- Full paper
- Open Access
Stress reversal recorded in calcite vein cuttings from the Nankai accretionary prism, southwest Japan
© Takeshita et al.; licensee Springer. 2014
- Received: 7 March 2014
- Accepted: 14 October 2014
- Published: 29 October 2014
The Nankai Trough subduction zone in southwest Japan is a typical convergent margin where the Philippine Sea plate subducts in the northwest direction beneath the Eurasian plate, and devastating earthquakes have repeatedly occurred in this region in the past. In order to investigate the evolution of the stress state in the subduction zone, we analyzed deformation microstructures and the preferred orientation of calcite grains in two cuttings of calcite veins from Hole C0002F that was drilled through the inner wedge of the Nankai accretionary prism during the Integrated Ocean Discovery Program (IODP) Expedition 338 in 2012. For both samples collected at depths of 1,085.5 and 1,885.5 meters below the sea floor (mbsf), the c-axes of calcite grains are preferentially oriented perpendicular to the vein wall, which is indicative of competitive growth of calcite during the vein opening caused by a vein normal extension. Also, mechanical e-twins were developed in both samples, and these are inferred to have been developed under the same stress field as that responsible for the formation of calcite veins based on the paleostress analyses in grains with e-twins. For the calcite vein retrieved at the depth of 1,885.5 mbsf, kink bands were also developed by the compression in the direction perpendicular to the vein wall, which is indicative of stress reversal after the formation of mechanical e-twins. Although we could not reach a definite conclusion for the cause of the stress reversal, it could have occurred during either fold development or seismic cycles in the Nankai accretionary prism.
- IODP expedition 338
- Nankai accretionary prism
- Calcite vein
- Stress reversal
- Paleostress analyses
Subduction zones, which are areas where an oceanic plate subducts underneath a continental or oceanic plate, are well-known places for the generation of large-scale earthquakes and magma production leading to arc volcanism. The Nankai Trough is formed by the subduction of the Philippine Sea plate in the northwest direction beneath the Eurasian plate at a rate of 4 to 6 cm/y (Seno et al. ; Miyazaki and Heki, ). Additionally, sediments of the Shikoku Basin, which opened as a back-arc basin behind the Izu-Bonin arc-trench system between 26 to 15 Ma (Chamot-Rooke et al. ), are actively accreting at the plate boundary and forming a modern accretionary prism. Devastating earthquakes have recently repeatedly occurred at three major districts called the Tokai, Tonankai, and Nankai districts from east to west along the subduction zone beneath the Nankai Trough (e.g., Ando, ; Park and Kodaira, ). The Nankai Trough Seismogenic Zone Experiments (NanTroSEIZE) project of the Integrated Ocean Drilling Program, now called the International Ocean Discovery Program (IODP), has been designed so that the processes and mechanisms of subduction zone earthquakes and tsunamis can be clarified through multidisciplinary approaches including geophysical logging, in situ geochemical observations, and sedimentological and structural observations of retrieved cores and cuttings (e.g., Tobin and Kinoshita, ; Moore et al.). With these approaches, much attention has been paid to analyses of the stress magnitude and orientation in the Nankai accretionary prism in order to understand the processes of interseismic stress accumulation (e.g., Kinoshita and Tobin, ) caused by plate convergence that result in the Nankai megaearthquakes. These analyses involve borehole breakout and drilling-induced tensile fractures (Lin et al. ), stress inversion from micro-fault sets with striations (Lewis et al.), the anelastic strain recovery (ASR) method (Byrne et al.; Yamamoto et al.), and various geophysical models (e.g., Wu et al. ).
In this paper, we present the analyses of the microstructures in calcite veins that occur in two cutting samples of mudstones retrieved by riser drilling through Hole C0002F during the IODP Expedition 338 in 2012. We clearly document the reversal of the stress field based on analyses of microstructures in one of the calcite vein samples, and then, we discuss the origin of such stress reversal in the Nankai accretionary prism.
Geological setting and sample description
Unit III (875.5 to 918.5 mbsf) is mainly composed of clay- to silt-rich sediments, with occasional thin, interbedded sand layers. Logging unit III identified in Hole C0002F correlates with Hole C0002A unit III defined during Expedition 314 (Expedition 314 Scientists, ), and also unit III in Hole C0002B, which was interpreted as basal Kumano Basin forearc sediment (Expedition 315 Scientists, ). While unit IV (918.5 to 1,638 mbsf) is composed of the alternations of thick sand-rich and mud-rich sediments with the variable sand ratios, unit V (1,638 to 2,005.5 mbsf) consists of homogeneous mud-rich sediments. Both units IV and V constitute the inner wedge of the Nankai Miocene accretionary prism.
For deformation structures, vein structures (Figure F10C of Moore et al.), which are similar to deformation bands (Figure F10D of Moore et al.) and not mineral veins such as the carbonate veins described in this study, were observed in cores and cuttings exclusively from unit III in Holes C0002F and C0002J. For units IV and V of the accretion prism, cuttings with slickenlined surface and carbonate veins occur, and these indicate the styles of deformation in the accretion prism (Moore et al.). Frequency distributions versus the depths of cuttings with these deformation structures are summarized in Figure 1c.
For mudstone cuttings with carbonate veins, which we described on board during the IODP Expedition 338, it was later discovered that almost all of the carbonate veins are felsic tuffs, which consist of glass shards and a very fine-grained matrix. While the very fine-grained matrix, which could have been also originally very fine-grained glass, has now been completely altered to calcite, the coarse-grained glass shards have only been partly altered to calcite. Occurrences of felsic tuffs, the composition of glass shards, and deformation microstructures in felsic tuffs will be reported elsewhere. Since calcite veins occur in the felsic tuffs as mentioned below, calcium carbonate was perhaps dissolved into pore fluids in the rocks and then precipitated in extension fractures forming calcite veins. We found only two calcite vein samples among all the cuttings during the expedition; the samples, CV-1 and CV-2, were collected from cutting samples of 56-SMW (drill bit depth, 1,085.5 mbsf) and 258-SMW (1,885.5 mbsf), respectively (Figure 1).
The results of the paleostress analysis with mechanical e-twins will be described below. While the occurrence of e-twins with a certain width in calcite grains is obvious in sample CV-1 (Figure 2c), their occurrence is not so clear in sample CV-2 under a petrographic microscope at low magnifications (Figure 2d). However, the very fine hair-like microstructures, which are oblique to the vein wall at low angles, can be clearly observed at high magnifications in sample CV-2 (Figure 2g). While these linear structures usually occur as a set of parallel lines in each of the fibrous grains, two sets of parallel lines in the different directions are sometimes developed in single grains in sample CV-2 (Figure 2d,g). Similarly, two sets of e-twins are sometimes developed in single grains in sample CV-1 (Figure 2c). These structural elements are in fact mechanical e-twins, which have been verified by the fact that the measured host c-axis and pole to e-twin orientations make an angle close to the fixed orientation of 26.25°. Here, mechanical e-twins were even formed at shear stresses as low as 10 MPa at room temperatures, and no other slip systems such as r-slip systems that can be activated at conditions higher than 100 MPa (Turner et al.) were in operation, as evidenced by the absence of wavy extinction. Hence, the magnitude of shear stresses, which is inferred to have varied between 10 to 100 MPa, cannot be constrained to a narrow range in the present calcite veins. Alternatively, Rybacki et al. () proposed a paleopiezometer as a function of e-twin density in calcite based on deformation experiments. According to their results, the measured twin densities of c. 100/mm and c. 140/mm in calcite grains from samples CV-1 and CV-2 are converted to very high differential stresses of c. 200 MPa and c. 230 MPa, respectively.
For sample CV-1, the inferred extension directions from the e-twin method are mostly oriented perpendicular to the vein wall, the preferred orientation of which is similar to that of the c-axis orientations, while the compression directions are parallel to the vein wall, although they are fairly scattered (Figure 3b). For sample CV-2, the extension and compression axes are oriented very similar to those in sample CV-1 and are much more concentrated, although the number of data points is scarce (Figure 3b). These orientations of principal stresses can also be easily inferred because of the bisectors of obtuse and acute angles of the crossing of two e-twins in single grains (Figure 2c,g), which are the directions of the extension and compression axes that are oriented in those directions mentioned above, respectively.
The preferred orientation of the c-axis perpendicular to the vein wall in both samples is probably caused by anisotropic growth (i.e., dependence of the growth rate on crystallographic orientation) of calcite grains from the solution. It is known that for quartz veins, the similar preferred orientation was developed as the constituting quartz aggregates precipitated from the solution (e.g., Takeshita and Hara, ; Nishikawa and Takeshita, ). The wall rocks consisting of calcite produced by the alterations of felsic tuff were dissolved into the fluid, which percolated along the extension fractures created parallel to the vein wall. The calcite crystals for both vein samples started to grow from the surface of the vein wall by using the crystals along it as seed crystals (i.e., syntaxial growth) as the extension fractures opened. Here, the growth of calcite crystals mainly occurred in the direction of the vein opening, and those calcite grains with a c-axis parallel to the opening direction grew faster than those with other orientations (i.e., competitive growth, Passchier and Trouw, ; Bons et al. ). As a result, the grains favorably oriented for growth became dominant as the veins widened, which led to the c-axis preferred orientation parallel to the vein opening direction (Figures 4 and 5). In fact, the grain size of calcite in sample CV-1 increased toward the center of the vein because the grains favorably oriented for growth grew faster via competitive growth during the vein opening. This interpretation is evidenced by the difference in preferred c-axis orientations between the fine- and coarse-grained parts, where the preferred c-axis orientation in the latter part is more closely oriented in the vein normal orientation than in the former part (Figures 2 and 4). We do not know the origin of the preferred c-axis orientation in the fine-grained part, which may have been inherited from that in calcite aggregates constituting the matrix of wall rocks. However, the difference in grain shapes in the veins, such as blocky versus fibrous shapes, has been interpreted in the following way. Following Urai et al. () and Oliver and Bons (), it is interpreted that veins consisting of fibrous grains were formed when the vein opening was by small increments, while blocky ones were formed when the rate of wall rock displacement surpasses that of crystal growth.
For sample CV-2, it has been shown that two microstructures, kink bands and mechanical e-twins, are developed in calcite grains. The kink bands were developed by the compression parallel to the long axis of fibrous calcite grains (i.e., buckling, Ramsay, ), and hence, it is perpendicular to the vein wall. The fact that fluid inclusions are concentrated in some parts of the kinked bands elongated parallel to the fiber long axis suggests that dilation occurred normal to the fiber long axis, thereby providing evidence that these microstructures that are correlated with dilation veins in a kink band (Ramsay, ) are in fact caused by kinking. Further, brittle fractures were formed along the axial plane of kink folds (Figure 2d), which indicates that the formation of kink bands (or folds) was accommodated by brittle fractures under very low temperatures. Therefore, the possibility that the apparently curved fiber veins were formed by a change in the opening direction of the veins (e.g., Passchier and Trouw, ; Bons et al. ) can be completely rejected.
Conversely, the mechanical e-twins with the pole orientation that makes small angles to the fibers long axis in the calcite grains, which is nearly parallel to the c-axis, were formed in CV-2, which indicates extension parallel to the fibers long axis. Therefore, it can be inferred that the fibrous grains in CV-2 were first formed by vein opening followed by precipitation of fibrous calcite grains, which was further followed by the formation of e-twins under extension perpendicular to the vein wall. Subsequently, the veins were compressed in the direction perpendicular to the vein wall, and kink bands and brittle fractures were formed along the axial plane of the kink folds, which indicates that the stress direction perpendicular the vein wall was reversed. In fact, the orientations of mechanical e-twins are rotated more than 10° about the axis of kink bands, thus showing the validity of the inferred order of microstructural development.
Other possible explanations for the stress reversal are related to seismic cycles. The Mw 9.0 Tohoku-Oki earthquake occurred off the Pacific coast of northeast Japan on March 11, 2011. Since this megaearthquake, some unexpected inland earthquakes have occurred along the Pacific coast of northeast Japan, which are mostly of the normal-faulting type including the April 11, 2011 Mw 6.6 Iwaki earthquake (e.g., Kato et al.; Okada et al. ; Fukushima et al.). These earthquakes are unusual because the hypocenters had been under a weak E-W compression before the megaearthquake, which changed to an E-W extension after it. These unusual earthquakes were interpreted to have been caused by the stress changes resulting from the release of elastic strain energy at places where the differential stresses were very low at an order of 1 MPa (Hasegawa et al.; Yoshida et al.). Therefore, it is possible that the repetition of compression and extension during the seismic cycles also occurred in the past along major subduction zones in the world, including the Nankai one, if the differential stresses were as low as that in the Tohoku forearc region before the earthquakes.
Alternatively, Sibson () interpreted this stress reversal associated with the Tohoku-Oki earthquake by the fault valve model (Sibson, ), where the pore fluid pressure is built up before the earthquake, and this lowers the effective normal stress and results in seismic rupture on the fault plane. According to his model, although the stress field in the forearc hanging wall above the megathrust was in an E-W horizontal compression state and a vertical extension before the Tohoku-Oki earthquake, that was switched to an E-W horizontal extension and vertical compression immediately after the earthquake due to the release of horizontal stress and fluid discharge leading to a decrease in the pore fluid pressure. Fluids, which were discharged from the megathrust, are inferred to have percolated along the vertical cracks under the horizontal, extensional stress in the hanging wall. In fact, such vertical, extensional fault-fracture systems of different scales were reported from ancient accretionary prisms where fluid percolation along the fractures was exemplified by the formation of mineral veins precipitated from the solution. Sibson () argued that different scales of extensional fault-fracture systems exist, which depend on the degree of release of seismic energy, and for example, one can refer to the large-scale Alsaska-Juneau Au deposit hosted by quartz veins (Goldfarb et al.; Miller et al.) and the small-scale quartz-carbonate veins in the Nobeoka thrust zone in the Shimanto accretionary complex in Kyushu, Japan (Yamaguchi et al.). The forearc horizontal extension immediately after the earthquakes is again succeeded by horizontal compression when the fractures along the megathrust are sealed by mineral veins and the strength is recovered. Therefore, the stress reversal in the present calcite vein sample can be also interpreted in this way. However, if the present calcite vein is originally formed in the horizontal direction associated with the buildup of pore fluid pressure along the megthrust, the stress reversal is caused immediately after the earthquake when the vertical stress is switched from σ3 to σ1. Although we cannot determine which model is most likely for the present case, it is worthwhile mentioning that such a stress reversal has been found for the first time at depths reaching up to 2,000 mbsf in the presently forming accretionary prism, and the exact cause for this might be deciphered if the oriented core samples with a known kinematic framework are analyzed in the future.
Deformation microstructures and preferred orientations of calcite grains in two calcite vein samples from Hole C0002F drilled at depths of 1,085.5 and 1,885.5 mbsf during the IODP Expedition 338 in 2012 were analyzed. For both samples, the c-axes of calcite grains are preferentially oriented perpendicular to the vein wall, which is indicative of competitive growth of calcite during the vein opening caused by vein normal extension. Additionally, mechanical e-twins are developed in both samples, which are inferred to have been developed under the same stress field as that responsible for the formation of calcite veins based on the paleostress analyses in grains with e-twins. For the calcite vein retrieved at the depth of 1,885.5 mbsf, kink bands that developed by compression in the direction perpendicular to the vein wall are also present, which is indicative of stress reversal after the formation of mechanical e-twins. Although we could not definitely reach a conclusion about the cause of the stress reversal at the present time, it could have occurred during either the development of folds or seismic cycles in the Nankai accretionary prism, and this can be analyzed using the oriented core samples in the future.
We thank Dr. W. Lin and an anonymous reviewer for their constructive review of the manuscript. This research used samples and data provided by the Integrated Ocean Drilling Program, now called the International Ocean Discovery Program (IODP). The authors thank Drs. M. Strasser, B. Dugan, K. Kanagawa, G. F. Moore, S. Toczko, L. Maeda, the IODP Expedition 338 scientists, the onboard laboratory technicians (Marine Works Japan), and the operation staff of D/V Chikyu for their assistance during our research.
- Ando M: Source mechanisms and tectonic significance of historical earthquakes along the Nankai Trough, Japan. Tectonophysics 1975, 27: 119–140. 10.1016/0040-1951(75)90102-XView ArticleGoogle Scholar
- Bons PD, Elburg MA, Gomez-Rivas E: A review of the formation of tectonic veins and their microstructures. J Struct Geol 2012, 43: 33–62. 10.1016/j.jsg.2012.07.005View ArticleGoogle Scholar
- Byrne TB, Lin W, Tsutsumi A, Yamamoto Y, Lewis JC, Kanagawa K, Kitamura Y, Yamaguchi A, Kimura G: Anelastic strain recovery reveals extension across SW Japan. Geophys Res Lett 2009., 36: doi:10.1029/2009GL040749Google Scholar
- Chamot-Rooke N, Renard V, LePichon X: Magnetic anomalies in the Shikoku Basin: a new interpretation. Earth Planet Sci Lett 1987, 83: 214–228. 10.1016/0012-821X(87)90067-7View ArticleGoogle Scholar
- Dietrich JH, Carter NL: Stress-history of folding. Am J Sci 1969, 267: 129–154. 10.2475/ajs.267.2.129View ArticleGoogle Scholar
- Kinoshita M, Tobin H, Ashi J, Kimura G, Lallemant S, Screaton EJ, Curewitz D, Masago H, Moe KT (Eds): Expedition 314 Site C0002 In Proc. IODP, 314/315/316. Integrated Ocean Drilling Program Management International, Inc, Washington, DC; 2009. doi:10.2204/iodp.proc.314315316.114.2009Google Scholar
- Kinoshita M, Tobin H, Ashi J, Kimura G, Lallemant S, Screaton EJ, Curewitz D, Masago H, Moe KT (Eds): Expedition 315 Site C0002 In Proc. IODP, 314/315/316. Integrated Ocean Drilling Program Management International, Inc, Washington, DC; 2009. doi:10.2204/iodp.proc.314315316.124.2009Google Scholar
- Fukushima Y, Takada Y, Hashimoto H: Complex ruptures of the 11 April 2011 Mw6.6 Iwaki earthquake triggered by the 11 March 2011 Mw9.0 Tohoku earthquake, Japan. Bull Seismol Soc Am 2013, 103: 1572–1583. 10.1785/0120120140View ArticleGoogle Scholar
- Goldfarb RJ, Leach DL, Pickthorn WJ, Paterson CJ: Origin of lode-gold deposits of the Juneau gold belt, southeastern Alaska. Geology 1988, 16: 440–443. 10.1130/0091-7613(1988)016<0440:OOLGDO>2.3.CO;2View ArticleGoogle Scholar
- Hasegawa A, Yoshida K, Okada T: Nearly complete stress drop in the 2011 Mw 9.0 off the Pacific coast of Tohoku Earthquake. Earth Planets Space 2011, 63: 703–707. 10.5047/eps.2011.06.007View ArticleGoogle Scholar
- Kato A, Sakai S, Obara K: A normal-faulting seismic sequence triggered by the 2011 off the Pacific coast of Tohoku Earthquake: wholesale stress regime changes in the upper plate. Earth Planets Space 2011, 63: 745–748. 10.5047/eps.2011.06.014View ArticleGoogle Scholar
- Kinoshita M, Tobin H: Interseismic stress accumulation at the locked zone of Nankai Trough seismogenic fault off Kii Peninsula. Tectonophysics 2013, 600: 153–164. 10.1016/j.tecto.2013.03.015View ArticleGoogle Scholar
- Lewis J, Byrne T, Kanagawa K: Evidence for mechanical decoupling of the upper plate at the Nankai subduction zone: constraints from core-scale faults at NantroSEIZE Sites C0001 and C0002. Geochem Geophys Geosyst 2013, 14: 620–633. doi:10.1029/2012GC004406View ArticleGoogle Scholar
- Lin W, Doan ML, Moore JC, McNeill L, Byrne TB, Ito T, Saffer D, Conin M, Kinoshita M, Sanada Y, Moe KT, Araki E, Tobin H, Boutt D, Kano Y, Hayman NW, Flemings P, Huftile GJ, Cukur D, Buret C, Schleicher AM, Efimenko N, Kawabata K, Buchs DM, Jiang S, Kameo K, Horiguchi K, Wiersberg T, Kopf A, Kitada K, et al.: Present-day principal horizontal stress orientations in the Kumano forearc basin of the southwest Japan subduction zone determined from IODP NanTroSEIZE drilling Site C0009. Geophys Res Lett 2010., 37: doi:10.1029/2010GL043158Google Scholar
- Miller LD, Goldfarb RJ, Gehrels GE, Snee LW: Genetic links among fluid cycling, vein formation, regional deformation, and plutonism in the Juneau gold belt, southeastern Alaska. Geology 1994, 22: 203–206. 10.1130/0091-7613(1994)022<0203:GLAFCV>2.3.CO;2View ArticleGoogle Scholar
- Miyazaki S, Heki K: Crustal velocity field of southwest Japan: subduction and arc-arc collision. J Geophys Res 2001, 106: 4305–4326. doi:10.1029/2000JB900312View ArticleGoogle Scholar
- Moore G, Kanagawa K, Strasser M, Dugan B, Maeda L, Toczko S, et al.: NanTroSEIZE Stage 3: NanTroSEIZE plate boundary deep riser 2. IODP Prel Rept 2013, ᅟ: 338. doi:10.2204/iodp.pr.338.2013Google Scholar
- Nishikawa O, Takeshita T: Dynamic analysis and two types of kink bands in quartz veins deformed under subgreenschist conditions. Tectonophysics 1999, 301: 21–34. 10.1016/S0040-1951(98)00219-4View ArticleGoogle Scholar
- Okada T, Yoshida K, Ueki S, Nakajima J, Uchida N, Matsuzawa T, Umino N, Hasegawa A: Shallow inland earthquakes in NE Japan possibly triggered by the 2011 off the Pacific coast of Tohoku Earthquake. Earth Planets Space 2011, 63: 749–754. 10.5047/eps.2011.06.027View ArticleGoogle Scholar
- Oliver NHS, Bons PD: Mechanisms of fluid flow and fluid-rock interaction in fossil metamorphic hydrothermal systems inferred from vein-wall rock patterns, geometry and microstructure. Geofluids 2001, 1: 137–162. 10.1046/j.1468-8123.2001.00013.xView ArticleGoogle Scholar
- Park J-O, Kodaira S: Seismic reflection and bathymetric evidences for the Nankai earthquake rupture across a stable segment-boundary. Earth Planets Space 2012, 64: 299–303. 10.5047/eps.2011.10.006View ArticleGoogle Scholar
- Passchier CW, Trouw RAJ: Microtectonics. Springer, Berlin; 2005.Google Scholar
- Ramsay JG: Folding and Fracturing of Rocks. McGraw-Hill, New York; 1967.Google Scholar
- Randle V: Microtexture Determination and Its Applications. Maney Publishing, London; 2003.Google Scholar
- Rybacki E, Janssen C, Wirth R, Chen K, Wenk H-R, Stromeyer D, Dresen G: Low-temperature deformation in calcite veins of SAFOD core samples (San Andreas Fault)—microstructural analysis and implications for fault rheology. Tectonophysics 2011, 509: 107–119. 10.1016/j.tecto.2011.05.014View ArticleGoogle Scholar
- Seno T, Stein S, Gripp AE: A model for the motion of the Philippine Sea plate consistent with NUVEL-1 and geological data. J Geophys Res 1993, 98: 17941–17948. doi: 10.1029/93JB00782View ArticleGoogle Scholar
- Sibson RH: Implications of fault-valve behaviour for rupture nucleation and recurrence. Tectonophysics 1992, 211: 283–293. 10.1016/0040-1951(92)90065-EView ArticleGoogle Scholar
- Sibson RH: Stress switching in subduction forearcs: implications for overpressure containment and strength cycling on megathrusts. Tectonophysics 2013, 600: 142–152. 10.1016/j.tecto.2013.02.035View ArticleGoogle Scholar
- Strasser M, Dugan B, Kanagawa K, Moore GF, Toczko S, Maeda L, Kido Y, Moe KT, Sanada Y, Esteban L, Fabbri O, Geersen J, Hammerschmidt S, Hayashi H, Heirman K, Hupers A, Jurado Rodriguez MJ, Kameo K, Kanamatsu T, Kitajima H, Masuda H, Milliken K, Mishra R, Motoyama I, Olcott K, Oohashi K, Pickering KT, Ramirez SG, Rashid H, Sawyer D, et al.: Site C0002. In Proc. IODP, 338. Edited by: Strasser M, Dugan B, Kanagawa K, Moore GF, Toczko S, Maeda L. Integrated Ocean Drilling Program, Yokohama; 2014.Google Scholar
- Takeshita T, Hara I: c -Axis fabrics and microstructures in a recrystallized quartz vein deformed under fluid-rich greenschist conditions. J Struct Geol 1998, 20: 417–431. 10.1016/S0191-8141(97)00108-9View ArticleGoogle Scholar
- Tobin HJ, Kinoshita M: NanTroSEIZE: the IODP Nankai Trough seismogenic zone experiment. Sci Drill 2006, 2: 23–27. 10.5194/sd-2-23-2006View ArticleGoogle Scholar
- Turner FJ, Weiss LE: Structural Analysis of Metamorphic Tectonites. McGraw-Hill, New York; 1963.Google Scholar
- Turner FJ, Griggs DT, Heard HC: Experimental deformation of calcite crystals. Geol Soc Am Bull 1954, 65: 883–934. 10.1130/0016-7606(1954)65[883:EDOCC]2.0.CO;2View ArticleGoogle Scholar
- Urai JL, Williams PF, van Roermund HLM: Kinematics of crystal growth in syntectonic fibrous veins. J Struct Geol 1991, 13: 823–836. 10.1016/0191-8141(91)90007-6View ArticleGoogle Scholar
- Wu H-Y, Chan C-H, Kinoshita M, Saito S: Stress field observation and modeling from the NanTroSEIZE scientific drillings in the Nankai Trough system, SW Japan. Tectonophysics 2013, 600: 99–107. 10.1016/j.tecto.2013.04.009View ArticleGoogle Scholar
- Yamaguchi A, Cox SF, Kimura G, Okamoto S: Dynamic changes in fluid redox state associated with episodic fault rupture along a megasplay fault in a subduction zone. Earth Planet Sci Lett 2011, 302: 369–377. 10.1016/j.epsl.2010.12.029View ArticleGoogle Scholar
- Yamamoto Y, Lin W, Oda H, Byrne T, Yamamoto Y: Stress states at the subduction input site, Nankai subduction zone, using anelastic strain recovery (ASR) data in the basement basalt and overlying sediments. Tectonophysics 2013, 600: 91–98. 10.1016/j.tecto.2013.01.028View ArticleGoogle Scholar
- Yoshida K, Hasegawa A, Okada T, Linuma T, Ito Y, Asano Y: Stress before and after the 2011 great Tohoku-oki earthquake and induced earthquakes in inland areas of eastern Japan. Geophys Res Lett 2012., 39: doi:10.1029/2011GL049729, 2012.703–707 doi:10.1029/2011GL049729, 2012.703–707Google Scholar
This article is published under license to BioMed Central Ltd. This is an Open Access article distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/4.0), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly credited.