The statistics of large earthquakes commonly involve large uncertainties due to the lack of long-term, robust earthquake recordings. Small-scale seismic events are abundant and can be used to examine variations in fault structure and stress. We report on the connection between stress and microseismic event statistics prior to the possibly smallest earthquakes: those generated in the laboratory. We investigate variations in seismic b value of acoustic emission events during the stress buildup and release on laboratory-created fault zones. We show that b values mirror periodic stress changes that occur during series of stick-slip events, and are correlated with stress over many seismic cycles. Moreover, the amount of b value increase associated with slip events indicates the extent of the corresponding stress drop. Consequently, b value variations can be used to approximate the stress state on a fault: a possible tool for the advancement of time-dependent seismic hazard assessment.
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 Seismicity provides the most readily available information about crustal stress heterogeneity [Schorlemmer et al., 2005; Narteau et al., 2009] and stress orientations [Gephart and Forsyth, 1984; Michael, 1987]. Recent studies of natural and induced microseismicity [Schorlemmer et al., 2004a; Bachmann et al., 2012; Tormann et al., 2012] have drawn from laboratory insights [Scholz, 1968; Main et al., 1989; Meredith et al., 1990; Lockner et al., 1991; Lei et al., 2000; Amitrano, 2003] to interpret spatial b value (slope of the frequency-magnitude distribution) variations in terms of crustal stress changes. Increasing stresses in laboratory experiments on intact samples cause b values to drop prior to failure. This drop is observed for a range of rock types [e.g., Main et al., 1989; Thompson et al., 2006]. In the Earth's continental crust, low b value anomalies have been widely observed, e.g., in California [Wiemer and Wyss, 1997; Wyss et al., 2000; Wyss, 2001] and also for induced microseismicity with magnitudes down to M=−4.4 [Kwiatek et al., 2010]. Regions of low b value can be connected to fault-structural heterogeneity and local stress concentrations which cause seismic events to grow to relatively larger sizes once they start to nucleate [Goebel and Becker, 2012].
 While spatial variation in b value have already been used to formulate forecasts for large earthquakes (M≥5.0) in a time-independent sense [Schorlemmer et al., 2004b; Wiemer and Schorlemmer, 2007; Gulia et al., 2010], temporal variations in b are more controversial, partially due to a lack of long-term, homogeneous earthquake recordings. A recent study suggested that there is no statistically significant predictive power in temporal variations of b values, at least for predictions of earthquakes with M=4.0–6.2 [Parsons, 2007]. Others, however, view decreasing b values as a possible precursor for the occurrence of large earthquakes (i.e., events with ) [Wyss, 1990; Imoto, 1991; Nanjo et al., 2012]. Part of the current controversy is due to a posteriori observations about phenomena preceding individual seismic events that would not withstand rigorous, statistical testing. Such observations are likely biased because of the intentional search for anomalies. Furthermore, the interpretation of b value variations in nature is nonunique due to the intrinsic complexity of the faulting process and the lack of supportive observations, e.g., of stress variations in borehole measurements. This emphasizes the importance of a detailed understanding of the mechanisms behind bvalue variations.
 Within the framework of our experiments, we are able to overcome some of these obstacles. We examine physical conditions that cause b values to decrease during several seismic cycles on laboratory faults, which cannot readily be done in nature. Despite the inherent difference in scale between laboratory and natural seismicity, several similarities have been highlighted by recent studies. In particular, sample-scale faults in the laboratory show structural similarities to upper crustal faults [Amitrano and Schmittbuhl, 2002], and the statistics of laboratory acoustic emission (AE) events exhibit patterns similar to natural seismicity [Goebel et al., 2012].
 High-frequency AE events in laboratory tests are associated with the formation of and slip on microcracks. This type of microseismic event activity can be associated with distinct pre-failure stages during loading of intact samples [Lockner et al., 1991; Lei et al., 2000]. The macroscopic failure of intact samples is generally preceded by abruptly increasing AE rates, increasing microseismic moment release, and decreasing Gutenberg-Richter b values [Main et al., 1989; Meredith et al., 1990; Sammonds et al., 1992; Liakopoulou-Morris et al., 1994]. A possible explanation for the connection between b and stress is the extension of preexisting microcrack populations by stress corrosion and crack coalescence leading up to the failure of intact samples [Main et al., 1992].
 Previous laboratory experiments predominantly focused on macroscopic failure of intact samples or stick-slip motion of planar interfaces. We expand on these experiments through creating structurally complex fault systems starting from incipient fracture surfaces and by documenting variations in stress and AE statistics during series of stick-slip events.
2 Experimental Setup, Methods, and AE Data
 In the following, we describe loading conditions and sample geometry which were chosen to represent natural faulting conditions as closely as possible. We report on four triaxial experiments (W4, W5, W7, and W8), conducted on cylindrical (radius = 2 cm, height = 10.7 cm) specimens at constant loading rates at GFZ-Potsdam, Germany. All experiments were performed on oven-dried samples at room temperatures, with constant confining pressures (Pc=150 MPa). We introduced 1.5–2.5 cm deep saw cut notches at a 30° angle to the loading axis to localize faulting at the center of the specimens during initial fracture and subsequent stick-slip sliding. The results presented here are from the stick-slip sliding stage of previously fractured specimens. Our initial condition, i.e., an incipient fracture surface that develops into a fault zone, can be seen as an analog for the structural complexity of natural fault zones. To monitor microcrack formation and sample deformation, strain gauges and AE sensors were glued to the specimen surface (Figure S1, left, in the supporting information). We employed a high-speed (10 MHz sampling frequency) and accuracy (16 bits amplitude resolution) AE system, enabling the documentation of micromechanical processes that occurred in temporal proximity to slip instabilities. AE events were recorded using a miniature seismic array, consisting of 16 one-component, piezoelectric transducers. The location uncertainty of AE hypocenters was estimated at 1–4 mm, depending on the proximity of the event to the edge of the array. The total number of successfully located AEs from each sample was between 34,141 and 97,847, which allowed robust measurements of b value as a function of time. Variations in b value were determined using a moving time window that contained an equal number of AE events. This optimized the temporal resolution of b value computations while ensuring the same statistical significance of each value. We also scrutinized the effects of different sample sizes and sampling techniques on b value trends to ensure reliability and consistency (see supporting information).
 If b value is indeed an indicator of stress [Schorlemmer et al., 2005], we expect to observe a systematic relation between b and stress for stick-slip cycles on a fault during our experiments. Figure 1 shows results from experiment W5, which are typical of all experiments. The differential stress shows a characteristic sawtooth pattern pattern of gradual increase followed by an abrupt decrease during slip. At the same time, b values decrease with increasing stresses and abruptly increase when the stresses drop during a slip event. The stress curve shows six slip events with large stress drops (LSDs), some of which were preceded by small stress-drop (SSD) events. The loading curve preceding the first three LSD events exhibits many SSDs. The b value curves also show more fluctuations during these early cycles. Fluctuations in b are strongest during the first stick-slip cycle and decrease with successive LSDs so that the last three stick periods show a smoother, monotonic decrease. This evolution may be related to progressive fault smoothing, which is also indicated by decreasing residual stresses with successive LSD events.
 Figure 2 shows b as a function of normalized stress (fraction of maximum stress) for the six LSD events in experiment W5. The relationship between b and stress is approximately linear for high differential stresses above ≈55% of the peak stress. Below this value, only few AE events were observed and b values tend to show more scatter. This scatter is likely related to AEs that occurred due to the reduction of pore space at the initial stage of a loading cycle.
 The three other experiments confirmed the relationship between b value and stress (Figure S5). This relationship was most pronounced for experiment W8 whereas experiment W4 showed the smallest change in b value with larger applied stresses and the scatter in b value was comparably large. The scatter at elevated stresses in Figure 2 and during the other experiments may be related to larger fluctuations in b associated with geometric complexity especially before the initial LSD events of an experiment.
 We also investigated if b values carry additional information during high-stress regimes, for example, about the amount of stress release connected to SSD or LSD events. We estimated the stress-drop-related increases in b value from the difference between minimum before and maximum b value after a stress-drop event. The SSD events produced relatively smaller increases in b while LSD events caused a larger upward jump in b values (Figure 3). On average, the b value jumps are higher for larger stress drops and exhibit a positive correlation with a Pearson's correlation coefficient of r=0.64 for a sample size of NAE=600. We explored this correlation over a range of sample sizes (r=0.53 for NAE=300, r=0.57 for NAE=1200, and r=0.57 for NAE=3000) confirming the connection between b increases and stress drops. Furthermore, we tested if this relation is also observed for shear stress drops which were computed for the effective fracture surface area, corrected for slip after each successive slip event [Scott et al., 1994; Tembe et al., 2010]. The linear regression between slip-corrected shear stress drop and b value increase was characterized by a correlation of r=0.65 which was significant at a 99% level. Thus, the amount of increase in b after slip appears to be related to the stress release due to slip.
 Assuming that the number of SSD events can serve as a proxy for the degree of structurally related complexity, we performed a systematic analysis of the connection between geometric complexity and bvalue variations. Stick-slip events that were preceded by fewer SSDs showed higher linear correlation coefficients between b and stress (Figure S8), consistent with the hypothesis that b value-stress relations are more pronounced for structurally less complex faults. Additionally, the times of b value minima were closer to the LSD for stick-slips with fewer SSDs (Figure S7). The bvalue-stress relations depended also on the lengths of the laboratory faults, i.e., they were less linear for longer faults (Figure S5). This is consistent with our observation that longer fracture surfaces showed more structural complexity in post-experimental X-ray computer tomography scans (Figures 1b and 1c), and structural complexity can obscure b value-stress relations.
 To investigate the importance of observational scales on the b-stress relation, we compared results from a LSD with a SSD event as well as with the failure of an intact sample (Figure 4). For the LSD and SSD event, we limited our observations to one dominant asperity region within the laboratory-created fault zone, identified through areas of low b value, high seismic moment, and large AE density gradients [Goebel et al., 2012]. The temporal variations of b values based solely on AEs within asperity regions in Figure 4 show a clear monotonic decrease with increasing stresses before both SSD and LSD event, similar to the fracture of the intact sample, but on a different time scale. The previously observed variations in b on short time scales before the LSD events, which seemed to be connected to SSD events (see Figure 1), have largely disappeared, presumably because the SSD events occurred outside the asperity area under study. The similarity in the temporal evolution of b value before an initial fracture and the fracture of a single asperity suggests that the underlying micromechanical processes are similar. The additional complexity observed during slip on a rough fault plane is probably due to fault-structural heterogeneity.
4 Discussion and Conclusion
 It is commonly assumed that b values are stable in time and only reflect spatial variations in stress [Wiemer and Wyss, 1997; Westerhaus et al., 2002; Schorlemmer and Wiemer, 2005; Parsons, 2007]. We observed that b values vary significantly within a seismic cycle in stick-slip experiments and that the amount of increase in b after a slip event is related to the stress drop (or the equivalent residual stress state on the fault after slip). This is consistent with a recent study of changes in b value following the 1989 M6.9 Loma Prieta and the 2004 M6.0 Parkfield event which suggested that a rapid return of bvalues to pre-failure levels indicates that the local stress field has not been reset and stresses quickly return to pre-failure levels [Tormann et al., 2012]. Our results suggest that the magnitude of increase in b value after failure can be associated with the effectiveness of a large earthquake to release stored shear stress on a fault. Relatively small amounts of stress release during a seismic event could possibly be caused by large structural heterogeneity within a fault zone.
 The observed connection between decreasing b values and increasing differential stresses substantiates previous findings of a b value-stress dependence [Scholz, 1968; Amitrano, 2003; Schorlemmer et al., 2005]. Our results are also in agreement with a stochastic model that explores variations of the Gutenberg-Richter relationship in the context of an inhomogeneous medium [Scholz, 1968]. This model predicts that b value is inversely related to the applied stress so that seismic events have a higher probability to grow to larger sizes if the stress level in the medium is high. Consequently, we also expect that an increase in the stress level on the fault, for example, by changing the fault angle or increasing the confining pressure would lead to a general decrease in b value. The role of increasing confining pressures in reducing b values has been shown during fracture and successive frictional sliding of granite samples [Amitrano, 2003].
 Our results provide an explanation for the observed decrease in b value in the source regions prior to large earthquakes [Nanjo et al., 2012]. We suggest that the underlying physical processes governing b value variations affect b values on different time scales and over different fault volumes. Disregarding the importance of temporal and spatial scales may lead to a loss of physically driven b value variations. bvalues are more strongly correlated with stress for faults with less structural complexity and stick-slip sequences with simple, monotonic stress curves, i.e., without SSD events. This suggest that bvalue-stress relations depend on fault complexity and are more strongly connected for smoother fault surfaces.
 Natural faults are likely to contain additional complexity that cannot readily be explored within the framework of the current set of experiments. Our results suggest that this complexity could partially be reduced by choosing an adequate subscale of a fault volume for the analysis of temporal b value variations, providing a possible means to explore the relative stress state of a fault segment and its position within the seismic cycle. Furthermore, a detailed understanding of temporal b value variations is important for intermediate and long-term earthquake forecasting efforts, especially time-dependent forecast models for hazard assessment.
 We thank Stefan Gehrmann and Matthias Kreplin for rock sample preparation at GFZ-Potsdam, Germany. We thank R. Shcherbakov and an anonymous reviewer for comments that helped improve the manuscript. This research was supported in part by the Southern Californian Earthquake Center under contribution 11017 and 13022.
 The Editor thanks Robert Shcherbakov and an anonymous reviewer for their assistance in evaluating this paper.