742

NOAA Technical Report NMFS SSRF- 742

WATER STRUCTURE AT
OCEAN WEATHER STATION V
NORTHWESTERN PACIFIC
OCEAN, 1966-71

D. M. Husby and G. R. Seckel

October 1980

Marine Biological Laboratory *:
LIBRARY 1

OCT 14 1992

Woods Hole, Mass.

I

U.S. DEPARTMENT OF COMMERCE

National Oceanic and Atmospheric Administration

National Marine Fisheries Service

NOAA TECHNICAL REPORTS
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"^^^H^

NOAA Technical Report NMFS SSRF- 742

WATER STRUCTURE AT
OCEAN WEATHER STATION V,
NORTHWESTERN PACIFIC OCEAN,
1966-71

D. M. Husby and G. R. Seckel

October 1980

Marine Biological Laboratory '

LIBRARY I

OCT 14 1992 I

Woods Hole, Mass. 1

U.S. DEPARTMENT OF COMMERCE

Philip M Klutznick. Secretary

National Oceanic and Atmospheric Administration

Richard A. Frank, Administrator

National Marine Fisheries Service

Terry L, Leitzell. Assistant Administrator for Fistienes

The National Marine Fisheries Service (NMFS) does not approve, rec-
ommend or endorse any proprietary product or proprietary m.aterial
mentioned in this publication. No reference shall be made to XMFS, or
to this publication furnished by XMFS, in any advertising or sales pro-
motion which would indicate or imply that NMFS approves, recommends
or endorses any proprietary product or proprietary material mentioned
herein, or which has as its purpose an intent to cause directly or indirectly
the advertised product to be used or purchased because of this NMFS
publication.

CONTENTS

Introduction 1

Processing procedures and analysis 1

The data 1

The isentropic format 2

Quality control of isentropic data 2

Harmonic analysis of isentropic data 2

Statistical characteristics of the harmonic analyses 5

Sampling gaps 12

Results of the harmonic analyses 13

Oceanographic conditions at OWS-V 13

The oceanographic setting 13

Variability and structure 1966-71 14

The water structure and air-sea interaction 24

Summary and conclusions 26

Acknowledgments 29

Literature cited 29

Appendix I 31

Appendix II 50

Figures

1. Sampling record of oceanographic stations at Ocean Weather Station V, 1966-72 3

2. Positions of oceanographic stations taken by U.S. Coast Guard Cutter Chautauqua at Ocean Weather
Station V, 4-22 January 1966 4

3. Original and expected salinity and depth values at (t, 26 and a^ 27 for the year 1967 6-7

4. Original and expected salinity and depth values at a, 26 and a 27 for the year 1971 8-9

5. Standard errors of estimate for harmonic fit of the 1971 temperatures at cr, 25 to (t, 27 10

6. Standard errors of estimate for harmonic fit of the 1971 salinities at o; 25 to (t, 27 10

7. Standard errors of estimate for harmonic fit of the 1971 depths at it, 25 to o; 27 11

8. Temperature-salinity diagrams for day 244 (1 September 1969) based on original isentropic data with
temperature-salinity values from the harmonic fit 12

9. Temperature-salinity diagrams for day 182 (1 July 1971) based on original isentropic data with tempera-
ture-salinity values from the harmonic fit 12

10. Dynamic topography of the sea surface relative to the 1,000 decibar surface derived from selected sta-
tions during the summer of 1957 14

11. Meridional sections, lat. 21° to 42°N, long. 168°E, of salinity and depth versus (r, based on 67 STD sta-
tions occupied 3-11 April 1971 and dynamic topography of sea surface relative to the 1,000 decibar sur-
face along same section 15

12. Sections of salinity versus thermosteric anomaly and thermosteric finomaly versus depth along right-
hand edge of Kuroshio 16

13. Monthly mean surface temperature-salinity relationships at Ocean Weather Station V, 1966-71 17

14. Vertical profiles of expected values of salinity and depth from harmonic series at the first day of each
month at Ocean Weather Station V, 1966-71 18-23

15. Absolute magnitude of the harmonic function for the 6-yr series of the depth of CT, 26.0 24

16. Heat content of the water column from the surface to a, 26.0 at Ocean Weather Station V at 30-day inter-
vals, heat content based on change in depth per month at the a, 26.0 level, and the depth of the o; 26.0
level computed at midmonth from the harmonic series 25

17. Heat content change per month based on the change in mean temperature per month in layer from sea
surface to a, 26.0 and heat content change per month contributed by net heat exchange across sea sur-
face 27

18. Change per month of the mean temperature from the sea surface to a, 26.0 at Ocean Weather Station V
computed from the harmonic series 28

Tables

1. Manner of obtaining first and last values in each of the annual harmonic analyses, 1966-71 4

2. Standard errors of estimate for Fourier series summations of temperature, salinity, and depth on ir,
25.0-27.4 at Ocean Weather Station V, 1966-71 5

3. Heat budget estimates at Ocean Weather Station V for the 6- mo cooling portion of the year, 1 October

tol April .••.•■■.■■■ ^^

4. Estimates of mean evaporation rates, mean precipitation rates, and evaporation minus precipitation at
Ocean Weather Station V 26

IV

Water Structure at Ocean Weather Station V,
Northwestern Pacific Ocean, 1966-71

D. M. HUSBY and G. R. SECKEL'

ABSTRACT

The oceanographic station data obtained at Ocean Weather Station V from 1966 to 1972 by the
U.S. Coast Guard have been analyzed and are presented in a form suitable for water structure studies.
Temperatures, salinities, and depths are given as a function of density (sigma-f). We used harmonic
analysis as a curve-fitting technique, to obtain parameters for these properties as a function of time.
The harmonic coefficients and interpolated values at the first of each month for the 6-year series are
tabulated in an appendix.

We describe the temporal distributions of salinity and depth in terms of the oceanographic setting.
At depths greater than sigma-f 26, temperature-salinity relationships remain relatively constant in
time. Depth variations at these levels are attributed primarily to meanders of the Kuroshio Extension.
The surface divergence, as reflected by changes in the depth of sigma-( 26, has no annual periodicity.
The 6-year record shows that large baroclinic variability occurs at time scales of more than 35 days
with largest variability occurring at the interannual scale.

Heat budget estimates show that the effects of local ocean-atmosphere exchange processes are ob-
scured by advected properties. For example, the heat content of the layer above sigma-(26is primarily
determined by the divergence of this layer and anomalies in the mean temperature are produced by
heat advection rather than heat exchange across the sea surface.

INTRODUCTION

Monitoring and predicting ocean variability in the
fishing areas of the eastern North Pacific are important
problems facing the fishery oceanographer. In contrast
to the global monitoring of the atmosphere at a network
of stations every 6 h, there is no network of monitoring
stations in the oceans. Oceanographers are therefore at-
tempting to infer ocean variability from atmospheric
forcing, i.e., the exchange of momentum, moisture, and
heat between the atmosphere and ocean, that can be
calculated from the regularly observed meteorological
properties. The temperature structure in the upper
layers of the ocean, for example, is affected by heat ex-
change and wind stress as well as by the changing cur-
rent field and diffusion. Inferring ocean variability from
atmospheric forcing, therefore, is not a trivial problem.

Conditioning of the water reaching the eastern North
Pacific Ocean begins in the western North Pacific, an
area characterized by a net annual heat loss across the
sea surface (Husby and Seckel 1975). Thus, studies of
the effects of heat exchange across the sea surface and
wind stress on ocean properties and structure must be
undertaken upstream of the fishing areas if predictions
of anomalous water conditions are to be made. The only
time series of concurrent meteorological and oceano-
graphic data for use in such studies are those that were
obtained at ocean weather stations. One of these, Ocean
Weather Station V (OWS-V) was located at lat. 34°N,

'Pacific Environmental Group, National Marine Fisheries Service,
NOAA, c/o Fleet Numerical Oceanography Center, Monterey, CA 93940.

long. 164°E within the net annual heat loss area that is
of concern to us.

At OWS-V meteorological observations were obtained
from 1951 to 1972 and oceanographic station data from
1966 to 1972. The large-scale air-sea interaction pro-
cesses derived from the station's meteorological data
were described by Husby and Seckel (1975). Our work is
a companion paper in which the oceanographic station
data are presented in a form suitable for studies of the
water structure. Temperatures, salinities, and depths at
selected density (sigma-t) levels are analyzed and
presented as a function of time. Harmonic analysis is
used as a curve-fitting technique, to obtain parameters
for these properties as a function of time. Results of the
analyses are presented in Appendices I and H. Finally,
the time variations in the distribution of properties, the
water structure, are described in terms of the oceano-
graphic setting at OWS-V.

PROCESSING PROCEDURES AND
ANALYSIS

The Data

Oceanographic sampling at OWS-V began in January
1966 with daily Nansen bottle casts by the U.S. Coast
Guard on alternate 3-wk patrols. In March 1968 the
program was expanded to daily observations on each
patrol. The temperature and salinity were sampled at
the sea surface and at the depths of 10, 30, 50, 75, 100,
150, 200, 300, 400, 600, 800, 1,000, and 1,500 m. The
observations and initial data processing methods were
described by Husby (1968).

From 1966 to March 1968 the sampling was intermit-
tent (Fig. 1). Subsequently, until January 1972, daily
sampling became nearly continuous with isolated gaps
of up to 20 days. In addition to the temporal gaps, sta-
tions were occasionally occupied outside the nominal
location, a 10 nautical mile (nmi) square centered on
lat. 34°N, long. 164°E (Fig. 2). We, however, used all
observations within a 60 nmi square centered on this
location. Sixty-seven percent of the stations were oc-
cupied within the 10 nmi square and 95% within the 60
nmi square.

The oceanographic station data were obtained from
the National Oceanographic Data Center (NODC) of
the National Oceanic and Atmospheric Administration
in two different formats: 1) temperature and salinity at
observed and standard (interpolated) depths, and 2)
temperature, salinity, and depth at increments of 0.2
sigma-t (ff, ) units between the surface and the deepest
observation (isentropic format). A cubic spline interpK)-
lation function was used to obtain the values of temper-
ature, salinity, and depth at the desired a, values.^

The Isentropic Format

The study of changes in water properties on surfaces
of constant potential density or a', called isentropic
analysis, was introduced to oceanography by Parr (1938)
and Montgomery (1938) and has been a valuable tool in
descriptive oceanography. The assumptions underlying
isentropic analysis are that mixing or interchange of
water masses on a constant density surface proceed with
a minimum of change in the potential energy and
entropy of the system and that surfaces of constant den-
sity are the preferred surfaces along which mixing oc-
curs. The method has been used in the identification
and tracing of water masses and also lends itself to the
analysis of temporal changes in the water structure as
was done, for example, at OWS-P by Tabata (1965). In
order to pursue the latter aspect of isentropic analysis
the temperature, salinity, and depth are presented as a
function of a, in this report.

Quality Control of Isentropic Data

The initial step of quality control is concerned with
the interpolated temperatures and salinities at
designated o^ values for each station received from
NODC. The spline interpolation function calculates the
temperature and salinity at designated a, values from
the two relationships: 1) observed temperature versus a,
and 2) salinity versus o; with a, as the independent
variable. A a, value was computed from the interpolated
temperature and salinity at each designated (t, using the
relationships (1) and (2). When the calculated a, dif-
fered from the designated by >±0.02 a, units at more
than one level, both interpolated and observed data
were used to plot two temperature-salinity (T-S) dia-

grams for the station. The T-S curve drawn through the
observed values together with the temperature-depth
curve was used to correct the interpolated values ob-
tained from the spline interpKjlation or to determine
whether the station should be rejected. These quality
control procedures frequently had to be used for values
that were erroneously produced by the spline interpwla-
tion because of an inadequate sampling interval in the
vicinity of the salinity minimum (a, 26.8). Out of a total
of 1,067 stations, 496 stations were corrected during this
quality control procedure.

Harmonic Analysis of Isentropic Data

Harmonic analysis was used as a curve-fitting
technique to summarize the daily oceanographic data in
a manner that lends itself to studies of temporal changes
in the water structure. The resulting analytical expres-
sions yield smoothed estimates of the water properties
for any time of the analysis period.

Harmonic (Fourier) analysis was performed on the
isentropic data for each year from 1966 through 1971
with a fundamental period of 366 days beginning on 1
January of one year and ending on 1 January of the next
year. In these data sets, values at the beginning and end
of the annual series were usually not equal and to
facilitate the curve-fitting procedure the harmonic
analyses were performed on the residuals produced by
subtracting the linear trend (day 1 to day 366) from the
observed value:

Rit) = fit) - [/(I) + M-(t -1)]

(1)

'Hamilton, D. 1973. Isentropic analysis and spline interpolation.
Natl. Oceanogr. Data Cent. Tech. Rep., 29 p.

where fU) is the value of the property (temperature,
salinity, or depth) at a constant (t, at day t, and t = 1 to
366. The slope of the straight line fitted to the values at
day 1 and day 366 is

M = [/(366) - /(I) 1/365. (2)

The expression for the fitted curve then becomes

E(t) =/(l) + M -(t - I) + F^{t) (3)

where FAt) = A^ + x(a^cos^SI^ + B„ sin ?^\

n = 1,2, . . .k (4)

is the Fourier series derived from the residuals, R(t).
The coefficients A„, i4„, and B„ were evaluated by use of
a standard computer program.

Data gaps in the time series were filled by linear inter-
polation between observed values in order to satisfy the
program requirement of equal time intervals between
data. When no observations were available for the first or
366th day of the year, data from the first (last) actual
station of the year was extrapolated backward (forward)
to the missing day. For the 1969 and 1971 analyses, the
values for the first day were computed from a harmonic

I

35N

30

34N

30'

33N

•

3
2

9« r"

• 4

5

•

'---•8

•

10 1

•1
•7

»

— \—

1

' \

1

-H — '

1

— i—

h-

—h-.

I63°E

30'

I64°E

30'

I65E

Figure 2— Positions of oceanographii' stations taken by I'.S. Coast Guard Cutler Chautauquit at Ocean Weather Sta-
tion V. 4-22 January IHBfi. Dashed line eneloses a lO-nmi square and solid line encloses a Wl-nmi square around Ocean
Weather Station V.

analysis of the 366 day period beginning and ending on 2
July. There were sufficient data from July 1968 to July
1971 to use the expected values from these analyses as
the interpolated values for the first days of 1969 and 1971
(Fig. 1). The values used for the 1st and 366th days of the
annual analyses at each level are listed in Appendix I.
Table 1 shows the manner in which these values were ob-
tained.

Before proceeding with the harmonic analyses of the
complete data set limited analyses were made as a
quality control procedure. Harmonic coefficients were
derived to the 12th harmonic for the salinity and depth
series at the ct, 26 and 27 levels of each year. Equation (3)
was then used to evaluate and plot the fitted curve

Table 1. — Manner of obtaining first and last values in each of the
annual harmonic analyses, 1966-71.

Year

Day=l

Day = 366

1966

extrapolation from 4 Feb.
1966

observation on 1 .Jan. 1967

1967

observation on 1 Jan. 1967

extrapolation from 24
Nov. 1967

1968

extrapolation from 1

harmonic analysis from 2

Mar. 1968

July 1968 to 2 July 1969

1969

harmonic analysis from
2 .Julv 1968 to 2 Julv 1969

observation on 1 Jan. 1970

1970

observation on 1 .Jan. 1970

harmonic analysis from
2 July 1970 to 2 July
1971

1971

harmonic analysis from
2.Julyl970to2.Julyl971

observation on 1 Jan. 1972

together with the isentropic data. Examples of these
curves for 1967 (a year with large data gaps) and 1971 (a
year with small data gaps) are shown in Figures 3 and 4.
Questionable values are revealed as large discrepan-
cies from the fitted curve. The questionable values were
usually associated with the previously mentioned poor
vertical sampling interval at individual stations or with
stations that were occupied outside the 60 nmi quad-
rangle about the nominal position of OWS-V (Fig. 2). Us-
ing this quality control procedure, 38 stations were re-
jected from the 6-yr series.

After this quality control procedure the harmonic coef-
ficients were calculated for the temperature, salinity,
and depth at a, levels between 22.0 and 27.4 with inter-
vals of 0.2 a, units, as well as for the surface temperature,
salinity, and a,. Although the analyses were carried out
to the 52d harmonic, resolving fluctuations with a 7-day
duration, only the first 12 harmonic coefficients are listed
in Appendix I. Also listed are the slope M, and initial
values, /(I), for the linear trend at each level. Thus, using
the values of Appendix I in Equation (3), expected values
for any day of the year for any of the given levels can be
obtained.

Because of the seasonal variation in the density of the
upper layers, properties at the lower a, values will not oc-
cur throughout the year. For these situations the dates of
the first and last observation are given in the tabulation
of Appendix I and derived values will be valid only for
the duration bounded by these dates.

Statistical Characteristics of
the Harmonic Analyses

Figures 3 and 4 show qualitatively that the fitted
curves follow the observed values very well, as they
should, because a Fourier series approximation is a least

squares fit regardless of the number of harmonics used in
the summation (Jenkins and Watts 1968). A quantitative
measure of the goodness of fit is provided by the unex-
plained variance.

S, =■

f =1

(5)

T-1

Equation (5) is an estimate of the mean square error or
variance of the difference between the observed values
and the Fourier series approximation. With an increas-
ing number of harmonics used in the approximation,
S,., the standard error of the estimate, should decrease.
These quantitative aspects are presented in Table 2 and
illustrated in Figures 5, 6, and 7 by graphs of S,, as a
function of the number of harmonics used in the
analyses of the temperature, salinity, and depth for
1971.

Considering the temperature and salinity graphs (Figs.
5, 6) first, there is a marked reduction in S, at the shal-
lower levels as n increases to 6, 6\. then decreases slowly
with increasing n. For example, at a, 25.2, S,. for the
temperature is 0.28°C at « = 1, 0.135°C at n = 6, and
0.12°C at n = 20. In the deeper layers the decrease in S^
with increasing harmonic used in the fitting procedure is
relatively small. For example, at a, 26.4, S, for the
temperature is 0.13°C at n = 1, 0.115°C at n = 6 and
0.11°C at n = 20. The greater variability of the prop-
erties at the shallower levels may reflect, in part, low fre-
quency variability in the air-sea interaction processes
directly affecting the upper layer of the ocean to approxi-
mately the (T, 25.8 level.

Figure 7 shows that the standard error of estimate for

Table 2.— Standard errors of estimate. S, . for Fourier series summations (n = 12) on a, 25.0-27.4 levels of temperature, °C, (upper
panel); salinity, */.., (middle panel); and depth, m, (lower panel). 5^ was computed only for times of actual observations, exclud-
ing interpolated values, 1966-71.

Level

Year

25.0

25.2

25.4

25.6

25.8

26.0

26.2

26.4

26.6

26.8

27.0

27.2

27.4 ,

1966

0.070

0.079

0.114

0.080

0.080

0.103

0.118

0.129

0.144

0.093

0.067

0.059

0.060

1967

0.079

.082

.079

.059

.058

.058

.068

.085

.109

.089

.044

.037

.027

1968

.135

.124

.122

.086

.097

.091

.118

.151

.151

.116

.069

.069

.050

1969

.144

.131

.142

.119

.100

.128

.129

.132

.172

.157

.105

.067

.064

1970

.150

.115

.125

.099

.060

.059

.075

.102

.097

.093

.078

.047

.033

1971

.096

.123

.141

.144

.111

.081

.072

.110

.133

.128

.063

.087

.075

1966

0.022

0.025

0.034

0.022

0.020

0.026

0.026

0.024

0.026

0.016

0.011

0.008

0.008

1967

.026

.025

.023

.017

.015

.015

.016

.018

.019

.015

.008

.005

.004

1968

.044

.039

.038

.025

.026

.024

.028

.032

.029

.020

.010

.011

.008

1969

.046

.041

.042

.034

.027

.033

.031

.029

.032

.026

.016

.011

.011

1970

.047

.036

.037

.028

.016

.015

.017

.022

.018

.015

.011

.006

.005

1971

.030

.038

.041

.041

.030

.021

.017

.020

.024

.021

.009

.013

.010

1966

5.7

10.9

21.8

24.6

23.2

23.5

24.1

24.1

24.0

24.4

26.0

28.4

35.9

1967

9.1

8.6

13.6

22.7

26.4

24.0

20.9

19.5

18.0

22.1

19.9

17.9

23.0

1968

10.7

12.9

15.5

35.5

38.5

40.7

33.6

28.0

25.4

24.7

27.7

35.8

37.1

1969

8.1

13.8

21.7

29.8

32.6

31.6

25.6

23.5

24.0

21.0

22.2

23.9

22.8

1970

7.9

6.1

10.7

15.2

19.5

22.9

20.1

18.3

17.4

16.4

17.0

16.7

27.8

1971

5.2

11.8

15.6

27.4

29.7

24.8

23.0

22.2

19.2

19.3

19.6

20.7

25.9

""/o'AllNlltfS

o

c
o

= <2

Is

a,

o,

3

tic
S,

""/o'AllNnWS
8

O

c
o

9^ V

s s

O
I

61

.36

STO
ERPOR

-

.36

[^]

-

[c]

-

.28

- V25.4

\\/25.2

.28

-

U^25.6

.20

_ Yy.25.0

.20

26.6

.12
.04

25.8

-^^,^^^^__

^^,,26.4 26.8

^"^-----^ .12

.04

"""^^^^^^^^^^^^zzir— ^

27^0 26.2 26.0

1

20 1 20

IMO. OF

HARMONICS NO. OF HARMOIMICB

Figure 5. — Standard errors of estimate for harmonic fit of the 1971 temperatures at a, 25 to a, 25.8 (left
panel) and at o^26 to ^,27 (right panel).

10

Figure 7.— Standard errors of estimate for harmonic fit of the 1971 depths at o, 25 to a, 25.8 (left panel) and

at (T, 26 to i;, 27 (right panel).

the depth is relatively large at all levels for low har-
monics. At the 26.0, 26.2, and 26.4 <t, levels significant
improvement in the standard error continues up to n =
10. Relatively high variance at (t, 26.6, 26.8 and 27 for
n = 6 indicates that low frequency baroclinicity, proba-
bly caused by eddies and current meanders, penetrates
deeper than 800 m. S^ approaches an asymptotic value of
about 20 m in the deeper a, layers indicating the magni-
tude of the residual variance associated with short-term
variability and sampling error.

One would assume that the variance of temperature
and salinity decreases with increasing a, . Figures 5 and 6
and the tabulated variances of the temperature and
salinity (Table 2) show that this assumption is not cor-
rect. There is a tendency for S^ to decline from higher
values in the upper layers to lower values at o, 25.8 or
26.2, then to rise again to higher values at o; 26.4, 26.6,
or 26.8 before finally declining to the lowest values at cr,
27, 27.2, and 27.4. In other words, the T-S relationships
are less variable below the level of seasonal influence
than in the deeper layers at and above the salinity
minimum. The reason for this curious tendency may be
the uncertainty in the T-S relationship introduced by
the inadequate vertical sampling interval (200 m at a,

Figure 6. — Standard errors of estimate for harmonic fit of the 1971
salinities at a^ 25 to cr, 25.8 (left panel) and at a, 26 to 7, 27 (right pan-
el).

26.4-26.8) that was previously mentioned. It is also pos-
sible that the relatively large variance at the ct, 26.4-26.8
levels reflects active mixing of water masses upstream.
Depths derived from the harmonic curve fitting can
produce density inversions in the seasonal pycnocline
during spring and summer months. These inversions are
small and are due to the uncertainty of the harmonic fit
being of the same order of magnitude as the depth incre-
ment between cr, levels. The depth intervals between
successive <t, levels from the surface to the a, 25.2 level
range from 1 to 5 m. The standard errors of estimate
listed in Table 2 generally are larger than these values
and range from 5 to 14 m. These uncertainties in the
depth estimates are unavoidable with the method
employed, but the errors produced in computations of
the integrated properties of the water column, e.g.,
mean temperature or heat content, will not be large
since the depth increments in the upper layer are so
small. The levels producing inversions can be deleted in
these computations without significantly affecting the
results. For example, consider the mean temperature of
the water column from the surface to the 0; 26.0 level on 2
days at OWS-V representing summer conditions, 1
September 1969 (Fig. 8) and 1 July 1971 (Fig. 9). The ex-
pected depth values for 1 September 1969 revealed an in-
version at (T, 22.8 and 23.0. Deleting these two levels, the
mean temperature was calculated to be 17.20°C, com-
pared with a value of 17.24°C calculated from the

11

SALINITY %o

Figure 8. — Temperature-salinity diagram for day 244 (1 September
1969) based on original isentropic data (o) with temperature-salinit\-
values from the harmonic fit (x). The numerals give the depth in
meters for the original isentropic data. The numbers in parentheses
represent the difference between the depth of the original isentropic
values and those from the harmonic fit.

original isentropic data. For 1 July 1971 the expected
isentropic values showed no inversions, but the com-
parison was made by deleting the u, 24.0 and a^ 24.2
levels at 3 and 9 m, respectively, giving a mean
temperature of 15.31 °C, which was identical with that
calculated from the original isentropic data and com-
pared with 15.25°C before the data were deleted.

Sampling Gaps

Figure 1 shows that there were gaps lasting up to
several months in the oceanographic data series. From
1966 to the winter of 1968 oceanographic stations at
OWS-V were occupied only on alternate Coast Guard
patrols. Subsequent to this time there were gaps of up to

"Original isentropic data ...•-

T-

■ expected values ...•••'

...•••'

-

..°-r3i+3)

-20 .-■•■■•'■■ r'*'' ,

•;

. ..•■■■■' Vis+i j ..■••■"

y V21I+.3+'

..V26!+3i
...••■•' '•3lf+31

OS

1 —
«x
oe

UJ

a.

UJ

►—

:i6 ...••■■•■•■■■■" [''"' '

...••■■' ...•/215( + 14)
"•*^ ^298 (+4)

-

/36I+41 %^y''

-

-8 *.449,-2i /

-

■j 552:.---(-2 1

/

y674(0)

¥

-4 / ,839!-3l

-

33 /34 ."09 -1 ■ 35

SALINITY %o

Figure 9. — Temperature-salinity diagram for day 182 (I July 1971)
based on original isentropic data (o) with temperature-salinity values
from the harmonic fit (x). The numerals give the depth in meters for
the original isentropic data. The numbers in parentheses represent
the difference between the depth of the original isentropic values
and those from the harmonic fit.

3 wk in the series. The data gaps were bridged by linear
interpolation, as previously described, solely to facilitate
the analysis procedure. Therefore, although Equation (3)
will provide interpolated values for the gaps, the
significance of such values is limited. The limitation is
related to the Nyquist frequency,

/

1

2At

n
T

(6)

specifying the highest harmonic to which, in theory,
Fourier analysis can be carried out when the data inter-
val is St (Jenkins and Watts 1968). Thus, with It =
T/2n, the longest 1966 data gap of about 40 days permits
interpolation if the summation in Equation (4) is carried
out to M = 4. The longest 1967 gap of about 60 days limits
meaningful summation in Equation (4) to n = 3.

The gap between day 325 of 1967 and day 55 of 1968
comprised almost 90 days. Again, in order to facilitate
the analysis procedure the values for day 60 of 1968 were

12

extrapolated backwards to day 1. Consequently, ex-
pected values for day 1 through day 60 have no validity.
Interpolated values could have been obtained if the har-
monic analyses were carried out from July 1967 to July
1968. A 90-day gap, however, permits meaningful sum-
mation only to R = 2 in Equation (3) which, as is evident
from Figures 5, 6, and 7, would resolve only a small por-
tion of the variance.

After the winter of 1968, the longest gap in the data
series of about 20 days occurred in 1969, limiting signifi-
cant interpolation for this gap to n = 9 in the summa-
tion of Equation (4). In general, all coefficients to n = 12
that are tabulated in Appendix I can be used to evaluate
the harmonic function for time spans, including those in
1966 and 1967, where data gaps are 15 days or less.

Results of the Harmonic Analyses

Within the limitations discussed in the previous sec-
tion the harmonic coefficients tabulated in Appendix I
can be used in Equation (3) to obtain smoothed values of
the temperature, salinity, and depth at any of the desig-
nated levels from the sea surface to ct, 27.4. This calcula-
tion was performed and the results were tabulated in Ap-
pendix II for the first of each month of each of the years
1966 through 1971. The values for the 1966 and 1967
periods were computed by summing the harmonic series
to the 3d harmonic, while the values for the succeeding
years were computed to the 12th harmonic. In addition,
the values for the 366th day for each analysis period are
included to allow the month-to-month changes in prop-
erties to be computed for the entire year. Because har-
monic analyses were performed for individual years, the
expected values on the 366th day of one year may not
match up with the corresponding values on the first day
of the following year.

In order to facilitate the computation of dynamic
heights at the surface and acceleration potentials at ct,
levels relative to 1,000 dB, interpolated temperatures,
salinities, and a, values at 1,000 m are included in the
tabulations of Appendix II.

OCEANOGRAPHIC CONDITIONS AT
OWS-V

The Oceanographic Setting

In addition to heat exchange and wind induced flow
processes, variability in surface properties and vertical
structure is affected by shifts of the ocean system
relative to the geographically fixed location, variations
in the intensity of currents, and eddies. A description of
the oceanographic setting of OWS-V, therefore, will aid
qualitative interpretations of the low frequency oceano-
graphic variations in the time series presented in this
report.

OWS-V is located in waters downstream of the
Kuroshio, called the Kuroshio Extension (Sverdrup et
al. 1942). Summaries of the oceanographic conditions of
this region have been given by Masuzawa (1972) and

Kawai (1972). These articles supplement the earlier
work of Fleming (1955), Muromtsev (1958), Uda (1963),
Barkley (1968), and others.

The surface distributions of temperature and salinity
of the North Pacific Ocean have been presented in
numerous atlases and other publications such as that
produced by the Japan Hydrographic Association
(1975). These show that isopleths of temperature and
salinity are generally zonal in the vicinity of OWS-V.
Meridional temperature gradients range from about
0.4°C per degree of latitude in summer to 0.9°C per de-
gree of latitude in winter. Salinities at OWS-V tend to
be highest in late winter and early spring when the
meridional gradient is about 0.04%. per degree of
latitude. Lowest salinities occur from July to October
when the meridional gradient is about 0.09%. per degree
of latitude.

Charts of the dynamic topography of the North
Pacific Ocean prepared by Reid (1961) and Wyrtki
(1975) show that OWS-V is located in the eastward ex-
tension of the Kuroshio. These charts, however, are
based on smoothed, long-term averages and do not ex-
hibit the nature of the flow near OWS-V that mate-
rially affects the variability of oceanographic properties
at the station. The dynamic topography presented by
Kawai (1972), based on observations during the summer
and fall of 1957, is reproduced in Figure 10. The tightly
packed isopleths of dynamic height show the meander-
ing nature of the Kuroshio Extension between lat. 32°
and 38°N. Eddies abound both to the south and to the
north of this current.

The existence of eddylike features associated with the
Kuroshio current system has been well documented in
the literature. The confluence area of the Kuroshio and
Oyashio has been called the "Transition Area" by Uda
(1938) or the "Perturbed Area" by Kawai (1972).
Barkley (1968) drew attention to the eddy structure of
this area, and Bernstein and White (1977) have shown
that the baroclinic mesoscale eddy energy in this ju-ea is
an order of magnitude higher than that east of long.
170°W.

In the illustration (Fig. 10), OWS-V is located within
the meandering current. It is conceivable that at various
times the current could pass either to the north or to the
south of the station, but OWS-V would remain in an
area of eddy-induced variability. This variability makes
analysis of the vertical temperature and salinity dis-
tribution difficult if these properties are presented as a
function of depth. However, if these properties are
presented as a function of density (isentropic format)
current and eddy-induced variability is reflected only in
the depth distribution of isopycnals.

Meridional and zonal sections of the salinity and
depth as a function of o; are useful in describing the
baroclinic setting. A meridional section of hydrographic
stations was occupied in April 1971 at long. 168°E
(Roden 1972). Although this section lies to the east of
OWS-V, it reflects the characteristic meridional distri-
butions to be found at the longitude of the station. The
dominant feature in the salinity section (Fig. 11, upper

13

Figure 10.— Dynamic topography (dynamic meters) of the sea surface relative to the 1,000 decibar surface derived from selected stations dur-
ing the summer of 1957 (from Kawai 1972). The location of Ocean Weather Station V is denoted by an "X".

panel) is the constancy of a, of the salinity minimum
layer. This layer protrudes southward from the subarc-
tic front between lat. 41° and 42°N and is identified
with the North Pacific intermediate water (Sverdrup et
al. 1942; Reid 1965). During the time of this section, at
the latitude of OWS-V, the salinity decreased
monotonically from the surface to the depth of the
salinity minimum. Farther south, however, shallow
salinity maxima occurred.

The distribution of depth as a function of a, in the sec-
tion (Fig. 11, middle panel) reflects the baroclinicity of
the zonal flow and embedded eddies. The bottom panel
of Figure 11 shows that the principal zonal geostrophic
flow occurs between lat. 29° and 35°N. Given the
meandering nature of this current (Fig. 10) it is p)ossible
that the vertical density structure at OWS-V may be
similar to that found within, to the north, or to the south
of the current.

Useful zonal sections have been produced by
Masuzawa (1972) from a selection of 18 stations during
the summer season on the south side of the Kuroshio
and Kuroshio Extension. The distribution of ther-
mosteric anomaly versus depth and salinity versus ther-
mosteric anomaly are reproduced in Figure 12. [Surfaces
of thermosteric anomaly are parallel to surfaces of a,
(Montgomery and Wooster 1954).] The middle portion
of this section from long. 130° to 170°E runs along
approximately lat. 32°N. Note the differences in the dis-
tribution of salinity above a, 26.0. East of long. 165°E
the highest salinities occur at or near the surface, iden-
tifying the North Pacific central water. West of long.
160°E a shallow salinity maximum occurs at about o;
25. This subtropical water structure with relatively low

salinity surface water is characteristic of the Kuroshio
during summer (Masuzawa 1972). At the longitude of
OWS-V, the thermosteric anomaly of 200 cl/f (about a,
26) is at 500 m (Fig. 12), but at long. 168°E and at the
same latitude as OWS-V a, 26 is near 200 m (Fig. 11).
This difference is consistent with the meanders of the
current shown in Figure 10.

Variability and Structure 1966-71

The seasonal variability of the sea surface
temperature and salinity for the 6 years of hydro-
graphic observations are shown in the T-S diagrams of
Figure 13. Six-year averages provide the reference T-S
relationships with temperatures ranging from about
16°C in March to 26°C in August and salinities ranging
from about 34.73%. in April to 34.437.. in September.
Departures from the average pattern during each year
appear to be more pronounced in the salinity than in the
temperature. For example, from June to December 1966
salinities were up to 0.2%. higher. Higher salinities also
occurred during spring and early summer of 1968.
Salinities were lower than the average during much of
the summer and fall of 1969 and again from June to
August of 1971.

A major departure from the average temperature,
lasting several months, occurred in 1969-70.
Temperatures were 1°C or more below average from

Figure 11.— Meridional sections, lat. 21° to 42''N, long. 168°E, based
on B7 STD stations occupied 3-11 .April 1971. Upper panel: Salinity
(7..) vs. (7, values. Middle panel: Depth (m) vs. <r, values. Bottom
panel: Dynamic topography (dyn. m.) at the sea surface relative to
1,000 decibar surface.

14

2.5-

-I 1 1 r

~1 I T"

-T 1 1 1 1 1 r

-1 1 1 r

DYN. M.

2.0-

1.0-

42 41 40 39 38 37 36 35 34 3,3 3,2 3f 3,0 29 2,8 27 2,6 25 24 2,3 22 21

_l I 1 1 I I I I I ' I I I 1 I I I 1 1 1 1 1 —

DEGREES NORTH LATITUDE

15

line along southern edge of Kuroshio

20N :5N 130E UO 130 I6OE 170 180 170W

500

000

Figure 12. — Section of salinity (7.=) versus tliermosteric anomaly (cl t ') along right-hand edge of Kuroshio
(upper panel). Section of thermosteric anomaU' versus depth (m) along right-hand edge of Kuroshio (lower
panel). (From Masuzav\-a 1972.)

September 1969 to June 1970. In March 1970 the sea-
surface temperature was 2.5°C below the 6 yr average.
Above-average temperatures occurred in the winters of
1966 and 1969.

The time variability in the vertical structure at OWS-
V as reflected by the smoothed isopleths of salinity and
depth versus ct, is shown in Figure 14. Harmonic func-
tions were evaluated at the first of each month using 12
harmonics for 1968-71 and only the first 3 harmonics for
1966 and 1967. The isopleths of salinity and depth are
not shown for the time from 1 November 1967 to 1
March 1968 due to the large data gap during this time.
However, the expected surface salinity and density for
day 331 of 1967 and days 1 and 31 of 1968 are plotted and
were derived from the harmonic coefficients for the sur-
face temperature and salinity at OWS-V (Yong 1971).

The common feature for all years in the isentropic

salinity distribution is the constancy of salinity versus a ,
at depths below the a, 26 level reflecting a constancy of
T-S relationships. Note the constancy of the salinity
minimum layer at a, 26.8, a feature that was also ap-
parent in both the meridional and zonal sections shown
in Figures 11 and 12.

Time variability in the salinity becomes pronounced
above the a, 26 level and is associated, in part, with the
seasonal change in the surface density. Maximum den-
sity at the surface occurs in March or April and
minimum density in August or September. In 1970, for
example, the maximum surface density was only a little
less than a, 26. During the summer when the surface
salinity is lower than in winter, a subsurface salinity
maximum forms. In winter the highest salinity of 34.6 or
34.7%. occurs at the surface. The structure of the subsur-
face salinity maximum is variable and may appear as

16

12--

T III

34.4

-) 1 1 (-

1967

28--

24-.

20-

16 ■■

12--

C 0,

J , /oc

1969

34.8

-i 1 1 1 1-

34.4

34.8

H 1 1 1 1-

1970

.-'".K7

34.4

348

-I 1 1 1 1 1 I

344 34.8

28-

24..

20-

16-

12--

28- ■

24-

20 ■■

16--

12-

1968

H 1 1— —I 1-

34.4

34.8

1971

-1 1 1 1 1-

34 4

34.8

Figure 13.— Monthly mean surface temperature-salinity relationships at Ocean Weather Station V, 1966-71, connected by dashed lines. Arabic
numerals represent months. Solid line connects 6-yr mean values. Roman numerals on the 1966 plot give months for the mean values.

well-developed cells as in June to August 1968, August
1969, and November 1971.

The baroclinicity of the area is reflected by the depth
of cr, levels. Time variability penetrates to the a, level.
The depth of a, 26, the level below the seasonal
temperature and salinity variability, ranges from about
200 to 400 m. These depth changes are not seasonal but
show longer term variations. For example, during much
of 1966 a, 26 was deeper than 300 m; during 1970 it
remained near 200 m. Superimposed on these variations
are perturbations of several months duration as in July
to September 1969. Amplitudes of the harmonic series,
C„ = (Ai + B;)"- , of the depth of the ff, 26 level for the
entire 6-yr record (Fig. 15) show that the greatest por-
tion of the variance, C„ >30 m; occurs on the interan-
nual time scale. Beyond the 39th harmonic (56 day
period) the absolute magnitudes of the amplitudes re-
main <10 m. Thus, changes in the depth of the pycno-
cline, as reflected by the a, 26 level, are climate-scale
phenomena.

In terms of the oceanographic setting of OWS-V, the
depth variations reflect north-south shifts of the
Kuroshio Extension and/or passage of baroclinic eddies.
The salinity variability above the a, 26 level permits
qualitative interpretation of the observed depth
changes. Whenever the depth of a, 26 increases to >300
m (see dashed lines in salinity sections. Fig. 14) there is
a concurrent increase in the salinity of the shallow max-
imum, and during the winter, an increase in the surface
salinity. Increases in depths began in February and June
1966, May 1968, April and July 1969, March and
November 1971. A shallow salinity maximum is charac-
teristic of Kuroshio water (Fig. 12). Thus, the coinci-
dent increases in salinity in the shallow maximum, or at
the surface during the winter with increasing depths of
a, 26 indicate a northward meander of the Kuroshio Ex-
tension.

In 1970, when a, 26 shoaled to <300 m, the salinity in
the shallow maximum during spring, summer, and fall
was relatively high in contrast to that in 1967 when the

17

I 1 —

1966
SALINITY, %o

-1 1 1 r

23.

24.0

25.0

26.0

27.0

----^4.0

34.1-
34.2-

J F M^A^M.J ,J A,S ,0,N,D,

23.0

24.0

25.0

26.0

27. C.

Figure 14.— Vertical pronies of salinity (upper panel) and depth (lower panell, wiih (t, as ordinate, at Ocean
Weather Station V. 1966-71. Values were calculated for first day of each month from the harmonic series car-
ried out to the .ird harmonic in 1!I66 and 19B7 and to the 12th harmonic in l%s through 1971. I ppermost solid
line connects surface a values. The contour intervals are 0.17.. for salinity and 100 m for depth. Dashed
curves on salinity plot represent 100 m and 300 m isopleths.

18

-I 1 1 1 1 1 1 1 1 1 I

23.0

24.0

25.0

26.0

27.0

T r

1967

SALINITY, %o

34.4

- 34.2
■34.1 -

n34.0

-34.1 —
-34.2—

J F,M A,M J, J A S O N D

'''''' 1 1 ■ ' I ' '

-I 1 1 1 1 1 1 r

1967

DEPTH

I I r

23.0

24.C

25.0.

26.0

27.0.

J,F,M,A,M,J,J,A,S,0,N.D

Figure 14. — Continued.

19

1968

1

1 1 1 1 r—

1

' '

SALINITY, %o

23.0

f\ 34. sX

// ^ \

V

24.0

J r^ \ ■^''■^

N.

V

25.0

-

^

/ Vy 34.9 ) \

>34.8 ° ,34t8.34. 7

X. .

^"^^^^

j^^::_

X

C

V.

>'

— ^_-_--^-34. 6 ~-^

26.0

-

--'

^j^^^

^£.

— — — _ -^4 4 —1300

34. 2 ____

27.0

—

34.1 .

34.1

J F M

A

M

J J A S ,

N

D

I I

1968
DEPTH

-I 1 1 1 r

23.0.

24.0

25.0

26.0

27.0

,J,F,M,A,M,J,J,A,S,0,N,D

Figure 14. — Continued.

20

-I 1 1 1 1 r

23.0

24.0

25.0

26.0

27.0

-1 1 i r

1969
SALINITY, %o

JF.M.A.M.JJ AS.O.N.D

T 1

1969
DEPTH, m

T 1 1 r

T 1 1 1 1 r

23,0

24.0

25,0

26,0

27.0

J,F,M|A,M,J,J,A,S,0,N,D

Figure 14. — Continued.

21

T 1

1970
SALINITY. %o

-I 1 1 1 1 1 1 r

23.0

24.0

25.0

26.0

27.0

J,F,M,A,M,J,J,A,S,0,N,D

— 1 I

1970

1 1 r

-I ; — 1 1 1 r

DEPTH, m.

23.0

-

[""^^^

-

24.0

-

/

50'

\

\

^

-

25,0

\^

-==

/>'"'

100 '^'^ v^

on A — - — — "" ^"^'^~~-.

/

^—~

-

26.0

_, -.„__

~~

_ 400 ---^^

—-

—^

27.0

—■

— 800 ^:::::=: —

—

"^ibo

1100

— — —

, J , F

M

, A , M

J

, J , A , S , O ,

N

■ D -

Figure 14. — Continued.

T 1 1 r

1971
SALINITY, %o

T 1 1 r

23.0

24.0

25.0

26.0

27.0

J ■ '^ M , A , M , J J , A , S , O , N , D .

23.0

24.0

25.0

26.0

27.0 _

"T 1 1 1 r

"I 1 r

1971
DEPTH. m.

J. P.M. A, M.J, J, A , S , O , N , D

J — -- — I — - — i—i: L.

Figure ]i.— Continued.

23

90- -m

IjillllHlJi

ilii

,il.illlii.illi.l.ii.iii..ijiill

"*' tn^i^f

period in days

Figure 15. — Absolute magnitude of the amplitudes of the harmonic function for the S-yr series of the depth of
o, 26.0. Procedure was identical to that used in the annual analyses.

depth of (Tj 26 was also shallow. The high salinity indi-
cates the presence of Kuroshio water at OWS-V al-
though the shallow depth of a, 26 did not indicate a
northward shift of the Kuroshio Extension. An explana-
tion may be a weakened baroclinic flow during 1970 or a
residual consequence of processes upstream of the sta-
tion that also caused the lower surface temperatures at
OWS-V during the first half of 1970.

The Water Structure and Air-Sea Interaction

A study of the effects of atmospheric forcing on ocean
variability at OWS-V is not within the scope of this
report. Nevertheless, some inferences can be made
about the changes described above in the light of the air-
sea interactions previously published (Husby and
Seckel 1975). For example, principal heat loss from the
sea surface occurs during the 6 mo from 1 October to 1
April, and one can inquire about the change in heat con-
tent of the water column between these dates.

Consider the layer above ct, 26 in which temperature
and salinity show seasonal changes. The heat content of
this layer is pc^ dz where p is the density of the water, Cp
is the specific heat at constant pressure, S is the mean
temperature of the layer and z is the depth of the layer.
With p and Cp assumed constant, the heat content of the
layer changes because of changes in the thickness of the
layer (divergence) and because of changes in the mean
temperature.

AH = PC Mdz) = pc [eiz + zse].

(7)

Changes in the last term are caused by the heat ex-
change across the sea surface, advection, and diffusion.
In Table 3, the heat content change, the heat content
change due to the mean temperature change, and the
total heat exchange across the sea surface are listed for

the fall and winter cooling seasons from 1966 to 1971.
Note the large interannual variability in the heat con-
tent changes with the layer actually gaining heat during
the 1967-68 season when the total heat loss across the
sea surface was anomalously high. Not only are these
changes much larger than can be accounted for by the
total heat exchange, they also bear no resemblance to
the year to year changes of this atmospheric forcing
process. The heat content change due to the change of
mean temperature has the same order of magnitude as
the total heat exchange but again, the interannual vari-
ability does not resemble that of the atmospheric forcing
process. For example, the total heat exchange in the
1968-69 season was less than half that of the previous
year, and yet the difference in the heat content change
due to change in mean temperature was only 8 kcal
cm"^. Evidently other processes such as heat advection,
play an important part in the change of mean
temperature.

The 6-yr series of heat content of the layer to the o; 26
level (Fig. 16) shows that during 1966 the heat content
was high, and during 1970 it was relatively low with ir-
regular fluctuations between these years. A seasonal

Table 3. — Heat budget estimates at Ocean Water Station V for the
6-mos cooling portion of the year, 1 October to 1 April.

A'

B^

C=

(kcal cm -2)

(kcal cm -)

(kcaJcm-2)

1 Oct. 1966-1 Apr. 1967

-228.6

-93.0

-62.3

lOct.1967-1 Apr. 1968

96.1

-76.4

-69.8

1 Oct, 1968-1 Apr. 1969

-137.1

-68.5

-33.1

1 Oct. 1969-1 Apr. 1970

-82.1

-51.7

-48.4

lOct. 1970-1 Apr. 1971

-139.6

-46.7

-53.6

'Heat content change in the layer from surface to (t^26.
•Heat content change due to the change in mean temperature in layer
from the surface to 0^26 (see text).

'Total heat exchange across sea surface.

24

I I I (

o .

«

a>

^

V)

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c

s
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25

pattern is not discernible. The 6-yr series of the depth of
a, 26 is shown in the lower panel indicating that the fluc-
tuations in depth of the lower boundary of the layer are
coherent with those in heat content: high heat content
corresponds to greater thickness of the layer and lower
heat content with reduced thickness. The coherence is
clearly shown by the dashed line in Figure 16, repre-
senting the heat content variability due to changes in
thickness {SAz) only. The values were obtained by se-
quentially adding the monthly changes {SAz) to the in-
itial heat content on day 1, 1966. (The series was re-
initialized on day 61, 1968.)

The seasonal aspects of the change of heat content per
month due to change in the mean temperature in the
layer above ct, 26.0 izAd), and the monthly heat ex-
change across the sea surface are shown in Figure 17.
The two quantities plotted are of equivalent magnitude
although the month to month variability of the change
of heat content is greater than that of the heat ex-
change. If one assumes that the magnitude of the heat
exchange is correct, then a greater decline in heat con-
tent than expected from heat exchange tends to occur
during fall and winter. Heat content increases, greater
than those expected from heat exchange, tend to occur
during spring and summer. According to our estimates
the heat exchange across the sea surface contributes
only 47?o to the variance in the rate of change of heat
content due to mean temperature change. The remain-
der must be attributed to advection and diffusion of
which the former is probably the dominant process.

Another opportunity to examine the effect of total
heat exchange across the sea surface occurred during the
time from the fall of 1969 to the spring of 1970 when both
the surface temperature and the mean temperature in
the layer above a, 26 were below the 6-yr average. Cool-
ing began in August, 2 mo earlier than average, and con-
tinued until March 1970 (Fig. 18). A greater than
average increase in temperature occurred in April 1970
(1.1°C instead of 0.1°C). Throughout this time there is
no indication of anomalous heat exchange across the sea
surface (Fig. 17). It is interesting to note that in April
1970 there was an increase in the surface salinity that
subsequently persisted as a shallow subsurface salinity
maximum (Fig. 14). There was no significant change in
depth of the thermal structure {a^ 26) during this month
of relatively large surface temperature and salinity
changes.

In summary, anomalous heat content changes in the
6-yr series cannot be attributed exclusively to
anomalous heat exchange across the sea surface. Pos-
sibly, effects of processes >1,(XX) km upstream in the
principal heat loss area of the North Pacific Ocean play
an important role in the temperature variability. Unfor-
tunately, heat advection cannot be calculated from the
properties that were measured at OWS-V.

The salinity and salt content are important prop-
erties in isentropic analysis. Salt budget analyses,
however, suffer from the lack of reliable precipitation
data. The association of a shallow salinity maximum
with the depth of tr, 26 has already been described. In

addition, there appears to be a seasonal trend in the 6-yr
average of the surface salinity with the maximum occur-
ring in late winter and spring and the minimum in late
summer and early fall. Departures during individual
years are large so that the average of only 6 yr may
depart significantly from a long-term mean.

Reed and Elliott (1973) have estimated the precipita-
tion at OWS-V from the present weather code in the
standard marine weather repwrts. Although absolute
magnitudes of these estimates may be in doubt, the
seasonal trend is probably correct. The mean monthly
values are listed in Table 4 together with the estimates
of mean evaporation at OWS-V (Husby and Seckel
1975). The evaporation minus precipitation values indi-
cate excess evaporation over precipitation during most
of the year with lowest values occurring from April to
August when the average salinities are also declining at
OWS-V.

As in the case of the surface temperature the effect of
advection on the surface salinity may be pronounced.

Table 4.— Estimates of mean evaporation rates (E)', mean precipita-
tion rates (P)", and evaporation minus precipitation (E-P), (in milli-
meters per month) at Ocean Weather Station V.

J

F

M

A

M

J

J

A

S

N

D

E

207

204

162

90

59

51

42

78

128

150

201

213

P

70

62

68

68

59

63

39

30

21

32

64

70

E-P

137

142

84

22

-12

3

48

107

118

137

143

'Husby and Seckel (1975).
'Reed and Elliot (1973).

SUMMARY AND CONCLUSIONS

In this report the oceanographic station data obtained
at OWS-V from 1966 to 1971 have been presented in a
form that lends itself to an examination of the effects of
atmospheric forcing on the water structure. The report
complements a previous report on large-scale air-sea
interactions at OWS-V (Husby and Seckel 1975). The
data processing and analysis procedures have been de-
scribed. In order to facilitate future analysis of ocean
structure, the principal features in the ocean variability
have been described and heat budget estimates have
been made that point to the important processes af-
fecting the temperature in the upper layer at OWS-V.

Rather than presenting the temperature, salinity, and
o; as a function of depth, the temperature, salinity, and
depth were presented as a function of ct, which we call
the isentropic format. Harmonic analysis was used as a
curve-fitting procedure to summarize the isentropic
data with a relatively small number of coefficients and
to provide smoothed estimates of daily observations.
Large gaps in the sampling record in 1966 and 1967 limit
the usefulness of the harmonic coefficients during these
time periods. Results of the harmonic analyses are
presented in the appendix showing the harmonic coef-
ficients for the temperature, salinity, and depth at inter-
vals of 0.2 a,

Presentation of the oceanographic station data in
isentropic format shows that the apparently complex

26

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. .Q

.<

O

JC

■*

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a>

c

.<

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1^

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bx

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to

(O
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I

28

distribution of properties at OWS-V have some order
and permit identification and isolation of different proc-
esses that contribute to changes in the distributions.
This point is illustrated by the time-series sections of
salinity versus a, (Fig. 14). At depths greater than a, 26
the T-S relationships remain relatively constant with
the salinity minimum occurring at a constant tr, level, <t,
26.8.

Variations in the depth of sigma-( below (T, 26 (Fig. 14)
reflect changes in the baroclinicity of the area. Deepen-
ing of the pycnocline as indicated by the depth of a, 26 is
associated with an increase in the surface salinity during
winter or the appearance of a shallow subsurface salinity
maximum at other times of the year. A shallow subsur-
face salinity maximum is characteristic of the Kuroshio
Current. Meridional sections near OWS-V show the pyc-
nocline depth to increase southward. Thus, the associ-
ated changes in the salinity of the upper layers above a,
26 indicate meandering of the Kuroshio Extension.

The net heat loss across the sea surface at OWS-V
during the fall and winter 1967-68 was anomalously high
and during 1968-69 anomalously low. These anomalies
were not reflected in changes of the heat content in the
layer above a, 26. In fact, changes in the thickness of the
layer are the dominant influence in changes of heat con-
tent, obscuring effects of the seasonal variation of the
heat exchange across the sea surface. The variation of
the heat content of the layer due to a change in the mean
temperature (Fig. 17) does reflect the seasonal variation
of heat exchange across the sea surface. Again, however,
the anomalous heat loss during 1967-68 and 1968-69 are
n )t reflected in anomalous declines of the mean
temperature of the upper layer. Anomalously low
temperatures beginning in the summer of 1969 and
lasting to the spring of 1970 were not caused by
anomalous heat exchange. Thus, horizontal advection
and possibly, to a lesser extent, diffusion play a domi-
nant role in the temperature variability at OWS-V.

It is interesting to note that the surface divergence as
reflected by changes in the depth of a, 26 has no annual
periodicity. The 6-yr record shows that large baroclinic
variability occurs at time scales of more than 55 days
with largest variability occurring at the interannual
scale.

OWS-V is located in a dynamically active ocean area
with the area of highest net annual heat loss in the
North Pacific lying over 1,(X)0 km upstream. Relatively
large meridional temperature gradients vary seasonally
and probably also from month to month. Velocity varia-
tions of the Kuroshio Extension at the time scales con-
sidered here must also be expected. Consequently, di-
vergence and horizontal advection play an important
role in the variability of the observed properties, ob-
scuring the effects of local atmospheric forcing.

The preliminary analyses reported here show that im-
portant properties of the ocean structure can be ob-
tained from a monitoring station such as OWS-V. It
may be more difficult, however, to relate changes in the
structure with local atmospheric forcing. In this case the
effects of heat exchange across the sea surface are ob-

scured by other processes. Some of these processes could
possibly be determined by measurements that have not
been made on weather ships. Obviously, anomalous
atmospheric forcing must produce anomalous ocean
conditions. It appears that these relationships can be es-
tablished best if fields of properties in ocean and atmos-
phere are monitored in order that the effect of diver-
gence and advection can be determined, or that area
integrals can be obtained.

ACKNOWLEDGMENTS

We thank A. Bakun, Pacific Environmental Group,
NMFS; R. L. Elsberry, Naval Postgraduate School; and
S. Tabata, Institute of Ocean Sciences, Sidney, B.C., for
reviewing the manuscript and making many useful com-
ments.

LITERATURE CITED

BARKLEY, R. A.

1968. Oceanographic atlas of the Pacific Ocean. Univ. Hawaii
Press, Honolulu, 20 p., 156 figs.
BERNSTEIN, R. L., and W. B. WHITE.

1977. Zonal variability in the distribution of eddy energy in the
mid-latitude North Pacific Ocean. J. Phys. Oceanogr. 7:123-126.
FLEMING, R. H.

1955. Review of the oceanography of the northern Pacific. Int.
North Pac. Fish. Coram., Bull. 2, 43 p.
HUSBY, D. M.

1968. Oceanographic observations North Pacific Ocean Station
VICTOR 34'>00'N, 164°00'E. December 1964— August 1966. U.S.
Coast Guard Oceanogr. Rep. 15, CG 373-15, 141 p.
HUSBY, D. M., and G. R. SECKEL.

1975. Large-scale air-sea interactions at ocean weather station V,
1951-71. U.S. Dep. Commer.. NOAA Tech. Rep. NMFS SSRF-
696. 44 p.
.JAPAN HYDROGRAPHIC ASSOCIATION.

1975. Marine environmental atlas, northwestern Pacific Ocean -
statistics of the oceanographic elements, 164 p.
.JENKINS, G. M., and D. G. WATTS.

1968. Spectral analysis and its applications. Holden-Day Inc.,
San Francisco, 525 p.
KAWAI, H.

1972. Hydrography of the Kuroshio Extension. In H. Stommel
and K. Yoshida (editors), Kuroshio: physical aspect* of the Japan
Current, p. 235-352. Univ. Wash. Press, Seattle.
MASUZAWA, J.

1972. Water characteristics of the North Pacific central region. In
H. Stommel and K. Yoshida (editors), Kuroshio: physical aspects
of the Japan Current, p. 95-127. Univ. Wash. Press, Seattle.
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1938. Circulation in upper layers of southern North Atlantic
deduced with use of isentropic analysis. Mass. Inst. Technol.,
Pap, Phys. Oceanogr. Meteorol. 6(2), 55 p.
MONTGOMERY, R. B.. and W. S. WOOSTER.

1954. Thermosteric anomaly and the analysis of serial oceano-
graphic data. Deep-Sea Res. 2:63-70.
MUROMTSEV, A. M.

1958. The principal hydrological features of the Pacific Ocean.
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the Russian by A. Birron and Z. S. Cole in 1963. Israel Program for
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PARR, A. E.

1938. Isopycnic analysis of current flow by means of identifying
properties. J. Mar. Res. 1:133-154.

29

REED, R. K., and W. P. ELLIOTT.

1973. Precipitation at ocean weather stations in the North
Pacific. J. Geophys. Res. 78:7087-7091.
REID, J. L., Jr.

1961. On the geostrophic flow at the surface of the Pacific Ocean

with respect to the 1,000-decibar surface. Tellus 13:489-502.
1965. Intermediate waters of the Pacific Ocean. John Hopkins
OceanogT. Stud. 2, 85 p.
RODEN, G. I.

1972. Temperature and salinity fronts at the boundaries of the sub-
arctic-subtropical transition zone in the western Pacific. J.
Geophys. Res. 77:7175-7187.
SVERDRUP, H. U., M. W. JOHNSON, and R. H. FLEMING.

1942. The oceans, their physics, chemistry, and general
biology. Prentice-Hall, N.Y., x + 1087 p.
TABATA, S.

1965. Variability of oceanographic conditions at ocean station "P"

in the northeast Pacific Ocean. Trans. R. Soc. Can. 3(Ser. 4):367-

418.
UDA, M.

1938. Researches on "Siome" or current rip in the seas and

oceans. Geophys. Mag. 11:307-372.
1963. Oceanography of the subarctic Pacific Ocean. J. Fish. Res.

Board Can. 20:119-179.

WYRTKl, K.

1975. Fluctuations of the dynamic topography in the Pacific
Ocean. J. Phys. Oceanogr. 5:4.50-459.

YONG, M. Y. Y.

1971. Sea surface temperatures and salinities collected between
1957 and 1969 at nine Pacific monitoring stations. U.S. Dep.
Commer.. NOAA, NMFS Data Rep. 69. 35 p., on 1 micro-
fiche. [Available Natl. Tech. Inf. Serv., 5285 Port Royal Road,
Springfield, VA 22151, as COM-72-10099.1

30

APPENDIX I

Tables of coefficients for the calculation of temperatures, °C,
salinities, %., and depths, m, at sigma-f levels at Ocean Weather Sta-
tion V, 1966-71, using the series

E{t) = /(I) + M • (t-1) + A+ Z [/!„ cos ^^ + B„ sin ^

n = 1, 2, . . . , 12

where /(I) = value of property at first day of year,

V = slope of straight line between /(I) and /(366),

o) = ^ day-', except for 1968 where uj = -'^- day',
366 367

t = Julian day of the year

Upper row of Fourier coefficients at each level contains A -coefficients
beginning with A i . Lower row contains B-coefficients beginning with Bj .

31

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49

APPENDIX II

Expected values of Ocean Weather Station V temperatures, °C x 100,
(top panel); salinities, %. X 100, (middle panel); and depths, m, (bot-
tom panel) at sigma-f levels evaluated at the first day of each month for
the years 1966-71.

Values were computed by using the tabulations of Appendix I in
Equation (3). Only the first three harmonics in the series were evaluated
for 1966 and 1967. All 12 harmonics in the series were evaluated for 1968
through 1971.

50

1966

2611

■

Z457

12581

• 2524

• 2483

2531
12521

.2454

• 2396

• 2396

.2387

• 2334

.2331

.2323

2306

2229

.2272

.2266

.2259

I 2243

.

:22B3

.2209

.2200

.2193

.2160

.2131

.2143

.2131

.2126

.2135

.2072

.2073

• 2053

.2061

• 2065

2020

leee

1902
• 1916

.2006

.1922

• 2003

• 1930

• 1995
.1922

.1994
• 192S

• 1996
. 1925

:i992
.1924

1905

.1893

- .1731

.1619

.1850

.1655

.1844

.1846

• 1852

. 1850

• 1831

. 1640

leee

1714

1740

1722

. 1731

. 1775

. 1777

• 1759

• 17S4

.1775

.1771

. 1779

. 1S69

.leas

Iiee2

.1670

. 1646

- 1647

. 1679

.1683

.1666

.1668

. 1683

.1886

• 1691

.1506

.1504

.153*

• 1562

.1562

.1554

.1567

.1555

.1563

.1563

• 1573

.1567

.1578

.lill7

. 14B1

. 1410

. 1411

.1452

• 1428

.1432

• 1431

• 1440

. 1437

.1436

.1437

.1443

. 1298

.1297

.1279

.1289

.1313

• 1297

. 1292

• 1288

• 1303

.1307

.1301

.1297

.1291

.1172

.11&0

.1140

.1131

. 1168

. 1149

.1135

• 1136

.1L46

.1155

.1155

• 1136

.1130

• 1004

.977

.961

■ 969

. 1014

.973

■ B64

.977

.375

• 982

.990

.967

• 349

.763

.768

.789

.785

.807

.764

.775

.764

• 777

.768

.803

.771

.761

.562

.569

.606

.605

.B2E

• 614

.606

• 617

.601

.604

.61.2

.606

.598

.479

.461

.476

.486

.484

.499

.472

.482

.478

.486

• 477

.477

.476

.386

.383

.372

.994

.393

.405

.391

.390

.392

.396

.390

.397

.387

-309

.291

.277

.305

.306

.317

.318

.314

• 308

.306

• 313

.323

• 309

.31J

.915

.311

.316

.328

.352

.378

.387

.372

.356

.346

.364

.379

1
1

32

1

60

1

91

1

121

1

152

1

182

I

213

1

244

1

274

1

305

1

335
1

36S

1

3459

-

3451

I 3458
.3452
.3465

3460
13461
.3461

.3465

.3465

.3461

.3468

.3466

• 3463

3464

3467

.3471

.3467

■ 3465

• 3459

.

13470

• 3473

.3469

■ 3456

.3463

.3470

• 3474

.3472

,3470

.3473

.3475

.3476

.3473

.3472

.9474

3475

3439

3485
13474

.3479
.3476

.3477
.3479

.3475
• 3476

.3475
• 3478

.3477
.3478

:9474
.3477

3467
• 3466

.3439

.3458

.3478

■ 3480

• 3477

.3476

.3479

.3476

.3473

.3438

3456

347 3

3476

3469

.3467

.3480

.3481

.3475

.3476

.3480

.3479

.3481

.3443

.3455

I347I

.3473

.3467

.3467

.3476

.3477

.3473

• 3473

.3476

• 3479

.3480

.3451

.3451

.3459

.3468

.3467

.3465

.3469

.3465

.3468

.3467

.3471

• 3469

.3472

.3453

.3446

.3450

.3452

.3461

.3456

.3456

-3456

.3456

.3458

.3458

.3457

• 3458

.3446

• 3443

• 3441

.3440

.3451

• 3446

.3444

• 3444

.3447

.3448

.3447

• 3445

• 3444

.3440

.3436

.3434

.3431

.3440

.3436

• 3432

• 3433

• 3434

.3436

.3436

.3433

• 3433

-3426

.3422

• 3423

.3422

.3428

• 3422

.3419

• 3421

.3421

.3423

.3424

• 3419

.3419

.3404

.34B7

• 3412

.3410

.3412

.3409

.3487

• 3409

.3407

• 3409

.3412

.3406

.3404

.3399

.3400

.3403

.3403

.3406

• 3405

.3402

.3404

• 3401

.3403

.3405

.3403

.3402

. .3409

.3409

.3408

.3410

.3409

.3412

.3406

.3409

.3406

.3409

.3409

.3409

• 3409

.3423

.3422

.3420

.3423

■ 3423

.3424

.3422

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1

O U S GOVERNMENT POINTING OFCICE: 1930-796.326 /22 REGION 10

56

NOAA TECHNICAL REPORTS
NMFS CIRCULAR AND SPECIAL SCIENTIFIC REPORT
GUIDELINES FOR CONTRIBUTORS

FISHERIES

CONTENTS OF MANUSCRIPT

First page. Give the title (as concise as possible) of the paper
and the author's name, and footnote the author's affiliation,
mailing address, and ZIP code.

Contents. Contains the text headings and abbreviated figure
legends and table headings. Dots should follow each entry and
page numbers should be omitted.

Abstract. Not to exceed one double-spaced page. Footnotes
and literature citations do not belong in the abstract.

Text. See also Form of the Manuscript below. Follow the U.S.
Government Printing Office Style Manual, 1973 edition. Fish
names, follow the American Fisheries Society Special Publica-
tion No. 6, A List of Common and Scientific Names of Fishes
from the United States and Canada, third edition, 1970. Use
short, brief, informative headings in place of "Materials and
Methods."

Text footnotes. Type on a separate sheet from the text. For
unpublished or some processed material, give author, year, title
of manuscript, number of pages, and where it is filed — agency
and its location.

Personal communications. Cite name in text and footnote.
Cite in footnote; John J. Jones, Fishery Biologist, Scripps Insti-
tution of Oceanography, La JoUa, CA 92037, pers. commun. 21
May 1977.

Figures. Should be self-explanatory, not requiring reference
to the text. All figures should be cited consecutively in the text
and their placement indicated in the left-hand margin of the
manuscript. Photographs and line drawings should be of
"professional" quality — clear and balanced, and can be re-
duced to G'h inches (40 picas) for page width or to S'A inches (19
picas) for single-column width, but no more than 9 inches (54
picas) high. Photos should be printed on glossy paper — sharply
focussed, good contrast. Label each figure. List, and typed dou-
ble spaced, each figure legend. DO NOT SEND original figures
to the Scientific Editor; NMFS Scientific Publications Office
will request these if they are needed.

Tables. Each table should start on a separate page and should
be self-explanatory, not requiring reference to the text.
Headings should be short but amply descriptive. Use only
horizontal rules. Number table footnotes consecutively across
the page from left to right in Arabic numerals; and to avoid con-
fusion with powers, place them to the left of the numerals. If the
original tables are typed in our format and are clean and leg-
ible, these tables will be reproduced as they are. In the text all
tables should be cited consecutively and their placement indi-
cated in the left-hand margin of the manuscript.

Acknowledgments. Place at the end of text. Give credit only
to those who gave exceptional contributions and not to those
whose contributions are part of their normal duties.

Literature cited. In text as: Smith and Jones (1977) or (Smith
and Jones 1977); if more than one author, list according to years
(e.g.. Smith 1936; Jones et al. 1975; Doe 1977). All papers re-
ferred to in the text should be listed alphabetically by the senior
author's surname under the heading "Literature Cited"; only
the author's surname and initials are required in the author line.
The author is responsible for the accuracy of the literature cita-
tions. Abbreviations of names of periodicals and serials should
conform to Biological Abstracts List of Serials with Title Abbre-
viations. Format, see recent SSRF or Circular.

Abbreviations and symbols. Common ones, such as mm, m,
g, ml, mg, °C (for Celsius), %, 'I.., etc., should be used. Abbrevi-
ate units of measures only when used with numerals; periods are
rarely used in these abbreviations. But periods are used in et al.,
vs., e.g., i.e., Wash. (WA is used only with ZIP code), etc.
Abbreviations are acceptable in tables and figures where there is
lack of space.

Measurements. Should be given in metric units. Other
equivalent units may be given in parentheses.

FORM OF THE MANUSCRIPT

Original of the manuscript should be typed double-spaced on
white bond paper. Triple space above headings. Send good
duplicated copies of manuscript rather than carbon copies. The
sequence of the material should be:

FIRST PAGE

CONTENTS

ABSTRACT

TEXT

LITERATURE CITED

TEXT FOOTNOTES

APPENDIX

TABLES (each table should be numbered with an Arabic
numeral and heading provided)

LIST OF FIGURE LEGENDS (Entire figure legends, includ-
ing "Figure" before each number)

FIGURES

ADDITIONAL INFORMATION

Send ribbon copy and two duplicated copies of the manuscript
to:

Dr. Jay C. Quast, Scientific Editor

Northwest and Alaska Fisheries Center

Auke Bay Laboratory

National Marine Fisheries Service, NOAA

P.O. Box 155

Auke Bay, AK 99821

Copies. Fifty copies will be supplied to the senior author and
100 to his organization free of charge.

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