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ORIGINAL RESEARCH article

Front. Earth Sci., 21 April 2021 | https://doi.org/10.3389/feart.2021.657487

Acoustic Emission Reveals Multiple Slip Modes on a Frictional Fault

Alexey Ostapchuk1,2*, Kseniya Morozova1, Vadim Markov1, Dmitry Pavlov1 and Maxim Popov1,3
  • 1Sadovsky Institute for Dynamics of Geospheres, Russian Academy of Sciences, Moscow, Russia
  • 2Department of Theoretical and Experimental Physics of Geosystems, Moscow Institute of Physics and Technology, Dolgoprudny, Russia
  • 3Department of Robotic Systems and Mechatronics, Bauman Moscow State Technical University, Moscow, Russia

The spectrum of fault slip modes spans a continuum from fast ruptures to slow slip events. The nucleation of a certain slip mode is governed by the frictional heterogeneity of fault interface and the rheological fault stiffness. There is a mounting evidence that a single fault can host multiple slip modes. In laboratory experiments we study acoustic emission (AE) initiated by a sliding frictional fault and focus our attention on gouge-filled faults hosting multiple slip modes. Deformation experiments were performed on a slider model setup with a precise control of mechanical parameters and monitoring the acoustic signal in the frequency range of 20–80 kHz. We have shown that the cumulative AE energy linearly depends on block displacement. Besides that, there is a high inverse correlation (-0.94) between fault friction and b-value of frequency-amplitude distribution of AE in the performed experiments. Provided that velocity weakening is specific for the fault interface, the self-organization of a gouge-filled fault at the micro scale is the key parameter that controls the frictional behavior of fault hosting multiple slip modes. Resting on a quantitative categorization of AE waveforms, two AE subpopulations have been distinguished. One of them manifests as AEs with harsh onsets. The second one exhibits a gradual amplitude rise and tremor-like waveforms. A longer duration of the intergrain rupture is specific for the second AE subpopulation. During a laboratory seismic cycle, the first AE subpopulation retains parameters, while the second one exhibits a pronounced cyclic recurrence of b-value. The b-value of the second subpopulation gradually decreases before slip events and recovers after them. Two AE subpopulations, probably, point to the coexistence of two dynamic subsystems. The revealed precursory changes of AE subpopulations are common for the entire spectrum of slip modes. We speculate on the unity of underlying mechanisms of different slip modes.

Introduction

The blocky hierarchical structure of the Earth’s crust determines its movability and localization of deformations in interblock zones. Faults and large fractures control regularities of accumulation and relaxation of the energy of elastic deformation in a blocky massif (Scholz, 2002; Kocharyan, 2016). The dynamics of relaxation processes that are accompanied by slips along faults is determined by the ratio of the rheological stiffness of the fault to the one of the enclosing massif (Leeman et al., 2016; Kocharyan et al., 2017a). Fault slip modes observed in nature span a continuum, given the heterogeneity and complexity of natural systems (Peng and Gomberg, 2010; Burgmann, 2018). Different faults may exhibit just fast slip modes (ordinary earthquakes), or just slow slip modes (slow or low-frequency earthquakes, slow slip events), or even both fast and slow modes together (Frank et al., 2016; Veedu and Barbor, 2016; Ostapchuk et al., 2020).

The frictional instability is the most probable mechanism of ordinary and slow earthquakes (Scholz, 2002; Nielsen, 2017). During fault evolution, earthquakes are initiated when shear stresses reach the ultimate strength at a local fault segment. In the vicinity of the ultimate strength the source stays in a metastable state, so that even a slight fluctuation of stress may lead to a loss of dynamic stability. The existing models of seismic activity, describing a certain fault or a source zone, suggest that earthquake nucleation area is an integrated dynamic system which has a specific property of self-organizing criticality (Kuksenko et al., 1996; Turcotte, 1999; de Arcangelis et al., 2016). At the initial stage damage accumulates at the micro-scale. Cracks are uncorrelated and occur randomly. Further evolution of the system lifts the destruction processes to a higher hierarchical level, thus, as the stresses approach the critical value, structural changes spread wider all over the system. Systems spontaneously evolve toward critical states described by power laws in the event size distribution. A loss of dynamic stability manifests at the macro-scale as a slip event. The more accurate the earthquake detection technique is, the more distinct is the pattern of large earthquake nucleation (Trugman and Ross, 2019).

The transition of a fault to a metastable state is accompanied by a decrease of the shear stiffness of source zone (Johnson and Jia, 2005; Kocharyan and Ostapchuk, 2011). At present measuring tectonic stress and fault stiffness “in situ” is a complex problem. There are several indirect ways to estimate the state of stresses near faults (Rebetsky et al., 2016; Brodsky et al., 2020) and to trace fault behavior up to earthquake nucleation (Frank et al., 2016; Trugman and Ross, 2019). Applying the AE technique to monitoring fault dynamics assumes correlation between the AE activity and the stress-strain state of the fault (Dixon et al., 2018; Bolton et al., 2020).

The laboratory experiment is a reliable tool to verify hypotheses/assumptions or to put forward new ones (Marone, 1998; Rosenau et al., 2017). AE experiments reproduce qualitatively the main statistical laws that describe natural seismicity (Gutenberg-Richter law, Omori law, inverse Omori law) (Lei, 2003; Johnson et al., 2013; Lherminier et al., 2019; Ostapchuk et al., 2019). Nucleation of slip events in laboratory is accompanied by variations of scaling properties of AEs (Goebel et al., 2013; Riviere et al., 2018), alterations of elastic/seismic wave properties (Hedayat et al., 2014; Shreedharan et al., 2021) and seismic quiescence (Ostapchuk et al., 2016). The similarity of recurrent fast and slow earthquakes has already been demonstrated (Hulbert et al., 2019). However, a limitation of AE analysis is that results often depend on reliable detection of acoustic pulses in the background noise. This work is devoted to investigation of the AE accompanying evolution of a simulated gouge-filled fault hosting multiple slip modes. We considered in detail fault self-organization produced by frictional intergranular sliding. There is no grain crushing here. We managed to reproduce the entire spectrum of slip modes by changing filler composition and its particle size distribution. A great number of AEs were detected during laboratory seismic cycles. Their quantitative categorization led to distinguishing two distinct AE subpopulations. Analyzing their scaling characteristics, we suggested a nucleation mechanism that, as we believe, underlies the entire spectrum of fault slip modes.

Materials and Methods

Laboratory experiments were performed on a slider model. A scheme of the setup is shown in Figure 1. The model fault—a confined granular layer between two blocks—was subjected to external normal and shear stresses. The moveable granite block (1) 8 × 8 × 3 cm3 in size was put on the middle of the granite base (2) rod 2.5 m long and 10 × 10 cm2 in cross section. The contact surfaces of the block and the base rod were made rough by introducing grooves 0.8–1.0 mm deep. The contact gap between the block and the base was filled with a layer of granular material 3 mm thick (3). The granular layer was prepared using a leveling frame, so that the initial thickness of the layer was the same in all the experiments. To the end of experiments the thickness of the layer usually decreased to 2–2.5 mm. Mixtures of different granular materials were used as fillers. All fillers are listed in the Supplementary Table 1. Their structural properties were responsible for reproduction of a certain slip mode (Mair et al., 2002; Anthony and Marone, 2005; Kocharyan et al., 2014). All the experiments were performed at room temperature and humidity.

FIGURE 1
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Figure 1. The slider-model performance test. Mechanical parameters (friction and displacement) and acoustic emission were measured during the experiments. (A) A scheme of the experimental setup: (1)—moveable block; (2)—base rod; (3)—gouge layer; (4)—laser sensor of displacement; (5)—force sensor; (6)—elastic element (spring); (7)—AE sensors. (B) Regular stick-slip with specific variations of friction and displacement in time (Exp. No 5). (C) Stochastic sliding regime (Exp. No 23). The point (0,0) corresponds to the moment when the ultimate strength of model fault is reached. We study the “mature” stage when friction varies in fixed range with upper limit τs. Insets (B,C) show the recurrence plot of slip events (number of slip events with peak velocity exceeding Vpeak).

The moveable block slid along the interface under the applied normal and shear forces. The normal force was FN = 300/400/500 N. It was applied by a set of weights. The shear force was applied to the block through an elastic element (6) with the stiffness of K = 55 kN/m. Its free end was pulled at a constant velocity of us = 8 μm/s. The shear force was measured with the sensor CFT/5kN (HBM, Germany) (5) accurate to 1 N. The displacement of the block relative to the base was measured with the laser sensor ILD2220-10 (Micro-Epsilon, Germany) (4) in the frequency band of 0–5 kHz, with the accuracy of 0.1 μm.

Figures 1B,C shows variations of fault friction and displacement during experiments. The fault evolution undergoes several stages (Gerasimova et al., 1995; Scuderi et al., 2017). At the initial stage the model fault reaches the ultimate shear strength. Further accumulation of shear deformation leads to the transition of the fault to a new state and a new characteristic strength τs is reached. Persistent cycles “loading/drop” are observed at this new stage, the frictional strength of the fault (τsN) remaining constant. We consider this stage in our detailed analysis. Regularities of a sliding regime are defined by structural and frictional properties of the filler. Parameters of sliding regimes are presented in Supplementary Table 1. Using, for instance, the filler composed of quartz sand with a narrow particle size distribution led to a regular stick-slip—quasi-periodically repeated fast slip events accompanied by huge drops of friction (Figure 1B). On the other hand, using the quartz sand with a wide particle size distribution resulted in a stochastic sliding regime, when the model fault hosted multiple slip modes and slip events were occasional (Figure 1C). Slip events are dynamic instabilities, during which the velocity of sliding block is higher than us and the relative friction decreases. The statistics of slip events for regular and stochastic sliding regimes differ.

One of the experimental outputs was the AE accompanying frictional fault evolution. Three AE sensors were mounted on the rod at the distances of 0.6 and 0.7 m at opposite sides of the moveable block using epoxy agent. The sensors were VS30-V (Vallen System, Germany). The operational frequency band was 20–80 kHz. The acoustic signal was processed by AEP5 charge amplifiers and acquired at the sample rate fs of 1 MHz with a 14-bit analog-to-digital converter E20-10 (L-Card, Russia). The signal was provided in units of voltage.

We used a threshold algorithm to detect AEs. An AE is detected when the energy flow exceeds a fixed threshold, according to the following relation:

π ( t ) = 1 t t t + t A ( t i ) 2 f s 1.5 A m i n 2 (1)

A(t) is the recorded signal filtered in the frequency band of 20–80 kHz, Amin2 is the variance of the signal. The energy flow was determined in the window Δt = 0.5 ms at steps of Δt/2. Amin2 was determined at 1 s intervals preceding the start of shear load, according to the following relation:

A m i n 2 = 1 f s - 1 t i > 0 t i 1 | A ( t i ) - 1 f s t i > 0 t i 1 A ( t i ) | 2 (2)

Figure 2 presents the algorithm of AE detecting. The time ts when the energy flow starts to exceed the threshold is taken to be the beginning of the AE, and the time te when the energy flow goes beyond the threshold—the end of the AE. The points of onset and termination were determined with the accuracy of 250 μs. We verified by visual inspection that every recorded AE was captured. Random choice of 1,000 AEs showed that only 47 multi-pulses were misidentificated as simple pulses.

FIGURE 2
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Figure 2. Algorithm of AE detection (Exp. No 5). First, the acoustic signal was filtered in the frequency band of 20–80 kHz with a Butterworth filter. Then, the energy flow (Π) was calculated (blue line). Red dots designate the excesses over a fixed experimental threshold determined by relation (1). Pulses identified as AEs are marked with dashed areas. The spectrogram of the acoustic signal clearly shows the AEs. Insets show parameters of AEs: onset (ts), termination (te), amplitude (As) and peak-to-peak amplitude (ΔA).

The following parameters were retrieved from the detected AEs: duration (dt), amplitude (As), peak-to-peak amplitude (ΔA), and energy (E), which was estimated as follows:

E = t t s t e A ( t i ) 2 (3)

Symbols used in the article are listed in the Table 1. We obtained amplitudes only from the digital waveforms and performed energy estimations by time integration of the signal in volts. So, these energy estimations were presented in non-physical energy units.

TABLE 1
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Table 1. List of symbols.

Assuming self-similarity of the deformation process, which consequently implies a power-law distribution, we checked the AE catalog. In order to compile a homogeneous and complete AE catalog with respect to duration and amplitude, we eliminated AEs with durations less than 1.5 ms and amplitudes As lower than 60 dB.

It seems likely that the waveform of an AE points to the mechanism and intensity of the evolution process inside the fault (Shiotani et al., 2001; Zigone et al., 2011; Ostapchuk et al., 2016). In order to describe both the stage of AE rise and the stage of decrease, we introduced the waveform index WI (Ostapchuk and Morozova, 2020). The WI-value was calculated through the formula:

W I = t m a x - t s t e - t m a x (4)

where tmax is the time when the maximum peak-to-peak amplitude was reached. WI-value is similar to the RA-value [RA = (tmaxts)/As] and a strong correlation between these two indexes is observed. The WI-value is dimensionless and allows to qualitatively evaluate AE waveform. Introduction of the WI-value is based on the assumption that various processes of self-organization take place in a stressed granular medium during formation of inhomogeneous stressed conditions in a gouge-filled fault during sliding (Hadda et al., 2015; Gao et al., 2019). More than 95% of the detected AEs had WI-value within the range of 0–1. The relative error of WI-value determination was less than 0.15. The AEs with the values of WI >> 1 were treated as double- or multi-pulses. They were not considered in our analysis.

AEs of different waveforms and amplitudes were emitted in fault sliding. Depending on the sliding regime the rate of AE varied from single “clicks” at intervals of several seconds to regularly repeating AEs at intervals of 1–2 ms. Among all the recorded AEs it was necessary to distinguish those emitted during slip events and at the stages of slip event preparation (Figure 3).

FIGURE 3
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Figure 3. AE data (Exp. No 13). (A) acoustic signal recorded during fault sliding (Exp. No 13); (B) “coseismic” AEs corresponding to slip events; (C) “interseismic” AEs corresponding to slip event preparation. In (B) the red line corresponds to variations in time of the velocity at which the moveable block slides. In (C) the WI-value is indicated in parentheses.

Results

Continuum of Fault Slip Modes at the Macro Scale

Using mixtures of different materials, we managed to reproduce in laboratory the entire spectrum of slip modes. We determine slip event as a dynamic instability characterized by a decreasing friction and block sliding at a velocity exceeding us. The time period when block velocity exceeds us, corresponds to the duration of the event (T); the displacement of block for that time period is treated as the coseismic slip (ΔL). We used the record of displacement of the block relative to the base to calculate peak velocities (Vpeak) during slip events. Figure 4 shows variation of parameters of slip events. They form a connected set in the space (Vpeak, T, ΔL). Considering different parameters lets us to qualitatively divide the events into three modes. The first mode is the fast slip events with peak velocities higher than 8 mm/s (1,000 us) and durations less than 0.8 s (Figure 3B). The fastest slip events had peak velocities up to 48 mm/s (6,000 us) and relative values of friction drops up to 0.1 (Figure 1B). Single high-amplitude AEs with durations corresponding to the ones of slip events were emitted in fast modes. The second mode is the slow slip events. Slow slip events had peak velocities of 2–5 us and relative changes of friction less than 10–2. Slow slip events were accompanied by emission of cascades of AEs (Figure 3B) that resembled low frequency earthquake bursts during slow slip events (SSE) in nature (Frank et al., 2016). Duration of laboratory slow slip events varied from 2 s to 15–20 s. It should be noted that slow slip events with durations exceeding 10 s were specific for the model fault with clay-rich gouge. The third mode is the intermediate slip events. It shows a high variety of parameters and demonstrates a diversity of slip events. The third mode fills in the gap between slow and fast slip events, indicating a continuum of slip modes.

FIGURE 4
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Figure 4. Variations of slip event parameters. Peak velocity dependences on slip duration (A) and on cumulative slip (B) show that the ensemble of slip events form a connected set in the space [cumulative slip (ΔL), peak velocity (Vpeak), slip duration (T)]. The area in the space of parameters specific for fast slip events is marked as FSE, intermediate slip events—ISE, slow slip events—SSE. (C) The energy of “coseismic” AEs vs. the laboratory “seismic” moment. Inset shows the results of Exp. No 23. The laboratory seismic moment is MlabK⋅△Ls (where K and s are spring stiffness and block length, respectively) (Kocharyan et al., 2017a). The symbols 1–24 correspond to different experiments listed in the Supplementary Table 1.

The ensemble of slip events demonstrates a high spread of the emitted cumulative AE energy. The magnitude of AE energy differs by more than 2 orders of magnitude for slip events with equal laboratory “seismic moments” (Supplementary Section 1). Considering the data of a single experiment, an increase in the seismic moment is accompanied by a power-law increase in the emitted AE energy (Figure 4C, inset). Unfortunately, it is impossible to detect an analogous regularity considering the complete ensemble of slip events. The reason is the alteration of the structure of the model fault filler. The filler composition controls the radiation efficiency of slip events (Kocharyan et al., 2017a). Hence, events with equal seismic moments can show different values of emitted energy on faults with different filler.

Two AE Subpopulations at the Micro Scale

The change of stress-strain state of the model fault results in a rearrangement of grains and is accompanied by a great number of AEs. In general, the amplitude-frequency distribution of AEs is a superposition of a power-law distribution in the low-amplitude range (As < 0.1 V) and a peak-like distribution in the high-amplitude range (As > 0.1 V) (Figure 5A).

FIGURE 5
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Figure 5. Probability density function (PDF) of AE. AE statistics demonstrates an essential difference between frequency-amplitude (A) and frequency-waveform (B) distributions. The “coseismic” AEs corresponding to slip events form a separate high-amplitude peak, which is marked by the filled area. The waveform index plot shows the characteristic (cut-off) value (WI = 0.1). Numbers correspond to experiments listed in Supplementary Table 1.

In the range of low As values the AE statistics is approximated with high accuracy by the power-law:

l g ( N ) = a - b l g ( A s A 0 ) (5)

where N is the number of AEs with amplitudes of As. The value lg (As/A0) corresponds to AE body-wave magnitude (Lei, 2003), a and b are two positive constants. The a-value is a measure of AE activity, which depends on the time window of observations. The slope of recurrence plot (b-value) is a scaling parameter, which characterizes the process of self-organization of the medium (Gutenberg and Richter, 1944; Turcotte, 1999). The power law is also typical for the AE distributions over energy (E) and duration (dt).

The distribution of AE over the WI-value shows persistence of the cut-off WI-value. WI varies from 10–2 to 1 and can be separated into two domains: WI ≤ 10–1 and WI > 10–1. An even distribution is observed for low values, and a power decrease—for high values (Figure 5B). It can be written as follows:

N = { a W I , W I 0.1 c W I W I - w , W I > 0.1 (6)

where N is the number of AEs whose waveform parameters equal to WI, aWI, and cWI are positive constants, which are determined by the intensity of AE activity.

The essential difference of the AE distributions over amplitude and over waveform index points to the necessity to consider the WI-value as an independent characteristic of the process of fault evolution. The presence of a specific cut-off point in the frequency-waveform distribution motivates to conduct a quantitative categorization of the ensemble of detected AEs over the WI-value. Quantitative categorization can be considered as a sort of clustering under unsupervised machine learning. AEs with WI ≤ 0.1 will compose Type I. They are wave trains with harsh onsets. Their spectra show maxima in the range of 50–65 kHz (Figure 6). Type II will include AEs with WI > 0.1. They exhibit gradual amplitude rises and tremor-like waveforms (Figure 3). A tendency of transition of vibrations to the low-frequency area is traced for the AEs of Type II and there is an obligatory maximum at 20 kHz (Figure 6).

FIGURE 6
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Figure 6. Power spectral density (PSD) of AE. Spectra specific for AEs with different waveforms. The AE with harsh onset shows maximum in the range of 50–65 kHz. For the AE with gradual amplitude rise two maxima emerge in the range of 18–25 and 50–65 kHz. For tremor-like AEs spectral maxima are shifted to the range of 18–25 kHz.

Figure 7 shows log-log trends between parameters of AEs of Type I and Type II. The scaling relationships provide important insights into and constraints on the dynamics of internal processes. Such a presentation gives an opportunity to qualitatively compare these trends to scaling laws for ordinary “fast” earthquakes and SSEs (Peng and Gomberg, 2010; Nishitsuji and Mori, 2014).

FIGURE 7
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Figure 7. Scaling of two AE subpopulations in Exp. No 13. (A) AE duration vs. AE amplitude (type I—yellow, type II—purple). The complete ensemble of AEs is limited by two solid lines given by relations (7). Right plots show the two-dimensional probability density functions of AEs type I (upper) and AEs type II (lower). (B) AE energy vs. AE amplitude. The energy varies by more than an order of magnitude for AEs with one and the same amplitude. Right plots show the two-dimensional probability density functions of AEs type I (upper) and AEs type II (lower).

The AE duration scaling is viewed as a key to unraveling the rupture mechanism in nature and in lab. All the recorded AEs form a connected set, which is limited by two boundaries:

dtupperAs1.2±0.2dtbottomAs0.5±0.1    (7)

In nature this may correspond to the scaling between the seismic moment M0 and the duration Teq ranging from TeqM00.8±0.1 to TeqM00.3±0.1 (Supplementary Section 2). At the same time one can see that AEs of Type I group closer to the lower boundary, than AEs of Type II (Figure 7). It means that for AEs of equal amplitudes, Type II should have longer failure duration than Type I. At the same time, scaling of emitted energy of two types differ insignificantly, indicating that the intergranular frictional sliding is the single source of AEs.

Illumination of Frictional Behavior

A stable repeated pattern of variations of sliding velocity and AE rate is observed during a regular stick-slip (Figure 8). We distinguish three typical stages of a seismic cycle. After the dynamic failure the post-seismic stage comes with a decreasing velocity of sliding block and a lowering AE rate. The falling activity is described by the law of Omori-Utsu (Lherminier et al., 2019; Ostapchuk et al., 2019). Then approximately stable minimal values of velocity and AE rate persist at the inter-seismic stage. As the system approaches a slip event, an accelerated block sliding starts accompanied by an increase of AE rate. At the final part of inter-seismic stage leading to failure, statistics of AEs can be described by the inverse Omori’s law (Johnson et al., 2013; Ostapchuk et al., 2019). In a stochastic regime the pattern of parameter alteration is more complicated (Figure 8). It seems impossible to detect stages of a cycle through AE rate and sliding block velocity. Only small relative variations of AE rate are observed before slip events, while abrupt drops occur only after the fastest slip events.

FIGURE 8
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Figure 8. Evolution of model fault state. Variations of sliding velocity and AE parameters for a regular stick-slip (Exp. No 3) (A–D) and a stochastic sliding regime (Exp. No 13) (E–H). Insets (D,H) show distributions of AEs in running windows for type I (yellow) and type II (purple). Unlike the stochastic regime, the regular regime shows a high correlation between the sliding velocity and the AE rate. Occasional variations of b-value are observed for both regular and stochastic regimes for the complete ensemble of AEs. Probability density function of b-value obeys the normal distribution law. Dividing AEs into two subpopulations shows an essential difference of time variations of b-value. Occasional alterations are observed for the AEs type I (WI ≤ 0.1), while the AEs type II (WI > 0.1) show systematic variations.

Peculiarity of frictional behavior can be illuminated by the AEs. Variations of cumulative displacement (D) and cumulative AE energy (Π) have similar tendencies (Figure 9). For all the sliding regimes correlation between D and Π exceeds 0.95, and the revealed regression model is:

FIGURE 9
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Figure 9. Variations of cumulative AE energy (Π) and block displacement (D). The inset shows the dependency Π (D). (A) Stochastic sliding regime, Exp. No 23—Π = 8.10−4⋅ D. (B) Regular sliding regime, Exp. No 5—Π = 5.10−4⋅D.

Π = γ D (8)

Also, we can evaluate the friction strength of model fault. In experiments with different gouge materials the friction coefficient varies significantly from 0.46 to 0.86 (Supplementary Table 1). The analysis of parameters of sliding regime have shown that the growth of friction coefficient is accompanied by a decrease in b-value, while the Pearson’s correlation is about 0.94. Besides that, the friction coefficient ranging from 0.65 to 0.83 corresponds to the b-value lower than 1.1.

Illumination of Slip Event Nucleation

Figure 8 shows variations of AE parameters for regular and stochastic sliding regimes. To investigate the temporal evolution of b-value, we calculated the b-value using the least squares regression in a running window for an equal number of AEs (nn = 100) at a running step of nn/2 (50% overlap). No clear staging of laboratory seismic cycles was observed when analyzing variations of the b-value of the complete population of AEs. The b-value distribution obeys the normal law. It should be noted that the cyclicity of b-value for the complete population of AEs in a limited range of amplitudes has been mentioned in a few works (Lei et al., 2018; Riviere et al., 2018). Clusterization of AEs into two subpopulations eliminates the ambiguity of the pattern of b-value variations.

For a regular stick-slip b-value histograms show that for AEs of type I (WI ≤ 0.1) b-value is almost constant and its changes are occasional (histogram obeys the normal distribution). At the same time the AEs of type II demonstrate certain periodic variations of b-value, and the histogram cannot be approximated by a normal distribution. If we look at the laboratory seismic cycle just after a dynamic failure at the first stage of fault recovery, we can see that a fast growth of b-value occurs. Then the stage of creep comes at a minimal velocity, and b-value remains almost constant, which in the histogram manifests as a peak of b-value around the value of 1.4 (Figure 8A). At the final stage, a monotonic decrease of b-value is observed, which means that the share of high-amplitude AEs of type II grows.

For a stochastic regime, the pattern of parameter alteration is much more complicated. But, if one performs clusterization of AEs, the duality of their population becomes apparent, and the staging of fault evolution manifests clearly (Figure 8D). The AEs of type I have only a single specific b-value during shear, and variations are random. The AEs of type II show staging of b-value alteration. The b-value decreases before each of the slip events and recovers after them.

Detecting the two subpopulations of AEs can form a new basis for revealing slip event nucleation. We have formulated a simple criterion of laboratory “alarm.” It is based on tracing specific features of AEs that reflect fault evolution in time. The alarm criterion is as follows. If for AEs type I a random variation of b-value is observed and for AEs type II for three successively estimated b-values a monotonic decrease is observed b(ti−2) > b(ti−1) > b(ti), then the alarm starts at the time ti (Figure 10). The end of the alarm is the time when the slip event starts (the “true” alarm), or the time tn, when an increase of b-value is observed again b(tn−1) < b(tn) (the “false” alarm) (Figure 10, the inset).

FIGURE 10
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Figure 10. Transition of the model fault to a critical state. Variations of block velocity and b-value of AEs type II for a regular stick-slip in Exp. No 4 (A) and a stochastic sliding regime in Exp. No 13 (C). The yellow areas correspond to alarm intervals, the red ones—to slip events. Insets show algorithms for a “true” alarm (A) and a “false” alarm (C). We use the Molchan’s diagram to evaluate the predictive power for regular (B) and stochastic (D) sliding regimes. Shaded circles show the performance of prediction algorithm. Random binomial predictions occupy the diagonal. Random predictions with fixed alarm time (τ) fall in the gray area with the probability of α = 10–5.

For a regular sliding regime, the alarm covers the whole pre-seismic stage of the seismic cycle. For example, in Exp. No 4 the duration of alarm was 3.9 ± 1.9 s, while the recurrent time of dynamic failures was 34.2 ± 0.8 s. At the same time, it is important to note that the critical stage (when an event can be triggered by a weak disturbance) emerges at stresses close to the critical ones at the end of the pre-seismic stage (Kocharyan et al., 2018). For a stochastic regime (Figure 10C) the pattern of b-value alteration is more complex, but the chosen alarm criterion is sensitive for such a regime too. The decrease of b-value signifies both the forthcoming fast and slow slip events, but more complex mechanisms of self-organization lead to “false alarms” (Ren et al., 2019) (Figure 10C, the inset). The Molchan’s error diagram is used to evaluate the predictive power of our prediction algorithm and its stability (Molchan, 2003, 2010). We use two interdependent measures of prediction quality: the fraction of unpredicted events ν, and the fraction of alarms τ. Each prediction corresponds to a single point in (τ, ν) space. The error diagram for our prediction of the transition of the fault to the critical state of seismic cycle is presented in Figures 10B,D. The τ-axis corresponds to the relative alarm time, the ν-axis—to the share of missed slip events. An extremely simple but easily tractable model of prediction which produces alarms independent of the target events is the random binomial prediction (Molchan, 2003; Shebalin et al., 2006). The probability for a random binomial prediction with a given value of τ to fall within the shaded area is less than or equal to 10–5 (0.001%). The point corresponds to our prediction algorithm indicating high predictive power both for the regular and the stochastic sliding regimes. The efficiency of the precursor Jm is defined as:

J m = 1 - ν - τ (9)

The value of Jm lies in the range of (0…1). The nearer the value to 1 is, the more reliable is the raise of alarm. For a regular stick-slip Jm is equal to 0.59–0.83, while for a stochastic sliding regime that includes multiple slip modes the value is Jm = 0.4 – 0.65 (Supplementary Table 1).

Discussion

Recent findings improve our understanding of the evolution of a frictional fault hosting multiple slip modes. It should be noted that laboratory experiments are by no means a sort of scale modeling since it is simply impossible to fulfill all the similarity criteria in this case (Rosenau et al., 2017). Results of laboratory experiments should be considered as insights into fundamental properties of geomaterials and their structural peculiarities which underly fault slip behavior. The similarities in the internal structures of experimental and natural faults point to similarities in the deformation mechanisms (Tchalenko, 1970). Findings should relate to the frictional instability of a model fault, just at the expense of self-organization of granular matter.

Natural faults show the evidence of localizing deformations along very narrow fault-parallel principal slip zones. These principal slip zones have undergone large cumulative deformations (Sibson, 2003). The wall rocks are separated by a layer of cataclastic rock (gouge) with self-similar structure over the range of particle diameters from 10 μm to 1 cm (Sammis et al., 1987). As a rule such faults are treated as strong faults, and their frictional strength is consistent with the Beyrlee’s rule of friction (from 0.6 to 0.85) (Collettini et al., 2019). The evolution of a laboratory gouge-filled fault is controlled by peculiarities of formation and destruction of conglomerates of loaded grains at the microscale, the so called “force chains” (Sammis et al., 1987; Mair et al., 2002; Hayman et al., 2011; Lherminier et al., 2019). The assembly of these chains has a certain spatial structure and a relatively low specific weight inside the medium (Gao et al., 2019). Thus, we may suggest that two structural subsystems emerge inside a stressed fault—a consolidated force skeleton and rather moveable relatively unloaded areas (Gao et al., 2019). Although we had no chance to visualize the inner processes of self-organization in the performed experiments, the revealed regularities of alteration of AE ensemble agree with numerical (Hadda et al., 2015; Gao et al., 2019) and laboratory (Mair et al., 2002; Hayman et al., 2011) experiments. The findings probably point to formation and evolution of two structural subsystems. When the force chains (loaded grain conglomerates with limited sizes) are destroyed, the high-frequency AEs with harsh onsets are emitted (Hadda et al., 2015; Ostapchuk et al., 2016; Gao et al., 2019). The uniformity of distribution for WI < 0.1 points to formation of stressed grain clusters of limited size which have approximately equal sizes (Hadda et al., 2015) (Figure 5B). Breaking force chain leads to increasing the volume of unloaded grain clusters, so, the size of unloaded areas varies during laboratory seismic cycle. Indeed, for AEs with WI > 0.1 the power law distribution is observed. Considering a blocky hierarchical structure of the Earth’s crust, the distribution of stresses inside separate structural forms can exhibit a partially inhomogeneous character (Sobolev and Zav’yalov, 1980; Schoenball and Davatzes, 2017). In the zones of tectonic faults stresses concentrate at asperities (Seno, 2003) or strong patches (Collettini et al., 2019), which probably correspond to laboratory force chains. It is the configuration and friction properties of asperities that determine the slip mode of the fault (Dublanchet et al., 2013; Barbot, 2019). Indeed, high temperature and stresses, specific for seismogenic depths, affect the deformation of gouge-filled faults, but under the velocity weakening it is the self-organization processes that will prevail in the evolution of fault behavior. One of the mechanisms of destruction of stressed clusters under high stresses is grain crushing. Grain crushing is accompanied by AEs with harsh onsets and low WI-values (Shiotani et al., 2001). So, grain crushing makes the structure of AE ensemble in the range of low WI-values more complex, but it is the frictional slippage that controls the rearrangement of unloaded zones. In this work we made the accent on the processes of self-organization provoked by frictional instability. Performing a quantitative categorization of AEs during grain crushing is a future prospect. We may identify qualitative similarity in the processes of self-organization of both natural and laboratory frictional faults (Mykulyak et al., 2019).

The experiments testify that the entire spectrum of slip modes results from the frictional instability of the model fault, just at the expense of friction (Figures 3, 4). Though we do not exclude other mechanisms, such as variations of fluid pore pressure, dehydration reactions, brittle-ductile transition and others (Reber et al., 2015; Saffer and Wallace, 2015; Burgmann, 2018; Cruz-Atienza et al., 2018). We demonstrate that frictional slip modes span a continuum and that the cumulative acoustic energy released during slip events varies in a wide range. From the mechanics of faults viewpoint and under velocity weakening the slip mode and the emissive efficiency of an event are determined by the ratio κ of the specific fault stiffness to the specific stiffness of the hosting rock (Leeman et al., 2016; Kocharyan et al., 2017a). When κ ∼ 1 slow slip modes prevail, when κ >> 1 fast events take place and their intensity increases as κ grows. If a fault has a spatially heterogeneous interface, reconfiguration/rearrangement of force skeleton caused by slip events may essentially change the ratio κ and different slip modes can be reproduced (Kocharyan et al., 2017b; Ostapchuk et al., 2020). In our experiments the stiffness of the hosting rock (the loading system is its analog in lab) remained constant, only the fault stiffness varied. This led to formation of a connected set in the space (Vpeak, T, ΔL). Our study shows that one and the same laboratory fault can host different slip modes. Meanwhile these different slip modes are described by one and the same scaling ratio (Figure 4C, inset). Recent observations in natural field suggest that SSEs follow the same moment duration scaling as earthquakes (Michel et al., 2019; Frank and Brodsky, 2020), unlike qualitatively different scaling proposed by earlier studies (Peng and Gomberg, 2010). For example, the Cascadia slow slip events demonstrate a cubic moment-duration scaling and can produce pulse-like ruptures similar to fast slip events (Michel et al., 2019). Numerical simulations urge the same frictional origin for both earthquakes and SSEs and show that both simulated and natural SSEs have rupture velocities and stress drops that increase with earthquake magnitudes (Dal Zilio et al., 2020).

Most scholars consider the regular stick-slip, when slip events take place quasi-periodically, as the dominant fault sliding regime. Laboratory investigations of fault behavior should take into account the stochastic sliding regime too. There are very few known faults with regular periodicity of characteristic earthquakes at the human timescale (Ben-Zion, 2008); meanwhile, evidence appears systematically, that a single fault hosts both fast and slow slips (Ito et al., 2013; Meng et al., 2015; Villegas-Lanza et al., 2016).

Regularities of the model fault evolution at the micro-scale determine its characteristics at the macro-scale. It has long been recognized in soil mechanics that the apparent coefficient of friction (μ), which is defined by the ratio of the shear (τ) to the normal (σN) stresses, is larger than the actual coefficient of friction between the particles (μ). For a 2D force chain consisting of equal size particles the apparent friction μ is as follows (Biegel and Sammis, 1989):

μ * = μ + t a n β 1 - μ t a n β , (10)

where β is the misalignment angle (the angle between the macroscopic shear plane and the interparticle slip plane). The value of β depends on particle size distribution and the packing geometry (Biegel and Sammis, 1989). Hence, changing fault structure causes a change in friction μ. But changing the structure also causes a change in the b-value of the frequency-amplitude distribution (Turcotte, 1999; de Arcangelis et al., 2016). Our experiments demonstrate a high inverse correlation (-0.95) between the b-value and the fault friction (τsN), that is, the spatial variation of b-value may point to spatial variations of frictional/structural properties of the fault.

Improving the techniques of detecting weak and slow earthquakes and performing their statistical analysis provide important information about tectonic fault dynamics and help to trace the nucleation of a large earthquake (Gulia and Wiemer, 2019; Trugman and Ross, 2019). The performed experiments have shown that for a stochastic regime it is appropriate to supplement a classical seismic catalog containing information about time, place and magnitude with parameters that describe the dynamics of coseismic rupture. Resting on a quantitative categorization of the AE catalog, a simple, but very efficient criterion of laboratory “alarm” has been formulated. The introduced alarm algorithm indicates that the frictional fault instability is imminent, but the precise time to failure is not defined. For a stochastic regime the efficiency of the algorithm is Jm = 0.54 ± 0.14, while for a regular stick-slip it rises to Jm = 0.74 ± 0.11. For comparison, the efficiency of the ETAS forecasting model for earthquakes M > 6 in Southern California is 0.29 (Lippiello et al., 2012). Predictions based on the ultralow frequency magnetic data show the efficiency of about 0.23 (Han et al., 2017). The forecasting technique based on the effect of modulation of high frequency seismic noise in Kamchatka gives the value of about 0.5 for target earthquakes M ≥ 6 (Saltykov, 2017). Thus, the implementation of quantitative categorization of seismic data may be the next stage which can potentially mark advances in fault mechanics.

Conclusion

A unified pattern of fault slip behavior evolution is a fundamental issue. It requires linking seismic, mechanical and structural data. In the present laboratory study we have revealed two distinct subpopulations of AEs, which reflects the complexity of frictional fault evolution at the micro scale. The self-organization of a gouge-filled fault at the micro scale is the key parameter that controls the frictional behavior of a fault hosting multiple slip modes. At the macro scale a similarity of precursory changes of AEs for fast, intermediate, and slow slip modes on a frictional fault is observed. Findings point to the unity of underlying frictional mechanisms of different slip modes.

Data Availability Statement

The datasets presented in this study can be found in online repositories. The names of the repository/repositories and accession number(s) can be found below: http://dx.doi.org/10.17632/kykwmjmpgf.3.

Author Contributions

AO was responsible for the research conceptualization, design, organization of the work, and writing the first draft of the article. KM, VM, and DP performed the experiments. KM and MP performed the data analyses and prepared some figures. KM was involved in the data curation. All authors took part in editing the final version.

Funding

This work was partially supported by the Russian Science Foundation according to the Research Project No. 20-77-10087 for KM, DP, and AO. VM and MP acknowledge Program No. AAAA-A17-117112350020-9 of the Ministry of Science and Higher Education of the Russian Federation.

Conflict of Interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2021.657487/full#supplementary-material

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Keywords: fault behavior, earthquake cycle, self-organization, frequency-amplitude distribution, laboratory experiment

Citation: Ostapchuk A, Morozova K, Markov V, Pavlov D and Popov M (2021) Acoustic Emission Reveals Multiple Slip Modes on a Frictional Fault. Front. Earth Sci. 9:657487. doi: 10.3389/feart.2021.657487

Received: 23 January 2021; Accepted: 29 March 2021;
Published: 21 April 2021.

Edited by:

Qiang Qiu, South China Sea Institute of Oceanology, Chinese Academy of Sciences (CAS), China

Reviewed by:

Jianye Chen, Utrecht University, Netherlands
Jinfeng Liu, Sun Yat-sen University, China
Lei Zhang, Institute of Geology, China Earthquake Administration, China
Zonghu Liao, China University of Petroleum, China

Copyright © 2021 Ostapchuk, Morozova, Markov, Pavlov and Popov. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.

*Correspondence: Alexey Ostapchuk, ostapchuk.aa@phystech.edu; ostapchuk.aa@idg.ras.ru