Journal of Oceanography

, Volume 73, Issue 4, pp 479–490 | Cite as

Long-term change and variation of salinity in the western North Pacific subtropical gyre revealed by 50-year long observations along 137°E

  • Eitarou Oka
  • Shota Katsura
  • Hiroyuki Inoue
  • Atsushi Kojima
  • Moeko Kitamoto
  • Toshiya Nakano
  • Toshio Suga
Open Access
Original Article


The 137°E repeat hydrographic section for 50 winters during 1967–2016 has been analyzed to examine interannual to interdecadal variations and long-term changes of salinity and temperature in the surface and intermediate layers of the western North Pacific, with a particular focus on freshening in the subtropical gyre. Rapid freshening on both isobars and isopycnals began in the mid-1990s and persisted for the last 20 years in the upper main thermocline/halocline in the western subtropical gyre. In addition, significant decadal variability of salinity existed in the subtropical mode water (STMW), as previously reported for the shallower layers. An analysis of the 144°E repeat hydrographic section during 1984–2013 supplemented by Argo profiling float data in 2014 and 2015 revealed that the freshening trend and decadal variability observed at 137°E originated in the winter mixed layer in the Kuroshio Extension (KE) region and was transmitted southwestward to 137°E 1–2 years later in association with the subduction and advection of STMW. The mechanism of these changes and variations in the source region was further investigated. In addition to the surface freshwater flux in the KE region pointed out by previous studies, the decadal KE variability in association with the Pacific Decadal Oscillation likely contributes to the decadal salinity variability through water exchange between the subtropics and the subarctic across the KE. Interdecadal change in both the surface freshwater flux and the KE state, however, failed to explain the rapid freshening for the last 20 years.


Western North Pacific subtropical gyre Main thermocline/halocline Long-term change Decadal variability Repeat hydrographic section 

1 Introduction

Long-term changes of salinity in the surface and intermediate layers of the world oceans have been investigated on the basis of repeat hydrography, historical data archives, and the Argo profiling float network (e.g., Wong et al. 1999; Boyer et al. 2005; Hosoda et al. 2009; Durack and Wijffels 2010) to detect intensification of salinity contrast between regions/basins suggesting that of the global hydrological cycle (Rhein et al. 2013). In the North Pacific subtropical gyre, both isobaric and isopycnal freshening has been widely observed in the main thermocline/halocline as well as the underlying salinity minimum layers of the North Pacific Intermediate Water (NPIW; Reid 1965) and the Tropical Salinity Minimum (TSM; Yuan and Talley 1992), and has been attributed to surface freshening and warming in the formation areas of these water masses and to the change of gyre circulation (Lukas 2001; Wong et al. 2001; Nakano et al. 2007; Ren and Riser 2010; Suzuki and Ishii 2011; Yan et al. 2013; Nan et al. 2015).

The rate and depths of observed freshening depend heavily on the period. When we compare the linear trend of isobaric salinity during 1967–2005 (Fig. 2a in Nakano et al. 2007) and that during 1992–2009 (Fig. 4c in Nan et al. 2015), both based on the repeat hydrographic section along the 137°E meridian, a freshening trend reaching −0.0015 (on the Practical Salinity Scale 1978) year−1 existed from the lower main halocline to NPIW/TSM during the former period, while the freshening trend was several times larger in magnitude and was located from the upper main halocline to the sea surface during the latter, more recent period. Such a difference suggests significant interdecadal variability and raises the following questions. How have the rate and depths of freshening in the North Pacific subtropical gyre changed over time? Has the freshening trend been accelerating in recent years? What water masses have played an important role for the recent rapid changes?

To answer these questions, long-term repeat observations at a fixed station or along a fixed line are indispensable. The aforementioned 137°E section traversing the western North Pacific (Masuzawa 1967; Fig. 1a) is the most appropriate one for such a purpose, achieving an unprecedented history of a half century in 2016. In this study, we analyze an extended time series of the 137°E section for 50 years from 1967 through 2016 to examine interannual to interdecadal variations and long-term changes of salinity and temperature in the surface and intermediate layers, with a particular focus on freshening in the subtropical gyre. By also using another repeat hydrographic section at 144°E, we will demonstrate that rapid freshening began in the mid-1990s and persisted for the last 20 years in the upper main halocline as a result of surface freshening in the KE region.
Fig. 1

a Geographical location of the 137°E section. Dots indicate grid points for optimal interpolation (Sect. 2). Light (dark) shading denotes regions shallower (deeper) than 4000 m (6000 m). Triangles indicate the location of CTD and expendable CTD stations at the 144°E section used in Sect. 4. Thick lines represent the area in which EP was averaged in Fig. 6c. b Latitude of observations at the 137°E section, plotted against year. Note that the data from summer observations were not used in this study

2 Data

Hydrographic observations at the 137°E section have been repeated every winter since 1967 and every summer since 1972 by the Japan Meteorological Agency (Masuzawa and Nagasaka 1975; Fig. 1b). The observations were conducted from 34°N to 1°S in earlier years, but have been limited to north of 3°N since winter 1987. The typical station spacing is 1° in latitude, except for 0.67° at 32–34°N. The collected data are publicly available online (

In this study, we used salinity (S) and temperature (T) data from 50 winter cruises in 1967–2016 because the winter observations have been repeated exactly in the latter half of January from the southern coast of Japan toward New Guinea and also because we liked to remove the influence of seasonal variations on our isobaric and isopycnal analyses. We optimally interpolated S and T between 3° and 34°N from each cruise onto grid points at every 1° (except for 0.67° at 32–34°N) meridional and 1 dbar vertical interval following Nakano et al. (2007) (Fig. 1a) and calculated potential temperature (θ) and density (σ θ ). It should be mentioned that the change of observation system in 1990, that is, switch from observations at standard depths by Nansen bottles to continuous measurements by a conductivity-temperature-depth profiler (CTD; Shuto 1996), does not affect the conclusions of this study. The measurement accuracy of S (T) has improved from 0.003 (0.004 °C) to 0.001 (0.002 °C) (Japan Meteorological Agency 1970; Talley et al. 2011), but even the earlier accuracy was sufficiently small compared to the observed variations and changes shown in the following sections (e.g., Fig. 3). As for the change in vertical sampling resolution, we made another dataset for 1990–2016 by extracting S and T values at the standard depths from the CTD data and combined it with the original data in 1967–1989 to obtain almost the same results (not shown).

We also used S and T data at a repeat hydrographic section along 144°E maintained by the Japan Coast Guard (its English name was the Japan Maritime Safety Agency before 2001) from 1984 through 2013. The observations were repeated every winter (mostly in February) using CTD and expendable CTD between 1°S and 35°N (Suga et al. 2000). Data after 1996 were downloaded online (, and those before 1995 were extracted from Japan Maritime Safety Agency (1986–1996). In addition, we used evaporation data from the Objectively Analyzed air–sea Fluxes (OAFlux) project (Yu and Weller 2007; Yu et al. 2008) and precipitation data from the Climate Prediction Center Merged Analysis of Precipitation (CMAP; Xie and Arkin 1996, 1997) and the Global Precipitation Climatology Project (GPCP; Huffman et al. 1997; Adler et al. 2003) during 1986–2014.

3 Long-term thermohaline variations and changes at 137°E

The linear trend of θ for 50 years (1967–2016) obtained by the least-squares method was positive at the sea surface throughout the 137°E section and exceeded 0.03 °C year−1 in two subsurface regions: 100–200 dbar at 8–17°N and 150–650 dbar at 30–33°N (Fig. 2a). The S trend was also positive in these regions, while it was mostly negative in the other part of the section and exceeds −0.001 year−1 at 100–600 dbar and 19–28°N (Fig. 2b). This large negative trend in the subtropical gyre, which was significant at the 95% confidence level, is shallower than that during 1967–2005 located mainly at 400–800 dbar (Fig. 2a in Nakano et al. 2007) and is a little deeper than that during 1992–2009 located between the sea surface and 600 dbar (Fig. 4c in Nan et al. 2015).
Fig. 2

Average (black contour; units °C in a) and linear trend (white contours with color; units °C year−1 in a and year−1 in b) of a θ and b S with respect to pressure in the 137°E section during 1967–2016. Crosses (dots) indicate regions where the linear trend is insignificant at the 90% (95%) confidence level. Green rectangles denote the regions where θ and S are averaged in Fig. 3. Linear trend of S during c 1967–1996 and d 1997–2016, otherwise following b

To examine the relation between trends and temporal variations, θ and S were averaged in three regions characterized by large trends (green boxes in Fig. 2a, b). In the first region at 100–200 dbar and 8–17°N, which corresponds to the upper permanent thermocline in the strong portion of the North Equatorial Current (NEC; e.g., Qiu and Joyce 1992), θ changed interannually and was high (low) during La Niña (El Niño) periods (Fig. 3a; θ anomalies from the low-pass filtered values were negatively correlated with 5-month running mean of the Niño-3 index with a coefficient R = −0.69), as demonstrated by previous analyses (e.g., Shuto 1996). It also showed a long-term increase after the mid-1990s, which is consistent with the southward shift of NEC detected by satellite altimeter measurements since 1992 (Qiu and Chen 2012). S in this region (Fig. 2b), which includes the most saline portion (S > 35) of the North Pacific Tropical Water (NPTW; Cannon 1966; Tsuchiya 1968) subducted from the central part of the subtropical gyre (Katsura et al. 2013), reflected not only the El Niño–Southern Oscillation state and the southward shift of NEC but also the long-term variation of NPTW (Saiki 1987; Suga et al. 2000; Fig. 3b). Its variation resembles well that in the area of NPTW south of 18°N in the 137°E section (Fig. 4c in Nakano et al. 2015).
Fig. 3

Time series of a θ and b S averaged at 100–200 dbar and 8–17°N in the 137°E section. Thick and thin curves denote the yearly values and values smoothed with a 10-year Gaussian filter, respectively. Horizontal bars at the top (bottom) of each panel indicate La Niña (El Niño) periods. c, d Time series averaged at 200–500 dbar and 30–32.67°N, otherwise following a, b. Horizontal bars at the bottom of each panel indicate large-meander periods of the Kuroshio. e, f Time series averaged at 200–500 dbar and 19–28°N, otherwise following a, b

The Kuroshio usually crosses the 137°E section near 33°N close to the southern coast of Japan, but occasionally shifts offshore as far south as 30°N (Qiu and Joyce 1992). Such a large meander state, which persists for several months to several years, frequently occurred during 1975–1991 and has hardly occurred since then (Kawabe 1995; Usui et al. 2013). θ and S in the second region at 200–500 dbar and 30–32.67°N concurrently dropped during large-meander periods (Fig. 3c, d) and showed an increasing trend (Fig. 2a, b) due to interdecadal change of large-meander occurrence (Fig. 3c, d).

In the third region at 200–500 dbar and 19–28°N in the subtropical halocline (Fig. 2b), which is the region of our interest, θ and S were highly correlated with each other on interannual time scales (Fig. 3e, f; R = 0.82 between anomalies from the low-pass filtered values), presumably associated with isopycnal depth variations, but were negatively correlated on interdecadal time scales (R = −0.40 between the low-pass filtered values). On interdecadal time scales, both θ and S gradually increased until around 1990, largely because of anomalously low values in 1973 under a strong El Niño condition (Masuzawa and Nagasaka 1975); subsequently, θ changed little, while S decreased significantly, particularly after the yearly values reached a pronounced maximum in 1997. When we divide the 50-year observation period into the former 30 years (1967–1996) and the latter 20 years (1997–2016) before and after the maximum, the S trend in the subtropical halocline for the former period was small with a magnitude mostly less than 0.001 year−1 (Fig. 2c), while that for the latter period was strongly negative with a minimum of −0.0064 year−1 located at 420 dbar, 22°N (Fig. 2d).

The freshening trend and the associated S variations in the subtropics are further examined on the σ θ coordinate to obtain more robust signals unaffected by isopycnal depth variations. The isopycnal S trend for 50 years was negative below the most saline portion of NPTW and exceeded −0.002 year−1 at σ θ  = 25.2–26.0 kg m−3 north of 14°N corresponding to the upper main halocline (Fig. 4a). By dividing again the observation period into two parts, we obtain clearly different trend distributions. In 1967–1996, a negative S trend less than −0.001 year−1 showed a patchy distribution at σ θ  = 25.5–27.0 kg m−3 north of 10°N, which corresponds mainly to the lower main halocline to the NPIW/TSM, while the trend was positive on isopycnals lighter than 25.2 kg m−3 (Fig. 4b). In 1997–2016, in contrast, a much stronger negative trend less than −0.005 year−1 existed at σ θ  = 25.0–26.2 kg m−3 north of 12°N corresponding mainly to the upper main halocline (Fig. 4c). The negative S trend during 1967–2016 (Fig. 4a) is greatly influenced by the rapid freshening for the last 20 years (Fig. 4c).
Fig. 4

Linear trend (white contours with color; units year−1) of S with respect to σ θ in the 137°E section during a 1967–2016, b 1967–1996, and c 1997–2016. Black contours indicate S averaged in 1967–2016. Crosses (dots) indicate regions where the linear trend is insignificant at the 90% (95%) confidence level

On the σ θ  = 25.5 kg m−3 isopycnal in the subtropical gyre, where the negative trend during 1997–2016 was strongest and reached a minimum of −0.0079 year−1 at 21°N, S fluctuated with a period of ~15 years from 1967 to around 1996 and then decreased significantly with a fluctuation with a period of ~10 years (Fig. 5b). S on σ θ  = 25.0 kg m−3 exhibited a similar variation with much larger decadal amplitude and led that on 25.5 kg m−3 by about 1 year, reaching pronounced maxima around 1969, 1982, 1996, 2006, and 2016 (Fig. 5a), as previously reported for the shallower layers including NPTW (Nakano et al. 2015; Nan et al. 2015). The 25.5 and 25.0 kg m−3 isopycnals correspond to the denser and lighter varieties of the subtropical mode water (STMW; Masuzawa 1969) formed in the eastern and western parts, respectively, of its formation region that extends zonally south of the Kuroshio and the Kuroshio Extension (KE) and north of 28°N (Suga and Hanawa 1990; Oka and Suga 2003). STMW, which ventilates the upper halocline in the 137°E section as far south as ~18°N (Suga et al. 1989; Oka 2009; Oka et al. 2015), seemed to contribute greatly to the observed changes and variations of subtropical S.
Fig. 5

Time series of S on isopycnals of σ θ  = a 25.0, b 25.5, c 26.0, d 26.4, and e 26.8 kg m−3, averaged at 14–16°N (black), 17–19°N (red), 20–22°N (yellow), 23–25°N (green), and 26–28°N (blue) in the 137°E section. Average during 1967–2016 was subtracted from each time series

On the σ θ  = 26.0 kg m−3 isopycnal, which corresponds to the lighter variety of the Central Mode Water (L-CMW) formed just north of the KE (Nakamura 1996; Suga et al. 1997; Oka and Suga 2005; Oka et al. 2011), S showed somewhat smaller decadal variations than that on the STMW isopycnals from 1967 to around 1996 and a steady decrease after that (Fig. 5c). S also decreased steadily for the last 20 years on the σ θ  = 26.4 kg m−3 isopycnal corresponding to the denser variety of CMW north of 17°N and TSM south of 17°N (Fig. 5d). On σ θ  = 26.8 kg m−3 corresponding to NPIW north of 17°N (Kaneko et al. 1998), unlike the shallower isopycnals, S fluctuated on an interannual time scale and gradually decreased for the past 50 years (Fig. 5e).

4 Relation to variations and changes in source region

The strong freshening trend for the last 20 years existing in the subsurface layers related to STMW and L-CMW at 137°E suggests that freshening originated in the late winter mixed layer in the KE region where these water masses are formed (e.g., Oka and Qiu 2012), as inferred by Yan et al. (2013) and Nan et al. (2015). We therefore analyzed the 144°E section in winter (mostly February) from 1984 through 2013. S and θ at 50 dbar were averaged at stations between 30° and 35°N because the station location differed among years. They were averaged only at those stations where θ at 300 dbar exceeded 15 °C to ensure that the observations were conducted in the STMW formation region located south of the KE and outside cyclonic eddies. The time series was extended to 2015 by using Argo profiling float data at 30–35°N, 143–145°E in February of 2014 and 2015, edited as outlined in Oka et al. (2007).

The obtained winter mixed layer S at 144°E fluctuated interannually from 1984 through 1995 and then showed a long-term decrease with a remarkable decadal variation (Fig. 6a), as recently reported for a broader KE recirculation region (Kitamura et al. 2016). S reached maxima in 1995, 2005, and 2015, each of which occurred 1–2 years earlier than that observed on the STMW isopycnals at 137°E (Fig. 5a, b). It is highly correlated (R = 0.80–0.90) with a time lag of 1 year with S on the σ θ  = 25.0 kg m−3 isopycnal north of 17°N shown in Fig. 5a. Furthermore, its decreasing trend during 1995–2015 (−0.0072 year−1), together with the decreasing trend of the winter mixed layer θ (−1.4 × 10−2 °C year−1; Fig. 6a), yields an isopycnal freshening trend of about −0.008 year−1, which is almost equal to that observed in the STMW layer at 137°E.1 Such a correspondence between the 144° and 137°E sections clearly demonstrates that the freshening trend and decadal S variation observed at 137°E originated in the KE region and was transmitted to 137°E 1–2 years later in association with the subduction and advection of STMW (Suga et al. 1989; Oka 2009; Oka et al. 2015).
Fig. 6

a Time series of S (black circles) and θ (white circles) at 50 dbar averaged between 30° and 35°N in the 144°E section. b Annual change of S shown in a. The change in 1986, for example, is defined as the difference in S between 1986 and 1987. c Time series of EP averaged annually at 30–35°N, 141–150°E using precipitation data from CMAP (black circles) and GPCP (white circles). d Time series of annual average of the KE index

What causes these S changes and variations in the source region? Following previous studies (Sugimoto et al. 2013; Nakano et al. 2015; Nan et al. 2015; Kitamura et al. 2016), we first examined the influence of the surface freshwater flux on the decadal S variation of STMW. Evaporation minus precipitation (E − P) averaged annually at 30–35°N, 141–150°E (Fig. 6c; the area is shown in Fig. 1a) was positively correlated with the annual change of the winter mixed layer S at 144°E during 1986–2015 (Fig. 6b) with R = 0.29 and 0.19 when precipitation data from CMAP and GPCP were used, respectively.

It has been revealed during the last decade that the KE jet and its associated eddy field exhibit decadal variability (Qiu and Chen 2005; Qiu et al. 2007) in association with the Pacific Decadal Oscillation (Mantua et al. 1997) and that the winter mixed layer depth in the STMW formation region decreases (increases) during the unstable (stable) KE period (Oka et al. 2015), likely because high (low) eddy activity transports more (less) high potential-vorticity water north of the KE to the STMW formation region to hinder (facilitate) mixed layer deepening (Qiu and Chen 2006). Such eddy activity, at the same time, is expected to transport more (less) fresher water north of the KE to the STMW formation region to decrease (increase) the mixed layer S. When we look at the relation to the KE index (Fig. 6d), which was defined by Qiu et al. (2014) as the average of four KE-related parameters based on the satellite altimeter measurements, there is a connection that the winter mixed layer S at 144°E decreased (increased) during the unstable (stable) KE period represented by a negative (positive) KE index. In fact, the annual change of the winter mixed layer S during 1993–2015 is highly correlated with the annual-mean KE index (R = 0.63; significant at the 99% confidence level). Thus, in addition to the surface freshwater flux, the KE state likely contributes to the decadal S variability of STMW. A similar relation between S of NPIW and the state of the downstream KE was reported by Qiu and Chen (2011).

Does either the surface freshwater flux or the KE state explain the freshening trend for the last 20 years, too? On average, E − P at 30–35°N, 141–150°E was −9.1 (−13.0) cm year−1 during 1979–1994 and 3.5 (4.9) cm year−1 during 1995–2014 with the CMAP (GPCP) precipitation data being larger during the latter period. The KE index extended back to 1977 using multidecadal hindcast simulation2 (Fig. 5b in Qiu et al. 2014) was −0.41 cm during 1977–1994 and 0.41 cm during 1995–2012, indicating that the KE tended to be slightly more stable during the latter period. Thus, both the surface freshwater flux and the eddy activity acted to increase the mixed layer S in the STMW formation region after 1995, compared to the prior period, and are not likely to explain the recent freshening.

5 Summary and discussion

Our analysis of the 137°E section from 1967 through 2016 demonstrated that rapid freshening on both isobars and isopycnals began in the mid-1990s and persisted for the last 20 years in the upper main thermocline/halocline related to STMW and L-CMW in the western North Pacific subtropical gyre. The freshening trend of −0.0064 year−1 on isobars is equivalent to a lightening trend of σ θ  = −0.005 kg m−3 year−1 and has decreased the density in the main pycnocline by 0.1 kg m−3 over the last 20 years. If such an amount of density change had occurred in a 300-m-thick water column, the sea level would have risen by 3 cm at a rate of 1.5 mm year−1, contributing significantly to the baroclinic sea level rise in the western subtropical gyre during the last few decades (Suzuki and Ishii 2011). In addition to the freshening trend, significant decadal S variability existed in the STMW layer, with a dominant period of ~15 years before the mid-1990s and ~10 years after that, as previously reported for the shallower layers including NPTW in the 137°E section (Nakano et al. 2015; Nan et al. 2015). Such large variability implies that the estimation of trends from relatively short time series like Argo (Roemmich et al. 2001) can lead to significant over/underestimation. The analysis of the 144°E section during 1984–2015 revealed that the freshening trend and decadal S variability observed at 137°E originated in the winter mixed layer in the KE region and was transmitted to 137°E 1–2 years later in association with the subduction and advection of STMW.

The mechanism of these changes and variations in the source region was further investigated. In addition to the surface freshwater flux in the KE region pointed out by previous studies, the KE state likely contributes to the decadal S variability. Specifically, high (low) eddy activity during the unstable (stable) KE period, which lags the warm (cool) phase of the Pacific Decadal Oscillation by 3–4 years (Qiu et al. 2007), transports more (less) fresher water north of the KE to the STMW formation region to decrease (increase) S of the deep winter mixed layer. The freshening trend for the last 20 years, however, cannot be explained by interdecadal change in either the surface freshwater flux or the KE state. This problem is left for a future study.

A noteworthy feature found in Fig. 5 is the coherent S variations among latitudes and isopycnals. First, decadal variations on each isopycnal in the STMW density range (σ θ  = 25.0 and 25.5 kg m−3) occurred almost simultaneously across the subtropical gyre between 14° and 28°N. If we assume streamlines on these isopycnals based on climatological S and T, a water parcel reaching a southern station of the 137°E section along an outer path from its outcrop region should take a much longer time than that reaching a northern station along an inner path (Fig. 3 in Bingham et al. 2002; for example, a water parcel on σ θ  = 25.0 kg m−3 reaching 24°N takes 4.3 years, while that reaching 16°N takes 11.4 years). In the real ocean, eddy mixing seems to spread rapidly the isopycnal θ/S anomalies, or spiciness anomalies, southward once STMW is subducted to the permanent pycnocline. This is supported by the recent observations along the 149°E meridian, where radiocesium released from the Fukushima Dai-ichi nuclear power plant in March 2011 spread as far south as 20°N in January 2012, only 10 months after the accident (Kumamoto et al. 2014). Secondly, the rapid freshening initiated almost simultaneously around 1996 between σ θ  = 25.0 and 26.4 kg m−3 (Fig. 5a–d) despite our expectation that CMW subducted from the region north of KE takes an even longer time (more than 16 years according to Fig. 3 in Bingham et al. 2002) to reach the 137°E section if we assume its large-scale circulation (Bingham et al. 2002; Suga et al. 2004; Oka et al. 2011). Since decadal variations were small on σ θ  = 26.0 and 26.4 kg m−3, the diapycnal-mixing mechanism is less likely. A possible explanation is that the southward, mesoscale subduction of CMW across the KE (Oka et al. 2009, 2014) occurs so vigorously that the CMW layer in the 137°E section quickly responded to the surface freshening north of the KE. Another possibility is that the area of surface freshening spread southward year by year, from the region north of the KE to that south of it.

Another remaining problem is that θ in the winter mixed layer at 144°E was negatively correlated with S (R = −0.35 during 1984–2015; Fig. 6a) in spite of our expectation that high (low) eddy activity during the unstable (stable) KE period transports more (less) not only fresher but also colder water north of the KE to the STMW formation region to decrease (increase) both S and θ. Actually, Sugimoto and Kako (2016) recently analyzed historical T profiles during 1968–2014 to claim that after ~1990 the winter mixed layer θ in the STMW formation region increases (decreases) during the unstable (stable) KE period, mainly as a result of a weaker (stronger) cooling effect of entrainment in association with the winter mixed layer shallowing (deepening). Since not only θ but also S decreases downward below STMW (e.g., Hanawa and Talley 2001), the weaker (stronger) entrainment effect during the unstable (stable) KE period acts to increase (decrease) both the mixed layer S and θ, in the opposite way to the high (low) eddy activity. The opposite effects of entrainment and eddy activity to the decadal S and θ variations in the STMW formation region need to be quantified for further understanding of the mechanism.


  1. 1.

    The trend of winter mixed layer θ during 1995–2015 was calculated without an anomalously high value in 1999 possibly owing to earlier observations around January 10. Assuming the θS relation in the main pycnocline in the western subtropical gyre, the trends of winter mixed layer θ and S yield those on isopycnals of about −0.009 and 0.001 year−1, respectively.

  2. 2.

    The KE index here is defined using sea surface height anomaly and has a unit of cm, while that shown in Fig. 6d is defined using four KE-related parameters and is unitless.



The authors are grateful to the past and present captains and crews of R/Vs Ryofu maru and Keifu maru and staff of the Marine Division (and the former Oceanographical Division), Japan Meteorological Agency, for their laudable efforts in long-term observations. They also thank Katsuro Katsumata, Shinya Kouketsu, Takashi Sakamoto, Shusaku Sugimoto, Tatsuro Suzuki, Hiroyuki Yoritaka, participants at the “Research Meeting on Air-Sea Interaction” in 2016 held as a part of the Collaborative Research Program of the Institute for Space-Earth Environmental Research, Nagoya University, and anonymous reviewers for helpful comments on the manuscript. E. O. and T. S. acknowledge support by the Japan Society for the Promotion of Science (JSPS) through Grant 21340133 and 25287118. T. S. also acknowledges support by JSPS through Grant 15H02129. S. K. is a research fellow of JSPS and is supported by JSPS through 15J05210.


  1. Adler RF et al (2003) The version-2 global precipitation climatology project (GPCP) monthly precipitation analysis (1979–present). J Hydrometeor 4:1147–1167CrossRefGoogle Scholar
  2. Bingham FM, Suga T, Hanawa K (2002) Origin of waters observed along 137°E. J Geophys Res 107:3073. doi: 10.1029/2000JC000722 CrossRefGoogle Scholar
  3. Boyer TP, Antonov JI, Levitus S, Locarnini R (2005) Linear trends of salinity for the world ocean, 1955–1998. Geophys Res Lett 32:L01604. doi: 10.1029/2004GL021791 CrossRefGoogle Scholar
  4. Cannon GA (1966) Tropical waters in the western Pacific Oceans, August–September 1957. Deep-Sea Res Oceanogr Abstr 13:1139–1148CrossRefGoogle Scholar
  5. Durack PJ, Wijffels SE (2010) Fifty-year trend in global ocean salinities and their relationship to broad-scale warming. J Clim 23:4342–4362. doi: 10.1175/2010JCLI3377.1 CrossRefGoogle Scholar
  6. Hanawa K, Talley LD (2001) Mode waters. In: Church J et al (eds) Ocean circulation and climate. Academic, London, pp 373–386Google Scholar
  7. Hosoda S, Suga T, Shikama N, Mizuno K (2009) Global surface layer salinity change detected by ARGO and its implication for hydrological cycle intensification. J Oceanogr 65:579–586. doi: 10.1007/s10872-009-0049-1 CrossRefGoogle Scholar
  8. Huffman GJ et al (1997) The Global Precipitation Climatology Project (GPCP) combined precipitation dataset. Bull Am Meteorol Soc 78:5–20CrossRefGoogle Scholar
  9. Japan Maritime Safety Agency (1986–1996) Data report of hydrographic observations—series of WESTPAC, Nos. 1–11Google Scholar
  10. Japan Meteorological Agency (1970) Manual on oceanographic observations. p 427 (in Japanese)Google Scholar
  11. Kaneko I, Takatsuki Y, Kamiya H, Kawae S (1998) Water property and current distributions along the WHP-P9 section (137°–142°E) in the western North Pacific. J Geophys Res 103:12959–12984CrossRefGoogle Scholar
  12. Katsura S, Oka E, Qiu B, Schneider N (2013) Formation and subduction of North Pacific tropical water and their interannual variability. J Phys Oceanogr 43:2400–2415CrossRefGoogle Scholar
  13. Kawabe M (1995) Variations of current path, velocity, and volume transport of the Kuroshio in relation with the large meander. J Phys Oceanogr 25:3103–3117CrossRefGoogle Scholar
  14. Kitamura T, Nakano T, Sugimoto S (2016) Decadal variations in mixed layer salinity in the Kuroshio Extension recirculation gyre region: influence of precipitation during the warm season. J Oceanogr 72:167–175CrossRefGoogle Scholar
  15. Kumamoto Y, Aoyama M, Hamajima Y, Aono T, Kouketsu S, Murata A, Kawano T (2014) Southward spreading of the Fukushima-derived radiocaesium across the Kuroshio Extension in the North Pacific. Sci Rep 4:4276. doi: 10.1038/srep04276 CrossRefGoogle Scholar
  16. Lukas R (2001) Freshening of the upper thermocline in the North Pacific subtropical gyre associated with decadal changes of rainfall. Geophys Res Lett 28:3485–3488CrossRefGoogle Scholar
  17. Mantua NJ, Hare SR, Zhang Y, Wallace JM, Francis RC (1997) A Pacific interdecadal climate oscillation with impacts on salmon production. Bull Am Meteorol Soc 78:1069–1079CrossRefGoogle Scholar
  18. Masuzawa J (1967) An oceanographic section from Japan to New Guinea at 137°E in January 1967. Oceanogr Mag 19:95–118Google Scholar
  19. Masuzawa J (1969) Subtropical mode water. Deep-Sea Res 16:463–472Google Scholar
  20. Masuzawa J, Nagasaka K (1975) The 137°E oceanographic section. J Mar Res 33(Suppl):109–116Google Scholar
  21. Nakamura H (1996) A pycnostad on the bottom of the ventilated portion in the central subtropical North Pacific: its distribution and formation. J Oceanogr 52:171–188CrossRefGoogle Scholar
  22. Nakano T, Kaneko I, Soga T, Tsujino H, Yasuda T, Ishizaki H, Kamachi M (2007) Mid-depth freshening in the North Pacific subtropical gyre observed along the JMA repeat and WOCE hydrographic sections. Geophys Res Lett 34:L23608. doi: 10.1029/2007GL031433 CrossRefGoogle Scholar
  23. Nakano T, Kitamura T, Sugimoto S, Suga T, Kamachi M (2015) Long-term variations of North Pacific tropical water along the 137°E repeat hydrographic section. J Oceanogr 71:229–238CrossRefGoogle Scholar
  24. Nan F, Yu F, Wang R, Si G (2015) Ocean salinity changes in the northwest Pacific subtropical gyre: the quasi-decadal oscillation and the freshening trend. J Geophys Res 120:2179–2192CrossRefGoogle Scholar
  25. Oka E (2009) Seasonal and interannual variation of North Pacific subtropical mode water in 2003–2006. J Oceanogr 65:151–164CrossRefGoogle Scholar
  26. Oka E, Qiu B (2012) Progress of North Pacific mode water research in the past decade. J Oceanogr 68:5–20CrossRefGoogle Scholar
  27. Oka E, Suga T (2003) Formation region of North Pacific subtropical mode water in the late winter of 2003. Geophys Res Lett 30:2205. doi: 10.1029/2003GL018581 CrossRefGoogle Scholar
  28. Oka E, Suga T (2005) Differential formation and circulation of North Pacific Central Mode Water. J Phys Oceanogr 35:1997–2011CrossRefGoogle Scholar
  29. Oka E, Talley LD, Suga T (2007) Temporal variability of winter mixed layer in the mid- to high-latitude North Pacific. J Oceanogr 63:293–307CrossRefGoogle Scholar
  30. Oka E, Toyama K, Suga T (2009) Subduction of North Pacific central mode water associated with subsurface mesoscale eddy. Geophys Res Lett 36:L08607. doi: 10.1029/2009GL037540 CrossRefGoogle Scholar
  31. Oka E, Kouketsu S, Toyama K, Uehara K, Kobayashi T, Hosoda S, Suga T (2011) Formation and subduction of Central Mode Water based on profiling float data, 2003–08. J Phys Oceanogr 41:113–129CrossRefGoogle Scholar
  32. Oka E, Uehara K, Nakano T, Suga T, Yanagimoto D, Kouketsu S, Itoh S, Katsura S, Talley LD (2014) Synoptic observation of Central Mode Water in its formation region in spring 2003. J Oceanogr 70:521–534CrossRefGoogle Scholar
  33. Oka E, Qiu B, Takatani Y, Enyo K, Sasano D, Kosugi N, Ishii M, Nakano T, Suga T (2015) Decadal variability of subtropical mode water subduction and its impact on biogeochemistry. J Oceanogr 71:389–400CrossRefGoogle Scholar
  34. Qiu B, Chen S (2005) Variability of the Kuroshio Extension jet, recirculation gyre and mesoscale eddies on decadal timescales. J Phys Oceanogr 35:2090–2103CrossRefGoogle Scholar
  35. Qiu B, Chen S (2006) Decadal variability in the formation of the North Pacific subtropical mode water: oceanic versus atmospheric control. J Phys Oceanogr 36:1365–1380CrossRefGoogle Scholar
  36. Qiu B, Chen S (2011) Effect of decadal Kuroshio Extension jet and eddy variability on the modification of North Pacific Intermediate Water. J Phys Oceanogr 41:503–515CrossRefGoogle Scholar
  37. Qiu B, Chen S (2012) Multidecadal sea level and gyre circulation variability in the northwestern tropical Pacific Ocean. J Phys Oceanogr 42:193–206CrossRefGoogle Scholar
  38. Qiu B, Joyce TM (1992) Interannual variability in the mid- and low-latitude western North Pacific. J Phys Oceanogr 22:1062–1079CrossRefGoogle Scholar
  39. Qiu B, Chen S, Hacker P (2007) Effect of mesoscale eddies on subtropical mode water variability from the Kuroshio Extension System Study (KESS). J Phys Oceanogr 37:982–1000CrossRefGoogle Scholar
  40. Qiu B, Chen S, Schneider N, Taguchi B (2014) A coupled decadal prediction of the dynamic state of the Kuroshio Extension system. J Clim 27:1751–1764CrossRefGoogle Scholar
  41. Reid JL Jr (1965) Intermediate waters of the Pacific Ocean. Johns Hopkins Oceanography Studies, vol 2. Johns Hopkins University Press, Baltimore, p 85Google Scholar
  42. Ren L, Riser SC (2010) Observations of decadal time scale salinity changes in the subtropical thermocline of the North Pacific Ocean. Deep Sea Res Part II 57:1161–1170CrossRefGoogle Scholar
  43. Rhein M, Rintoula S, Aoki S, Campos E, Chambers D, Feely R, Gulev S, Johnson G, Josey S, Kostianoy A, Mauritzen C, Roemmich D, Talley L, Wang F (2013) Observations: ocean. In: Stocker TF, Qin D, Plattner GK, Tignor M, Allen SK, Boschung J, Nauels A, Xia Y, Bex V, Midgley PM (eds) Climate change 2013: the physical science basis. Contribution of working group I to the fifth assessment report of the intergovernmental panel on climate change. Cambridge University Press, CambridgeGoogle Scholar
  44. Roemmich D, Boebel O, Desaubies Y, Freeland H, King B, LeTraon PY, Molinari R, Owens WB, Riser S, Send U, Takeuchi K, Wijffels S (2001) Argo: the global array of profiling floats. In: Koblinsky CJ, Smith NR (eds) Observing the oceans in the 21st century. GODAE Project Office, Bureau of Meteorology, Melbourne, pp 248–258Google Scholar
  45. Saiki M (1987) Interannual variation of the subtropical gyre in the western North Pacific. Umi to Sora 63:113–125 (in Japanese with English abstract)Google Scholar
  46. Shuto K (1996) Interannual variations of water temperature and salinity along the 137°E meridian. J Oceanogr 52:575–595CrossRefGoogle Scholar
  47. Suga T, Hanawa K (1990) The mixed layer climatology in the northwestern part of the North Pacific subtropical gyre and the formation area of subtropical mode water. J Mar Res 48:543–566CrossRefGoogle Scholar
  48. Suga T, Hanawa K, Toba Y (1989) Subtropical mode water in the 137°E section. J Phys Oceanogr 19:1605–1618CrossRefGoogle Scholar
  49. Suga T, Takei Y, Hanawa K (1997) Thermostad distribution in the North Pacific subtropical gyre: the central mode water and the subtropical mode water. J Phys Oceanogr 27:140–152CrossRefGoogle Scholar
  50. Suga T, Kato A, Hanawa K (2000) North Pacific Tropical Water: its climatology and temporal changes associated with the climate regime shift in the 1970s. Prog Oceanogr 47:223–256CrossRefGoogle Scholar
  51. Suga T, Motoki K, Aoki Y, Macdonald AM (2004) The North Pacific climatology of winter mixed layer and mode waters. J Phys Oceanogr 34:3–22CrossRefGoogle Scholar
  52. Sugimoto S, Kako SI (2016) Decadal variation in winter mixed layer depth south of the Kuroshio Extension and its influence on winter mixed layer temperature. J Climate 29:1237–1252CrossRefGoogle Scholar
  53. Sugimoto S, Takahashi N, Hanawa K (2013) Marked freshening of North Pacific subtropical mode water in 2009 and 2010: influence of freshwater supply in the 2008 warm season. Geophys Res Lett 40:3102–3105CrossRefGoogle Scholar
  54. Suzuki T, Ishii M (2011) Long-term regional sea level changes due to variations in water mass density during the period 1981–2007. Geophys Res Lett 38:L21604. doi: 10.1029/2011GL049326 Google Scholar
  55. Talley LD, Pickard GL, Emery WJ, Swift JH (2011) Descriptive physical oceanography: an introduction. Academic, New York, p 560Google Scholar
  56. Tsuchiya M (1968) Upper waters of the intertropical Pacific Ocean. Johns Hopkins Oceanography Studies, vol 4. Johns Hopkins University Press, Baltimore, p 50Google Scholar
  57. Usui N, Tsujino H, Nakano H, Matsumoto S (2013) Long-term variability of the Kuroshio path south of Japan. J Oceanogr 69:647–670CrossRefGoogle Scholar
  58. Wong APS, Bindoff NL, Church JA (1999) Large-scale freshening of intermediate waters in the Pacific and Indian Oceans. Nature 400:440–443CrossRefGoogle Scholar
  59. Wong APS, Bindoff NL, Church JA (2001) Freshwater and heat changes in the north and south Pacific Oceans between the 1960s and 1985–94. J Clim 14:1613–1633CrossRefGoogle Scholar
  60. Xie P, Arkin PA (1996) Analyses of global monthly precipitation using gauge observations, satellite estimates, and numerical model predictions. J Clim 9:840–858CrossRefGoogle Scholar
  61. Xie P, Arkin PA (1997) A 17-year monthly analysis based on gauge observations, satellite estimates and numerical model outputs. Bull Am Meteorol Soc 78:2539–2558CrossRefGoogle Scholar
  62. Yan YF, Chassignet EP, Qi YQ, Dewar WK (2013) Freshening of subsurface waters in the northwest Pacific subtropical gyre: observations and dynamics. J Phys Oceanogr 43:2733–2751CrossRefGoogle Scholar
  63. Yu L, Weller RA (2007) Objectively Analyzed air-sea heat Fluxes (OAFlux) for the global ocean. Bull Am Meteorol Soc 88:527–539CrossRefGoogle Scholar
  64. Yu L, Jin X, Weller R (2008) Multidecade global flux datasets from the Objectively Analyzed Air-sea Fluxes (OAFlux) Project: latent and sensible heat fluxes, ocean evaporation, and related surface meteorological variables. OAFlux Proj technical report OA-2008-01Google Scholar
  65. Yuan X, Talley LD (1992) Shallow salinity minima in the North Pacific. J Phys Oceanogr 22:1302–1316CrossRefGoogle Scholar

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Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (, 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

  • Eitarou Oka
    • 1
  • Shota Katsura
    • 1
  • Hiroyuki Inoue
    • 2
  • Atsushi Kojima
    • 2
    • 3
  • Moeko Kitamoto
    • 2
    • 3
  • Toshiya Nakano
    • 2
    • 3
  • Toshio Suga
    • 4
    • 5
  1. 1.Atmosphere and Ocean Research InstituteThe University of TokyoKashiwaJapan
  2. 2.Global Environment and Marine DepartmentJapan Meteorological AgencyTokyoJapan
  3. 3.Oceanography and Geochemistry Research DepartmentMeteorological Research InstituteTsukubaJapan
  4. 4.Department of Geophysics, Graduate School of ScienceTohoku UniversitySendaiJapan
  5. 5.Research and Development Center for Global ChangeJapan Agency for Marine-Earth Science and TechnologyYokosukaJapan

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