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Geoscience Letters

, 5:11 | Cite as

Supercycle in great earthquake recurrence along the Japan Trench over the last 4000 years

  • Kazuko Usami
  • Ken Ikehara
  • Toshiya Kanamatsu
  • Cecilia M. McHugh
Open Access
Research Letter
  • 825 Downloads

Abstract

On the landward slope of the Japan Trench, the mid-slope terrace (MST) is located at a depth of 4000–6000 m. Two piston cores from the MST were analyzed to assess the applicability of the MST for turbidite paleoseismology and to find out reliable recurrence record of the great earthquakes along the Japan Trench. The cores have preserved records of ~ 12 seismo-turbidites (event deposits) during the last 4000 years. In the upper parts of the two cores, only the following earthquakes (magnitude M ~ 8 and larger) were clearly recorded: the 2011 Tohoku, the 1896 Sanriku, the 1454 Kyotoku, and the 869 Jogan earthquake. In the lower part of the cores, turbidites were deposited alternately in the northern and southern sites during the periods between concurrent depositional events occurring at intervals of 500–900 years. Considering the characteristics of the coring sites for their sensitivity to earthquake shaking, the concurrent depositional events likely correspond to a supercycle that follows giant (M ~ 9) earthquakes along the Japan Trench. Preliminary estimations of peak ground acceleration for the historical earthquakes recorded as the turbidites imply that each rupture length of the 1454 and 869 earthquakes was over 200 km. The earthquakes related to the supercycle have occurred over at least the last 4000 years, and the cycle seems to have become slightly shorter in recent years. Earthquakes off the Sanriku coast forming the alternative deposition of turbidites in the two cores have released a part of accumulated slip, as indicated by the turbidites deposited in only one core. Decreases in the release of accumulated slip have possibly caused the recent shortening of the supercycle.

Keywords

Japan Trench Earthquake Turbidite Supercycle 

Abbreviations

MST

mid-slope terrace

PSV

paleomagnetic secular variation

Hr-FP

Haruna-Futatsudake-Ikaho tephra

PGA

peak ground acceleration

JAMSTEC

Japan Agency for Marine-Earth Science and Technology

Background

The 2011 off the Pacific coast of Tohoku earthquake (2011 Tohoku earthquake) occurred on March 11, 2011. It was an interplate earthquake that occurred along the Japan Trench with Mw 9.0 (Suzuki et al. 2011). This earthquake triggered huge destructive tsunamis that hit the Pacific coast of Northeast Japan, thus causing extensive damage. This earthquake forced a revision of the conventional understanding of the recurrence patterns of great earthquakes along the Japan Trench (Satake 2015). These recurrence patterns have conventionally been studied through historical and instrumental records on the last few centuries. Therefore, the use of geological records has become more important source of long time-scale evidence about the recurrence of great earthquakes.

Onshore tsunami deposits provide evidence that significant earthquakes and tsunamis have impacted the Pacific coast of Tohoku in the past (Abe et al. 1990; Minoura and Nakaya 1991; Minoura et al. 2001; Sawai et al. 2012, 2015; Ishimura and Miyauchi 2015; Takada et al. 2016; Ishimura 2017). Even before the 2011 Tohoku earthquake, two earthquakes along the Japan Trench (the A.D. 869 Jogan earthquake and the 1454 Kyotoku earthquake) that generated giant tsunamis similar to the one in 2011 are indicated by historical records and tsunami deposits (Satake et al. 2008; Namegaya and Yata 2014; Sawai et al. 2015). The 1896 Sanriku earthquake known as “tsunami earthquake” also caused serious damage to the Tohoku region (Kanamori 1972; Tanioka and Satake 1996; Satake et al. 2017) and formed tsunami deposits (e.g., Takada et al. 2016). Although tsunamis that originated at great distances have also produced some onshore deposits on the Sanriku coast (e.g., the 1960 Chilean tsunami deposits; Kon’no et al. 1961), the major cause of large tsunamis in this area is interplate earthquakes along the Japan Trench (Minoura and Nakaya 1991; Minoura et al. 2001; Namegaya and Satake 2014; Sawai et al. 2015). However, submarine landslides could also cause some large tsunamis (Tappin et al. 2001; Kawamura et al. 2014). In general, it is difficult to discern the cause of a tsunami solely on the basis of the characteristics of onshore tsunami deposits. Seismo-turbidites (turbidites deposited by earthquake-triggered turbidity currents) have been also used to estimate the recurrence history of earthquakes in other active tectonic margins (Goldfinger et al. 2012; Gutierrez-Pastor et al. 2013; Pouderoux et al. 2014; Patton et al. 2015). According to analysis of turbidites corresponding to the 2011 Tohoku earthquake, the upper few centimeters of surface sediments (as distinct from large-scale slope failure) were the primary contributors to sediment remobilization along the Japan Trench when the 2011 earthquake occurred (Ikehara et al. 2016; McHugh et al. 2016). Repeated depositions of seismo-turbidites due to similar remobilizations of surface sediments are speculated to have occurred along the Japan Trench.

On the landward slope of the Japan Trench, the mid-slope terrace (MST) is recognized at a depth of 4000–6000 m (Fig. 1A; Cadet et al. 1987). This terrace was reported by the Deep Sea Drilling Project Leg 57 as an area with turbidites at a high sedimentation rate (Shipboard Scientific Party 1980), and thus, the terrace is expected to be suitable for seismo-turbidite analysis.
Fig. 1

A Bathymetric image along the Japan Trench. Two red circles indicate coring sites of NT13–19 PC08 and PC10. The orange point to the left of the coring sites is the hypothetical source of the turbidity currents for calculating PGA in this study. Line C transects the inset in C. Green inverted triangles indicate the sites of onland tsunami deposits (Sawai et al. 2012; Hirakawa 2012; Takada et al. 2016; Ishimura 2017). Yellow ellipses summarize the suggested rupture areas of historical earthquakes (M ~ 7.4 and larger) over the most recent 200 years (Koper et al. 2011; Toda 2016); 2: 1994 Sanriku-oki earthquake, 8: 1896 Sanriku earthquake. The rectangles with black solid lines are the suggested rupture areas of the 869 Jogan earthquake (Namegaya and Satake 2014). The rectangle with yellow solid lines is the suggested rupture area of the 1454 Kyotoku earthquake (Sawai et al. 2015). Numbers (1–8) of the rupture areas correspond to those in Additional file 7: Table S3. Irregular ellipses with yellow solid line indicate the area of coseismic slips, which were 4 m or greater when the 2011 earthquake occurred (Ozawa et al. 2011). Earthquakes other than those mentioned above (a–i) occurred in the following years: (a) 1856, (b) 1931, (c) 1901, (d) 1897, (e) 1936, (f) 1933, (g) and (h) 1938. The bathymetric chart (shaded-relief) is based on ETOPO1 (Amante and Eakins 2009). B Detailed bathymetry of the coring sites at NT13-19 PC08 and PC10. This inset is indicated by the green rectangle in A. Both coring sites PC08 and PC10 are in small basins in the MST. The bathymetric chart (shaded-relief) is based on a data-set provided by the Hydrographic and Oceanographic Department, Japan Coast Guard. C Migrated seismic profile of line C in A. Green areas show isolated basins above the onlap unconformities

The Pacific plate subducts beneath the North America plate (Okhotsk plate) at a rate of ~ 8.6 cm/year (DeMets et al. 2010). This subduction is associated with tectonic erosion that results in forearc subsidence (von Huene and Lallemand 1990). The episodic subsidence in the forearc slope forms an isolated basin, where upper-slope sediment is trapped. The trapped sediments have been resulting in stratified onlapping formations (Fig. 1C; Arai et al. 2014). In addition, obvious submarine canyons are not present (Fig. 1A). This means that no direct pathway allows the long-distance transportation of terrigenous and coastal sediments. As a result, the MST is difficult to be affected by meteorological and tsunami events in terms of its sediment supply. These bathymetrical conditions provide “linear sources” of sediments to the MST that faces a deep-sea steep landward slope (> 5°). The “linear sources” means that few lateral migrations on sediment transport (Reading and Richards 1994). Thus, the origin of sediment on the MST is basically confined to sediments on adjacent landward slope. This condition is useful for identifying the area of earthquakes that triggered turbidity currents resulting in the turbidites in the MST.

The MST has been formed by continuous fault activity associated with the backstop interface (Fig. 1C). The resulting landward-dipping basement under the MST has been filled by stratified strata derived from slope sediments, which have flattened the terrace (von Huene et al. 1980; von Huene and Culotta 1989; Tsuru et al. 2002). The terrace has a trench-ward edge with undulating features that originate from frontal prism structures. These features trap the gravity flow from the landward slope, and then deposit their transporting sediments (von Huene and Culotta 1989; Tsuru et al. 2002). Consequently, the sedimentological conditions lead to the high sedimentation rate of the MST. This high sedimentation rate is expected to be effective for successive recording of the earthquakes.

In this way, MST is speculated to be suitable for seismo-turbidite analysis; however, the sedimentological information in previous studies is limited. Therefore, we analyzed two piston cores from the MST to assess the applicability of the MST for turbidite paleoseismology, and to find out reliable recurrence record of the great earthquakes along the Japan Trench. The two cores PC08 (39.2741°N, 143.9447°E; 4983 m depth) and PC10 (39.1206°N, 143.9026°E; 5398 m depth) were recovered from different small basins in the MST, during the NT13-19 cruise with R/V Natsushima (Fig. 1A, B). Both cores show relatively clear sedimentary structures, compared to all 23 cores recovered from a broad area of the MST during the cruise (all the coring sites are shown in: McHugh et al. 2016). The hemipelagites of these cores are intercalated by obvious event deposits (about three layers per 1 m). Such structures of the two cores are considered to be suitable for the foregoing objective. Because it is difficult to figure out the depositional interval of the event deposits using too many (amalgamated) or too small number of event deposit layers in the core. The two coring sites are ~ 20 km apart. This distance is relatively small considering the scale of the Japan Trench. However, it is expected that the core selection provides relatively simple sedimentological and seismological conditions, ensuring reliability of the records by the correlations between the two cores. In this study, we finally conduct a comparison of the records from offshore seismo-turbidites with onshore tsunami deposits, and offer new insights into the recurrence interval and characteristics of great earthquakes that have occurred along the Japan Trench.

Results and discussion

Characteristics of the turbidites and age model

The two recovered cores are characterized by alternating bioturbated hemipelagites (diatomaceous mud) and massive event deposits with a sharp base and upward fining grading structure. The cores each have 12 distinct event deposits preserved in their upper 4 m (Fig. 2). The grading structure shows changes from “parallel or cross-laminated basal fine sand–coarse silt layer” to “upper mud layer” (Fig. 2, Additional file 1: Figure S1, Additional file 2: Figure S2). Sedimentary structures of event deposits suggest that the deposits are considered as “fine-grained turbidite” (Stow and Shanmugam 1980), except for T1–2 in PC10, which consists of only two semi-indurated gravels. Although the structure of the event deposits shows occasional disturbance by bioturbation, the basal layers are relatively well preserved. Not only the hemipelagites but also the event deposits contain few carbonates (Additional file 3: Figure S3), suggesting that the origins of the turbidity currents are below the carbonate compensation depth (CCD; Berger et al. 1976), which is deeper than the forearc basin.
Fig. 2

Soft-X radiographs, photographs, lithological column, magnetic susceptibility, and PSV records. In the column, yellow layers indicate coarse layers (> course silt); blue layers are hemipelagite (silt ~ clay); gray horizons are turbidite-mud; red layers and patch are tephra layers or patches. Apparent turbidites (event deposits) are indicated by blue lines, and are numbered beginning at the top layer. Relatively indistinct turbidites are assigned branch numbers. The letters “A”–“E” (relative declination) and “a”–“l” (inclination) added to the PSV records are PSV labels for prominent features of age control (Kanamatsu et al. 2017). Shaded intervals of the PSV record are horizons disturbed by inclinations of minimum axes of anisotropy of magnetic susceptibility (Kanamatsu et al. 2017). Stars indicate horizons at the excess 210Pb detection limit and the 137Cs maximum (McHugh et al. 2016)

A volcanic ash layer with a 2–3 cm thickness is observed in both cores. The ash layers are composed of pumice-type volcanic glass shards with hornblende and clinopyroxene as heavy minerals. The petrographic characteristics (heavy mineral composition, morphotypes of volcanic glass shards, and refractive index of glass shards: 1.505–1.509) of the ash layers are correlated with those of the Haruna-Futatsudake-Ikaho (Hr-FP) tephra (Ikehara et al. 2017), products of a historical eruption of Mt. Haruna during the 6th century (Geshi and Oishi 2011; Fig. 1A). For determining the depositional ages and correlation of the turbidites, radioisotopes (137Cs and excess 210Pb; McHugh et al. 2016) and paleomagnetic secular variation (PSV) records (Kanamatsu et al. 2017) were used in addition to the tephra evidence. MST is located below the CCD; therefore, 14C dating cannot be used for these cores that contain few calcium carbonates. In the case of radioisotopes, horizons in the two cores that excess 210Pb detection limits (A.D. 1860) and the maximum for 137Cs (A.D. 1963; Peirson 1971) were referred to in previous studies (McHugh et al. 2016) (Figs. 2 and 3). The quality of the PSV records is excellent for deep-sea sediments. The obvious changes allow many of the turbidites in the two cores to be correlated with each other (Fig. 2, Additional file 4: Figure S4, Additional file 5: Table S1, Additional file 6: Table S2). The turbidites are numbered from T1 to T12 in descending order of age. Based on the age model and correlations, we found that the two cores have preserved ~ 12 turbidites (event deposits) during the last 4000 years. “Methods” section describes the specific procedure of the stratigraphic correlation between the turbidites in PC08 and PC10.
Fig. 3

Stratigraphic correlation between turbidites in the NT13-19 PC08, PC10, and onland tsunami deposits in the Tohoku region during the last 4000 years. References: 1 Sawai et al. 2012; 2 Hirakawa 2012; 3 Takada et al. 2016. Areas (a)–(d) correspond to those in Fig. 1A. *northern part of (d); **possibly the quake of A.D. 1454 (Takada et al. 2016); (a); (a) and northern part of (b); Δ: northern part of (a). Estimated depositional age of the tsunami deposits is shown by green rectangles with error bars (2σ) based on results that have smaller margins of error among the values reported in previous studies. The error range of the tsunami deposit around A.D. 0 is unclear. 1896, 1611, 1454, and 869 are the ages of historical earthquakes/tsunamis. The ages corresponding to PSV labels are from Ali et al. (1999)

Cause of the turbidite deposition and correlation of the upper turbidites with historical earthquakes

Generally, in addition to gas-hydrate destabilization, earthquakes, and tsunamis, turbidity currents that deposit turbidites are triggered by events such as storms and hyperpycnal flows in coastal areas (e.g., Goldfinger et al. 2012; Polonia et al. 2013). Based on the submarine topography mentioned earlier, MST is difficult to be affected by shallow water areas in terms of the sediment supply. Besides, the compositions of the turbidites within the two cores suggest that the origins of the turbidity currents are below the CCD, suggesting that the main source of the turbidity currents is a scarp in the middle slope. In addition, no gas hydrates have been reported in this area. For these reasons, earthquakes that result in ground motion are the most-likely trigger of the turbidity currents.

The estimated depositional ages of the four turbidites above the Hr-FP can be related to the ages of historical earthquakes. It is possible that the uppermost turbidites T1 and T1–2 are related to the 2011 (Mw 9.0) and the 1896 (Mw 8.1) earthquakes based on the results from radioisotope dating. T1 is found out from each core top, and is immediately above the maximum for 137Cs (A.D. 1963; Peirson 1971). T1–2 is immediately above excess 210Pb detection limit (A.D. 1860). From the stratigraphic relationship with PSV labels, the turbidites T2 (below PSV label “b” and above “c” in the inclinations, approximately A.D. 1470 and A.D. 1220) and T3 (around PSV label “d” and “B” approximately A.D. 730) can be attributed to the 1454 Kyotoku (Mw 8.4 or larger) and the 869 Jogan (Mw ~ 9) earthquakes, respectively. Even though no other historical records are available, the estimated age of the turbidites implies a relatively shorter interval (100–300 years) prior to the last 2300 years, pointing to different depositional timings between the two cores for T6–T8 and T10–T12 (Fig. 3).

Sensitivity of turbidity current generation to earthquake ground shaking

Concerning the interpretation of these turbidite records, we must find a way to quantify the extent of the rupture areas and the magnitudes of the earthquakes recorded in the turbidite. As noted above, only great (Mw ~ 8) or giant (Mw ~ 9) earthquakes are clearly recorded above Hr-FP in the two cores. Based on this result, the sensitivity of turbidity-current generation to earthquake ground shaking is discussed below. Historical earthquakes over the last 200 years are mapped in Fig. 1A (Koper et al. 2011; Toda 2016). This distribution of past earthquakes indicates that few large earthquakes (with M ~ 7.5 and larger) have occurred in the forearc off Kamaishi, which is near the coring sites. The reason of the distribution pattern has been discussed based on seismic tomography in the megathrust zone off Tohoku. Most large interplate thrust earthquakes occurred in high-velocity areas that may represent high-strength asperities (Huang and Zhao 2013); In contrast, a low-velocity area associated with abundant sediments supplied from the incoming plate lies off Kamaishi (Tsuru et al. 2002; Huang and Zhao 2013). Weak interplate locking off Kamaishi is also implied by the degree of periodicity and the dominant period of slow slip (Uchida et al. 2016). The absence of large earthquakes in the areas adjacent to the coring sites owing to these tectonic settings has likely facilitated the successive recording of the great-giant earthquakes in the cores. In this case, turbidity currents can be generated only by such great-giant earthquakes, and surface sediments could continue to accumulate during the other periods without being interrupted by earthquakes in adjacent areas. The accumulated sediments result in thick turbidites that are difficult to disturb by benthos activities mainly from the seafloor. These sedimentary conditions mean that only records of great-giant earthquakes have been preserved clearly as turbidites in the coring sites that we studied.

Next, based on the suggested rupture areas of historical earthquakes around the coring sites, we roughly estimated the peak ground acceleration (PGA) at the possible source zone of the turbidity currents resulting in the turbidites in the two cores (Fig. 1A) using an empirical attenuation relation commonly used in Japan (Additional file 7: Table S3; Si and Midorikawa 1999). In general, the initiation of slope failure depends on excess pore pressure caused by earthquake-induced ground acceleration (Seed and Idriss 1971). Other factors also contribute to actual slope failures, such as the duration of ground motion and the time elapsed since the previous earthquake, the latter of which is the period over which hemipelagite was deposited on the slope. We assume that slope failure was triggered simply by ground acceleration because the details of the historical earthquakes are unknown.

The estimation results infer that the PGA could be large (over ~ 200 cm/s2) at the hypothetical source zone, for fault models of the giant and great earthquakes recorded as the turbidites; the A.D. 869 Jogan (uniform-slip model with a fault length of 200 km; Namegaya and Satake 2014), 1454 Kyotoku (Sawai et al. 2015), 1896 Sanriku (Satake et al. 2017), and 2011 Tohoku (Yoshida et al. 2011)(No. 6, 7, 8 and a yellow irregular ellipse in Fig. 1A, Additional file 7: Table S3). On the other hand, great earthquakes that occur near the coring sites could have also produced large acceleration (over ~ 240 cm/s2) within ~ 100 km from the area, such as the 1897 (Sato 1989) and 1994 Sanriku-oki (Nakayama and Takeo 1997) earthquakes (No. 4 and 2 in Fig. 1A, Additional file 7: Table S3). As for the 1897 earthquake, the rupture area is thought to be close to the trench axis. It has been reported that earthquakes with low short-period energy stand out near the trench axis (water depth > 3500 m) (Koper et al. 2011; Lay et al. 2012; Huang and Zhao 2013). Considering that the ground acceleration caused by weak short-period radiation is generally slight, earthquakes near the trench axis have a lower potential for triggering turbidity currents in the source zone, than a case suggested by results from the attenuation relation. Note that, this speculation does not apply to the case in which earthquakes are extraordinarily large and/or their rupture areas lie just below the source zone, like the 1896 Sanriku earthquake.

However, the 1994 Sanriku-oki earthquake is not considered as the above-mentioned “near-trench” earthquake (Nakayama and Takeo 1997; Yamanaka and Kikuchi 2004). This earthquake is supposed to have caused larger ground acceleration at the hypothetical source zone, than those of the 869 Jogan (uniform-slip model with a fault length of 200 km; Namegaya and Satake 2014) and 1454 Kyotoku (fault model in Sawai et al. 2015; 200 km long) earthquakes. After the 1994 earthquakes, dives of submersible “Shinkai 6500” were performed at the northern MST (40°7.8′–10.5′N, 143°58.8′–144°2.2′E). According to the reports, no evidence of resedimentation was found, even though the dive locations were only ~ 25 km from the hypocenter of the earthquake (Ogawa et al. 1996). In terms of the 869 earthquake, 300 and 400 km long fault models have been assumed in addition to the model with a fault length of 200 km, for a uniform-slip model (Namegaya and Satake 2014; Fig. 1A). Using fault parameters of these models for the calculations, the estimated PGAs can be significantly large (over ~ 370 cm/s2) compared to that of the 1994 earthquake, at the hypothetical source zone (Additional file 7: Table S3). Thus, the obvious turbidites T3 in the two cores may suggest that the fault models with a fault length of 300 km or longer are more probable for the 869 earthquake. The 869 Jogan tsunami deposits found in the Sanriku coast in recent years (Takada et al. 2016; Ishimura 2017) seem to support this inference. Similarly, the fault model of the 1454 earthquake is also based on a estimation with a minimum magnitude (Sawai et al. 2015). Given the turbidites T2, clearly recorded in the two cores, the rupture length of this earthquake could be much longer than 200 km.

Correlation of offshore turbidite records with onland tsunami deposits

Subsequently, we compared the estimated turbidite depositional ages with those of onland tsunami deposits reported by previous studies (Sawai et al. 2012; Hirakawa 2012; Takada et al. 2016; Ishimura 2017). The ages of the tsunami deposits that disagree with the turbidites, such as those from the 12–13 century, and A.D. 1611, may have been related to tsunamis begun in other far-field areas or submarine landslides instead of earthquakes along the Japan Trench (Fig. 3). Recently, Ishimura (2017) re-examined the depositional ages of tsunami deposits at Koyadori [located near the middle latitude of area (b) in Fig. 1A], and found tsunami deposits formed in A.D. 510–240 (“E5 bed”) and A.D. 260–270 (“E6 bed”). The E5 bed may be correlated with the tsunami deposits from A.D. 430 in the Sendai and Ishinomaki plains (Fig. 3; Sawai et al. 2012), and may also be correlated with the T4-1 turbidite. The E6 bed has no correlating turbidite, thus suggesting that it may be the product of a tsunami of far-field or landslide origin, although the bed may also be correlated with a tsunami deposit formed around A.D. 0 reported by Hirakawa (2012); (Fig. 3). Except for the few disagreements, many of the estimated ages of the tsunami deposits in the Tohoku region can be correlated with those of turbidites in the two cores. In addition, the tsunami deposits are thought to have been deposited at different times across the north and the south regions between 2000 and 4000 years ago (Takada et al. 2016). The turbidite depositional ages may also be correlated with those ages, thus reflecting the latitudinal difference of the coring sites. PC08 is located approximately 20 km north of PC10, and the ages of its turbidites are better correlated with those of onland tsunami deposits found on the northern part of the Sanriku coast (Figs. 1 and 3). The turbidite ages of PC10 correspond to those of the southern part. Overall, these turbidites seem to have been deposited alternately at northern and southern sites, during the periods between concurrent depositional events (e.g., T5, T8, T9, and next to T12) at intervals of 500–900 years. The difference in timing of the turbidite deposition in the two cores is likely significant, considering its correlation with the distribution of tsunami deposits on the Sanriku coast. In other words, the turbidites recorded in only one core (T6–T7, T10–T12) may record the difference of source region of earthquakes off the Sanriku coast, even though PC10 and PC08 are only 20 km apart.

Supercycle

A “supercycle” of giant (M ~ 9) earthquakes with a recurrence interval of ~ 700 years and superimposed on the cycle (~ 37 years) of earthquakes off Miyagi (Fig. 1A) has been proposed along the Japan Trench (Satake and Fujii 2014; Satake 2015; Fig. 4a). These authors have also suggested that the large coseismic slip near the trench axis of the 2011 Tohoku earthquake can be explained by this model of earthquake cycles. The typical slip of the off-Miyagi earthquakes is ~ 2 m, accompanied by a cumulative slip of ~ 6 m per century, as the subduction rate of the Pacific plate is ~ 8 m per century. Such cumulative slips have been interpreted to have been released by infrequent earthquakes with recurring at an interval of ~ 700 years (Satake 2015).
Fig. 4

a Schematic for earthquake supercycle off Miyagi in red and near the trench axis in blue (Satake and Fujii 2014; Satake 2015). If slip accumulated from the remainders from off-Miyagi earthquakes is released by giant earthquakes, the recurrence interval or supercycle measures ~ 700 years (Satake 2015). b Time-series diagram for turbidite depositions of NT13-19 PC08 and PC10. Earthquakes related to the supercycle are implied to have occurred for the last 4000 years, and the cycle has become slightly shorter in recent years, considering the concurrent depositional events. The types of earthquakes recorded only in one core have decreased in recent years

Considering the suggested magnitudes and source regions of the past earthquakes along the Japan Trench, the events recorded concurrently in the two cores studied above may correspond to earthquakes that are a part of this supercycle (Fig. 4b). The earthquakes related to the supercycle are implied to have occurred over at least the last 4000 years, and the cycle may have shortened slightly in recent years (Fig. 4b). If the earthquake supercycle is regulated by cumulative slip as previous studies have indicated, these shorter intervals are a potentially influenced by the decrease in number of earthquakes that were recorded only in one core. These earthquakes (other than giant earthquakes) might have also contributed to partial releases of cumulative slip in common with the off-Miyagi earthquakes. Meanwhile, the accumulated slip off the Sanriku coast may have contributed to the size of giant earthquakes, such as the 2011 Tohoku and the 869 Jogan earthquakes.

Conclusions

Deep-sea seismo-turbidites in two piston cores recovered from the MST along the Japan Trench have preserved the earthquake records associated with tsunamis that have damaged the Pacific coast of the Tohoku region over the last 4000 years. Approximately 12 turbidites, or event deposits, have been formed at the coring sites, and we dated them with a PSV method along with tephrochronology and radioisotopes. These turbidites were deposited alternately in the northern and southern sites during the periods between concurrent depositional events occurring at intervals of 500–900 years. The concurrent depositional events likely correspond to a supercycle of giant (M ~ 9) earthquakes along the Japan Trench, recurring at an interval of ~ 700 years. The earthquakes related to the supercycle have occurred over at least the last 4000 years, and this recurrence interval has shortened slightly in recent years. Decreases in the release of accumulated slip caused by earthquakes in the northern and southern areas off the Sanriku coast have likely affected the recent shortening of the supercycle.

Methods

Soft-X radiograph

Recovered cores were carefully observed visually, and detailed sedimentary structures were observed using soft-X radiographs. The samples for soft-X radiographs were prepared continuously using plastic cases (length 20 cm, width 5 cm, thickness 1 cm) with no gap, from one side of the halved cores, following visual descriptions and photographs on board. The samples were then refrigerated and analyzed with soft X-ray imaging. Smear slides were observed and used to determine the horizons of typical sedimentary facies (Additional file 3: Figure S3).

Magnetic susceptibility and PSV records (inclination and relative declination)

MST is located below CCD (Berger et al. 1976); therefore, 14C dating method cannot be used for these cores as they contain few calcium carbonates. Therefore, we used a PSV method that has not been previously used for dating the deep-sea turbidites. The measurement procedure and the PSV records and magnetic susceptibility results are based on Kanamatsu et al. (2017). Obvious peak and trough intervals on the graphs of paleomagnetic inclinations and declinations (PSV labels; “A”–“E” and “a”–“i” in Fig. 2) were correlated with those of a Holocene secular variation curve from Lake Biwa (Ali et al. 1999) to infer the age of the cores. Refer to Additional file 4: Figure S4, Additional file 5: Table S1, Additional file 6: Table S2 for more details. Generally, directional deflections are clearly marked in the turbidite layers in our profiles (Fig. 2). These deflections are likely related to coarse material intercalations. Thus, the intervals, which show larger deflections, may not indicate proper PSV records. Therefore, we made stratigraphic correlations without those data.

Stratigraphic correlation between the turbidites in PC08 and those in PC10

Stratigraphic correlations between the turbidites in NT13-19 PC08 and those in PC10 are based on the stratigraphic relationships of radioisotope marker horizons (McHugh et al. 2016), Hr-FP tephra, and PSV labels in PSV records (Kanamatsu et al. 2017). Magnetic susceptibility is also taken into account (Fig. 2, Additional file 5: Table S1, Additional file 6: Table S2). In the following explanation, the letters “A”–“E” (relative declination) and “a”–“i” (inclination) are PSV labels.

Specific procedure:
  1. 1.

    [Above Hr-FP] Three turbidites (event deposits) occurred in PC08 and four occurred in PC10. Those turbidites show similar stratigraphy in the two cores, except for T1–2 which is indistinct in PC08. T1 is found out from each core top, immediately above the maximum for 137Cs (A.D. 1963; Peirson 1971). T1–2 is immediately above the excess 210Pb detection limit (A.D. 1860). T2 is above “c” on the inclination in each core and is below “b” in PC08. T3 is adjacent to “d” and “B” in both cores. Although the PSV record of PC10 is slightly different from that of PC08, we consider that PC08 has better PSV records because of the relatively rapid accumulation.

     
  2. 2.

    [Hr-FP–“h” on the inclinations] T4-1 (below “f”) and T5 (immediately above “h”) are clearly marked in both cores. A turbidite below T4-1 in PC08 is named T4-2 (below “g” and above “C”). In PC10, T4-2 is not obvious from the soft X-ray radiograph, although magnetic susceptibility profiles show slight fluctuations in the horizon that correspond to T4-2.

     
  3. 3.

    [“h” on the inclinations–“D” on the declinations] We considered a turbidite immediately above “D” in PC08 as T7, and two turbidites in the middle horizon between “h” and “D” as T6-1 and T6-2 in PC10. T6 of PC08 and T7 of PC10 are not obvious in soft X radiographs, although magnetic susceptibility profiles show slight fluctuations in the horizon corresponding to the turbidites.

     
  4. 4.

    [“D” on the declinations–T9] “i” and “D’” in PC10 cannot be marked because the PSV record of PC10 is unclear relative to that of PC08. Therefore, a characteristic turbidite with peculiarly high magnetic susceptibility is found out and named as T9 in each core. Two turbidites occur above T9 in PC08 and PC10. The turbidites below “D” are named as “T8-1”; the turbidites below “T8-1” are “T8-2” in PC08 and PC10. However, “T8-1” and “T8-2” in PC08 cannot be correlated with those of PC10, considering the thicknesses of the hemipelagites between “D” and T-9. If the accumulation rates are assumed to have been nearly constant, “T8-1” and “T8-2” of PC08 would have formed later than those of PC10 (Fig. 4).

     
  5. 5.

    [Below T9] Three turbidites, T10 (above “j”), T11 (below “j,” and above “k”), and T12 (below “k,” and above “l”) are evident in PC08 and PC10. In addition to these, another turbidite is observed the vicinity of “l” in PC08. On the other hand, a turbidite below “l” is found in PC10. Given that this correlation is relatively unclear, these two turbidites are not numbered in the figure.

     

In this study, the identification of turbidites (event deposits) is based only on the obvious sedimentary structure (or evidently bioturbated event layer) to have a clear criterion for identification. For example, horizons with high magnetic susceptibility lie between T2 and T3 in both PC08 and PC10; however, soft-X radiographs, photos, and visual observations (sediment grain size, sedimentary structure, and sediment color) do not present evidence of resedimentation. In this case, these layers probably indicate environmental changes in the bottom water. Hence, we do not consider these horizons to be turbidites or event deposits in this study.

Preliminary estimation of PGA

We estimated approximate maximum accelerations at an assumed source point (39.25°N, 143.75°E; Fig. 1A) of the turbidity currents, which resulted in the turbidites when historical earthquakes occurred. The assumed source point is located on the slope adjacent to the coring sites, and ~ 4000 m in depth because of few carbonate fractions in the turbidites (Additional file 3: Figure S3). Considering the accuracies of the suggested rupture areas of the historical earthquakes, we chose only one assumed source point for the two cores for the calculations, except for the 1994 Sanriku-oki earthquake as an example. Actual source point for the two cores is considered to have been differ from one another; however, if we chose different source points for each core, the resulting difference of calculated values would have little meaning in this case. Eight historical earthquakes and the 2011 Tohoku earthquake that occurred around the coring sites are selected for calculation (Fig. 1A, Additional file 7: Table S3). Fault parameters of the earthquakes have been discussed in previous studies, and we summarize them in Additional file 7: Table S3. The 1933 earthquake (rupture area f in Fig. 1A) is excluded from the estimations, because of the source fault in the incoming plate.

We use an empirical attenuation relation commonly used in Japan (Si and Midorikawa 1999):
$$ \log ({\text{PGA}}) \, = b - \log (x \, + c) - 0.003x, $$
(1)
where
$$ b = 0.5{M\text{w}} + 0.0043D + d + 0.61 $$
(2)
$$ c = 0.0055*10^{{0.50{M\text{w}}}}. $$
(3)
Here x is the shortest distance from the fault plane (fault distance); D is the focal depth (average depth of the fault plane); d corresponds to the type of earthquake (crustal: 0.00; interplate: 0.01; intraplate: 0.22). We applied 0.01 for the calculations because the earthquakes we estimated were all interplate earthquakes. Si et al. (2016) reported that strong ground motion will stop to increase with Mw  for earthquakes with Mw  larger than 8.3 (it is called magnitude saturation) when using fault distance. Therefore, we have substituted 8.4 for Mw  in the equation, for the A.D. 869, 1454, and 2011 earthquakes. This attenuation formula was derived from records of ground motion on land. Therefore, the actual PGAs in the deep sea close to the Pacific plate were possibly stronger. Along the Japan Trench, the subducting Pacific plate has been reported to guide high-frequency seismic wave efficiently more than the overriding (landward) plate (Furumura and Kennett 2005).

Notes

Authors’ contributions

KU, KI, and CM observed turbidites. KU and KI also analyzed the detailed turbidite stratigraphy. KU identified components of sediments by use of the smear slides and estimated ground motion. TK analyzed paleomagnetic data of the cores and managed the cruise. All authors contributed to the writing of the manuscript and to scientific discussions. All authors read and approved the final manuscript.

Acknowledgements

We express our heartfelt thanks to the officers, crew, and on-board scientists of the NT13-19 cruise including T. Aoki who provided assistance with core recovery. We also acknowledge K. Arai for providing seismic profile of Fig. 1C. Finally, we thank anonymous reviewers for constructive comments on the earlier version of this manuscript.

Competing interests

The authors declare that they have no competing interests.

Availability of data and materials

Additional files 1, 2, 3, 4, 5, 6, 7 are available. Correspondence and requests for materials should be addressed to KU.

Consent for publication

Not applicable.

Ethics approval and consent to participate

Not applicable.

Funding

This work was financially supported in part by the Ministry of Education, Culture, Sports, Science and Technology (MEXT) of Japan via the research projects “Geophysical and Geological Studies of Earthquakes and Tsunamis for off-Tohoku District, Japan” and “Regional Study on Hazard Mitigation along the Nankai Trough”, and Kaken-hi “Japan Trench Deep-Sea Research Project for Assessing Shallow Seismic Slips and Their History (No. 260000002).” This work was also financially supported in part by “Study on Coastal Sediments” funded by the Geological Survey of Japan (GSJ), AIST, and “Tephra in the Japan Trench Cores” by a special research fund of the Research Institute of Geology and Geoinformation, GSJ, AIST.

Publisher’s Note

Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Supplementary material

40562_2018_110_MOESM1_ESM.png (4.3 mb)
Additional file 1: Figure S1. High-resolution soft X radiographs and color photos of NT13-19 PC08. Solid arrow: basal part of turbidite (sand or coarse silt); dotted arrow: turbidite mud. T1-T12: turbidite numbers correspond to those in Figs. 2, 3, and 4. A-I: horizons of the smear slides in Additional file 3: Figure S3: Hr-FP: Haruna-Futatsudake-Ikaho tephra.
40562_2018_110_MOESM2_ESM.png (3.9 mb)
Additional file 2: Figure S2. High-resolution soft X radiographs and color photos of NT13-19 PC10. . Solid arrow: basal part of turbidite (sand or coarse silt); dotted arrow: turbidite mud. T1–T11: turbidite numbers correspond to those in Figs. 2, 3, and 4. Hr-FP: Haruna-Futatsudake-Ikaho tephra.
40562_2018_110_MOESM3_ESM.pdf (1.7 mb)
Additional file 3: Figure S3. Selected representative smear slide images showing typical microscopic characteristics of basal sand ~ coarse silt layer and upper mud layer of the turbidites, in addition to the hemipelagites in NT13-19 PC08 core. Both the hemipelagites and the turbidites (both of the basal sands and the turbidite muds) contain few carbonate fractions, suggesting that the origins of turbidity currents are below carbonate compensation depth (CCD). The diatomaceous hemipelagic mud (A, D, and G) is almost composed of diatoms and siliceous sponge spicules accompanied by few clastics. Turbidite muds (B, E, and H) consist of diatoms, siliceous sponge spicules, and few clastics, with amorphous organic matter particles. Basal sands of the turbidite (C, F and I) include rock fragments and minerals such as quartz and aegirine-augite, as well as diatoms, siliceous sponge spicules, and organic matter particles. A: diatomaceous hemipelagic mud, 51 cm (in core depth); B: turbidite (T2) mud, 64 cm; C: basal sand of the turbidite T2, 71 cm; D: diatomaceous hemipelagic mud, 194 cm; E: turbidite (T4-2) mud, 202 cm; F: basal sand of the turbidite T4-2, 205 cm; G: diatomaceous hemipelagic mud, 268 cm; H: turbidite (T7) mud, 281 cm; I: basal sand of the turbidite T7, 290 cm. a: parallel nicols; b: crossed nicols. Scale bars: 100 μm. The horizons of A-I are shown in Additional file 1: Figure S1.
40562_2018_110_MOESM4_ESM.png (285 kb)
Additional file 4: Figure S4. Correlations between PSV records of NT3-19 (PC08 and PC10) and those of Lake Biwa (Ali et al. 1999). The letters “A”–“G” (relative declination) and “a”–“n” (inclination) added to the PSV records are PSV labels for prominent features of age control (Ali et al. 1999; Kanamatsu et al. 2017).
40562_2018_110_MOESM5_ESM.xlsx (28 kb)
Additional file 5: Table S1. Variations in magnetic susceptibility, declination, and inclination obtained from NT13-19 PC08.
40562_2018_110_MOESM6_ESM.xlsx (198 kb)
Additional file 6: Table S2. Variations in magnetic susceptibility, declination, and inclination obtained from NT13-19 PC10.
40562_2018_110_MOESM7_ESM.xlsx (16 kb)
Additional file 7: Table S3. Estimated PGAs and parameters of fault models used in the trial calculations.

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Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

Authors and Affiliations

  1. 1.Geological Survey of JapanNational Institute of Advanced Industrial Science and Technology (AIST), Tsukuba Central 7TsukubaJapan
  2. 2.Research and Development Center for Earthquake and TsunamiJapan Agency for Marine-Earth Science and Technology (JAMSTEC)YokosukaJapan
  3. 3.Earth and Environmental SciencesQueens College, City University of New YorkFlushingUSA
  4. 4.Marine Geology and GeophysicsLamont-Doherty Earth Observatory of Columbia UniversityPalisadesUSA
  5. 5.Atmosphere and Ocean Research InstituteThe University of TokyoKashiwa-shiJapan

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