- Open Access
Small-scale stress fluctuations in borehole breakouts and their implication in identifying potential active faults around the seismogenic megasplay fault, Nankai Trough, SW Japan
© Yamada and Shibanuma; licensee Springer. 2015
- Received: 12 March 2014
- Accepted: 20 December 2014
- Published: 6 February 2015
Borehole breakouts are enlargements and elongation of a borehole in a particular direction, caused by failure of the borehole wall rock due to concentration of stresses around the borehole, and thus, have been widely used to determine the in situ stress orientation. We used electrical borehole wall images obtained during offshore scientific drilling (IODP) that penetrated through a seismogenic megasplay fault in the Nankai Trough, off SW Japan, and extracted a number of borehole breakouts. Most of the breakouts show directions that can be explained by the regional convergence, but some are obviously rotated by faults and fractures in the megasplay fault zone and in its hanging wall. Stress magnitudes estimated from the width of the breakouts also show some decrease in the horizontal stresses, suggesting that slip along the faults and fractures release shear stress affecting these surfaces. Since such surfaces may have the capability to reactivate where the stresses affecting the surface are geometrically appropriate, the method presented in this paper may contribute to identifying active fault surfaces. This knowledge allows us to identify which surfaces need to be examined in detail to assess their potential for future activity.
- Borehole breakout
- Stress rotation
- Active fault identification
- Nankai Trough
Underground stresses are primarily controlled by combinations of three kinds of stresses: overburden stress, overburden-related confining stress, and tectonic stress. We can precisely determine the overburden stress at a particular depth by measuring the density of the sedimentary sequence (Jaeger and Cook 1979). Overburden-related confining stress is induced by the elastic effect of rock, and the horizontal compressive stress can be estimated by the Poisson’s ratio of the rock and the overburden stress at that depth (Jaeger and Cook 1979). Tectonic stresses, however, show significant variations depending on the measurement location relative to the regional tectonic environment and cannot be simply estimated. This is why in situ measurements are required to recognize underground stresses.
There are several techniques of in situ stress measurements, depending on the situation of the measurement point. The easiest and most widely used technique is the use of borehole wall failures (see Zoback 2007), such as borehole breakouts (BOs) and drilling-induced tensile fractures (DITFs). BOs and DITFs are both induced by stress field fluctuations where ‘open space’ exists underground, i.e., borehole drilling. Such fluctuation occurs because the borehole wall behaves as a free surface, and shear stress parallel to the wall does not propagate (Zoback 2007). As a result, stress concentrates on the borehole wall and fails if the stress condition fulfills an appropriate failure criterion of compressional or tensional environment. These phenomena of borehole failure are called BOs and DITFs, respectively. Significant BOs lead to drilling problems; thus, an appropriate drilling mud is used in oil/gas wells to prevent such failures. In scientific drilling, however, such costly mud is not used, and BOs occur frequently; nevertheless, these borehole failures have been positively used as important data to estimate underground stress fields.
In the past few decades, one or just a few measured values have been regarded as representative of an area of a few dozen square kilometers, assuming a simple homogeneous stress field. Such measured stress values are sometimes inconsistent with the regional stress field where discontinuity surfaces release the shear stress affecting these surfaces (Shamir and Zoback 1992; Barton and Zoback 1994; Zhang et al. 1994; Finkbeiner et al. 1997; Camac et al. 2006; Wu et al. 2007; Lin et al. 2010). Chang et al. (2010) conducted stress analysis at a subduction margin and reported a systematic change from a normal fault regime to a strike slip regime with depth. Most of these studies, however, used only the overall trend of stress orientations and gradual changes in stress magnitude. This paper reveals the detailed nature of the in situ stress state, detected by a stress analysis method using borehole wall failures, and shows frequent fluctuations in stress orientation and stress magnitude. The results can be applied to examine possible active faults around the megasplay fault zone at the Nankai subduction margin, off southwest Japan.
Methods of stress analysis
where μ is the sliding frictional coefficient, σ 1 is the effective maximum compressive principal stress, σ 3 is the effective minimum compressive principal stress, S 1 is the maximum compressive principal stress, S 3 is the minimum compressive principal stress, and P p is the pore pressure.
Stresses around a borehole
where σ θθ is effective circumferential stress around the borehole, σ rr is effective stress normal to the borehole axis, and σ ZZ is effective stress in the vertical direction (along the borehole axis); θ is the angle from the S Hmax direction; P0 is pore pressure; ΔP is the difference between mud water pressure Pmud and pore pressure P P ; σ ΔT is a stress caused by the difference of temperature between the mud and the formation; ν is the Poisson’s ratio.
This modified Wiebols-Cook failure criteria looks complicated, but the only required parameters are UCS and μ i . These parameters can be measured and determined directly from rock tests on the core or samples obtained from appropriate outcrops. UCS can also be estimated using empirical equations between UCS and sonic velocity (e.g., Chang et al. 2006).
Stress analysis at the Nankai accretionary wedge
Data and methods
Rock mechanical data used in this study
Internal friction co.
Results and discussions
This study found frequent stress rotations and localized negative anomalies in stress magnitude at the megasplay fault zone and its hangingwall. The following sections describe and discuss these findings.
As briefly introduced earlier, such rotations of stress orientations have been observed at some discontinuity surfaces, probably from the release of shear stress affecting these surfaces (Shamir and Zoback 1992; Barton and Zoback 1994; Zhang et al. 1994; Finkbeiner et al. 1997; Camac et al. 2006; Wu et al. 2007; Lin et al. 2010). In order to examine this possibility, we looked at the fractured zones reported by Yamada et al. (2011) at C0004B. The fractured zones are defined by intense development of conductive fractures and recognized in the megasplay fault zone and its hangingwall, but there is no such zone in the footwall (Figure 4). By comparing the locations of the fractured zones and the stress rotations, we found that some of the fractured zones correspond to the depths of significant stress rotations (cf. 180 and 260 mbsf, Figure 4). These fractured zones may include faults that release the shear stresses affecting the surfaces. There is a slight difference in the overall breakout orientations between the hangingwall (N44.8° W) and the footwall (N49.8° W), which could be due to the megasplay fault zone behaving as a mechanical decoupling surface as a whole. The overall (average) S Hmax orientations based on the BO direction agree with the overall shortening direction (Seno et al. 1993; Miyazaki and Heki 2001).
Similar to the BO orientations, the stress magnitude shows frequent fluctuations (Figure 4), which may be due to several factors, as suggested by equation (5): UCS, pore pressure, pressure difference between borehole and rock pore, the temperature effect, and stress fields. The modified Wiebols-Cook failure criterion (see above) suggests that the internal friction should also control the failure. Other possible causes include 3D geometric problems, such as non-Andersonian stress states and inclined fault surfaces relative to the borehole.
In this study, UCS is approximated from P-wave velocity using the empirical relation (see above). The P-wave velocity from LWD geophysical logging data at C0004B shows a fluctuating pattern (Kinoshita et al. 2009), which may be induced by fractures and faults at the borehole wall. This is because of the data acquisition system of the measurement tool, which has a source and receiver for P-waves, and the time required to transmit the wave delays if any discontinuity surface with aperture exists between these sensors (Kinoshita et al. 2009). This means that the approximated UCS will be reduced where mechanically decoupled surfaces exist.
Pore pressure along the megasplay fault surface has been a major target of investigations in the Nankai Trough, and reflection seismology data have been used for this purpose (e.g., Tsuji et al. 2008; Tobin and Saffer 2009). P-wave analysis suggests that overpressure could exist beneath the megasplay fault (Tsuru et al. 2005; Tsuji et al. 2006) but should not be significant in this region (Tsuji et al. 2011). These conclusions strongly depend on the spatial resolutions of seismic data, the theoretical limit of vertical resolution, λ/4 (a quarter of the wavelength), being 5 to 7 m for near-surface sediments (Moore et al. 2007; Yamada et al. 2011); thus, there is still the possibility of elevated pore pressure along minor fault surfaces.
If we assume the pressure gradient to be hydrostatic at this site, the pressure difference between borehole and rock pore is generated by drilling mud pressure, because the drilling mud density was 1.024 (Kinoshita et al. 2009). A temporal increase in the mud pressure can be observed by the average annular pressure (APRS) profile in Figure 4, which has the effect of increasing S Hmax, but the magnitude of stress fluctuation is much more significant.
Site C0004B is located at 2,637 m of water depth and was drilled with a non-riser drilling system (Kinoshita et al. 2009), suggesting that the drilling mud may not have a significant temperature difference compared to the surrounding seawater at the ocean floor. The drilling interval at C0004B is only 400 m from the ocean floor; thus, the temperature around the borehole may also not be very different from the ocean floor temperature. These factors suggest that the temperature effect in equation (5) may be negligible.
Recent modeling studies (e.g., Yamada et al. 2014) suggest that stress fields in accretionary prisms may have temporal and spatial changes and are commonly inclined (i.e., non-Andersonian). This is primarily because of ‘stick-slip’ motion along faults that accumulates and releases elastic strain around the faults. The stress fluctuations due to such fault behavior can only be observed around active faults, and no fluctuation can be identified once fault activity has ceased. These modeling results suggest that the stress fluctuations found in this study may be associated with active faults.
The lithology at site C0004 has been reported to be mostly clay within the megasplay fault zone and in the hangingwall, based on core sample observations (Kinoshita et al. 2009). Although the core mechanical data (Table 1) show that the values of the internal friction coefficient have a variation of 30% from the average, there should not be any significant variation in the physical properties among such a small variety of rock types.
The dip of fault surfaces also has a significant impact on the breakout orientations (e.g., Shamir and Zoback 1992). This is because the orientation of the fault surface relative to the stresses defines the magnitude of release of shear stresses along the fault surface. The fracture surfaces identified in the borehole images at this site are scattered (Yamada et al. 2011); thus, this dip effect could explain the stress fluctuations.
As a result, our calculation shows that the magnitude of S V may be smaller than that of S Hmax, but within the possible range of S hmin, suggesting that the stress around this borehole would be in a reverse fault or strike-slip fault regime (Figure 4). Since S V seems to be close to the lower limit of the S hmin range, the stress at the shallow horizons (e.g., 120 mbsf) may have a higher possibility to be a reverse fault stress regime. If time-dependent failure of borehole wall due to drilling-induced overconsolidation of porous sediments (Moore et al. 2011) occurred, the magnitudes of horizontal stress that also favor thrust faulting would be even higher. These may agree with the strike-slip and thrusting motion of the megasplay fault suggested by the geometric features around the fault on seismic profiles and ocean floor topography (Tsuji et al. 2014).
Implications for identifying active fault surfaces
Yamada et al. (2013) analyzed the detailed 3D geometry of the megasplay fault and argued that the megasplay fault may have been most active around the C0004B site. Since this part of the megasplay fault is thicker than the surrounding region (Yamada et al. 2013), the fault may have been generated during a long period of activity that contributed to form several possible active zones. The active parts of the fault zone, however, cannot be identified by such geometric investigations.
The analysis in this study identified systematic rotations of stress orientation and decreases in the stress magnitude, not only within the megasplay fault zone but also in its hangingwall. Since these stress fluctuations can be explained, at least partly, by stress release along mechanically decoupled surfaces, the depths that show such fluctuations may correspond to ‘active faults’ in terms of stresses. These active faults have not been completely healed by mineral precipitation but still have the capability to reactivate, where the stresses affecting on the surface are geometrically appropriate (e.g., Sibson 1995). Identification of discrete active fault surfaces among a number of possible discontinuity surfaces around an active fault zone is generally difficult, but this study showed that not only the megasplay fault zone but also several faults in its hangingwall may also currently have the potential to reactivate at site C0004 (see arrows in Figure 4). The spatial distribution of these potential active faults could also explain the anomalous heat flow distributions at the ocean floor (e.g., Yamano et al. 2014).
The stress state analyzed with the borehole breakouts identified in the borehole wall images obtained at site C0004B in the Nankai Trough, southwest Japan, shows that there are frequent but systematic stress fluctuations, i.e., rotations in stress orientation and decreases in stress magnitude, in the megasplay fault zone and its hangingwall. These fluctuations are probably induced by stress release along fault surfaces that can be regarded as active faults in terms of stresses and may still have the capability to reactivate. The approach presented in this paper allows us to identify which fault surfaces need to be examined in detail to understand the past development processes in order to assess their potential for future activity.
We thank the editor M. Kinoshita and two anonymous reviewers for their comments and suggestions, which greatly helped to improve the manuscript. This research used data provided by the Integrated Ocean Drilling Program (IODP). Funding for this research was provided by Grants-in-Aid for Scientific Research (KAKENHI: 213101115 and 24540489) and for Scientific Research on Innovative Areas (21107002).
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