NOVEMBER 2005

OKA AND SUGA

1997

Differential Formation and Circulation of North Pacific Central Mode Water
EITAROU OKA
Institute of Observational Research for Global Change, JAMSTEC, Yokosuka, JapanTOSHIO SUGA
Institute of Observational Research for Global Change, JAMSTEC, Yokosuka, and Department of Geophysics,
Graduate School of Science, Tohoku University, Sendai, Japan(Manuscript received 23 July 2004, in final form 4 May 2005)
ABSTRACTA repeat hydrographic section along 165°E was analyzed to verify a westward extension of the formation
region of the North Pacific Ocean Central Mode Water (CMW) suggested by previous synoptic observations, and to investigate the relation between the formation region and thermohaline fronts. The CMW
formation region extends at least as far west as 155°E, much farther than recognized in a previous study
based on climatology. It is located in two interfrontal regions between the Kuroshio Extension front and theKuroshio Bifurcation front (KBF), and between the KBF and the subarctic front, where two types of
CMW—namely, the lighter variety with potential density of 25.8–26.2 kg m⫺3 and the denser one of 26.3–26.4
kg m⫺3—are formed. How this differential formation of CMW is reflected in its gyrewide distribution was
examined using one-time sections of the World Ocean Circulation Experiment (WOCE) Hydrographic
Program in the North Pacific. The main circulation paths of the two types of CMW diverge east of the dateline; the lighter variety is located in the inner part of the eastern subtropical gyre, and the denser variety is
located in the outer part. These results demonstrate that the frontal structure around the northern boundaryof the subtropical gyre, particularly the existence of KBF, is essential in determining the properties and the
gyrewide distribution of CMW.

1. Introduction
The North Pacific Ocean Central Mode Water(CMW) is characterized by a pycnostad of ␴␪ ⫽ 26.0–
26.5 kg m⫺3 (␴␪ is potential density; Nakamura 1996),
or a thermostad with a core temperature of 10°–13°C(Suga et al. 1997), thus identified by its low potential
vorticity (PV), lying in the lower ventilated pycnocline,
mainly in the central part of the subtropical gyre (Fig.
1). It is formed in late winter in the deep mixed layer
near the northern boundary of the gyre and spreads
through advection by the clockwise gyral circulation.
Suga et al. (1997) analyzed the climatology of upper
thermal fields and inferred that CMW is formed between 175°E and 160°W. However, other studies havepresented examples of synoptic observations suggesting

Corresponding author address: Dr. Eitarou Oka, Institute ofObservational Research for Global Change, JAMSTEC, 2-15
Natsushima-Cho, Yokosuka, Kanagawa 237-0061, Japan.
E-mail: okae@jamstec.go.jp© 2005 American Meteorological Society

JPO2811that CMW is also formed farther west: at 40°N, 154°E
in April 1971 (Nakamura 1996); at 37°N, 165°E in May
1993 (Kawabe and Taira 1998); and at 37°N between
151° and 165°E in February and March 2003 (Oka andSuga 2003). If these examples are not exceptional, theCMW formation region extends much farther westward(upstream) than is recognized in the climatology ofSuga et al. (1997). To verify this westward extension, we
need to examine a number of synoptic observations
west of 175°E near the northern boundary of the subtropical gyre.
Along this northern gyre boundary there are threethermohaline fronts: the Kuroshio Extension front(KEF), the Kuroshio Bifurcation front (KBF), and thesubarctic front (SAF), from south to north. Here, theterm SAF is used for a boundary between the warmer,
saltier water in the subtropical gyre, and the colder,fresher water in the subarctic gyre, characterized bylarge horizontal gradients of temperature and salinity at
depths less than 100 dbar (Roden 1970, 1972; Zhang
and Hanawa 1993; Yuan and Talley 1996). Nakamura

1998

JOURNAL OF PHYSICAL OCEANOGRAPHY

VOLUME 35

FIG. 1. Annual-mean climatology of PV (10⫺10 m⫺1 s⫺1; thin black contours with shade) andpressure anomaly streamfunction (m2 s⫺2; thin white contours) relative to 2000 dbar on the
isopycnal of ␴␪ ⫽ 26.2 kg m⫺3, adapted from Suga et al. (2004). The thick white contour
denotes the winter outcrop of the isopycnal. The thick black line denotes the part of the 165°E
section used in this study.

(1996) inferred that CMW is formed between the SAF
and the “9°C front” at 300-m depth, which represents,
by his definition, a branch of the main path of the Kuroshio Extension rather than the KBF. Suga et al. (1997)
mentioned that CMW is formed between the KEF and
the KBF, although they did not examine the region
north of the KBF because of a lack of salinity data.
Both of these studies described the formation region in
relation to the frontal structure but were based on climatologies in which fronts with high temporal and spatial variability are not adequately depicted. To clarify
the relation between the CMW formation region andthe fronts, an examination of synoptic sections acrossthem is crucial.
Kawabe and Taira (1998), analyzing the World
Ocean Circulation Experiment (WOCE) Hydrographic
Program (WHP) P13J section along 165°E in May 1993,
indicated that CMW is formed between the KEF and
the KBF, which agrees with the inference of Suga et al.
(1997). Furthermore, a recent numerical simulation by
Tsujino and Yasuda (2004) demonstrated that CMW isformed both between the KEF and the KBF, and between the KBF and the SAF, with different densities
across the KBF. These results need to be verified byanalyzing more synoptic sections across the fronts.
The Japan Meteorological Agency (JMA) has repeated hydrographic and chemical observations at asection along 165°E (Fig. 1) a couple of times per year
since 1996 to quantitatively understand oceanic variations and greenhouse gas circulations in the western
North and equatorial Pacific that are closely related toclimate variations. This paper analyzes this repeat section in 1996–2003, supplemented by three WHP onetime sections along 165°E in 1991–93, to verify the possible westward extension of the CMW formation re-gion and to investigate the relation between theformation region and the fronts. Since the mean flow at
this section is predominantly eastward, the CMW appearing there is believed to be formed to the west.
Therefore, constant existence of the CMW in the section will verify that the CMW formation region extends
at least as far west as 165°E. We will also clarify that
CMW is formed in the two interfrontal regions between
the KEF and the KBF and between the KBF and the
SAF and that the CMW formed in the southern interfrontal region is significantly warmer and lighter thanthat formed in the northern region, which agrees with
the numerical result of Tsujino and Yasuda (2004).
How this differential formation of CMW is reflected inits gyrewide distribution is further investigated using
the WHP one-time sections in the North Pacific.
The data used are explained in section 2. The locations of the fronts at the 165°E section are determinedin section 3. In section 4, the CMW appearing in the
165°E section is examined in detail, focusing on thetime and the locations of its formation. The gyrewide
distribution of the two types of CMW is studied in section 5. Summary and discussion are given in section 6.

2. DataTemperature and salinity data of the 165°E section
between 30° and 45°N in springs of 1996–98 and 2000–
03, and summers of 1996–98, obtained by the JMA(1997, 1998, 1999, 2001, 2002, 2003), were used (Table1). The data from spring 1999 were not used because
the observations were limited to the north of 40°N,
covering only a small portion of the CMW distribution
range. The observations were conducted at intervals of
1° latitude using a conductivity–temperature–depthNOVEMBER 2005

OKA AND SUGATABLE 1. Latitudes and dates of the observations at 165°E in (a)spring and (b) summer, used in this study. Latitudes of the KEF,
KBF, and SAF at 165°E are also presented.
(a)
Year

Lat
(°N)

Date

KEF
(°N)

KBF
(°N)

SAF
(°N)

1993
1996
1997
1998
2000
2001

30–45
32–45
30–45
30–45
30–45
35–45

18–25 May
19–24 May
07–11 Jun
17–21 Jun
09–14 May
16–19 May

33–34
31–32
34–35
35–37
33–34
33–35

37–39
37–38
37–38
39–40
37–39
37–38

2002
2003

30–45
37–45

18–22 May
03–06 May

36–37
No data

38–40
37–39

39–41
40–41
40–41
41–42
40–41
40–41,
42–43
41–42
40–42

Year

Lat
(°N)

Date

KEF
(°N)

KBF
(°N)

SAF
(°N)

1991
1992
1996
1997
1998

30–40
30.7–45
30–45
30–45
30–45

17–22 Aug
30 Aug–10 Sep
14–19 Oct
18–22 Sep
23–27 Sep

34–35
34–34.7
35–36
33–34
35–36

38–39
38.5–39.5
37–38
37–38
—

No data
41.5–42
40–42
41–42
41–42

1999

to increase because of the oxygen consumption throughremineralization of organic matter after the water parcel is isolated from the atmosphere. This is used in
section 4 to estimate the ages of CMW parcels.
CTD and dissolved oxygen data at three WHP onetime sections along 165°E, named P13, P13C, and P13J,
were also used. The P13J section occupied in May 1993
was supplemented as a spring section; P13C in August
1991 and P13 in August–September 1992 were added assummer sections (Table 1). The data from these sections between 30° and 45°N, obtained at intervals of
0.5°–2° latitude, were downloaded from the WHP office
Web site (see online at http://whpo.ucsd.edu) and processed in the same way as the JMA data.

(b)

profiler (CTD), except at 34°N in spring 1998, where an
expendable CTD (XCTD) was used, and at 40° and
41°N in summer 1996 and 41°–45°N in summer 1998,
where an expendable bathythermograph (XBT) wasused.
The temperature and salinity data at every 1 dbar
were vertically smoothed using a seven-point medianfilter, and then a three-point Hanning filter withweights of 0.25, 0.5, and 0.25, 10 times. From these data,
potential temperature and density referred to the surface were calculated. Assuming that relative vorticity is
negligible, PV was calculated fromPV ⫽ ⫺

f ⭸␳␪
,
␳ ⭸z

共1兲

where f is the Coriolis parameter, ␳ is in situ density, ␳␪potential density, and z is the upward coordinate.
Dissolved oxygen was measured at 85% of the hydrographic stations by Niskin bottle sampling at about
20 standard depths, typically at an interval of 25 dbar at
depths less than 150 dbar, an interval of 50 dbar at
150–300 dbar, and an interval of 100 dbar or more in the
deeper layer. From the dissolved oxygen data, apparent
oxygen utilization (AOU), which is the difference between saturated and observed concentrations of dissolved oxygen, was calculated for each standard depth
and then interpolated on a 1-dbar grid using the Akima
spline (Akima 1970). The AOU of a water parcel tends

3. Thermohaline fronts at the 165°E section
The locations of the KEF, KBF, and SAF at the
165°E section in each observation period were determined (Table 1), from the temperature and salinity distributions (Figs. 2 and 3, left panels), and the following
definitions. The SAF is defined as the southward salinity gradient maximum at 100-dbar depth around isohalines of 33.5 to 34.0, based on inspections of salinity
sections around 165°E presented in previous studies(Roden 1972; Zhang and Hanawa 1993; Yuan and Talley 1996; Kawabe and Taira 1998). The KEF is definedas the southward temperature gradient maximum at
300 dbar across the 12°C isotherm because the Kuroshio Extension is generally represented by this isothermat that depth (Mizuno and White 1983). The KBF isdefined as the southward temperature gradient maximum at 300 dbar between the KEF and the SAF (Levine and White 1983; Mizuno and White 1983). Locations of the KEF in springs of 1996 and 2001 were beyond the observation range and were estimated using
the surface velocity fields of Uchida and Imawaki(2003) as the latitude of the eastward meandering jet of
the Kuroshio Extension at 165°E.
In each period, the three fronts are located at intervals of a few degrees latitude (Table 1). The KBF exists
in most of the periods but is not distinguished in summer 1998. The SAF separates into two fronts in spring
2001. This is consistent with Yuan and Talley (1996),
who mentioned that in the western North Pacific thisfront is usually a single front but is occasionally divided
into two parts.

4. CMW in the 165°E section
a. CMW pycnostads in the 165°E section
In the 165°E section for each observation period, several areas of low PV—namely, pycnostads—are ob-

2000

JOURNAL OF PHYSICAL OCEANOGRAPHY

VOLUME 35

FIG. 2. Distributions of (left) potential temperature (black contours) and salinity (white contours with color), (middle) potential
density (black contours) and PV (white contours with color), and (right) PV with respect to potential density at 165°E in spring.
Contours for PV are drawn at 0.5, 1, 1.5, 2, 5, and 10 ⫻ 10⫺10 m⫺1 s⫺1. Black (white) inverted triangles on the top of each panel indicate
locations of hydrographic stations with (without) dissolved oxygen measurements, and horizontal bars with “E,” “B,” and “S” indicate
locations of the KEF, KBF, and SAF. A red “P” in the right panels denotes pycnostads examined in this study.

NOVEMBER 2005

OKA AND SUGA

2001

FIG. 2. (Continued)

served above the deep, low-PV layer at ␴␪ ⫽ 26.8 kg
m⫺3 and greater (Figs. 2 and 3, middle and right panels). In this study, we define a pycnostad as an area of
PV lower than 1.5 ⫻ 10⫺10 m⫺1 s⫺1 above the deep,
low-PV layer, and treat only those pycnostads that extend for two or more successive stations with a thickness greater than 50 dbar, or that exist at a station witha thickness greater than 100 dbar, neglecting smallerscale features. Each area of low PV extending for multiple stations is regarded as one pycnostad. In the spring(summer) sections for 8 (5) yr, a total of 24 (14) such“significant” pycnostads are recognized.
In spring, seven pycnostads are located south of the
KEF, 13 are located between the KEF and the SAF,
and four are located north of the SAF (Fig. 2). Basedon the properties (Fig. 4a and Table 2a), the pycnostads
south of the KEF are identified as the North Pacific
Subtropical Mode Water (STMW) (Masuzawa 1969,1972), which prevails in the western part of the subtropical gyre, with a density of 24.8–25.7 kg m⫺3 (Sugaet al. 2004). The pycnostads between the KEF and the
SAF, except for one at 33°–35°N in 1996 with the properties of STMW, are identified as CMW, which is characterized by a density of 25.9–26.5 kg m⫺3 (Nakamura
1996; Suga et al. 2004) or a core temperature of 10°–13°C (Suga et al. 1997). The pycnostads north of the
SAF have cold, fresh properties that are characteristicof the subarctic region and are clearly different from
CMW. They may be a type of mode water prevailing inthe subarctic region of the North Pacific.
In summer, six pycnostads are located south of the
KEF, seven are located between the KEF and the SAF,
and one is located north of the SAF (Fig. 3). Five of thesix pycnostads south of the KEF are STMW, while theother is considered to be CMW (Fig. 4b and Table 2b).
Six of the seven between the KEF and the SAF are2002

JOURNAL OF PHYSICAL OCEANOGRAPHY

FIG. 3. Distributions in summer, otherwise following Fig. 2.

VOLUME 35

NOVEMBER 2005

OKA AND SUGA

2003

they are not likely to survive in climatologies that aresmoothed spatially and temporally.
Also, the temperature and density ranges of the
CMW pycnostads identified here are adjacent to thoseof the STMW pycnostads (14.4°–17.8°C, 25.15–25.80 kgm⫺3) and slightly overlap with them near ␴␪ ⫽ 25.8 kg
m⫺3 (Fig. 4). This boundary isopycnal between CMWand STMW is believed to be correct, because Suga et al.
(2004) demonstrated that the isopycnal of ␴␪ ⫽ 25.8 kg
m⫺3 corresponds to both the lowermost isopycnal of
STMW and the uppermost isopycnal of CMW, basedon climatological isopycnal PV maps.

b. Age of CMW pycnostads

FIG. 4. Potential temperature–salinity relations for pycnostads
south of the KEF (circles), between the KEF and the SAF(squares), and north of the SAF (triangles) at 165°E in (a) springand (b) summer. Black symbols indicate the relations at the coreof the pycnostads. Solid and dashed contours denote potential
density (kg m⫺3).

CMW, while the other is STMW. Thus, 12 pycnostads
in the spring sections and seven pycnostads in the summer sections are identified as CMW (Table 3). The
CMW pycnostads exist in every observation period.
The temperature and density ranges of the CMW
pycnostads identified here (6.2°–14.5°C, 25.75–26.65 kgm⫺3) are somewhat wider than those presented in previous studies based on climatic data (Nakamura 1996;
Suga et al. 1997, 2004). To further compare between theformer and the latter, the properties at the core of the
CMW pycnostads, which is defined by the PV minimum, are examined. The core is considered the least
modified portion of a pycnostad since its formation.
Therefore, the original properties of the pycnostad at
the time of formation are most likely preserved there
while the pycnostad is modified through mixing withsurrounding water. The core properties of the CMW
pycnostads are in ranges of 6.6°–14.1°C and 25.80–26.55
kg m⫺3 (Fig. 4). These more closely resemble temperature and density ranges of the climatological CMW.
Since the CMW pycnostads other than the core parts
should be small in volume relative to the core parts,

The ages of the CMW pycnostads are deduced from
AOU. A similar analysis was performed by Suga et al.
(1989) and Suga and Hanawa (1990) for STMW pycnostads near the northwestern corner of the subtropicalgyre. We first examine how the AOU values at the coreof the eight STMW pycnostads in the spring 165°E sections and the six STMW pycnostads in the summer sections depend on the time of year (Fig. 5a). The AOU is
5–15 ␮mol kg⫺1 in May and gradually increases in thefollowing months to 26–29 ␮mol kg⫺1 in September andOctober. The values in May are comparable to, orslightly higher than, the AOU of the late-winter mixed
layer in the STMW formation region southeast of Japan, which is 5–10 ␮mol kg⫺1 on average, with a standard deviation of about 5 ␮mol kg⫺1 (Suga and Hanawa 1990). This indicates that the STMW pycnostads
at 165°E observed in May are formed in the late winterof the same year (hereinafter referred to as “new”).
Moreover, the gradual increase of AOU in the following months implies that the STMW pycnostads in June
through October are also new.
The difference among the AOU values in eachmonth is due partly to the degree of dissipation among
the STMW pycnostads and partly to how well the discrete dissolved-oxygen data from Niskin bottles resolve
vertical AOU minima associated with the cores of
STMW pycnostads. When we look at the lowest AOU
value for each month that is most unlikely to be affected by such dissipation or discrete sampling, it increases roughly at a rate of 25 ␮mol kg⫺1 yr⫺1, whichcorresponds to the rate obtained by Suga et al. (1989)
for STMW observed in a repeat section along 137°E. It
should be mentioned that these STMW pycnostads are
not considered to be formed in the late winter of theprevious year. If they were formed in the previous year,
those in the spring sections would have an AOU of
about 35 ␮mol kg⫺1 at the core, and those in the summer sections, about 45 ␮mol kg⫺1, assuming an oxygen
utilization rate of 25 ␮mol kg⫺1 yr⫺1 (Suga et al. 1989).

2004

JOURNAL OF PHYSICAL OCEANOGRAPHY

VOLUME 35

TABLE 2. Locations relative to the fronts (location), number, potential temperature (␪), salinity (S), potential density (␴␪), andwater types (type) of pycnostads at 165°E in (a) spring and (b) summer.
(a)
LocationNo.

␪ (°C)S␴␪ (kg m⫺3)

Type

South of KEF
KEF–SAF7
1
12
4

14.7–17.8
16.4–17.2
6.2–14.5
3.8–6.6

34.62–34.83
34.78–34.86
33.86–34.56
33.42–33.91

25.15–25.75
25.35–25.50
25.75–26.65
26.45–26.80

STMW
STMW
CMW
(Subarctic)

North of SAF(b)LocationNo.

␪ (°C)S␴␪ (kg m⫺3)

Type

South of KEF

5
1
1
6
1

14.4–17.5
12.3–13.8
15.2–15.4
6.3–14.3
5.9–6.5

34.62–34.86
34.45–34.57
34.62–34.64
33.72–34.57
33.65–33.81

25.30–25.80
25.90–26.10
25.60–25.65
25.80–26.60
26.50–26.55

STMW
CMW
STMW
CMW
(Subarctic)

KEF–SAF
North of SAF

pycnostad at 35°–36°N in spring 2000, is higher than theother values in May, by roughly 30 ␮mol kg⫺1. This
pycnostad is believed to be formed in the late winter ofthe previous year, assuming that the oxygen utilization
rate of 25 ␮mol kg⫺1 yr⫺1 can also be applied to CMW
at 165°E.
Since dissolved oxygen data are not available for the
two CMW pycnostads in spring 2001 (Table 3a), theirformation time is deduced using a CTD-oxygen profile
obtained at 40°N a month later (Fig. 6). At this loca-

The observed AOU for both spring and summer sections is much lower than that value.
The AOU at the core of the CMW pycnostads (Table3) increases in a similar manner to the STMW pycnostads, except for a high value of 40 ␮mol kg⫺1 in May(Fig. 5b). Except for this anomalous value, the AOU is
0–16 ␮mol kg⫺1 in May and gradually increases in thefollowing months. It is therefore inferred that these
CMW pycnostads are also new. The high value of 40
␮mol kg⫺1 in May, which corresponds to the CMW

TABLE 3. Latitudes (lat), potential density (␴␪), potential temperature (␪), pressure (p), AOU at the core (AOU), and locations
relative to the fronts (location) of CMW pycnostads at 165°E in (a) spring and (b) summer.
(a)
Year

Lat (°N)␴␪ (kg m )␪ (°C)p (dbar)

AOU (␮mol kg⫺1)

Location

1993
1996
1997

35–37
38–40
36–37
38–40
37–41
35–36
36–37
39–40
37
38–40
40–41
38–40

26.00–26.25
26.30–26.45
26.00–26.35
26.35–26.55
26.30–26.55
26.25–26.35
25.85–26.15
26.25–26.50
25.75–25.85
26.40–26.65
26.35–26.50
26.10–26.40

10.9–12.8
9.0–10.1
10.2–13.1
7.7–10.1
7.4–10.6
9.6–10.7
11.5–13.9
7.7–10.7
13.8–14.5
6.2–9.3
7.2–9.2
9.1–12.2

80–372
91–285
113–358
104–329
141–377
219–462
75–408
101–307170–327
133–422
92–152
18–307

10
9
15
11
24
40
8
16
No data
No data
9
0

KEF–KBF
KBF–SAF
KEF–KBF
KBF–SAF
KEF–SAF
KEF–KBF
KEF–KBF
KBF–SAF
KEF–KBF
KBF–SAF
KBF–SAF
KBF–SAF

1998
2000

2001
2002
2003

⫺3

(b)
Year

Lat (°N)␴␪ (kg m )␪ (°C)p (dbar)

AOU (␮mol kg⫺1)

Location

1991
1992

37–38
36–38.5
41–41.5
34
36–39
38–41
36–40

25.80–25.90
26.05–26.25
26.50–26.60
25.90–26.10
26.35–26.50
26.35–26.55
26.30–26.60

13.6–14.3
10.9–12.5
6.3–7.8
12.3–13.8
8.3–10.0
6.3–10.1
6.8–10.6

236–370
153–396
157–255
299–420
173–376
154–312
179–367

10
9
31
27
17
32
30

KEF–KBF
KEF–KBF
KBF–SAF
south of KEF
KEF–SAF
KBF–SAF
KEF–SAF

1996
1997
1998

⫺3

NOVEMBER 2005

OKA AND SUGA

2005

FIG. 5. Plots of AOU at the core of (a) the STMW pycnostadsand (b) the CMW pycnostads at 165°E against the observation
month.

tion, a pycnostad of 6.3°–9.3°C and 26.41–26.65 kg m⫺3
is observed between 170 and 440 dbar. It is considered
to be identical to the CMW pycnostad at 38°–40°N inthe spring section because the properties are almost
coincident. It is judged to be new, since it has an AOU
of 3 ␮mol kg⫺1 at the core at 210 dbar. We therefore
assume that the two CMW pycnostads in the spring
section are new as well. After all, all CMW pycnostads
in the spring and summer sections are new, except for
one at 35°–36°N in spring 2000 formed in the late winterof the previous year, 1999.
The CMW pycnostad in spring 2003 is located only 20
dbar below the sea surface (Fig. 2), having a particularly low core AOU of 0 ␮mol kg⫺1 (Table 3a). It has
probably been outcropped until just before the observation in early May, that is, until around the end of
April. If we assume that the other pycnostads have also
been outcropped until around the end of April, we canestimate that the new CMW pycnostads in the spring
sections in May and June are aged less than 2 months,
and those in the summer sections in August–October
are aged 4–6 months. The CMW pycnostad at 35°–36°N
in spring 2000 is aged a little over 1 yr.

c. Formation region of CMW pycnostads
Where are these CMW pycnostads formed? The climatological pressure anomaly streamfunction (Zhang
and Hogg 1992) relative to 2000 dbar around the 165°E
section decreases northward at a rate of 0.5 m2 s⫺2 per

FIG. 6. A vertical profile of potential temperature (thick solid
curve), potential density (thick dashed curve), PV (thin dashedcurve), and AOU (thin solid curve), obtained at 40.0°N, 165.0°E
on 18 Jun 2001 during the R/V Mirai MR01-K03 cruise.

degree latitude (Fig. 1). This gradient is equivalent toan eastward geostrophic flow with a speed of 5 cm s⫺1.
If the new CMW pycnostads at 165°E are advectedfrom their formation regions by this mean flow, those
aged 0–2 (4–6) months are to be formed 0–260 (520–780) km west of 165°E, specifically at 162°–165°E(156°–159°E).
The new CMW pycnostads exist at 165°E in every
observation period. This implies that CMW is formed
between 155° and 165°E every winter. Thus, the CMW
formation region extends at least as far west as 155°E,
much farther than recognized in our previous study
based on climatology.
The CMW pycnostad at 35°–36°N in spring 2000,
aged a little over 1 yr, is expected to be formed farther
west than the new ones. If the above flow speed issimply applied to this pycnostad, it is to be formed
around 147°E. This may occur, because Suga et al.
(2004), constructing a winter mixed layer climatology
less smoothed than the previous ones, suggested that
the CMW formation region possibly extends as far west
as 143°E. Unfortunately, the present data at 165°E areinsufficient to investigate whether CMW is constantly

2006

JOURNAL OF PHYSICAL OCEANOGRAPHY

VOLUME 35

formed west of 155°E, since the majority of CMW
formed there could be reentrained into the mixed layer
and renewed in the next winter, before reaching the
165°E section. Therefore, we leave this problem for a
future study, which needs to use synoptic sections in thefarther upstream region.

d. Relation between CMW formation region andfrontsThe new CMW pycnostads in the spring sections arelocated in either the interfrontal region between the
KEF and the KBF, or between the KBF and the SAF,
except for one in spring 1998 (Fig. 2 and Table 3a). The
pycnostads between the KEF and the KBF (10.2°–
14.5°C, 25.75–26.35 kg m⫺3) are warmer and lighter
than those between the KBF and the SAF (6.2°–12.2°C,
26.10–26.65 kg m⫺3; Fig. 7). The difference is clearer
when we compare the core properties of these pycnostads, which are 11.6°–14.1°C and 25.80–26.20 kg m⫺3
for the southern ones, and 8.3°–10.9°C and 26.25–26.45
kg m⫺3 for the northern ones.
Since these pycnostads are aged less than 2 months
and are formed just west of the 165°E section between
162° and 165°E, their locations relative to the fronts
have probably been unchanged since their formation.
That is, these pycnostads were probably formed in theinterfrontal region where they are observed. Thus, twotypes of CMW, the lighter variety of 25.8–26.2 kg m⫺3
and the denser one of 26.3–26.4 kg m⫺3, are formed
between the KEF and the KBF, and between the KBF
and the SAF, respectively. This agrees adequately with
the numerical result of Tsujino and Yasuda (2004).
The preferential formation of CMW in these interfrontal regions is explained as follows. These regions,probably corresponding to the “stability gap” south of
the SAF (Roden 1970, 1972; Yuan and Talley 1996), areassociated with deep winter mixed layers (Suga et al.
2004). The properties of these mixed layers are much
more meridionally uniform in the interfrontal regions
than within the fronts themselves. Consequently, deep
and relatively horizontally uniform mixed layers areformed in each interfrontal region in late winter. They
remain as CMW pycnostads in the following seasons,after being capped by the seasonal pycnocline due tothe surface warming.
The CMW pycnostad in spring 1998 crosses the KBF,
extending over both interfrontal regions (Fig. 2 andTable 3a). Since its properties are of the denser variety,it appears to be formed in the northern interfrontal
region and to subsequently intrude into the southern
region. The same applies to the pycnostad at 36°–39°N
in summer 1996 (Fig. 3 and Table 3b). The pycnostad at
35°–36°N in spring 2000, aged a little over 1 yr, is lo-

FIG. 7. Potential temperature–salinity relations for the new
CMW pycnostads between the KEF and the KBF (circles), between the KBF and the SAF (triangles), and between the KEF
and the SAF (squares) at 165°E in spring. Black symbols indicate
the relations at the core of the pycnostads. Solid and dashed contours denote potential density (kg m⫺3).

cated between the KEF and the KBF, having propertiesof the denser variety. It is likely to be formed in thenorthern interfrontal region and then migrate southward across the KBF. This southward migration to another interfrontal region, where the winter mixed layer
density is smaller, must help it to survive the next winter and persist for more than 1 yr. If it stayed in thenorthern interfrontal region after its formation, it
would be largely reentrained into the mixed layer andrenewed in the next winter.
The pycnostad at 34°N in summer 1996 is locatedsouth of the KEF and has properties of the lighter variety. It appears to be formed in the southern interfrontal region and to subsequently migrate southward
across the KEF. This case supports Mecking andWarner (2001), who suggested that CMW intrudes
southward into the KEF and migrates across it, using
distributions of chlorofluorocarbon, PV, and dissolved
oxygen in two WHP one-time sections along 165° and
179°E. [The former section is identical to the summer
section in 1992 in this study, in which the CMW pycnostad at 36°–38.5°N does not intrude into the KEF at
34°–34.7°N (Fig. 3). This is probably due to the difference in the definitions of CMW and the KEF between
Mecking and Warner (2001) and this study.] Thus,
some of the CMW pycnostads intrude or migrate southward across the KEF or the KBF as they are advected
eastward. This is a form of CMW subduction into thepermanent pycnocline.

e. Discussion
While the above analysis has shown that the lighter(denser) variety of CMW is formed in the southern

NOVEMBER 2005

OKA AND SUGA

(northern) interfrontal region between the KEF and
the KBF (the KBF and the SAF), the interfrontal region in which CMW is actually formed varies from year
to year. The spring and summer 165°E sections indicatethat both varieties of CMW pycnostads are formed in
winters of 1992, 1996, 1997, 2000, and 2001, while only
the lighter (denser) variety is formed in winters of 1991
and 1993 (1998 and 2002). However, if we consider “insignificant” pycnostads of CMW—namely, smallerscale, low-PV areas of CMW that were neglected in
section 4a—the other variety is also formed in most of
the latter winters, as clarified below.
In spring 1993, an area of PV lower than 1.5 ⫻ 10⫺10⫺1 ⫺1m s exists at ␴␪ ⫽ 26.50 kg m⫺3 at 39°N in thenorthern interfrontal region (Fig. 2). This is an insignificant pycnostad of the denser variety of CMW,
whose extent is limited both meridionally and vertically. It is considered new because it has an AOU of 21
␮mol kg⫺1 at the core. Its insignificance may be due tothe coarse station spacing in the neighborhood, that is,a lack of observations at 38° and 40°N. In summer 1991,
an area of PV less than of 1.5 ⫻ 10⫺10 m⫺1 s⫺1 is seenat ␴␪ ⫽ 26.55–26.60 kg m⫺3 at 40°N in the northern
region, which is also an insignificant pycnostad of thedenser variety (Fig. 3). Its insignificance is possibly due
to a lack of observations north of 40°N. Since the dissolved oxygen data at 40°N are of poor quality in thedepth range of this pycnostad, we cannot judge whether
it is new.
In spring 1998, a PV minimum of 1.93 ⫻ 10⫺10 m⫺1⫺1
s , with an AOU of ⫺1 ␮mol kg⫺1 (indicating that it isnew), exists at 26.00 kg m⫺3 at 37°N in the southerninterfrontal region (Fig. 2). This is an insignificant pycnostad of the lighter variety of CMW. Below this exists
a significant pycnostad of the denser variety, intrudingfrom the northern interfrontal region. The insignificance of the lighter variety in the southern region may
result from mixing with the water coming from thenorthern region. In spring 2002, a PV minimum of 1.70
⫻ 10⫺10 m⫺1 s⫺1, with an AOU of 16 ␮mol kg⫺1 (new),is seen at 25.95 kg m⫺3 at 37°N in the southern region,
which is also an insignificant pycnostad of the lighter
variety. In this period, the significant pycnostads of
CMW and STMW are thinner than those in the othersprings; they are shallower than 250 dbar, whereas
those in the other springs are typically located as deepas 300 dbar. Such thinner pycnostads are likely to bedissipated earlier than the average year. After all, if
smaller-scale pycnostads are considered, both varieties
of CMW are formed in the two interfrontal regions
almost every winter, to a varying degree.
The temperature at the core of the two varieties of
CMW pycnostads, including insignificant pycnostads,

2007

FIG. 8. Time series of (a) potential temperature at the core of
pycnostads of STMW and the lighter and denser varieties of
CMW (L-CMW, D-CMW) at 165°E, (b) the North Pacific index
averaged for Dec–Feb, and (c) potential temperature of the KEF,
KBF, and SAF at 300-dbar depth at 165°E. In (a), the temperature for pycnostads in spring is denoted by circles, and that insummer is denoted by triangles; the temperature for significant
pycnostads is indicated by black symbols, and that for insignificant
pycnostads is indicated by white symbols. In (c), the temperature
for the fronts in spring is shown for 1993–2003, and that for thefronts in summer is shown for 1991 and 1992.

changes considerably from year to year (Fig. 8a). The
core temperature of the lighter variety fluctuates between 11.6° and 14.1°C, with a mean and standard deviation of 12.9 (⫾0.9) °C, while that of the denser variety is more variable, between 6.6° and 10.9°C, with 8.8(⫾1.2) °C. These contrast with the core temperature of
the STMW pycnostads, which changes much less [between 16.0° and 17.0°C, with 16.6 (⫾0.4) °C].
What causes such large interannual variations of the
CMW core temperature? According to Hanawa andKamada (2001), the core layer temperature of STMW
from 1957 to 1996 is positively correlated with theNorth Pacific index (NPI; Trenberth and Hurrell 1994)
on a time scale shorter than 10 yr. The NPI is the areaaveraged sea level pressure over the region of 30°–65°N
and 160°E–140°W and is a measure of the strength of
the Aleutian low. The core temperature of the STMW
pycnostads in the 165°E section is positively correlatedwith the NPI, averaged for December through Feb-

2008

JOURNAL OF PHYSICAL OCEANOGRAPHY

ruary as in Hanawa and Kamada (2001), with a coefficient of 0.48 (Figs. 8a,b). Therefore, the interannual
variation of the STMW core temperature is partly due
to that of winter surface cooling. However, the coretemperature of the lighter and denser varieties of CMW
pycnostads bears little correlation with the NPI (coefficients 0.26 and ⫺0.35). This may imply that the properties of CMW pycnostads are strongly influenced by
the associated fronts, particularly the KBF, which havehigh temporal and spatial variability (e.g., Levine andWhite 1983; Mizuno and White 1983; Sainz-Trapaga et
al. 2001).
Consequently, we examine the relation between thecore temperature of the two varieties of CMW pycnostads and the temperature of the KEF, KBF, and SAF
at 300-dbar depth (Fig. 8c), calculated as the average ofthe temperature at two stations immediately south andnorth of these fronts (Table 1). The 300-dbar temperature for each front is negatively correlated with thelatitude of the front, with a coefficient of about ⫺0.5
(not shown), so these fronts tend to be colder as they
are located northward. The core temperature of thelighter variety of CMW is positively correlated with the
300-dbar temperature of both the KEF and the KBF(coefficients 0.46 and 0.37). The core temperature of
the denser variety is highly correlated with the 300-dbar
temperature of the SAF (0.77), exceeding the 95% significance level. Thus, it is likely that the properties ofthe lighter variety of CMW are influenced by both the
KEF and the KBF, while those of the denser one aregoverned primarily by the SAF.

5. Distribution of two types of CMW in thesubtropical gyre
How is the differential formation of the two types of
CMW reflected in its gyrewide distribution? We examine it by using isopycnal PV distributions constructed from the WHP one-time sections listed inTable 4 (Fig. 9), since the climatological PV maps may
not properly represent the CMW distribution, particularly in the upstream region, as mentioned in section 1.
Isopycnals of ␴␪ ⫽ 26.1 and 26.4 kg m⫺3 were chosen to
represent the lighter and denser varieties of CMW. At
179°E, the low-PV cores of the two varieties lower than
1.5 ⫻ 10⫺10 m⫺1 s⫺1 are meridionally adjacent at 36°–38°N (lighter) and 38°–42°N (denser), as at 165°E, as
noted by Mecking and Warner (2001). In the downstream region farther east of the date line, the two varieties diverge considerably. The lighter variety proceeds to 168°–166°W along 30°N, while the denser one
is advected along an outer path, to 38°–40°N along
165°W, then to 30°–35°N along 152°W. At 30°N, thetwo varieties are 1500 km apart.

VOLUME 35

TABLE 4. WHP one-time sections used to draw Fig. 9.
SectionNominal location

Period

P02E
P03
P10
P13
P13C
P14N
P15N
P16N
P16C
P17N
P17C

30°N
24°N
149°E
165°E (north of 30°N)
165°E (south of 30°N)
179°E
165°W
152°W
152°W
135°W (north of 34°N)
135°W (south of 34°N)

Oct–Nov 1993
Mar–Jun 1985
Oct–Nov 1993
Aug–Sep 1992
Aug–Sep 1991
Jul–Sep 1993
Sep–Oct 1994
Feb–Apr 1991
Sep 1991
May–Jun 1993
May–Jul 1991

Interestingly, the pathways of both varieties, derived
by connecting data points with low PV, cross the contours of climatological pressure anomaly streamfunction and shift to the inner side of the subtropical gyre,
toward the downstream. This feature is not caused by
the use of the WHP data collected in various years(Table 4), because the same feature is recognized inclimatological isopycnal PV maps (see, e.g., Fig. 5 ofSuga et al. 2004). The feature occurs possibly because
the outer part of CMW is dissipated through mixing
with high-PV water on the outer side of the gyre, originated from the northeastern corner of the gyre, while
the inner part of CMW is relatively unaffected by dissipation. Alternatively, the inward migration of CMW,
which is observed as the southward migration in the
165°E section (section 4d), may be so effective that PV
is not conserved along streamlines.
It is also interesting that when the two varieties return to the date line after circulating through the eastern subtropical gyre, they are located at a similar latitude (about 25°N), overlapping each other. This agrees
with the result of numerical experiments in Kubokawa
and Inui (1999), in which low-PV waters of different
densities, formed in different locations near the northern edge of the subtropical gyre, gather in the southwestern part of the gyre after circulating along different
paths. The resultant low-PV pool in the model is accompanied by an eastward upper current, resembling
the Subtropical Countercurrent in the North Pacific(Uda and Hasunuma 1969), at its southern edge. Basedon observations, Aoki et al. (2002) indicated that thislow-PV pool is composed not only of CMW, but also ofother lighter waters, and is actually accompanied by aneastward current flowing along 18°N (Nitani 1972),
which is distinct from the classical Subtropical Countercurrent.
As the WHP sections were observed in various years(Table 4), the CMW circulation presented here needs
to be reexamined in a future study, using synoptic data

NOVEMBER 2005

OKA AND SUGA

2009

FIG. 9. Distribution of PV on the isopycnals of ␴␪ ⫽ (a) 26.1 and (b) 26.4 kg m⫺3 at the WHP one-time
sections in the North Pacific, indicated by symbols. PV was smoothed isopycnally along each section
using a running mean of five hydrographic stations. The dashed arrow roughly encloses a region of PV
lower than 1.75 ⫻ 10⫺10 m⫺1 s⫺1. The solid contours illustrate pressure anomaly streamfunction (m2 s⫺2)
relative to 2000 dbar on the isopycnals, adapted from Suga et al. (2004).

over the North Pacific obtained in a relatively shortperiod. Data from Argo profiling floats (Argo Science
Team 2001) are expected to provide such instantaneous
CMW distributions and reveal the temporal variationof CMW on a gyre scale.

6. Summary and discussion
We analyzed CTD and dissolved oxygen data of the
165°E section in springs of 1993, 1996–98, and 2000–03,
and summers of 1991, 1992, and 1996–98, to verify thepossible westward extension of the CMW formation
region and to investigate the relation between the formation region and the thermohaline fronts. The CMW
formation region extends at least as far west as 155°E,
much farther than recognized in the previous study
based on climatic data. It is located in the two interfrontal regions between the KEF and the KBF, and be-

tween the KBF and the SAF, where the two types of
CMW—namely, the lighter variety of ␴␪ ⫽ 25.8–26.2 kgm⫺3 and the denser one of 26.3–26.4 kg m⫺3—areformed. The properties of both varieties exhibit significant year-to-year variations, which seem to be influenced by the KEF and the KBF (lighter variety) and by
the SAF (denser variety) that have high temporal andspatial variability.
How the differential formation of CMW is reflected
in its gyrewide distribution was further examined using
the WHP one-time sections in the North Pacific. The
main circulation paths of the two types of CMW diverge east of the date line; the lighter variety is locatedin the inner part of the eastern subtropical gyre, and thedenser variety is located in the outer part. Interestingly,
the paths of both varieties depart from the climatological pressure anomaly streamfunction and shift to theinner side of the subtropical gyre, although the reason

2010

JOURNAL OF PHYSICAL OCEANOGRAPHY

is unclear. The gyrewide CMW distribution and its temporal variation, and their relation to the subtropicalgyre circulation need to be reexamined quantitatively
in a future study, using synoptic data over the subtropical gyre, for example, from Argo profiling floats.
The results of this study demonstrate that the frontal
structure around the northern boundary of the subtropical gyre is essential in determining the properties
and the gyre-wide distribution of CMW. The existenceof KBF is particularly important because it leads to thedifferential formation. The numerical simulation of
Tsujino and Yasuda (2004) was able to reproduce theformation of two types of CMW on each side of the
KBF because it successfully reproduced the KBF.
As mentioned in section 1, the western part of the
CMW formation region west of 175°E has not been
detected in climatological PV maps (e.g., Fig. 1). This is
explained as follows. If we suppose a synoptic PV map
on a given isopycnal in the CMW density range, PV
south (north) of the winter outcrop of the isopycnal
must be low (high) because the isopycnal lies in thepermanent (seasonal) pycnocline. On the map, the
CMW in the western formation region is considered toappear as a zonal band of particularly low PV with ameridional width of a few degrees, located just south ofthe outcrop. The smoothing process in climatology,
however, averages the low PV south of the outcrop andthe high PV north. This significantly weakens the lowPV signature of CMW just south of the outcrop, as thesmoothing scale is typically as large as the meridional
width of the CMW band.
In a future study, we also need to clarify which partof the CMW observed in the 165°E section has been
subducted into the permanent pycnocline and whichpart will be reentrained into the mixed layer in the next
winter. Modeling studies have demonstrated that CMW
is permanently subducted east of the date line, by crossing a zone of sharp horizontal gradient in the wintermixed layer depth—namely, a mixed layer front—at
the eastern end of a region of deep mixed layers (e.g.,
Kubokawa and Inui 1999; Xie et al. 2000; Tsujino and
Yasuda 2004). However, the winter mixed layer climatology of Suga et al. (2004) indicates that such a mixed
layer front for CMW does not exist in the real ocean,and CMW is likely to be permanently subducted in azonally elongated region along the northern boundaryof the subtropical gyre between 143°E and 170°W,
where the winter mixed layer depth gradually decreases
eastward (downstream), while the mixed layer densitychanges little. Therefore, at least part of the CMW observed in the 165°E section is likely to have been permanently subducted. In addition to this along-stream
subduction of CMW, part of the CMW in the 165°E

VOLUME 35

section has also been permanently subducted by migrating southward across the fronts, as explained in section 4d. Thus, the subduction process of CMW is quite
complicated and cannot be thoroughly clarified by analyzing one repeat section at 165°E. It needs to be further examined using synoptic data at various locations
over the possible CMW formation region.
Acknowledgments. The authors are grateful to the
Climate and Marine Department of the Japan Meteorological Agency for supplying the hydrographic dataof the 165°E section, including those in 2004 that are
unpublished. They also thank Hiroshi Uchida for providing the surface velocity data and Shuichi Watanabe
for supplying the Mirai hydrographic data. They thankan anonymous reviewer for detailed, insightful, andconstructive comments that greatly improved themanuscript. This work was supported by “The Argo
Project–Advanced Ocean Observing System” as one of
the Millennium Projects of the Japanese Government.
Author TS was partly supported by the Japan Society
for Promotion of Science [Grant-in-Aid for Scientific
Research (B), No. 16340135].
REFERENCES
Akima, H., 1970: A new method of interpolation and smooth
curve fitting based on local procedures. J. Assoc. Comput.
Meth., 17, 589–603.
Aoki, Y., T. Suga, and K. Hanawa, 2002: Subsurface subtropicalfronts of the North Pacific as inherent boundaries in the ventilated thermocline. J. Phys. Oceanogr., 32, 2299–2311.
Argo Science Team, 2001: Argo: The global array of profiling
floats. Observing the Oceans in the 21st Century, C. J. Koblinsky and N. R. Smith, Eds., GODAE Project Office, Bureau of Meteorology, 248–258.
Hanawa, K., and J. Kamada, 2001: Variability of core layer temperature (CLT) of the North Pacific Subtropical Mode Water. Geophys. Res. Lett., 28, 2229–2232.
JMA, 1997: Data report of oceanographic observations. No. 87,
CD-ROM.
——, 1998: Data report of oceanographic observations. No. 88,
CD-ROM.
——, 1999: Data report of oceanographic observations. No. 89,
CD-ROM.
——, 2001: Data report of oceanographic observations. No. 91,
CD-ROM.
——, 2002: Data report of oceanographic and marine meteorological observations. No. 92, CD-ROM.
——, 2003: Data report of oceanographic and marine meteorological observations. No. 93, CD-ROM.
Kawabe, M., and K. Taira, 1998: Water masses and properties at
165°E in the western Pacific. J. Geophys. Res., 103, 12 941–
12 958.
Kubokawa, A., and T. Inui, 1999: Subtropical countercurrent in an
idealized ocean GCM. J. Phys. Oceanogr., 29, 1303–1313.
Levine, E. R., and W. B. White, 1983: Bathymetric influences
upon the character of North Pacific fronts, 1976–1980. J. Geophys. Res., 88, 9617–9625.

NOVEMBER 2005

OKA AND SUGA

Masuzawa, J., 1969: Subtropical Mode Water. Deep-Sea Res., 16,
463–472.
——, 1972: Water characteristics of the North Pacific central region. Kuroshio—Its Physical Aspects, H. Stommel and K.
Yoshida, Eds., University of Tokyo Press, 95–127.
Mecking, S., and M. J. Warner, 2001: On the subsurface CFC
maxima in the subtropical North Pacific thermocline andtheir relation to mode waters and oxygen maxima. J. Geophys. Res., 106, 22 179–22 198.
Mizuno, K., and W. B. White, 1983: Annual and interannual variability in the Kuroshio Current System. J. Phys. Oceanogr.,
13, 1847–1867.
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, 171–188.
Nitani, H., 1972: Beginning of the Kuroshio. Kuroshio—Its Physical Aspects, H. Stommel and K. Yoshida, Eds., University ofTokyo Press, 129–163.
Oka, E., and T. Suga, 2003: Formation region of North Pacific
Subtropical Mode Water in the late winter of 2003. Geophys.
Res. Lett., 30, 2205, doi:10.1029/2003GL018581.
Roden, G. I., 1970: Aspects of the mid-Pacific transition zone. J.
Geophys. Res., 75, 1097–1109.
——, 1972: Temperature and salinity fronts at the boundaries ofthe subarctic-subtropical transition zone in the western Pacific. J. Geophys. Res., 77, 7175–7187.
Sainz-Trapaga, S., G. J. Goni, and T. Sugimoto, 2001: Identification of the Kuroshio Extension, its bifurcation and northernbranch from altimetry and hydrographic data during October
1992–August 1999: Spatial and temporal variability. Geophys. Res. Lett., 28, 1759–1762.
Suga, T., and K. Hanawa, 1990: The mixed layer climatology inthe northwestern part of the North Pacific subtropical gyreand the formation area of Subtropical Mode Water. J. Mar.
Res., 48, 543–566.

2011——, ——, and Y. Toba, 1989: Subtropical Mode Water in the
137°E section. J. Phys. Oceanogr., 19, 1605–1618.
——, Y. Takei, and K. Hanawa, 1997: Thermostad distribution in
the North Pacific subtropical gyre: The Central Mode Waterand the Subtropical Mode Water. J. Phys. Oceanogr., 27,
140–152.
——, K. Motoki, Y. Aoki, and A. M. Macdonald, 2004: The North
Pacific climatology of winter mixed layer and mode waters. J.
Phys. Oceanogr., 34, 3–22.
Trenberth, K. E., and J. W. Hurrell, 1994: Decadal oceanatmosphere variations in the Pacific. Climate Dyn., 9, 303–
319.
Tsujino, H., and T. Yasuda, 2004: Formation and circulation ofmode waters of the North Pacific in a high-resolution GCM.
J. Phys. Oceanogr., 34, 399–415.
Uchida, H., and S. Imawaki, 2003: Eulerian mean surface velocity
field derived by combining drifter and satellite altimeter data.
Geophys. Res. Lett., 30, 1229, doi:10.1029/2002GL016445.
Uda, M., and K. Hasunuma, 1969: The eastward subtropical countercurrent in the western North Pacific Ocean. J. Oceanogr.
Soc. Japan, 25, 201–210.
Xie, S.-P., T. Kunitani, A. Kubokawa, M. Nonaka, and S. Hosoda,
2000: Interdecadal thermocline variability in the North Pacific for 1958–97: A GCM simulation. J. Phys. Oceanogr., 30,
2798–2813.
Yuan, X., and L. D. Talley, 1996: The subarctic frontal zone in the
North Pacific: Characteristics of frontal structure from climatological data and synoptic surveys. J. Geophys. Res., 101,
16 491–16 508.
Zhang, H.-M., and N. G. Hogg, 1992: Circulation and water massbalance in the Brazil Basin. J. Mar. Res., 50, 385–420.
Zhang, R.-X., and K. Hanawa, 1993: Features of the water-mass
front in the northwestern North Pacific. J. Geophys. Res., 98,
967–975.