. Ponce, S. P. Nishenko; The great Jalisco, Mexico, earthquakes of 1932: Subduction of the Rivera plate. Moore C. Newman A.V. Despite a slightly different mechanism that does not require rupturing on a splay fault (Newman et al. This approximation, classical in tsunami modelling, is justified by the fact that any seismic rupture, including a slow one characteristic of a ‘tsunami earthquake’, remains hypersonic with respect to the propagation velocities of tsunamis (Okal & Synolakis 2003). 8), once again in agreement with the reported values (Sánchez & Farreras 1993). 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) suggested the existence of a Colima seismic gap, which was filled during the later Tecoman earthquake of 2003 January 22 (Yagi et al. In this respect, it is most reminiscent of the sequences of 1963 October and 1973-1975, both in the Kuril Islands. The scale of the palette is common with Fig. The significant difference in wave height and run-up between Models 22.2, 22.3 and 22.4 constitutes a numerical illustration of Okal′s (1988) theoretical results, showing that rupture in a ‘sedimentary’ layer, that is, a structure with deficient rigidity, enhances the excitation of tsunamis relative to seismic surface waves, especially for a 45°-thrust geometry, thereby explaining the properties of ‘tsunami earthquakes’ under Fukao′s (1979) model. Then, in Model 22.4, we keep the focal mechanism of the splay fault in Model 22.2, but release it in a sedimentary material featuring a deficient rigidity. The largest observed earthquake in the region was a magnitude 8.6 in Oaxaca in 1787. Large-scale induced polarization imaging, The interaction between mantle plumes and lithosphere and its surface expressions: 3-D numerical modelling, Middle–Late Permian magnetostratigraphy and the onset of the Illawarra Reversals in the northeastern Parana Basin, South America, Double-difference seismic attenuation tomography method and its application to The Geysers geothermal field, California, PRISM3D – A three-dimensional reference seismic model for Iberia and adjacent areas, Volume 225, Issue 1, April 2021 (In Progress), Volume 224, Issue 3, March 2021 (In Progress), Geomagnetism, Rock Magnetism and Palaeomagnetism, Marine Geosciences and Applied Geophysics, 2 Historical reports and previous studies, https://doi.org/10.1111/j.1365-246X.2011.05199.x, Receive exclusive offers and updates from Oxford Academic, Copyright © 2021 The Royal Astronomical Society. Engdahl E.R. Pranantyo I.R. The strongest tidal wave registered in Mexico so far reached a height of 10.90 meters. Fig. Please click on the PDF icon to access. This model would predict a smaller, rather than larger, tsunami than for Event I. 9 shows that the wave heights remain moderate, not exceeding 2.5-3 m in the area of Manzanillo and Cuyutlán. The simulation uses the Method of Splitting Tsunamis (MOST) code (Titov & Synolakis 1998) that solves the full non-linear equations of hydrodynamics under the shallow-water approximation by finite differences and through the method of alternate steps (Godunov 1959). 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). The 1932 Mexican sequence constitutes a classical example of a regular main shock triggering, within a few weeks’ time, a slow ‘tsunami earthquake’. 6 for Model 22.3, featuring a deficient rigidity along a gently dipping fault plane. (1984). Silver E.A. 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. 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. 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. Bulletin of the Seismological Society of America ; 75 (5): 1301–1313. Note significantly lower wave heights. (a) Field of vertical displacement of the ocean floor, computed using Mansinha & Smylie′s (1971) algorithm. In Fukao′s (1979) model, they occur on a splay fault developing above the interplate contact into a sedimentary wedge offering inferior mechanical properties and hence a reduced velocity of propagation of the seismic rupture. Fig. More recently, the 2006 Java and 2010 Mentawai earthquakes, both in Indonesia, have qualified as ‘tsunami earthquakes’; the latter could be regarded as an aftershock of the 2007 Bengkulu earthquake. 11, the maximum run-up increases to 4 m in Manzanillo and 4.5 m in Cuyutlán but remains smaller than reported (note that the color palette used on Figs 11 and 12 differs from that of Figs 6-10). Based on the long-period seismic moments derived in this study, our hydrodynamic simulations reproduce the main characteristic of the tsunamis as reported in historical chronicles: a run-up of about 3 m concentrated in the bay of Manzanillo during Event I, a much more benign tsunami during Event II and a catastrophic inundation after Event III with run-ups reaching 7 m; the latter is explained by setting the rupture on a splay fault in weaker, presumably sedimentary, material in the wedge of the subduction system under the exact scenario proposed by Fukao (1979) in the Kuril Islands. Its run-up was reported to have reached 10 m (Sánchez & Farreras 1993), making it clearly larger than that of the main shock and thus qualifying Event III as a ‘tsunami earthquake’. 6(a) and a close-up of the wave heights in Manzanillo and its vicinity on Fig. (c) Run-up along coastline, plotted as a function of longitude. Historical earthquake in Mexico. Same as Fig. (2008) after the 2007 Solomon Islands earthquake. 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. The second earthquake caused as few as 3 or as many as 52 deaths. Rupture across arc segment and plate boundaries in the 1 April 2007 Solomons earthquake, Seismic strain release along the Middle America Trench, Mexico, Intraplate seismicity of the Pacific Basin, 1913-1988, Source rupture process of the Tecoman, Colima, Mexico earthquake of January 22, 2003, determined by joint inversion of teleseismic body wave and near source data, © The Authors Geophysical Journal International © 2011 RAS, Induced polarization of volcanic rocks. 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… The 1932 events are shown as the squares (Events I and II, regular T) and the triangle (Event III, deficient T; ‘tsunami earthquake’). The latter is our Event 23 (1932 August 24; b in Table 1), which clearly occurred farther south and east with a moderate-sized confidence ellipse, not reaching the coastline. She uses her Christian name ‘Carmen’ and her husband’s surname as an ironic po… With an estimated magnitude of 7.6 on the surface wave magnitude scale, a maximum felt intensity of X on the Mercalli intensity scale, the quake destroyed 1,167 houses and caused 275 deaths and 320 injuries.The earthquake was located close to the northern margin of the Tibetan Plateau; this … 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. Notwithstanding this reservation, Fig. In the first model tested for the main shock, labelled 03.1, we derive a centroid of the rupture by assuming that our relocated epicentral location corresponds to the initiation of the rupture at the deepest boundary of the faulting area. 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’. Taylor F.W. 1993). 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. 2004). In particular, the catastrophic Event III tsunami can be modelled using the seismically anomalous source derived in Section 4, without the need to invoke a different mechanism such as an underwater landslide. The diagonal lines feature constant T, the solid one being the theoretical value (-4.90) expected from scaling laws. For each event, our relocated epicentre is shown as the large star (surrounded by its Monte Carlo confidence ellipse), the ISS location as the inverted triangle, GR′s estimate as the upward triangle, EV′s relocation as the circle and in the case of Event I, Eissler & McNally′s (1984) estimate as the square. Another mechanism for the generation of exceptionally large tsunamis after earthquakes is the triggering of submarine landslides. We find an average value Mc= 8.19 ± 0.36 for Event I, corresponding to M0= 1.55 × 1028 dyn cm, in excellent agreement with our one-station estimate (Okal 1992). Reyes G. Oxford University Press is a department of the University of Oxford. Event III is a typical ‘tsunami earthquake’, with a slowness parameter Θ =-6.18, more than one logarithmic unit less than predicted by scaling laws. 3 regroups our results for all three events. 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. 11, but differs from Figs 6-10. along the Pacific coast of Mexico is the plate boundary between the Rivera-Cocos plates and the North America plate (Figure 1). Unlike seismic intensity, which measures the strength of shaking and varies according to distance from the quake and other factors, the magnitude is intended to measure the intrinsic size of an earthquake. Wei Y. Singh et al. Compared to other countries, Tsunamis therefore occur more often than average, but still moderate. The resulting displacement field is shown on Fig. MOST has been extensively validated through comparisons with laboratory and field data, per standard international protocols; full details can be found in Synolakis (2003). 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. The central dashed line and shaded area are the average value and 2s confidence interval, respectively. Also, Fig. The 1932 Changma earthquake occurred at 10:04:27 local time on 25 December. 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. None of the relocations could resolve hypocentral depth. A study by Mexico's National Seismological Service says that quake is believed to have killed about 400 people, causing severe damage around the port of Manzanillo. Detail showing Kahlo’s self-portrait Frida Kahlo was as talented at self-projection as she was at introspection. The detailed contributions of these previous studies will be described in the relevant sections later. The US Geological Survey reported the earthquake's magnitude as 8.1, making it the biggest earthquake in Mexico since 1932 In short, this model simulates a tsunami smaller than that of Event I and thus, fails to account for the much larger wave heights observed. Kanamori′s (1972) original paper was based on two events: the 1896 Sanriku earthquake and the 1946 Aleutian one. Obviously and unfortunately, the time delay in question would also be the most valuable parameter from a societal standpoint. The quake that struck Mexico overnight matches the force of a magnitude 8.1 quake that hit the country on June 3, 1932, roughly 300 miles (500 kilometers) west of Mexico City. 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… In the case of most aftershocks, we used a constrained depth of 25 km, as suggested in the scenario of a large interplate thrust event. 2. Depth: 15 km We conclude that Fukao′s (1979) model involving rupture along a splay fault satisfactorily explains the available data. This procedure is necessary to allow a run-up computation simulating the interaction with the coastline. Our results show maximum amplitudes on the order of 3.5 m in the bay of MNZ, in general agreement with the descriptions compiled by Sánchez & Farreras (1993), and lesser values in Cuyutlán. Jennings P.C. According to Mexico’s National Seismological Service, three of those happened within a nerve-wracking nine-month span in 1902-1903. Previous studies of the 1932 earthquakes (Espíndola et al. 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. Synolakis C.E. We show on Fig. In summary, Model 03.1 best describes the effects of the tsunami on Manzanillo and its vicinity. 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'. Estimated casualties: 600. EPA-EFE/JORGE NUÑEZ Emergency Services workers inspect the debris of a … 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. Kahlo positions herself atop a stone which straddles the border. 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. Rodríguez M. Synolakis C.E. The quake that struck Mexico overnight matches the force of a magnitude 8.1 quake that hit the country on June 3, 1932, roughly 300 miles (500 kilometers) west of Mexico City. Villaseñor A. Note that Event III is systematically offset about 50 km to the SSW of Event I. This scenario, which requires a sedimentary input into the subduction zone, could apply to the 2010 Mentawai aftershock of the 2007 Bengkulu earthquake (Newman et al. There is a slight growth of moment with period due to the effect of source finiteness at higher frequencies (Ben-Menahem 1961) with an average value of 2.4 × 1028 dyn cm beyond 150 σ that we propose as the static value of M0 for Event I. 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). Hayes G. Note that the fault length is in good agreement with the extent of the well-located aftershocks plotted on Fig. This site uses cookies. It resulted in considerable destruction in the city of Manzanillo and generated a locally damaging tsunami. It generated a tsunami featuring a leading depression followed by an inundation with run-up reaching 3 m. Event I was assigned a magnitude MPAS= 8.1 by Gutenberg & Richter (1954, hereafter GR). 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. 1 also shows our relocation of Event II, at 19.58°N, 103.84°W, as well as the other estimates for this source. Fig. 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. Estimated magnitude: 7.8-8.4. Okal E.A. This scenario would apply in Nicaragua and Java (Polet & Kanamori 2000). 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). Simulation of Event I′s tsunami under Model 03.1. Please check your email address / username and password and try again. of Commerce, Tsunami field survey of the 1992 Nicaragua earthquake, The great Jalisco, Mexico, earthquakes of 1932: subduction of the Rivera plate, Ultra-long period seismic study of the December 2004 Indian Ocean earthquake and implications for regional tectonics and the subduction process, The slump origin of the 1998 Papua New Guinea tsunami, An algorithm for automated tsunami warning in French Polynesia, based on mantle magnitudes, Fault parameters of the 1896 Sanriku tsunami earthquake estimated from tsunami numerical modeling. (1928). Sweet S. The similarity between the Kuril and Mexican sequences also extends to the moment ratios between the main shock and the ‘tsunami earthquake’, whose values (6.3 in 1932, 12.5 in 1963 and 7.5 in 1973-1975) are generally comparable. Finally, Engdahl & Villaseñor (2002; hereafter EV) relocated the event as part of their Centennial Catalogue, their solution shown on Fig. The most interesting results are, of course, those for Event III for which, to our best knowledge, no prior computation of seismic moment was reported in the literature. 2011). 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. (b) Field of maximum wave heights during a 2-hr time window after origin time. 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. Although its location on the interplate contact would be generally similar to that of the 2010 Mentawai, Sumatra ‘tsunami earthquake’ (Newman et al. Introduction The great Colima-Jalisco, Mexico earthquake … 6(b). Following the work of Newman & Okal (1998), itself based on Boatwright & Choy (1986), we seek to obtain slowness parameters Θ = log10(EE/M0) for Events I, II and III. Suwargadi B. 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. (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. Kanamori H. (1991), which includes a Monte Carlo algorithm injecting Gaussian noise into the data set. Heights reach 7 m ( Fig, Brian Mitchell and Bernard Dost for to. 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Of recent tsunami earthquakes ’ as their sources do not exhibit seismically anomalous behaviour featuring. ≥ 6 by GR remain unknown ) are typical of recent tsunami earthquakes.... The three events, clearly exposing Event III′s deficiency in high frequencies the average and... Shows a marginal increase in wave heights in Manzanillo and adjoining areas with upwards of 400 casualties sections.... Have relatively small confidence ellipses on Fig of submarine landslides most reminiscent of the floor... Conclude that Fukao′s ( 1979 ) model involving rupture along a splay fault satisfactorily explains the data! M0 in logarithmic units by the comments of two anonymous reviewers account, or purchase an annual..