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• W1863242008 abstract "GEOPHYSICAL RESEARCH LETTERS, VOL. 34, L16309, doi:10.1029/2007GL030917, 2007 Creep events slip less than ordinary earthquakes Emily E. Brodsky 1 and James Mori 2 Received 8 June 2007; revised 9 July 2007; accepted 24 July 2007; published 24 August 2007. [ 1 ] We find that slow seismic events have smaller fault slips compared to ordinary earthquakes with similar dimensions. For ordinary earthquakes, the ratio of slip to fault length is largely consistent, yet the physical controls on this ratio are unknown. Recently discovered slow slip or creep events in which faults move quasi-statically over periods of days to years shed new light on this old conundrum. For example, large slow events that extend over 100 km have slips of centimeters, while ordinary earthquakes that rupture a comparable length of fault typically slip meters. The small slips of quasi-static events compared to the large slips of earthquakes show that dynamic processes significantly control the rupture growth of ordinary earthquakes. We propose a model where slip on a heterogeneous fault accounts for the difference. Inertial overshoot may result in larger final slips for earthquakes than comparable creep events. Citation: Brodsky, E. E., and J. Mori (2007), Creep events slip less than ordinary earthquakes, Geophys. Res. Lett., 34, L16309, doi:10.1029/2007GL030917. 1. Introduction and Observations [ 2 ] Average slip and rupture length are two of the most fundamental quantities defining the size of an earthquake. Somewhat mysteriously, their ratio has long been observed to be largely independent of size for a wide variety of earthquakes [Kanamori and Anderson, 1975; Scholz, 1990; Abercrombie, 1995]. Any situation in which the slip-rupture length ratio varies systematically would provide a window into a major feature of earthquake rupture. [ 3 ] Slow slip events open up just such a window. We use the terms ‘‘slow’’ or ‘‘creep’’ for events that have durations of days to years. Creep events have been recently shown to be a major feature of tectonic systems [e.g., Fujii, 1993; Linde et al., 1996; Hirose et al., 1999; Dragert et al., 2001; Kostoglodov et al., 2003; Ozawa et al., 2005; Ohta et al., 2006; Wallace and Beavan, 2006]. Enough data now exists that we can meaningfully contrast the creep events with ordinary earthquakes. [ 4 ] The ratio of slip to rupture length is often parameter- ized with the static stress drop Ds s . In order to make a convenient comparison between events of varying geome- tries, we use the approximate relationship Ds s ¼ mD=L where m is the shear modulus, D is the average slip and L is the square root of the rupture area. Equation 1 is Department of Earth and Planetary Sciences, University of California Santa Cruz, Santa Cruz, California, USA. Disaster Prevention Research Institute, Kyoto University, Kyoto, Japan. Copyright 2007 by the American Geophysical Union. 0094-8276/07/2007GL030917 appropriate for studying relative values of the average properties over the slip surface. It should not be strictly interpreted as stress for a particular geometry, however, it captures the dependence of static stress changes on two key physical variables. [ 5 ] Figure 1 shows a comparison of the static stress drops of ordinary earthquakes and the longer duration slow events. For earthquakes, we use representative datasets to illustrate typical behavior with the usual range of stress drops of 0.1– 10 MPa. 1 For the slow events, stress drops were calculated from equation 1 using the determinations of rupture area and average slip in the papers cited in the caption of Figure 1. The slow events include episodic slab creep and transient San Andreas fault creep. [ 6 ] Nine out of the ten well-recorded slow events have static stress drops <0.2 MPa while the mean of the earth- quake static stress drops is 2 MPa. The only slow event in the range of regular earthquakes is the 1998 Guerrero event that appeared to slip 1.4 m with L = 57 km, based on a single-station observation. A multiple station observation of another slow event in the same region in 2001 – 2002 yielded an average of 10 cm slip with L = 275 km [Kostoglodov et al., 2003]. [ 7 ] Earthquakes that generate seismic waves, but rupture more slowly than normal, are called tsunami earthquakes because of their ability to perturb the water column through large seafloor offsets despite relatively low levels of high frequency radiation [Polet and Kanamori, 2000]. The tsunami earthquakes cluster at stress drops near those of ordinary earthquake stress drops, and generally at the low end of the range. The special case of shallow very low frequency earthquakes (VLF) in accretionary wedges seems to be the only group of earthquakes with stress drops substantially below those of the creep events [Ito and Obara, 2006]. [ 8 ] The data from the ordinary earthquakes is primarily seismic, while that for the slow slips is primarily geodetic. However, entirely geodetic inversions of moderate seismic events agree with the typical range of earthquake average slips reflected in Figure 1 [Hurst et al., 2000]. In summary, earthquakes that rupture a 100 km fault slip an average of a few meters whereas slow creep events with the same rupture length slip an average of several centimeters. This relationship poses an additional constraint for otherwise successful models of creep events [Liu and Rice, 2005]. 2. Possible Mechanisms Based on Previous Work [ 9 ] The order of magnitude difference in stress drops of slow events and ordinary earthquakes may clarify the role of inertia or rapid slip in determining the final slip in Auxiliary materials are available in the HTML. doi:10.1029/ 2007GL030917. L16309 1 of 5" @default.
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