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Continuous depth profile of the rock strength in the Nankai accretionary prism based on drilling performance parameters

Abstract

A new method for evaluating the in situ rock strength beneath the seafloor is proposed and applied to the Nankai Trough accretionary prism. The depth-continuous in situ rock strength is a critical parameter for numerous studies in earth science, particularly for seismology and tectonics at plate convergence zones; yet, measurements are limited owing to a lack of drilled cores. Here, we propose a new indicator of strength, the equivalent strength (EST), which is determined only by drilling performance parameters such as drill string rotational torque, bit depth, and string rotational speed. A continuous depth profile of EST was drawn from 0 to 3000 m below the seafloor (mbsf) across the forearc basin and accretionary prism in the Nankai Trough. The EST did not show a significant increase around the forearc basin–accretionary prism boundary, but it did show a clear increase within the prism, ca. below 1500 mbsf. This result may indicate that even the shallow accretionary prism has been strengthened by horizontal compression derived from plate subduction. The EST is a potential parameter to continuously evaluate the in situ rock strength during drilling, and its accuracy of the absolute value can be improved by combining with laboratory drilling experiments.

Introduction

The in situ continuous strength of the crust is one of the most fundamental and vital information in various research fields of earth sciences. In geological and geophysical research in subduction zones in particular, the rock strength is necessary for evaluating development mechanisms of accretionary prism/forearc basins1,2, spatiotemporal variations in the stress state3,4,5, and fault reactivation potentials (slip tendency)6,7. The triaxial compression experiment is a common approach to measuring the strength of rock core materials recovered by deep-sea drilling8,9. Assumptions of the in situ stress conditions, however, are necessary for experimental strength measurements. As the experiments depend on core quality and availability, the experimentally determined strength data is intermittent and its continuous profile cannot be visualised. Even at the Nankai Trough, the most studied plate subduction zone by the Integrated Ocean Drilling Program (IODP)10, we were forced to utilise either the strength indirectly estimated through the empirical correlation between the strength and P-wave velocity or the experimental strength from limited cores11,12,13. A similar situation also arises in most offshore drilling sciences14. Despite its importance, the depth profile of in situ strength has been practically left unknown. Therefore, we propose a method for the direct and continuous measurement of the relative in situ rock strength using only drilling performance parameters. Drilling parameters can be easily obtained from any drill hole, even in non-coring and non-logging operations or in challenging environments.

Evaluation of the formation rock properties from drilling parameters such as weight on bit (WOB) and drill string rotational torque (Tr) was first proposed by Teal (1964)15 and denoted the “specific energy” (SE). SE is used mainly for drilling optimisation in resource industries and has been further developed into the mechanical specific energy16,17. Several data conversion techniques have also been proposed to evaluate the in situ rock strength during drilling with various types of bits, such as roller-cone bits18,19 and fixed-cutter bits20,21,22,23,24. Recently, in a scientific deep-sea drilling operation, the evaluation of the apparent rock frictional strength was attempted based on WOB and Tr23. These researchers discussed the relationship between the rock strength and drilling parameters, considering the bit shape and input energy, using highly accurate and well-stabilised drilling parameters23,24. On the other hand, during typical offshore drilling operations, the recorded drilling data are usually disturbed by sea undulation. Additionally, large frictional forces can occur between the seawater or borehole wall and the drill string pipe, rather than the formation rock at the drill bit. Thus, if an on-bottom measurement-while-drilling system is not implemented, the above methods cannot be applied in typical deep-sea drilling operations25.

Here, we define a background-removed mechanical parameter, the equivalent strength (EST), derived from only Tr, bit depth, and pipe rotation speed measured at the surface of the rig during drilling. The proposed method was applied to drilling data obtained from IODP Site C0002 at the Nankai Trough, which is the main site for deep drilling to the seismogenic zone, to evaluate the continuous in situ strength in the Nankai accretionary prism. This method allows estimation of the strength without assuming uncertain in situ conditions (e.g., stress and fluid pressure conditions) or using special techniques. The continuous strength was also evaluated by applying previously obtained drilling parameters, which enabled us to clarify the strength profile extracted from the limited experimental strength data.

Results

Drilling parameters at IODP Site C0002 in the Nankai Trough

The Nankai Trough is a major subduction zone where the Philippine Sea Plate is subducting beneath the Eurasian Plate at a rate of 4.1–6.5 cm/year26 (Fig. 1a). The IODP Nankai Trough Seismogenic Zone Experiment (NanTroSEIZE) Expeditions 314, 315, 332, 338, and 348 drilled 14 holes in Site C0002 from the forearc basin to the accretionary prism in order to reach the hanging wall of the plate boundary fault and the fault itself6 (Fig. 1b). Shallow non-riser drillings for both coring and logging-while-drilling (LWD) were conducted mostly in the forearc basin to investigate the physical properties, structure, and stress state. The riser drilling method was also applied in the vicinity of non-riser holes to penetrate the accretionary prism beneath the forearc basin (holes F, N, and P), and this method will be used to penetrate the megathrust in the future. Core samples and logging data collected from these holes show that the drilled formations (lithofacies) are consistent with each hole; the forearc basin consists of greenish-grey silty sandstone (0–975.5 mbsf), while the accretionary prism is composed mainly of greenish-grey silty claystone and fine silty claystone (975.5 mbsf)27. From eight holes (F, H, I, J, K, L, N, and P) drilled at Site C0002, basic drilling parameters, such as weight on bit (WOB), top drive torque, and bit depth, were recorded at the surface, and seven of these holes (excluding Hole F) were targeted in this study (Fig. 1c). The data can be accessed or requested at http://sio7.jamstec.go.jp/. Although WOB was not well stabilised at all holes, possibly because of rough seas, the rotations per minute (RPM) values showed steady rotation, and Tr showed little fluctuation and tended to increase with depth. The mechanical specific energy (MSE) calculated from the above parameters15,16 also increased with depth from 0 to ~1 GJ/m3, with large variations. The hole properties and the drill assemblies used in the drillings are summarised in Table 1. Data from hole F cannot be applied in this research because an underreamer was used during downward drilling, which may have generated extra cutting resistance. As described above, the drilling methods (riser/non-riser, coring/LWD) and conditions were quite different among the various holes (Table 1). However, in this study, the EST can be evaluated for each hole using the equations described below (see Methods section and Supplementary Table S1).

Depth profile of the EST at Site C0002

Figure 2 summarises composites of the lithologic data of the core and cuttings from the cruise reports27,28 as well as the calculated EST profile at Site C0002. The colours of the data indicate the different holes. The black line in the centre column is the running average of 5 points of aggregated data from different holes. The EST profile at all holes increases gradually with depth. The values are almost 0 MPa at the surface and 40–100 MPa at the bottom of the holes. We defined the mechanical zones (Zones A–D) based on the EST, independent of the lithological unit, to characterise the depth profiles of the EST. Zone A (0–132.3 mbsf) is the uppermost portion of the holes. The EST increases gradually to ~1 MPa by 77.6 mbsf and then increases suddenly to 6.2 MPa at the bottom of Zone A. Zone B (132.3–1458.5 mbsf) is characterised by a constant baseline for the EST of ~20 MPa. In this zone, the mean values of the EST do not show a clear change, though some positive peaks appear at 150–400 mbsf and 800–1000 mbsf. In Zone C (1442.5–2141.5 mbsf), the EST profile shows an overall steep increasing trend with larger fluctuations than in the upper zones. The amplitude of the fluctuation reaches ~39.8 MPa at around 2000–2100 mbsf, even in the running-averaged values. The EST reaches 53.7 MPa at the bottom of Zone C. In Zone D (2141.5–3011.5 mbsf; the lowest part of the holes), the mean value of the EST again tends to be constant at 2850.0 mbsf but then jumps to ~100 MPa at ~2900 mbsf. Note that the described mechanical zones do not correspond to the lithologically defined units (Fig. 2), except for Zone A, which is approximately consistent with Unit I. A major lithological boundary of unconformity between the forearc basin and accretionary prism was reported at 921.7–1025.5 mbsf27,28,29. However, the EST profile does not indicate any significant change or gap in that interval but shows a steeper baseline from around 1500 mbsf. In contrast to the large variation in the EST, the background torque shows a smooth increase from 0 to ~20 kN-m from top to bottom (Fig. 2). The slope of the background torque in Hole N is steeper than in the others, which corresponds to higher torque and RPM values (Fig. 1).

Discussion

An attempt to extract the formation mechanical properties from the drilling parameters was made as described above15,24. Comparing the EST (Fig. 2) with the MSE (Fig. 1c), the EST shows relatively stable profiles and reasonable absolute values. Many of the deviated values or large profile gaps between holes in the MSE (e.g., 2200 mbsf) are not observed in the EST. This is because the background torque consumed by different types of resistance, such as torsion of the drill strings and friction between the pipe and borehole, is approximately subtracted from the measured torque during data processing, revealing the distinct formation properties. Large fluctuations can still be seen in the EST at the depth interval of 2270–2275 mbsf (Supplementary Fig. S3). In the EST calculation, we assumed that 5 m calculation intervals consist of homogeneous formation. This assumption is not entirely satisfactory, as a visible lithological boundary was observed in the logging data in this fluctuation interval (see Methods section).

To examine the validity of the EST, we compared it with the downhole logging data of the P-wave velocity of formation10,27,28,29 (Vp) and the strength data experimentally determined in previous studies11,13 (Fig. 3). Vp is known to be correlated with unconfined compressive strength (UCS)30. The Vp logging tool used at this site is located 6–27 m above the bit10,27,28,29. Although there is a time lag of several minutes to several hours between the drilling operation and Vp measurement, it is expected that Vp shows some correlation with strength. The general depth trends of the EST and Vp are consistent (Fig. 3). Both the EST and Vp gradually increase with depth up to ~2000 m in Zones A to C, and their baselines are almost constant, particularly in Zone D. At smaller scale depth intervals (e.g., several metres in Fig. S3), the EST correlates with local fluctuations in the Vp data much more so than at larger scales, as shown in Fig. 3. All of the peaks in the Vp data do not correspond to peaks in the EST. This is because the data sampling intervals are different for the EST calculations and Vp measurements: the former is approximately 5 m, while the latter is 15 cm (see Methods section).

The core sample strengths under in situ conditions determined by triaxial compression experiments9 are consistent with the EST (red squares in Fig. 3). The experiments were conducted on intact specimens, assuming that the pore pressure is hydrostatic and the vertical stress is the minimum principal stress (i.e., reverse-fault stress regime)11. However, the current accretionary prism lies in a strike-slip faulting regime5,12. Therefore, the experimental strength may be overestimated compared to the actual in situ strength, suggesting that the EST may also be overestimated.

On the other hand, the strength estimated from the empirical Vp-porosity-strength relation13 shows smaller values compared with the EST (blue dots in Fig. 3). Kitajima et al.13 first constructed the relationship between porosity and Vp. They converted the porosity measured from core samples into the in situ porosity using the recompression index values determined by consolidation experiments on samples recovered from 553–2018 mbsf31,32,33. Extrapolating the porosity-Vp relation, they defined the in situ porosity from the seafloor to the bottom of the hole (3058.5 mbsf). The relationship between porosity and strength was also derived from triaxial experiments on siltstones from the subducting Philippine Sea Plate under two end-member loading conditions of both triaxial extension and triaxial compression32. Then, they estimated the in situ formation strength from the Vp data using the above relations, assuming loading conditions of one-dimensional vertical consolidation in the forearc basin (~ 920 mbsf) and critical state loading in the accretionary prism (920–bottom of the hole). The difference between the strength derived from the Vp-porosity-strength relation13 and the EST may arise because (1) the possible overconsolidation of sediments in the accretionary prism is not taken into account in the estimation; (2) the porosity calculated from Vp may be overestimated due to the time lag between the drilling operation and Vp measurement, as described above, which results in the estimated strength being lower than the EST; or (3) the EST may be overestimated because the EST is consistent with the triaxial strength of the sample under reverse-fault regime conditions11. It is difficult to identify the cause of the EST overestimation. One possibility is the effect of deformation rate on rock strength. As evidenced by laboratorial experiments, brittle strength is affected by strain rate; the higher strain rate is applied, the larger the strength becomes34,35,36. The experimental strength is generally determined at a displacement rate of ~ μm/s2,9,11,31,33. On the other hand, the displacement rate at a drill bit is ~ 0.3 m/s during the drilling in C0002P (12–1/4 in-diameter bit and 100 rotations-per-minute). The influence of the deformation rate on the strength of sedimentary rocks is insensitive compared to igneous rocks, however, it is reasonable to suppose that the effect is a cause of overestimation in the EST.

Theoretically, the relative value of the EST corresponds to the hardness of the drilled rock, and this is also supported by laboratory experimental data37. Hoberock and Bratcher (1996) suggested that the minimised drilling specific energy15,20 corresponding to the EST in this study can approximate the in situ compressive rock strength37,38. However, it cannot be assumed that the absolute value of the EST is equivalent to the rock strength under in situ stress conditions. The rock strength is generally measured by compression experiments in which differential stress is applied to a specimen assuming in situ stress conditions34,39. Although the EST is derived from drilling parameters that reflect the formation mechanical properties under in situ conditions, the in situ stress and pore pressure cannot be determined continuously, and hence, a verification experiment in the exact situation is not practical in principle. Thus, the EST at present should be treated as only an “equivalent strength”, which can be thought of as the relative in situ rock strength over a wide depth scale. The EST is obtained by stacking data from 5 m segments without the assumption of in situ stress conditions. Compared to laboratory experiments, which usually require intact specimens of several centimetres and supposition of the stress field, the EST has advantages of providing the relative in situ strength over a larger scale under in situ conditions, including the stress state, pore pressure and temperature. The large scale of the “drilling experiment” can reflect the representative formation strength. Numerous drilling experiments in the laboratory under various pressure and temperature conditions may allow determination of the correlation and lead to more accurate estimations of in situ formation rock strengths from the drilling parameters.

The EST profile shows characteristic positive peaks in Zone B (around 150–400 mbsf, 800–1000 mbsf, and some other depths) as well as larger amplitude fluctuations in Zones C and D. A comparison of the EST, carbonate content, and lithology at the site (Fig. 2) indicates that the local increases in the EST in Zone B may be due to strength hardening by carbonate materials. In this zone, the carbonate content is significantly higher (>20 wt%), which could make the sediments harder as a result of the cementing effect. In Zone C, the carbonate content profile shows a small peak at 1900–2000 mbsf, despite the absence of a significant spike in the EST at that depth. This could be due to the thinness of the carbonate layer, which may be too thin to affect the drilling parameters, or to the low strength contrast between the formation and carbonate layers. Sedimentological observations of cuttings did not indicate any remarkable cementation of formation in the interval27,29. This suggests that hardening due to cementation may control the strength in the forearc basin, but it is not significant in the accretionary prism.

Below lithological Unit IV ( > ~1000 mbsf), the EST profile shows larger fluctuations than the EST increases in the cementation zones. The fluctuation seems to correspond to the sand/mud ratio; the EST decreases in clay-rich intervals, likely indicating the baseline of the EST profile (e.g., around 1400 mbsf, 1800 mbsf, and 1950 mbsf).

One remarkable point is the absence of significant EST changes at the forearc basin–accretionary prism boundary (Fig. 2). This was also indicated in triaxial experiments on core samples11. The basin sediments overlying the accretionary sediments generally lie in a neutral stress state40; thus, the Kumano forearc sediments are expected to be consolidated in an isotropic manner, and the strength of the forearc sediments is expected to be smaller than that of the accretionary prism, which is older, deeper, and more consolidated by horizontal compression parallel to the subduction direction. Nevertheless, the baseline of the EST is roughly maintained at 20 MPa from 180 mbsf to 1410 mbsf across the major unit boundary and the recognised Zone B. Such strength contrast between the forearc basin and accretionary prism was not observed, likely because (1) carbonate cementation controls the strength baseline and (2) the horizontal compaction was not sufficient to strengthen the sediments in the shallow portion of the accretionary prism.

On the other hand, changes in the depth profile of the EST were observed in Zone C and around the Zone C–D boundary. The slope of the trend in Zone C (approximately 40 MPa/km) is steeper than that above 1442.5 mbsf (~20 MPa/km), and the EST maintains a high mean value (~60 MPa) in Zone D. The high EST value can be attributed to two possible effects: compaction by horizontal stress and/or diagenesis of the sediments. Common diagenetic processes in the shallow part of the accretionary prism, which consists mainly of detritus and sedimentary sand and mud, are albitisation, transitions of opal to quartz and smectite to illite, veining of quartz and carbonate minerals, and pressure solution41. Mineral measurements along Holes B, N, and P, however, do not show any significant increases in total clay or quartz abundance in the lower part of Zone B to Zone C27. Although the gradual transition of smectite to illite can be observed below ~2200 mbsf42,43, it does not explain the steeper EST increase in Zone C and the roughly stable profile in Zone D. Additionally, temperature estimation at site C0002 suggests that the in situ temperature does not exceed 100 °C, even at the bottom of the hole44, which is too low for other diagenetic processes. Structural observation of a spot core sample from 2163.0–2215.5 mbsf revealed that the bedding angle is almost vertical (~90°)27, indicating that the sediments were deformed mainly by horizontal compression. The folding of formations by compressive deformation at the shallower portion of the accretionary prism has been observed and identified by seismic images and LWD data28,45,46,47 Therefore, it is plausible that the increasing EST is caused by horizontal compression rather than mineral diagenesis. This interpretation does not mean that the sediments now experience such horizontal compression or suffer it at the present location; in fact, the accretionary prism lies in the strike faulting regime5,12.

The EST is a valuable geological-geophysical parameter because it is independent of other basic measurements, such as seismic reflection surveys and downhole logging, and is obtained without core samples or assumptions of the in situ environmental conditions. Although further study is necessary to assess the accuracy of the EST through laboratory drilling experiments, the EST analysis we presented here has significant advantage, particularly in non-core drilling or drilling in technically challenging areas, such as tectonically active margins and hydrothermal regions.

Methods

Definition of the equivalent strength (EST)

We proposed an evaluation of the depth profile of the equivalent strength (EST) to investigate continuous variations in the mechanical properties. Here, we define the EST based on the stress supplied to the formation assuming a simplified bit shape (see Supplementary Fig. S1) as:

$EST[Pa]= F a v e [ N ] h [ m ] × ( R 1 2 − R 2 2 ) [ m ]$
(1)

where F ave is the force at the cutter face when the formation brakes, h is the cutting depth, and R1 and R2 are the external and inner diameters of the drill bit, respectively. F ave can be represented by the input torque measured at the surface (T m ) and various unknown background torques (T b ), and multiplying the right-hand side of equation (1) by the radius and integrating over the working face (A) gives:

$∫ A r F a v e h ( R 1 2 − R 2 2 ) dA= ∫ R 2 2 R 1 2 r F a v e h ( R 1 2 − R 2 2 ) h d r = 1 2 F a v e ( R 1 2 + R 2 2 ) = T m − T b$
(2)

Although it is impossible to measure or estimate h at any time from the recorded drilling parameters, the drilling advance per revolution (ROP/RPM) can represent the mean value of h for each rotation. Thus, the right-hand side of equation (1) can be rewritten using the recorded drilling parameters as:

$EST[Pa]= 2 ( T m − T b ) R O P R P M { ( R 1 2 ) 2 − ( R 2 2 ) 2 }$
(3)

Strictly, the work of the weight on the bit (WOB) is also consumed to deform or break the formation at the bottom of the hole during drilling. If the drilled formation is weak enough and easily fragmented or deformed by vertical loading, the work of the WOB should be added next to the right-hand term of equation (3). However, the work of the WOB is generally negligible compared to the rotary work15. Equation (3) has the same style in principle as the mechanical specific energy (MSE) and the drillability strength of rock (Ds) proposed by previous reports15,34, despite the different definitions and derivations. The EST represents a generalised form of these parameters, taking the background torque and inner diameter of a PCD bit.

It is difficult to measure or estimate T b directly because it is a composite of torque losses, such as from friction between the pipe and formation, lateral acceleration, whirl, pipe torsion, fluid resistance, and so on. To eliminate these unknown toque losses and to estimate EST independently, equation (3) can be modified to provide a formula for the measured torque by the rate of penetration:

$2 T m ×RPM=ROP× { ( R 1 2 ) 2 − ( R 2 2 ) 2 } ×EST+2 T b ×RPM$
(4)

In this equation, EST represents the gradient of the relationship between the measured torque energy per minute (left-hand term) and the volume rate of penetration. The stack of torque losses is shown by the intercept of the relation.

Procedure of the EST calculation

Before applying the data collected at the C0002 holes to this equation, the data were resampled as mean values over 1 minute at every 10 seconds to reduce noise. Cross plots were created for each 5 m on the basis of the assumption that the formation properties are roughly homogeneous within the interval. If the mechanical properties are heterogeneous in the 5 m interval, the torque and the drilled volume will not be proportional, and equation (4) cannot be applied. In the ROP variation in the interval is small, a regression line cannot be determined, and the data cannot be used in the calculation. Therefore, we performed correlation analysis for each plot, and the EST and Tb were calculated when the correlation coefficient (R) was >0.4 and the p-value was <0.05 (5%). Examples of the torque-volume relations for the Nankai Trough drillings are shown in Supplementary Fig. S2.

The calculated EST profile (Fig. 2) fluctuates despite the above processing. To verify the cause of the variation, the validity of the EST is checked over the closed section at 2270–2275 mbsf, where the calculated EST is large (~122 MPa; Supplementary Fig. S3). In this 5-m section, two clusters are identified, and they follow each optimal fit line (Fig. S3a). These clusters are separated by 2272.1 mbsf. The trends in the logging data also change depending on the depth (Fig. S3b–e), indicating that the muddy (high gamma ray; GR, low resistivity, low Vp) and easy-to-collapse (large calliper) formation gradually changes to a sandy and harder formation. The EST for the muddy (2270.0–2272.1 mbsf) and sandy (2272.1–2275.0 mbsf) regions was calculated as 25.0 MPa and 45.3 MPa, respectively. The clustering corresponds to the lithological boundary, and the EST values calculated from each cluster seem to correspond to each lithological feature. All data in this 5 m section were fitted with one line, satisfying the above significance criteria, and a very large EST was automatically calculated (black line in Fig. S3a). Thus, the EST includes variations due to section partitioning for automatic calculation. To avoid this problem, it is desirable to reduce the calculation interval to less than 5 m, shorter than the thickness of each lithofacies, for example, to several tens of centimetres. However, if the calculation interval is decreased to be applied to each lithology, the correlation line of each cluster cannot be obtained due to the small number of data points. Since 5 m is the minimum interval allowing sufficient correlation and to avoid artificial data selection from the Nankai data, we do not focus on each variance in the EST but use a moving average value for interpretation. By using more frequent data or more complex criteria for the lithology data, it would be possible to reduce variations in the EST.

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References

1. 1.

Dahlen, A. F. Critical taper model of fold-thrust belts and accretionary wedges. Annu. Rev. Earth Planet. Sci. 18, 55–99 (1990).

2. 2.

Kamiya, N. et al. Major variations in vitrinite reflectance and consolidation characteristics within a post-middle Miocene forearc basin, central Japan. Tectonophysics 710–711, 69–80 (2017).

3. 3.

Davis, D., Suppe, J. & Dahlen, A. F. Mechanics of fold-and-thrust belts and accretionary wedges. J. Geophys. Res. 88, 1153, https://doi.org/10.1029/JB088iB02p01153 (1983).

4. 4.

Dahlen, A. F. Noncohesive critical Coulomb wedges: an exact solution. J. Geophys. Res. 89, 10125, https://doi.org/10.1029/JB089iB12p10125 (1984).

5. 5.

Huffman, K. A., Saffer, M. D. & Dugan, B. In situ stress magnitude and rock strength in the Nankai accretionary complex: a novel approach using paired constraints from downhole data in two wells. Earth, Planets and Space 68, 123, https://doi.org/10.1186/s40623-016-0491-4 (2016).

6. 6.

Morris, A., Ferrill, D. & Henderson, D. Slip-tendency analysis and fault reactivation. Geology 24, 275–78 (1996).

7. 7.

Van Tuyl, J., Alves, T. M. & Moore, G. F. Strain decoupling reveals variable seismogenic risk in SE Japan (Nankai Trough). Geochem. Geophys. Geosyst. 16, 2025–2037, https://doi.org/10.1002/2015GC005778 (2015).

8. 8.

Zhang et al. The brittle-ductile transition in porous sedimentary rocks: geological implications for accretionary wedge aseismicity. J. Struct. Geol. 15, 819–830 (1993).

9. 9.

Kitajima, H., Chester, M. F. & Biscontin, G. Mechanical and hydraulic properties of Nankai accretionary prism sediments: Effect of stress path. Geochem. Geophys. Geosyst. 13, Q0AD27, https://doi.org/10.1029/2012GC004124 (2012).

10. 10.

Hirose, T. et al. NanTroSEIZE Stage 3: NanTroSEIZE plate boundary deep riser 3. IODP Sci. Prosp. https://doi.org/10.2204/iodp.sp.348.2013 (2013).

11. 11.

Takahashi, M. et al. Contrasting hydrological and mechanical properties of clayey and silty muds cored from the shallow Nankai Trough accretionary prism. Tectonophysics 600, 63–74, https://doi.org/10.1016/j.tecto.2013.01.008 (2013).

12. 12.

Chang, C. & Song, I. Present-day stress states underneath the Kumano basin to 2 km below seafloor based on borehole wall failures at IODP site C0002, Nankai accretionary wedge. Geochem. Geophys. Geosyst. 17, 4289–4307, https://doi.org/10.1002/2016GC006562 (2016).

13. 13.

Kitajima, H. et al. In Situ Stress and Pore Pressure in the Deep Interior of the Nankai Accretionary Prism, Integrated Ocean Drilling Program Site. Geophys. Res. Lett. 44, 9644–9652, https://doi.org/10.1002/2017GL075127 (2017).

14. 14.

Roller, S., Pohl, C. & Behrmann, J. H. Data report: Triaxial shear strength investigations of sediments and sedimentary rocks from the Japan Trench, ODP Leg 186. In Suyehiro, K., Sacks, I. S., Acton, G. D., & Oda, M. (Eds), Proc. ODP, Sci. Results 186, 1–19 (2003).

15. 15.

Teale, R. The concept of specific energy in rock drilling. Int. J. Rock Mech. Min. 2, 57–73 (1965).

16. 16.

Dupriest, F. E. & Koederitz, W. L. Maximizing drill rates with real-time surveillance of mechanical specific energy. SPE/IADC Drilling Conference 23–25, 1–10, https://doi.org/10.2118/92194-MS (2005).

17. 17.

Bevilacqua, M., Ciarapica, F. & Marchetti, B. Acquisition, processing and evaluation of down hole data for monitoring efficiency of drilling processes. J. Pet. Sci. Technol. Res. 2, 49–56 (2013).

18. 18.

Bingham, M. G. How rock properties are related to drilling. Oil & Gas Journal 62, 94, 96–98, 101 (1964).

19. 19.

Wolcott, D. S. & Bordelon, D. R. Lithology determination using downhole bit mechanics data. SPE 26492, the 68th ATCE of the SPE, 769–778 (1993).

20. 20.

Pessier, R. C. & Fear, M. J. Quantifying common drilling problems with mechanical specific energy and a bit-specific coefficient of sliding friction. SPE 24584, the 67th Annual Technical Conference and Exhibition of the SPE 373–388 (1992).

21. 21.

Warren, T. M. Drilling model for soft-formation bits. J. Pet. Technol. 33, 963–969 (1981).

22. 22.

Detournay, E. & Defourny, P. A phenomenological model for the drilling action of drag bits. Int. J. Rock Mech. Min. Sci. Geomech. Abstr. 29, 13–23 (1992).

23. 23.

Ujiie, K., Inoue, T. & Ishiwata, J. High-velocity frictional strength across the Tohoku-Oki megathrust determined fromsurface drilling torque, Geophys. Res. Lett. 43, https://doi.org/10.1002/2016GL067671 (2016).

24. 24.

Wyering, L. D. et al. Using drilling and geological parameters to estimate rock strength in hydrothermally altered rock —A comparison of mechanical specific energy, R/N-W/D chart and Alteration Strength Index. Geothermics 69, 119–131, https://doi.org/10.1016/j.geothermics.2017.05.008 (2017).

25. 25.

Belkacem L. et al. Tensile and Torsional Loads Stress Distribution Along the Drill String for Deep Wells. In: Oral A., Bahsi Oral Z., Ozer M. (eds) 2nd International Congress on Energy Efficiency and Energy Related Materials (ENEFM2014). Springer Proceedings in Energy. Springer, Cham (2015).

26. 26.

Heki, K. & Miyazaki, S. Plate convergence and long-term crustal deformation in central Japan. Geophys. Res. Lett. 28(12), 2313–2316 (2001).

27. 27.

Tobin, H. et al. Site C0002. In Tobin, H. et al. Proc. IODP, 348. Integrated Ocean Drilling Program https://doi.org/10.2204/iodp.proc.348.103.2015 (2015).

28. 28.

Kinoshita, M. et al. Proc. IODP, 314/315/316. Integrated Ocean Drilling Program Management International, Inc. https://doi.org/10.2204/iodp.proc.314315316.2009 (2009).

29. 29.

Strasser, M. et al. Site C0002. In Strasser, M. et al. Proc. IODP, 338. Integrated Ocean Drilling Program https://doi.org/10.2204/iodp.proc.338.103.2014 (2014).

30. 30.

Horsrud, P. Estimating mechanical properties of shale from empirical correlations. SPE Drilling & Completion 16(2), 68–73 (2001).

31. 31.

Guo, J. et al. Data report: Consolidation characteristics of sediments from Sites C0002, C0006, and C0007, IODP Expeditions 315 and 316, NanTroSEIZE Stage 1. In M. Kinoshita et al. (Eds), Proceedings of the Integrated Ocean Drilling Program (Vol. 314/315/316). Washington, DC: Integrated Ocean Drilling Program Management International, Inc. https://doi.org/10.2204/iodp.proc.314315316.213.2011 (2011).

32. 32.

Kitajima, H. & Saffer, D. M. Elevated pore pressure and anomalously low stress in regions of low frequency earthquakes along the Nankai Trough subduction megathrust. Geophys. Res. Lett. 39, L23301, https://doi.org/10.1029/2012GL053793 (2012).

33. 33.

Kuo, S. T., Kitamura, M., & Kitajima, H. Evolution of mechanical properties and microstructures in the inner accretionary prism of the Nankai Subduction Zone. Abstract T51B-2901 Presented at the 2016 AGU Fall Meeting, San Francisco, CA, 12–16 Dec. (2016).

34. 34.

Paterson, M. S., & Wong, T-F. Experimental rock deformation: The brittle field, 2nd edn. Springer-Verlag, Berlin (2005).

35. 35.

Xia, K. & Yao, W. Dynamic rock tests using split Hopkinson (Kolsky) bar system-A review. Journal of Rock Mechanics and Geotechnical Engineering 7, 27–59 (2015).

36. 36.

Zhou, Y. X. et al. Suggested methods for determining the dynamic strength parameters and mode-I fracture toughness of rock materials. International Journal of Rock Mechanics and Mining Sciences 49, 105–112 (2012).

37. 37.

Karasawa, H., Ohno, T., Kosugi, M. & Rowley, C. J. Methods to estimate the rock strength and tooth wear while drilling with roller-bits—Part 1: Milled-Tooth Bits. J. Energy Resour. Technol. 124/125, https://doi.org/10.1115/1.1482405 (2002).

38. 38.

Hoberock, L. L. & Bratcher, G. J. A new approach for determining in-situ rock strength while drilling. ASME J. Energy Resour. Technol. 118, 249–255 (1996).

39. 39.

Jaeger, J. C., Cook, N. G. W. & Zimmerman, R. W. Fundamentals of Rock Mechanicsfourth edition. Blackwell, Malden, Mass. (2007).

40. 40.

Wang, K., Hu, Y. Accretionary prisms in subduction earthquake cycles: the theory of dynamic Coulomb wedge. J. Geophys. Res. 111, B0641010.1029/2005JB004094 (2006).

41. 41.

Dixon, T. H. & Moore, J, C. editors. The seismogenic zone of subduction thrust faults. Columbia University Press. https://doi.org/10.7312/dixo13866 (2007).

42. 42.

Underwood, M.B. Data report: clay mineral assemblages and illite/smectite diagenesis in cuttings from Hole C0002P, IODP Expedition 348, Nankai Trough accretionary prism. In Tobin, H. et al. Proceedings of the Integrated Ocean Drilling Program, 348. College Station, TX (Integrated Ocean Drilling Program). https://doi.org/10.2204/iodp.proc.348.204.2017 (2017).

43. 43.

Underwood, M. B. Data report: clay mineral assemblages in cuttings from Hole C0002N, IODP Expedition 348, Nankai Trough accretionary prism. In Tobin, H. et al. Proceedings of the Integrated Ocean Drilling Program, 348: College Station, TX (Integrated Ocean Drilling Program). https://doi.org/10.2204/iodp.proc.348.203.2017 (2017).

44. 44.

Sugihara, T. et al. Re-evaluation of temperature at the updip limit of locked portion of Nankai megasplay inferred from IODP Site C0002 temperature observatory. Earth, Planets and Space 66, https://doi.org/10.1186/1880-5981-66-107 (2014).

45. 45.

Moore, G. F., Boston, B. B., Strasser, M., Underwood, B. M. & Ratliff, A. R. Evolution of tectono-sedimentary systems in the Kumano Basin, Nankai Trough forearc. Mar. Pet. Geol. 67, 604–616, https://doi.org/10.1016/j.marpetgeo.2015.05.032 (2015).

46. 46.

Boston, B., Moore, F. G., Jurado, J. M. & Sone, H. Deformation of the Nankai Trough inner accretionary prism: The role of inherited structures. Geochem. Geophys. Geosyst. 17, 485–500, https://doi.org/10.1002/2015GC006185 (2016).

47. 47.

Yamada, Y., McNeill, L., Moore, C. J. & Nakamura, Y. Structural styles across the Nankai accretionary prism revealed from LWD borehole images and their correlation with seismic profile and core data: Results from NanTroSEIZE Stage 1 expeditions. Geochem. Geophys. Geosyst. 12, Q0AD15, https://doi.org/10.1029/2010GC003365 (2011).

48. 48.

Kikuchi, M., Nakamura, M., Yoshikawa, K., Source rupture processes of the 1944 Tonankai earthquake and the 1945 Mikawa earthquake derived from low-gain seismograms. Earth Planets and Space 55(4), 159–172 (2003).

49. 49.

Hamada, Y. et al. Estimation of slip rate and fault displacement during shallow earthquake rupture in the Nankai subduction zone. Earth Planets and Space 67, 39, https://doi.org/10.1186/s40623-015-0208-0 (2015).

Acknowledgements

We are grateful to Dr. W. Tanikawa for his repeated help with the numerical calculations. We greatly appreciate the advice given by Dr. Hiroko Kitajima in designing the calculations. This study is supported by JSPS KAKENHI grant 16H04064, 15H05717, and a grant-in-aid for Fellows of the Japan Society for the Promotion of Science (JSPS) 14J06074.

Author information

Author notes

• Manami Kitamura

Present address: Geological Survey of Japan, National Institute of Advanced Industrial Science and Technology (AIST), 1-1-1 Higashi, Tsukuba, 305-8567, Japan

Affiliations

1. Kochi Institute for Core Sample Research, Japan Agency for Marine-Earth Science and Technology, 200 Monobe-otsu, Nankoku, Kochi, 783-8502, Japan

•  & Takehiro Hirose
2. Department of Earth and Planetary Systems Science, Graduate School of Science, Hiroshima University, 1-3-1 Kagami-yama, Higashi-Hiroshima, 739-8526, Japan

• Manami Kitamura
3. Research and Development Center for Ocean Drilling Science, Japan Agency for Marine-Earth Science and Technology, 3173-25, Showa-machi, Kanazawa-ku, Yokohama-city, Kanagawa, 236-0001, Japan

• , Saneatsu Saito
• , Kyaw Moe
•  & Takehiro Hirose
4. The Center for Deep Earth Exploration, Japan Agency for Marine-Earth Science and Technology, 3173-25, Showa-machi, Kanazawa-ku, Yokohama-city, Kanagawa, 236-0001, Japan

•  & Takamitsu Sugihara

Contributions

Y.H., S.S., K.M. and Y.Y designed and supervised the research. Y.H., Y.S. and T.S. performed the data processing and calculations. Y.H., M.K. and T.H. wrote the paper, and all authors reviewed the manuscript.

Competing Interests

The authors declare no competing interests.