SEA SURFACE AND RELATED SUBSURFACE
TEMPERATURE ANOMALIES AT SEVERAL
POSITIONS IN THE NORTHEAST PACIFIC OCEAN
By
Conrad Lucien Be land
United States
Naval Postgraduate School
m
XT'
I
SEA SURFACE AND RELATED SUBSURFACE TEMPERATURE
ANOMALIES AT SEVERAL POSITIONS IN THE NORTHEAST
PACIFIC OCEAN
by
Conrad Lucien Beland
Thesis Advisor:
Dale F. Leipper
March 1971
Approved fion. pub tic <izlza.be.; dutxibtjutlon unlimited.
T13747^
Sea Surface and Related Subsurface Temperature
Anomalies at Several Positions in the Northeast
Pacific Ocean
by
Conrad Lucien Beland
Lieutenant, United States Navy
B.S.E.E., Auburn University, 1963
Submitted in partial fulfillment of the
requirements for the degree of
MASTER OF SCIENCE IN OCEANOGRAPHY
from the
NAVAL POSTGRADUATE SCHOOL
March 1971
-8 2
ABSTRACT
Sea surface temperature (SST) anomalies from previous sources have
been related to subsurface temperature anomalies obtained from BT's at
six positions in the Northeast Pacific. In this manner some under-
standing of the value of SST anomalies as indicators of ocean energy
states is achieved. Results show that for about 507o of the time, the
SST anomaly generally extended to depths of 100 meters or more. November
through April were found to be the months most favorable for the
occurrence of these deeply penetrating anomalies. Summertime SST
anomalies were determined to be shallow features of less than 40 meters
and were not indicative of subsurface heat content. A close linear
relationship was observed year round between SST anomalies and heat
content anomalies in the top 30 meters of the ocean. There was little
correlation between SST and heat content anomalies in the 91-122 meter
layer.
TABLE OF CONTENTS
I. INTRODUCTION 11
A. BACKGROUND H
B. OBJECTIVE 12
C. SEA SURFACE TEMPERATURES 13
II. APPROACH 18
A. GENERAL 18
B. DATA SOURCES 18
C. DATA PROCESSING 20
III. OCEANCGRAPHIC CLIMATOLOGY OF THE REGION 23
A. GENERAL 23
B. THE SUBTROPIC REGION 23
C. ANNUAL CYCLE OF TEMPERATURE STRUCTURE 24
IV. ANALYSIS OF RESULTS 25
A. GENERAL 25
B. STATION N (1965-69) 25
C. STATION N (1946-50) 28
D. OTHER STATIONS 29
E. COMPOSITE VIEW OF STRUCTURE ' 30
1. October 1963 30
2. May 1964 30
3. June 1965 31
4. April 1967 31
5. September 1967 31
6. July 1968 31
7. February 1969 32
3
F. VERTICAL SECTIONS 32
G. SUMMARY 33
V. CORRELATION STUDIES 36
VI. CONCLUSIONS 39
VII. RECOMMENDATIONS 41
APPENDIX A: Computer Programs 43
APPENDIX B: Tabulation of Heat Content Values in the Surface
Layer 57
LIST OF REFERENCES 142
INITIAL DISTRIBUTION LIST 145
FORM DD 1473 " ... 147
LIST OF FIGURES
Figure Page
1 Effects of Heat Exchange on Vertical
Temperature structure [after LaFond 1954] . 69
2 Effects of Different Wind Forces on Vertical
Temperature Structure Rafter LaFond 1954] . 69
3 FNWC's 30-day Mean SST Analysis for Janury 1971. 70
4 FNWC's 30-day SST Anomaly for January 1971. 71
5 Sample Charts of SST and SST Anomalies for
November 1968 [after Renner 1968^ . 72
6 Location of Stations Used. 73
7 Drift in the North Pacific. Shaded Rectangle is
Area of Study [after Reid 196l] .
74
8 Oceanographic Climatic Regions of the North
Pacific. Shaded Rectangle is Area of Study
[after Tully 1964] . 75
9 Typical Temperature, Salinity, and Density
Structures in the Subtropic Region Rafter
Tully 1964] . 76
10 Seasonal Types of Vertical Thermal Structure
(Schematic) and Growth and Decay of the
Thermocline at Ocean Station N. 77
11 ' Smoothed Average Annual Temperature Cycles for
Station N (30° N, 140° W) at the Surface, 30,
61, 91, and 122 meters. 78
12 Observed Annual Temperature Variations for
Station U (28° N, 145° W) at the Surface, 30,
61, 91, and 122 meters. 79
13 Observed Annual Temperature Variations for
Station N (30° N, 140° W) at the Surface, 30,
61, 91, and 122 meters. 80
14 Observed Annual Temperature Variations for
Station 4 (33° N, 135° W) at the Surface, 30,
61, 91, and 122 meters. 81
Figure Page
15 Observed Annual Temperature Variations for
Stations 4 (33° N, 135° W) and 16 (33°-23'N,
128°-38' W) at the Surface, 30, 61, 91 and
122 meters. 82
16 Observed Annual Temperature Variations for
Station 16 (33°-23' N, 128°-38' W) at the
Surface, 30, 61, 91, and 122 meters. 83
17 Observed Annual Temperature Variations for
Station 18 (32°-10' N, 132°-47 ' W) at the
Surface, 30, 61, 91, and 122 meters. 84
18 Observed Annaul Temperature Variations for
Station 19 (30°-51' N, 128°-37'W) at the
Surface, 30, 61, 91, and 122 meters. 85
19-22 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station U. The Average Observed SST is
also Plotted. Shaded Areas Indicate
Warmer than Normal Water. 86
23-25 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station N. The Average Observed SST is
also Plotted. Shaded Areas Indicate 90
Warmer than Normal Water.
26-29 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station 4. The Average Observed SST is
also Plotted. Shaded Areas Indicate Warmer
than Normal Water. 93
30-33 ' Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station 18. The Average Observed SST is
also Plotted. Shaded Areas Indicate
Warmer than Normal Water. 97
34-38 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station 16. The Average Observed SST is
also Plotted. Shaded Areas Indicate
Warmer than Normal Water. 101
39-43 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station 19. The Average Observed SST is
also Plotted. Shaded Areas Indicate
Warmer than Normal Water 106
Figure Page
44-45 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Station N. The Average Observed SST is
also Plotted. Shaded Areas Indicate
Warmer than Normal Water. Ill
46 Comparison of Computed Mean Monthly BT for
Specific Years with Long Term Mean for
Stations 4 and U. The Average Observed SST
is also Plotted. Shaded Areas Indicate
Warmer than Normal Water. 113
47 Time Series Plot of Vertical Temperature
Anomalies at Station U with Comparison of
Robinson, NMFS, and Sette SST Anomalies.
The Shaded Areas Indicate Warmer than
Normal Water. 114
48 Time Series Plot of Vertical Temperature
Anomalies at Station N with Comparison of
Robinson, NMFS, and Sette SST Anomalies.
The Shaded Areas Indicate Warmer than
Normal Water. 115
49-50 Time Series Plot of Vertical Temperature
Anomalies at Station 4 with Comparison of
Robinson, NMFS, and Sette SST Anomalies.
The Shaded Areas Indicate Warmer than
Normal Water. 116
51-52 Time Series Plot of Vertical Temperature
Anomalies at Station 18 with Comparison of
Robinson, NMFS, and Sette SST Anomalies.
The Shaded Areas Indicate Warmer than
Normal Water. 118
53-54 Time Series Plot of Vertical Temperature
Anomalies at Station 16 with Comparison of
Robinson, NMFS, and Sette SST Anomalies.
The Shaded Areas Indicate Warmer than
Normal Water. 120
55-56 - Time Series Plot of Vertical Temperature
Anomalies at Station 19 with Comparison of
Robinson, NMFS, and Sette SST Anomalies.
The Shaded Areas Indicate Warmer than
Normal Water. 122
57 Comparison of the Surface Anomaly Chart with
the Associated Subsurface Thermal Structure
for October 1963. Shaded Areas on BT's
Indicates Warmer than Normal Water. 124
Figure Page
58 Comparison of the Surface Anomaly Chart with
the Associated Subsurface Thermal Structure
for May 1964. Shaded Areas on BT's Indicates
Warmer than Normal Water. 125
59 Comparison of the Surface Anomaly Chart with
the Associated Subsurface Thermal Structure
for June 1965. Shaded Areas on BT's Indi-
cates Warmer than Normal Water. 126
60 Comparison of the Surface Anomaly Chart with
the Associated Subsurface Thermal Structure
for April 1967. Shaded Areas on BT's Indi-
cates Warmer than Normal Water. 127
61 Comparison of the Surface Anomaly Chart with the
Associated Subsurface Thermal Structure for
September 1967. Shaded Areas on BT's indicates -
Warmer than Normal Water. 128
62 Comparison of the Surface Anomaly Chart with the
Associated Subsurface Thermal Structure for
July 1968. Shaded Areas on BT's Indicates
Warmer than Normal Water. 129
63 Comparison of the Surface Anomaly Chart with the
Associated Subsurface Thermal Structure for
February 1969. Shaded Areas on BT's indicates
Warmer than Normal Water. 130
64 Vertical Sections of Temperatures (°C) for
February 1969 Comparing Norm to Observed Values
Along Lines as Indicated in Station Plot. 131
65 Vertical Sections of Temperatures (°C) for
September 1969 Comparing Norm to Observed Values
Along Lines as Indicated in Station Plot. 132
66 Plot of Depths to Which the Surface Anomaly
Existed Versus the Percentage of the Total
Observations for all Stations. 133
67. . Plot of the Magnitude of the Surface Anomaly that
Existed to 100M versus the Percentage of the
Total Observations for all Stations. 134
68 Plot of Month of Occurrence for Surface Anomalies
that Existed to 100M versus the Percentage of
the Total Observations for all Stations. 135
69 Plot of the Magnitude of the Surface Anomaly that
Existed to 40M versus the Percentage of the
Total Observations for all Stations. 136
Figure Page
70 Plot of Month of Occurrence for Surface
Anomalies that Existed to 40M versus the
Percentage of the Total Observations for
all Stations. 136
71 Correlation Plot of SST Anomaly versus heat
Content Anomaly at Station N from 0-30M. 137
72 Correlation Plot by Season of SST Anomaly
versus Heat Content Anomaly at Station N
from 0-30M. 138
73 Correlation Plot of SST Anomaly of SST
Anomaly versus Heat Content Anomaly at
Station N from 0-91M. 139
74 Correlation Plot by Season of SST Anomaly
versus Heat Content Anomaly at Station N
from 0-91M. 140
75 Correlation Plot of SST Anomaly versus Heat
Content Anomaly at Station N from 91-122M. 141
ACKNOWLEDGEMENTS
The author wishes to express his sincerest appreciation to Dr. Dale F.
Leipper, my confidant, for his advice and guidance throughout the study.
Appreciation is also due to Professor Noel E. J. Boston for his review
of the thesis and for his constructive comments.
My thanks are extended to all others who have assisted in many ways.
I would like to gratefully acknowledge the assistance of Dr. Tavio
Laevastu, LCDR W. A. Raines, and other personnel of Fleet Numerical
Weather Central in gathering data used in this study.
To my wife, Barbara, I offer my special thanks for her encouragemenc
and cooperation, without which this project would have been impossible
to complete.
10
I. INTRODUCTION
A. BACKGROUND
The connecting links in the ocean-atmosphere system are numerous and
complex. On a large scale the system is analogous to a servomechanism
wherein the ocean absorbs heat energy from the sun which is later fed
back to the atmosphere to modify its wind patterns. The atmosphere in
turn feeds energy back into the ocean to initiate another stage of the
cycle.
On a smaller scale, storm systems may be generated or strengthened
by interaction with the ocean. Numerous authors have attributed the
development of cyclones over the ocean to the heat energy flux received
from the sea jpyke 1965] . Namias |_1968j suggested that warmer than
normal water lying in the path of migratory fronts and cyclones speeds
up their cyclonic growth through the feedback of heat and moisture.
Warm surface water conditions existed in the North Pacific during the
summer-fall season of 1962 and could have been instrumental in causing
the highly abnormal and adverse weather conditions in the Northern
Hemisphere during the winter of 1962-63 J Namias 1963J . Annual precipi-
tation patterns can be subtly affected by the heat distribution in the
ocean and its year to year changes. Although significant correlation
exists between energy feedback from the sea and weather patterns,
Murray and Ratcliffe \ 1969J cautioned that the interactions are generally
complex and that abnormal occurences cannot always be explained
satisfactorily.
11
The majority of the heat energy available for transfer to the
atmosphere is contained in the top 300 to 400 feet of the ocean. This
is usually the greatest depth range to which seasonal changes in tempera-
ture are felt in the ocean for mid- latitude regions. An understanding
of spatial and time variation of the thermal structure in the seasonal
zone is required for an adequate explanation of ocean feedback effects
on the atmosphere. Development of synoptic oceanographic analysis and
weather forecasting requires quantitative knowledge of the amount of
heat energy exchanged between the ocean and the atmosphere JLaevastu
1965J .
Calculations of energy transfer across the air- sea interface are
based on many parameters, one of which is the sea surface temperature
JWyrtki 1965 J . Sea surface temperature is used in energy feedback
computations because it is a critical parameter and is generally the
only synoptic information available on the thermal conditions of the
oceans. Isa.ics J1969J has said that we need to know more than the
surface temperature: "We need to know what is transpiring below the
surface of the sea... so that we can determine such critical matters as
the fluctuations in heat content...". Ideally, synoptic information on
the subsurface temperature structure to the depth of seasonal influence
should be used to provide heat content changes for feedback considera-
tions, but the lack of sufficient observational coverage does not permit
this as yet.
B. OBJECTIVE
Considerable emphasis to date in oceanographic and weather fore-
casting has been placed on sea surface temperature and sea surface
temperature anomalies. The sea surface temperature anomaly is readily
12
available and can provide important information on the thermal energy
content of the ocean. However, a large positive anomaly extending to
100 meters in depth represents a sizable amount of excess heat energy
whereas the same anomaly existing to only 25 meters may not be as
important in feedback considerations. Thus, knowledge of surface
anomalies alone may not be sufficient to determine the potential effect
of the ocean upon the atmosphere.
The object of this thesis is to study subsurface thermal structure
anomalies to a depth of 122 meters (400 feet) and their relationship to
the corresponding sea surface temperature (SST) anomalies at several
locations in the Northeast Pacific Ocean from 1962-70. This will lead
to a better appreciation for the reliability of SST anomalies as an
indicator of the ocean energy levels. Such information might then be
used to supplement the conclusions of Namias and others, that warmer than
normal sea surface temperatures in the North Pacific provide an impetus
for changes in the long-range weather patterns affecting the Northern
Hemisphere.
C. SEA TEMPERATURES
To understand sea temperature anomalies at various depths, the
factors affecting temperature structure through the layers involved must
be considered. The factors that have the most effect on the surface and
subsurface temperature structure may be divided into three groups (1)
heat exchange, (2) mixing, and (3) advection [Wolff, et. al. 1965J .
These three factors interact simultaneously in a non- linear manner to
produce changes in the heat content and its distribution in the surface
layer.
Changes in the thermal structure due to heat exchange across the
air-sea interface result in near surface temperature gradients:
13
negative gradients for heat gained from or through the atmosphere and
generally small positive gradient for heat loss to the atmosphere
ILaFond 1954 J . Heating at the surface is primarily caused by radiation
from the sun and sky and produces negative temperature gradients, some
of which may become large (Figure lb). Conversely, removal of heat from
the surface by: (1) back radiation from the sea surface, (2) sensible
heat transfer to the atmosphere, and (3) evaporation, leads to positive
gradients below the surface which usually remain small because of the
associated convective mixing (Figure la) .
Mixing and advection are described by LaFond J_1962j as being the
vertical and horizontal movements of water and the associated transfers
of heat within the ocean which occur without loss or gain to the
atmosphere. Local changes in the vertical and horizontal temperature
gradients may result if the temperature of the advected water is different
than that of the water it displaced.
Vertical mixing redistributes the heat in the ocean and is primarily
responsible for determining the thermal structure with depth. There
are two types of vertical mixing: (1) convective and (2) mechanical.
Convective mixing will take place where a heat loss at the surface
causes the cooled, denser water at the surface- to sink.
Mechanical mixing is a forced mixing which may result from wave
action produced by the wind. The primary effect of mechanical mixing
is to produce a homogeneous layer with isothermal temperature structure.
The higher the wind force, the greater the depth to which such mixing
will take place (Figure 2).
Horizontal movement of water or advection will often result in the
local temperature of the whole water column being changed in a similar
14
manner. A more complete discussion of all the factors that may affect sea
temperatures is given by LaFond 11954, 1962J .
In discussing the thermal structure characteristics of the ocean
(i.e., SST, mixed layer depth, ect.) the problem of defining the elements
of "normal" structure arises. The normal thermal structure can be
visualized as a climatic entity analogous to some in meteorology, depend-
ent on time series data spanning a period of years; the larger the
period the closer the approach to true climatological normals.
Once the mean thermal structure is known, it is possible to describe
the ocean environment in terms of its variability around these mean
values. In this case the variability can be depicted in terms of
"persistence" and "anomalies".
Persistence is defined as the tendency of a disturbance in a fluid
to continue for a period of time and then gradually die out. By knowing
the persistence factor, it is possible to estimate when the environment
will return to normal after a given time interval.
Anomalies are the departures of the observed state of the fluid in a
given region over a specified time from the normal state for the same
region and time. An anomaly is arrived at by subtracting the given
temperature from the long term mean. Figure J shows the 30 day average
SST analysis for January 1971 and Figure 4 is the SST anomaly analysis
for the same month in 1971 when compared with the corresponding long
term mean as computed by Fleet Numerical Weather Central (FNWC).
A variety of long term mean charts of SST have been generated over
the years for the world's oceans and used for anomaly calculations.
Wolff [1965^ lists over twenty hydrographic and maritime climatologic
15
charts and atlases dating from 1898 to 1961 that are available for the
Pacific Ocean. Some of the more recent publications of monthly mean SST
for the Pacific were produced by Sette _et. .al. 1 1968J and LaViolette
et. al. ll 9 6 9j . Both Sette and LaViolette used bucket temperature and
ship injection temperature reports for their analyses.
The Sette charts include means for each year in the period from 1949
to 1962. The SST data used to compute the monthly means were averaged
over 2 quadrangles of latitude and longitude. Investigators such as
Isaacs £L969j , Namias [1968] , and Laevastu \personal communication^
have used Sette 's means in their computations.
LaViolette used over 6 million SST observations made between 1854
and 1960 in the North Pacific. The SST's were all averaged together by
month in 1 quandrangles. In addition to the charts of long term
monthly means, LaViolette' s work includes charts of monthly maximum and
minimums of SST for the North Pacific.
Another source of monthly mean SST charts for the Northeast Pacific
is the National Marine Fisheries Service (NMFS). This government organi-
zation within NOAA distributes charts of mean SST based on reported
temperatures and computes SST anomalies from the long term mean. The
primary use of this information is for the benefit of commercial fisher-
men in determining prime fishing areas. Typical NMFS sea surface
temperature and anomaly charts are given in Figure 5.
A popular long term mean used by many, including Namias [1969J and
NMFS, is given in an atlas published by the U. S. Naval Oceanographic
Office I 1944J . The atlas means are based on a 40 year period from about
1900 to 1940.
16
Some investigators have calculated their own norms using data from
a particular period of interest. Clark [1967J found it useful to use a
7 year base (1951-1958) for his norm while studying SST fluctuations in
the same period.
The mean SST values already discussed are based on bucket tempera-
tures and merchant ship injection temperature reports. Robinson [un-
publishedj has compiled SST means for the North Pacific using all
available bathythermograph (BT) and Nansen cast data since about 1946.
FNWC is in the process of converting to the Robinson means in their
anomaly computations Laevastu, personal communicationj .
Data to define long term mean temperature structure for the North
Pacific is much less plentiful than data for SST norm values. Muromtsev
Il963 J gives the latitude-mean values of Pacific water temperatures at
standard depths along longitude lines 10 apart. Muromtsev based his
calculations on 11,000 Nansen casts and 6,000 BT's. Panfilova |_1968]
produced similar charts, but used additional data and computed temperature
o
values along longitude lines 1 apart.
By far the most complete and probably the most reliable long term
means of sea temperature in the vertical for the North Pacific are those
compiled by Robinson. Her 20 year data base incorporates over 1.2
million BT's and Nansen casts. Temperature values were arrived at by
o
averaging over 1 quadrangles such that mean values are available for
each whole degree of latitude and longitude for depths of 0, 100, 200,
300, and 400 feet.
17
II. APPROACH
A. GENERAL
Because temperature soundings are generally widely distributed in
time and space and for practicality reasons, the study of SST and re-
lated subsurface temperature structure was limited to several positions
in the Northeast Pacific. The main criteria for selecting a particular
position for examination was the availability of data. Six locations
were selected and are listed in Table I along with the inclusive dates
covered by the data used.
These stations are located on a line between the California coast
and Hawaii as shown in Figure 6. It can be seen that the stations lie
along the well travelled shipping lanes that lead into San Francisco and
Los Angeles, thus providing many opportunities for sea temperature
reports in the vicinity of the selected points.
B. DATA SOURCES
Temperature data at the stations listed in Table I was obtained from
several sources. Leipper J1954J summarized BT data taken by weather
ships in the North Pacific from 1943 to 1952. Data for stations U, 4,
and N were extracted from Leipper' s report.
Scripps Institution of Oceanography was another source of data. They
provided temperature measurements made from moored buoys on stations
16, 18, and 19. Evans, _et. _al. 11968J presents some of the temperature
data collected in graphic and tabular form.
The largest portion of all BT data assembled for all stations was
supplied by FNWC. It was not possible to obtain a sufficient density of
18
TABLE I
STATION POSITIONS AND DATES OF INCLUSIVE DATA USED
Station
Designation
Position
Dates
16
33° 23' N
128° 38' W
10/62 - 3/70
18
32° 10' N
132° 47' W
10/62 - 3/70
19
30° 51' N
128° 37' W
10/62 - 3/70
N
30° 00' N
140° 00' W
7/46 - 6/50
1/65 - 2/70
4
33° 00' N
135° 00' W
7/50 - 6/52
10/62 - 3/70
U
28° 00' N
145° 00' W
7/50 - 6/52
10/62 - 3/70
19
BT's from FNWC by limiting the data to a 10 mile radius around each
point, except for station N. Therefore, it was necessary to expand the
area of interest and accept data within a 3 quadrangle centered upon
each point. Approximately 4600 BT's were finally accumulated in this
manner .
C. DATA PROCESSING
All data from Scripps and FNWC was received on 7-track magnetic
tape. It was necessary to convert the information on the 7-track tape
to a 9-track tape for use on the Naval Postgraduate School IBM 360
computer. Appendix A contains a sample computer program for accomplishing
this purpose.
Initially the plan was to select one BT per day taken at the same
time each day in order to minimize the diurnal effect and possibly that
of internal waves. However, the lack of BT coverage at all stations but
N precluded this. At station N, which is an Ocean Weather Station (OWS),
only the 0600 G.M.T. BT was used. At all other stations, any BT that
fell within the 3° quadrangle was used with no restrictions on the time
of day it was taken.
For each station, all BT's in the same month and year were averaged
to obtain the mean vertical temperature structure to a depth of 122
meters. The limitation imposed by using averaged temperature data in
space and time are described by Holly \ 1968 J . In this regard an assump-
tion is made that the temperature soundings are evenly distributed
throughout the month and the sample area such that the average is repre-
sentative of the temperature structure at the point of interest. In
some cases when only one sounding was available on the temperature
structure for a particular month, it was used anyway and a note made.
20
The mean monthly BT's computed were used to calculate the heat content
or heat excess in the water column for each month of the year.
Heat excess is defined as the difference in heat between the water
sampled and a similar column of water at a temperature of 0 C. 0 C.
is an arbitrary reference temperature and its choice was based only on
previous usage I Pattullo, et. al. 1969 J .
Heat content was computed using the formula
:P
-3
Q = /»C T AZ x 10 (1)
where :
Q = heat content in layer (kcal/cm)
y = average density in layer (gm/cm)
Cn = specific heat at constant pressure of water in
-« -i
layer (cal gm deg )
T = average temperature in layer ( C)
AZ = thickness of layer (cm)
The temperatures used were picked off the mean monthly BT's at the
standard depths, plus the even 100 foot depths to 400 feet (0,10,20,25,
30,50,61,75,91,100, and 122 meters). A linear temperature profile
between depth points was assumed in computing the average temperature
in each layer.
In computing Q from equation (1), the product of J>C is assumed to
-3 -I
equal 1 cal cm deg. This appears to be a valid assumption in view of
the fact .that actual values of />C~ computed by Pattullo [1969J from
Nansen bottle data turned out to be .94 plus or minus a few percent.
Robinson's 20 year means for the vertical temperature profile were
utilized in making the anomaly calculations of temperature and heat
content for each month at intervals of 0, 30, 61, 91, and 122 meters.
21
The computer program used to compute the temperature means,
anomalies, and heat content in the manner discussed above is given in
Appendix A.
22
III. OCEANOGRAPHIC CLIMATOLOGY OF THE REGION
A. GENERAL
The oceanographic mechanisms involved in the formation of the
surface layer in the North Pacific have been discussed in some detail
by Tully Il964j . In order to familiarize the reader with the oceano-
graphic properties of the ocean area under study, a few of the main
topics in that paper are summarized below.
B. THE SUBTROPIC REGION
A region, as defined by Giovando [1965J , is an area of the ocean
characterized by the unique distribution cf one or more oceanographic
properties in the horizontal and/or vertical direction. Figure 7
depicts the major surface circulation as found in the North Pacific,
while Figure 8 shows its oceanographic Regions as defined by Tully
J_1964j . The area of interest is outlined by the rectangle and is seen
to lie in tha Subtropic Region.
The Subtropic Region is the largest of the oceanographic regions.
In the eastern part of the Subtropic gyre the flow is southward and
moves at relative slow speeds (y* 2 mi/day). This means that the surface
waters will be continually changing their properties in adjusting to the
local climate effects enroute.
In the Subtropic Region, evaporation exceeds precipitation year
round. This results in evaporation-driven convection, where the denser
water formed at the surface by evaporation sinks until it reaches an
equilibrium level. Thus, a mixed layer can be formed that will exceed
that produced by simple wind mixing. In the vertical, the salinity
23
distribution reaches a minimum between 200 and 800 meters and the density
structure is largely a function of the temperature (Figure 9).
C. ANNUAL CYCLE OF TEMPERATURE STRUCTURE
The Subtropic Region undergoes a seasonal cycle of heating and
cooling. The cycle features growth and decay of a seasonal thermocline
which underlies a nearly isothermal surface layer (Figure 10) . The
seasonal thermocline develops and is maintained by the interaction of
heating/cooling processes at the sea surface in addition to mechanical
wind mixing. The depth to the top of the thermocline usually varies
between 40 to 60 meters for this area. Depending upon the time of the
o
year, the temperature at the bottom of the thermocline can be from 1 to
8 C less th?n that generally prevailing at the surface.
The season for net heating of the sea in the vicinity of station N
(30 N, 140°W) usually is from mid-April to mid-September. Figure 11 is
a plot of Robinson's long term mean temperatures for N and it shows the
seasonal variation of temperature that occurs at different levels. The
observed annual variation for all six stations using the monthly mean
data are shown in Figures 12 to 18.
Cooling dominates the period from mid-September to mid-April. The
seasonal thermocline is eroded away and sinks to about 150 meters; below
this depth there is a permanent thermocline in the non-seasonal zone.
The primary mixing agent during this period is convective overturn
induced by surface cooling, although wind mixing is surely a factor in
the near-surface layers. The surface layer will therefore become
progressively thicker and will gradually become isothermal throughout.
24
IV. ANALYSIS OF RESULTS
A. GENERAL
Since all six stations lie within the same oceanographic region, the
thermal structure at each was probably affected in similar ways by the
surface processes during any given month. Therefore, in order to avoid
being repetitious, only the thermal structure and changes thereto at
station N will be described in a qualitative sense. Except for some
general inferences, no attempt will be made to explain any heating or
cooling observed in a quantitative manner. Such a study would be a
topic for further research. Any unusual occurrences at the other stations
will be discussed. In the end, all stations will be viewed collectively
as a means of picturing the anomalous conditions that existed under the
surface for this area of the North Pacific.
The results for each station are presented in two forms. First,
Figures 19 through 46 show the mean monthly BT's for single years as
computed from the data, along with the corresponding Robinson long-term
monthly mean temperature structure. Thus, one can see at a glance the
anomalously warm (shaded portions) or cold water layers.
The second series of plots, Figures 47 to 56, depict the anomalies
that existed at various depths versus time in months. This presentation
allows the reader to observe the persistence of various anomalies in
addition to the times and depths of positive or negative anomalies.
B. STATION N (1965-69)
It is readily apparent from Figure 48 that the temperature anomaly
at the surface in many cases is not of the same sign (i.e., positive or
25
negative) throughout the layer. The same figure also compares three SST
anomalies and shows that there is disagreement among them. The Sette
and NMFS anomalies depended upon ship injection temperature reports
which are subject to various errors [_Saur 1963J . Likewise the averages
taken from BT's lead to other difficulties. In addition, differences
could also result from the smoothing techniques used. Such a comparison
points up the variability that can occur in anomalies depending on what
long term mean was used.
Referring to Figures 23, 24, and 25, it can be seen that in January
1965 the surface mixed layer is warmer than normal to 75 meters but has
colder than normal water below the thermocline. By March, mixing
processes have distributed the heat in the upper layer throughout the
column, bringing about isothermal and warmer than normal water conditions.
Apparent cooling at the surface probably resulted in convective overturn
through April 1965 and introduced below normal temperatures in the
layer. It is possible that advection of cooler than normal water into
the region maintained the below normal structure through June. Note how
the SST anomaly from March through August 1965 is representative of the
whole column. Cooling at the surface commenced in September introduces
convective mixing, thus deepening the mixed layer. The surface cooling
was apparently fairly rapid because of the negative anomaly that developed
in the mixed layer from October to December. Below the thermocline, a
region of warmer than normal water is seen to exist.
By January 1966 the whole layer has become isothermal, but slightly
cooler than normal. The fall of 1966 was nearly "normal" except for the
month of September which experienced less than normal warming at the
surface, resulting in a negative anomaly in the mixed layer. In October,
26
the water above the thermocline warmed up either through insolation or
advection of warm water, while conditions below the thermocline remained
nearly constant. Cooling did not start until December and continued
through February 1967. Slightly cooler than normal water was initiated
and these conditions lasted until July 1967. In August 1967 a warm pool
of water is seen in the surface layers, possibly brought about by strong
heating under calm conditions. Figure 24 shows that a sharp negative
thermocline has formed, presenting an extremely stable condition that
inhibits the flow of heat downwards 1 Dietr:.ch 1963 f page 174_\ „ Thus a
situation occurred where the surface temperature indicated anomalously
warm water but at depths below the thermocline (25-50 meters) , colder
than normal water existed. Again in the late fall, cooling at the
surface takes place, leading to convective overturn and this combined
with probable mechanical wind mixing, deepens the isothermal mixed layer.
The warmer than normal conditions of 1967 plus possible advection of
warm water has helped to retard the normal rate at which the water is
usually cooled, resulting in warmer than normal conditions for January-
February 1968. By March, the water has returned to a near normal state
and remains so through May 1968. Commencing in June 1968 a sharp
thermocline appears at about 40 meters, once more indicating strong
heating at the surface. Here again a very warm upper layer develops and
the heat is contained in the near surface layers by the presence of the
thermocline. Since in the spring of 1968 the water column was near
normal or slightly warmer than normal, the deeper layers (below 50 m.)
were near normal from June through September 1968. The usual cooling
processes leading to mixing take over in October to erode away the
thermocline. Overall in 1968, station N was characterized by warmer
than normal water above 50 meters.
27
January of 1969 was very much warmer than normal as a result of a
very warm year in 1968. Cold water possibly moved into the region
beginning in February and brought temperatures down to below normal. A
warming trend set in from May through July 1969. Apparently very little
surface heating occurred from August to October and this led to below
normal conditions. Advection of warm water could have been responsible
for warming the surface layers in the fall of 1969.
In summary then, it has been indicated that at station N anomalous
cooling or heating in the spring is primarily accomplished through
advection since the whole water column is affected in the same manner.
Support for this is evidenced in a study by Bathen I1971J , who calcu-
lated that on the average, advection is responsible for 63% of the local
monthly change in heat storage for most of the North Pacific.
If strong heating occurs during the summer months, the SST anomaly
does not appear to be a true indicator of the thermal structure in the
whole water column. The development of a strong thermocline leads to
very stable water conditions, preventing the transport of heat downward.
The water temperatures below the thermocline will depend on what thermal
conditions existed prior to the onset of the rapid surface heating. The
fall months are charcterized by "a leveling out" of the thermal
structure and a general cooling of the column through convective over-
turn and mixing processes.
C. STATION N (1946-50)
Vertical temperature structure for station N from 1946 to 1950 is
shown in Figures 44 and 45. Data for these BT's was extracted from the
report by Leipper j_1954j who compiled temperatures for these years at
28
depths of 0, 100, 200, and 350 feet. As a result, the temperature
structure shown in the BT profiles may not be the true structure since
there was linear interpolation for the intermediate temperature values.
However, valid anomalies do exist at 0, 30, 61, 91, and 106 meters
which correspond to the depths used by Leipper.
It is evident from Figures 44 and 45, chat similar processes affected
the temperature structure at station N during 1946-50 as have been
described for 1965-69.
D. OTHER STATIONS
In general, observations were not as numerous at stations 4, 16, 18.
19, and U as they were at N and therefore the computed means may not
truly represent the average conditions of the month. It can be seen
from the comparison of the SST anomalies at each station (Figures 47 to
56) that the general trends of the Robinson anomaly agrees with the Sette
and NMFS anomalies, but that there are greater differences between these
than there are at station N.
Two years where no data were available from station N, 1963 and
1964, are available for study at these other stations. The principal
features prevailing at many stations during the summer of 1963 was the
fact that the surface layers were cooler than normal for these months.
The year 1964 had a very similar occurrence during the summer with
negative anomalies from the surface to depths varying from 25-75 meters.
In most cases there was warmer than normal water at greater depths.
A feature of some interest in the thermal structure is the appearance
of a sub- thermoc line duct which is related to subsurface anomalies. The
ducts appeared primarily in the summertime at the more northerly
stations (4, 16, 18, 19). Sub-thermocline ducts were very prominent at
29
station 16 from May through August 1964 (Figure 35), with an indication
that they were also present at stations 18 and 19 for the same period
(Figures 30 and 40). This is in agreement with Burrows' |_1968J observa-
tions which showed that although the ducts are characteristic of the
Subarctic Region (See Figure 8), small ducts do occur during the summer
months for this area.
E. COMPOSITE VIEW OF STRUCTURE
In order to tie together the observations made of the average sub-
surface temperature structure at different locations, it is interesting
to look at the surface anomaly chart for the Northeast Pacific that
existed at the same time.
1. October 1963. Figure 57 shows that all of the stations lie in
a positive surface anomaly area. The BT plots associated with
this month all have positive anomalies at the surface. All have
very small or positive anomalies existing over the whole depth
of the water column. Stations 16 and 19 lie in or are adjacent
to the relatively large positive surface anomaly area on the
chart and appear to maintain a constant anomaly with depth.
2. May 1964. In Figure 58 all stations lie in a negative anomaly
region except for 19. From the BT!s it is seen that the negative
anomaly exists to only very shallow depths, with generally
warmer than normal water below 50 meters. A discrepancy at
Station 19 exists between the chart and the BT anomaly at the
surface. The BT structure is probably more correct based on the
fact that its thermal structure is in general agreement with the
other stations nearby and because it is a moored buoy station
with hourly recorded temperatures.
30
3. June 1965. From the SST anomaly chart in Figure 59, one sees
that station U and N lie in a positive anomaly area, station 4
is on the dividing line between negative and positive anomalies,
and that stations 16, 18, and 19 all have negative SST anomalies.
In the BT plot, stations 16 and 18 show very shallow negative
anomaly layers near the surface and warmer than normal water
below 25 meters. For station 19, the negative anomaly exists to
90 meters before changing to a positive anomaly. station U
shows that it is warmer than normal from the surface to 122 meters.
The average BT at station N reveals a slightly negative anomaly
at the surface which is contrary to the SST anomaly chart. It
does not appear to be consistent with the other stations.
4. April 1967. The surface chart in Figure 60 places all stations
in the negative anomaly region except for U which is on the
fringe of a positive anomaly area. The subsurface structure
discloses the fact that the negative anomaly at the surface is
generally found to exist to 100 meters except for station 16.
5. September 1967. A positive SST anomaly now occupies most of the
Northeast Pacific as shown in Figure 61. The average thermal
structure below the surface in this area of positive surface
anomalies reveals a shallow, warmer than normal mixed layer
about 25 meters deep, a sharp thermocline, and generally cooler
than normal water below the thermocline. The structure at
station 16 is based on only one BT and may not portray the true
average structure.
6. July 1968. Another large positive SST anomaly formed in 1968.
Figure 62 depicts the associated subsurface thermal structure
31
that also occurred. The shallow, warm, mixed layer is again
in evidence.
7. February 1969. All of the stations shown in Figure 63 are
situated in a positive anomaly locale. The related BT's for
the month indicate that the warmer than normal water which formed
at the surface in 1968 has now been mixed vertically to pro-
duce a warmer than normal column of water to a depth of 122
meters.
F. VERTICAL SECTIONS
Local temperature anomalies can be thought of as a displacement of
isotherms from their normal positions because of advection. Vertical
temperature sections comparing the observed temperature values with the
norm would reveal the amount of lateral displacement that occurred. Two
contrasting vertical sections representing the coolest and warmest
months are shown in Figures 64 and 65. Section A-A1 is taken through
stations U, N, 18, and 16, while section B-B' is through stations 4, 18,
and 19. Section A-A1 is aligned so that the general surface drift is
nearly perpendicular to it.
Section A-A1 and B-B' made in February (representing the coolest
month) 1969 and depicted in Figure 64 shows that there was a possible
shift in the isotherms to the northeast of about 120 miles.
For September 1969, Figure 65, indicates that above 50 meters the
shift in isotherms was to the southwest, while below 50 meters there may
have been a slight shift to the northeast. The displacement of iso-
therms above 50 meters also seemed to increase as one went westward from
station 16.
32
G. SUMMARY
The above composite views suggest that for this region, an anomaly
at the surface (without regard as to the sign) exists to depths of 100
meters or more during the late fall and early spring months. The depths
of penetration for all observed surface anomalies versus the percentage
of the total observations are plotted in Figure 66. This graph shows a
small peak for negative anomalies at 20-40 meters and large peak at
100-120 meters. The positive anomalies have a broad peak between 40-80
meters in addition to a sharp peak at 100-120 meters. These results
indicate that for about 507> of the time the anomaly at the surface
exists throughout the water column. This outcome called for further
investigation of the anomalies extending throughout the surface layers.
Figure 67 is a breakdown of the magnitudes of the surface anomalies that
existed at times when the anomalies also penetrated to at least 100
meters. There is a hint, from Figure 67, that the magnitude of the
o
positive anomaly was generally less than 1.0 C while the negative
o
anomaly was usually greater than 1.0 C. In addition, more negative than
positive anomalies were observed to extend from the surface to 100
meters. This might well be expected because convective mixing processes
would tend to deepen negative anomalies that appear at the surface. The
number of anomalies whose magnitudes were greater than 1.6°C is not
considered sufficient to indicate any valid conclusions. The distribu-
tion by month of occurrence for surface anomalies that penetrated to
100 meters is shown in Figure 68. The preferred months for the positive
anomalies were January and February, while the negative anomalies
favored March and April. The positive anomalies during the winter
possibly can be explained through persistence mechanisms. The warm
33
anomaly forms at the surface during the summer and if it is large enough
it will persist into the winter gradually becoming deeper with the
increasing depth of the mixed layer.
Figure 21 for station U (1968-1969) is an example of how the positive
anomaly develops at the surface during the summer and eventually works
its way down to the bottom of the layer by February of the following
year.
Negative anomalies penetrating from the surface to 100 meters can be
expected for the months of February, March, and April, because these are
generally the coolest months of the year for this region. Once cooling
at the surface has introduced a negative anomaly, convective mixing will
bring about a net cooling of the deeper layers. If cooling at the
surface continues, then a deep negative temperature anomaly will result.
Graphs showing the distribution of magnitude and month of occurrence
for surface anomalies that existed to 40 maters are given in Figures 69
and 70. Figure 69 shows a sharp cut-off in the number of surface
o
anomalies whose magnitudes are larger than 1.5 C, whereas anomalies that
extend to 100 meters have a cut-off at values greater than 2.0 C.
(Figure 67).
Negative anomalies to 40 meters were most common during the month of
August as depicted in Figure 70. A possible explanation for this is
that during the summer season positive anomalies are usually shallow
features that can be easily wiped out by cooling at the surface and
result in negative anomalies.
Figure 70 shows that positive anomalies existing to 40 meters occurred
primarily during July and November. The high number of occurrences in
34
November is the result of a deepening of the mixed layer during the fall
months of the year. It was previously noted that positive anomalies to
100 meters favored the months of January and February, therefore
anomalies to some intermediate depth between 40 and 100 meters must be
prevalent during December.
35
V. CORRELATION STUDIES
The relationship between the SST anomaly and the heat content
anomaly in layers of various thicknesses was evaluated first on an
annual and then on a seasonal basis. The year was divided into three
seasons for the seasonal correlation study. The choice of seasons was
based upon the seasonal variation of temperature displayed in the upper
122 meters (see Figure 11).
The average linear correlation coefficients obtained for all six
stations is given in Table II. The coefficients in Table II indicate
that there is an almost linear relationship between the SST and heat
content anomalies in the top 30 meters for this particular area of the
North Pacific. There is a decrease in correlation values as the layer
thickness increases. The seasonal coefficients for the heating season
are lower than those for other times of the year. This is evidence that,
in general, only shallow mixed layers (less than 30 m) are formed from
May to August. Very little linear correlation exists between the SST
and heat content anomalies in the bottom most layer of 91-122 meters.
Some typical correlation plots for station N, Figures 71 to 75, portray
some of the observations made above.
An attempt was made to improve the correlation coefficients between
SST and heat content anomalies in the layers of 30-61, 61-91, and 91-122
meters by applying lags of 1, 2, or 3 months. For the 30-61 meter
layer, there was no improvement in the coefficients for lags from 1 to
3 months, indicating possible relationships of less than one month's
36
lag. Correlations with applied lags in the other two layers were not
very conclusive, however, the best correlations were obtained with 3
months lag.
37
TABLE II
CORRELATION COEFFICIENTS BETWEEN SST ANOMALY
AND THE HEAT CONTENT ANOMALY IN THE LAYER
a. Annual
Depth Interval (m)
0-30
0-61
0-91
0-122
30-61
61-91
91-122
Correlation
Coeff .
,98
.91
.84
.79
.77
.63
.54
b. Seasonal
Depth Interval (m)
0-30
0-61
0-91
0-122
30-61
61-91
91-122
Season
.99
.98
.95
.91
.96
.85
.67
Jan-Apr
May -Aug
.94
.83
.76
.71
.63
.55
.54
Sep-Dec
.99
.92
.81
.71
.73
.44
.34
38
VI. CONCLUSIONS
This study was involved with the description of subsurface tempera-
ture anomalies and the associated SST anomalies for a restricted area of
the Subtropical Northeast Pacific.
The results of this research show that:
1. Positive SST anomalies that formed during the heating season
generally penetrated to less than 30 meters. This may be related
to the action of a stronger seasonal thermocline in preventing
transfer of heat downward.
2. Negative SST anomalies that occurred in the heating season usually
existed only in shallow depths (10-20 m) .
3. SST anomalies observed during the months of December through April
were usually indicative of thermal conditions to at least 80-100
meters.
a) About 507o of all the positive SST anomalies observed extended
to 100 meters. The majority of these "deep" anomalies were
found to occur in the months of December, January, and February,
It is suggested that once a large positive SST anomaly is
established in the early fall months, the mixing processes
help to distribute the excess heat vertically to at least 100
. meters to form a warmer than normal mixed layer. This
anomalously positive layer then may persist through February.
b) The majority of the negative SST anomalies observed that
existed throughout the surface layer, occurred during the
months of March and April. Since these are the coolest months
39
of the year for this region, any negative anomaly formed at
the surface would soon be felt to 100-120 meters through the
action of connective mixing.
4. A very close linear relationship between SST anomaly and heat
content anomaly was observed year round for the top 30 meters of
the ocean.
5. The linear correlation coefficient decreased as the layer thickness
from the surface increased.
6. The seasonal correlation between SST anomaly and heat content
anomaly was always the lowest during the heating season (May-
August) . Significant drop off in the coefficient value occurred
in this season if the layer thickness increased beyond the 0-30
meter level.
7. Little linear correlation was observed between the SST and the
heat content anomalies in the 91-122 meter layer. There was some
indication that the correlation could be improved for this layer
if a 3 month lag time was applied. Non-linear relationships
between the SST and heat content anomalies below 100 meters may
exist because of possible non-seasonal fluctuations in heat
content.
40
VII. RECOMMENDATIONS
Recent studies suggest that the North Pacific is a highly influential
factor in controlling the development of this nation's winter weather
patterns. A greater understanding of the air-sea interation relation-
ships in this ocean area could aid in developing more reliable long-
range weather predictions.
It is recommended that a study of the type just completed, be con-
ducted over a larger area of the Northeast Pacific with a reasonable
grid network superimposed for sampling points. An interesting period
that might be considered for observation is from 1967 through 1970.
This four year period includes contrasting sea surface temperature
anomalies in the Northeast Pacific as well as contrasting weather types
on the east and west coasts of the U. S. that might be related.
There are numerous avenues available for research in this type of
study once the subsurface thermal structure has been reconstructed.
Some of the research possibilities are:
1) Develop the heat budget for the region; determining the quantity
of heat advected into and out of the region in addition to the
heat exchange across the air-sea interface on a monthly, seasonal,
and yearly basis.
2) Attempt to relate the heat exchange values to any major storm
systems that may have crossed the region to see if the heat flux
from the ocean could have played an important role in intensifying
them.
41
3) Test presently developed empirical relationships between the
atmosphere, sea surface, and subsurface parameters to check their
validity and areas for possible improvement.
In the end, perhaps a better comprehension of how the North Pacific
Ocean affects this continent's weather will result.
42
APPENDIX A
Computer Programs
7-TRACK TO 9-TRACK TAPE CONVERSION PROGRAM
THIS PROGRAM WILL CONVERT DATA WRITTEN ON THREE 7-TRACK
MAGNETIC TAPES ONTO ONE 9-TRACK TAPE. THE FIRST RECORD ON
THE 9-TRACK TAPE IS PRINTED OUT AS A CHECK THAT THE
CONVERSION WAS CARRIED OUT PROPERLY.
FOR FURTHER INFORMATION ON MAGNETIC TAPE CONVERSION AND
PROCESSING AT THE NAVAL POSTGRADUATE SCHOOL SEE:
RANEY, S.D., "PROCEDURE FOR CONVERTING 7-TRACK
MAGNETIC TAPE TO 9-TRACK MAGNETIC TAPE", NPGS TECH.
NOTE NO. 0211-08, JUNE, 1970.
//NAME, ECT. JOB CARD
//CCNVERT EXEC FORTCLG , TI ME .G0=1 2
DIMENSION INDATAOO)
REWIND 4
J = 0
NT=2
32 REWIND NT
31 J = J + 1
200 READ(NT,3,END=40,ERR=50) INDATA
3 F0RMAT(30A4)
90 WRITE(4,3) INDATA
GO TO 31
50 WRITE(6,51) J
51 FORMAT( • 0« ,5X, 'READ ERROR, RECORD NO. =«,I8)
GO TO 31
40 WRITE(6,44) J
44 FORMAT (»0S5Xf "END OF TAPE, RECORD NO. =,,I8)
END FILE 4
REWIND 4
DO 100 K=l,2
READ(4,3) INDATA
WRITE(6,3) (INDATA(I), 1=1,30)
ICO CONTINUE
STOP
END
//G0.FTC2FOO1 DD U NIT=2400-1 , VOLUME=SER=( BELA 1 , BELA2 ,
// BEL A3) ,LABEL=( ,NL) , D ISP=OLD, DCB=( DEN= 1 , RECFM = F ,
// BLKSIZE=120,TRTCH=ET)
//G0.FTC4F001 DD UN IT=2400 , V0L=SER=NPS261 , LABEL= ( , SL ) ,
// DSNAME = BELAND,DISP=(NEW,KEEP) ,DCB=(DEN=2,
// RECFM=FB,LRECL=120,BLKSIZE=120)
43
TAPE EXTRACT PROGRAM
THIS PROGRAM WILL EXTRACT UP TO 350 BT ■ S FROM 9-TRACK
MAGNETIC TAPE AND PUNCH OUT THE TEMPERATURE VALUES ON CARDS
WITH DATE, LATITUDE, LONGI TUDE, AND TIME. BT AND NANSEN CAST
DATA ON THE TAPE IS WRITTEN IN THE STANDARO FNWC FORMAT AND
CONTAINS TWO FILES OF DATA. IF ADDITIONAL BT'S ARE ON THE
TAPE AND HAVE NOT BEEN SEARCHED BECAUSE THE MAXIMUM LIMIT OF
350 HAS BEEN REACHED, THEN RERUN THE PROGRAM INSERTING THE
PROPER IF STATEMENT AS SHOWN BELOW IN THE PROGRAM
DEFINITION OF PARAMETERS USED
INDATA
ISST =
ID, IT
TAPE
D,T =
Z = ST
INTERP
KK1,KK
AREA T
3100 W
ITAG3
MAX OF
TEMP =
= LAT, LONG, DATE, TIME
BT SEA SURFACE TEMP IN DEG F
= BT DEPTHS IN FEET AND BT TEMP IN DEG F AS READ OFF
CONVERTED DEPTH TO METERS AND TEMP TO DEG C
ANDARD DEPTHS(ll) FOR WHICH DATA WILL BE LINEARLY
OLATED FOR
2,KK3,KK4 = LATITUDE AND LONGITUDE COORDINATES OF
0 BE SEARCHED. FOR EXAMPLE, 31 DEG OO'N IS WRITTEN AS
HILE 127 DEG OO'W BECOMES 1270
= MONTH AND YEAR FOR SEARCH TO BEGIN ON RERUN AFTER
350 BT'S WAS REACHED ON FIRST RUN.
INTERPOLATED TEMPERATURE VALUES IN DEG C.
//NAME (JOB CARD)
//PROCESS EXEC FORTCLG P, REGION. G0=200K , TI ME . G0=3
//FORT.SYSIN DD *
DIMENSION INDATA (6, 350) , I SST ( 3 50 ) , I D( 24 , 350 ) ,
SIT (24, 3 50) ,D(2 4,350 ),T(24,350) ,SST( 350) ,Z( 11) ,
$DUMMY(80)
CCMMON TEMP (11, 350)
DATA ITAGl/'A «/,ITAG2/,C ' / , KK 1/ ' 3 100 « / ,
$KK2/,350C'/,KK3/,1270,/,KK4/, 1300'/, I T AG3/ ■ 096 8' /
DEPTHS
FOR
IN METERS AT WHICH TEMPERATURES WILL BE INTERPOLATED
DATA Z/0. 0,10. 0,20
$100.0, 122.0/
J = 0
N = 0
NR = 1
NK=1
REWIND 4
ICO IFU.EQ.351) GO TO 551
CALL REREAD
READ(4,500,END=551
500 F0RMAT(8X,A1,2X,A4
IF( IDENT.EQ. ITAG1)
IF( IDENT.EQ.IT AG2)
IF( LAT.LT.KK1) GO
0,25.0,30.0,50.0,61.0,75.0,91.0,
) IDENT
,2X,A4,
GO TO
GO TO
TO 101
, IDATE, LAT, LONG, ITIME
1X,A4,2X,A4)
101
101
IF(LAT.GT.KK2) GO TO 101
IF(LCNG.LT.KK3 ) GO TO 101
IF(L0NG.GT.KK4) GO TO 101
BT'S ARE- IN CHRONOLOGICAL ORDER ON TAPE. THEREFORE, IF
SECOND RUN IS NEEDED TO COMPLETE SEARCH, SIMPLY INSERT
FOLLOWING IF STATEMENT WITH MONTH AND YEAR OF LAST BT
EXTRACTED FRCM PRIOR RUN.
THE
******IF( IDATE.LT. ITAG3) GO TO 101********
102 J=J+1
READ(99,10) (INDATA( I, J) , 1=1,6), ISST(J),
$(ID( I , J) ,IT( I, J) , 1=1,6)
10 FORM AT (9X, 16, 2X, 212, IX, 12, 13, IX, 14, 9X, 13, 6( IX, 12, 13))
IF(J.EQ.l) GO TO 20
IF( INDATA(6, J) .NE. INDATA(6, J-l) ) GO TO 20
44
IF(INDATA( 1, J) .NE. INDATA ( 1 , J- 1 ) ) GO TO 20
NR=NR+1
NK=NK+1
IFCNK.GE.5) GO TO 100
GO TO 21
20 N=N+1
ISST(N)=ISST( J)
DO 11 1=1,6
INDATA( I,N)=INDATA( I ,J)
ID( I,N) = ID( I, J )
IT( I,N) = IT( I, J )
11 CONTINUE
GO TO 90
21 IF(NR.EQ.3) GO TO 13
IF(NR.EQ.4J GO TO 15
K = 7
DO 12 1=1,6
ID(K,N) = ID( I, J )
IT(K,N) = IT( I, J )
K = K+1
12 CONTINUE
GO TO 100
13 K=13
DO 14 1=1,6
ID(K,N) = ID( I ,J )
IT(K,N) = IT( I, J )
K=K+1
14 CONTINUE
GO TO 100
15 K=19
DO 16 1=1,6
ID(K,N)=ID( I ,J )
IT(K,N)=IT( I, J )
K = K+1
16 CONTINUE
GO TO 100
101 READ(99,550) DUMMY
550 F0RMAT(80A1)
GO TO 100
90 NK=1
NR=1
GO TO 100
THIS LOOP CONVERTS FEET TO METERS AND DEG F TO DEG C.
551 DO 30 J=1,N
DO 31 1=1,24
D( I, J)=3. 048*1 D( I , J)
T(I,J)=(5.0/9.0)*((0.1*IT(I,J))-32.0)
31 CONTINUE
SST(J)=(5.0/9.0)*((0.1*ISST(J) )-32.0)
30 CONTINUE
CALL TINPOL(D,Z,T,SST,N)
WRITE(6,70) ((TEMP(I,J), I =1 , 1 1 ) , ( INDATA ( I , J ) , 1=1,61,
$J=1,N)
WRITE(7,71) ((TEMP(I,J), 1 = 1,11), ( I NDAT A ( I , J ) , 1 = 1,6)
$, J=1,N)
70 F0RMAT(1X,11F5.1,1X,I6,3X,2I2,1X,I2,I3,1X,I4)
71 FORMAT ( 11F5.1,1X,I6,3X,2I2,1X,I2,I3,1X,I4)
STOP
END
THIS SUBROUTINE TAKES 'NR« BT'S AND INTERPOLATES FOR TEMPS
AT THE STANDARD DEPTHS.
SUBROUTINE T IN POL ( DEP , ZZ ,TT, SST , NR )
DIMENSION DEP(24,NR ),ZZ( 11 ),TT(24,NR) ,SST(NR)
COMMON TEMPdl ,350)
DO 10 J=1,NR
L=l
DO 20 1=1, 11
45
40
30
32
21
33
31
20
10
THE F0
AS SER
THE LA
(2rSL)
//GG.F
//
//
//GO.S
IF( I .E0.1J GO TO 21
IF(DEP(L,J)-ZZ( I ) ) 30,31,32
L = L+1
IF(L.EQ.25) GO TO 10
GO TO 40
IF(L.EQ.l) GO TO 33
DIFF=DEP(L, J)-DEP(L-1, J)
DIFF1=ZZ(I )-DEP(L-l,J)
PER=DIFF1/DIFF
DIFFT=TT(L, J)-TT(L-1,J)
FACT=PER*DIFFT
TEMP( I , J) = TT(L-1,J )+FACT
GO TO 20
TEMP( I , J)=SST( J)
GO TO 20
PER=ZZ( I )/DEP(L, J)
DIFFT=TT(L,J)-SST( J)
FACT=PER*DIFFT
TEMPd , J) = SST( J) +FACT
GO TO 2 0
TEMPI I , J)=TT(L,J)
GO TO 20
CONTINUE
CONTINUE
RETURN
END
LLOWING JCL CARDS IDENTIFY THE TAPE BEING SEARCHED
IAL NO. NPS261 . THE FILE NUMBER 1 IS INDICATED IN
BEL PARAMETER AS (,SL); FILE NO. 2 WOULD BE CODED AS
TC4F001 DO UNIT=2400,V0L=SER=NPS261,LABEL=( ,SL) ,
DSNAME=BELAND,DISP=0LD,DCB=(DEN=2,RECFM=FB,
LRECL=120, BLKSIZE=120
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HEAT
LOSS
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b.
FIGURE 1. EFFECTS OF HEAT EXCHANGE ON VERTICAL TEMPERATURE
STRUCTURE [after La Fond 1954].
WIND FORCE 0
WIND FORCE 3
WIND FORCE 6
SURFAC E
HEATING
MIXING
WIND FORCE 0
WIND FORCE 3
SURFACE
HEATING
REMIXING
FIGURE 2. EFFECTS OF DIFFERENT WIND FORCES ON VERTICAL TEMPERATURE
STRUCTURE [after La Fond 1954].
69
FIGURE 3. FNWC'S 30-DAY MEAN SST ANALYSIS FOR JANUARY 1971.
70
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" FIGURE 4. FNWC'S 30 -DAY SST ANOMALY FOR JANUARY 19 71
71
FIGURE 5. SAMPLE CHARTS OF SST AND SST ANOMALIES FOR
NOVEMBER 1968 [after Renner 1968].
72
73
74
75
TEMPERATURE (°C)
SALINITY ( %o)
DENSITY (gm/cm*)
13 15 17
19 21 23 25
34.0 35.0 36.0
1.024 1.025 1.026
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FIGURE 9. TYPICAL TEMPERATURE, SALINITY, AND DENSITY STRUCTURES
IN THE SUBTROPIC REGION [after Tully 1964].
76
WINTER
SPRING
EARLY
SUMMER
LATE
SUMMER
AUTUMN
SEASONAL CYCLE
19 20 21 22 23 18 C 19 20 21 22 23
J U_i l__J I L
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FIGURE 10. SEASONAL TYPES OF VERTICAL THERMAL STRUCTURE (SCHEMATIC)
AND GROWTH AND DECAY OF THE THERMOCLINE AT OCEAN STATION N,
77
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FIGURE 11. SMOOTHED AVERAGE ANNUAL TEMPERATURE CYCLES FOR
STATION N (30°N,140°W) AT THE SURFACE, 30, 61,
91, and 122 METERS.
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OCTOBER 1-31 , 1963
ocv.«'ic« or wi su»f«ct Tt»» m
"O" LOW rOM KU B.TCHfo
MCtl COLOCft IN i»«s
FIGURE 57
COMPARISON OF SURFACE ANOMALY CHART WITH THL ASSOCIATED
SUBSURFACE THERMAL STRUCTURE FOR OCTOBER 1963. SHADED
AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.
124
MAY I- 31 . 1964
DEVIATION Of SEA SURFACE TEMP IT)
FROM lOKG Tt»«i MEAN BATCHED
AREAS COLDER N 964
%jhjk. (after Renner 1964)
• ' V V
125
FIGURE 58. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED
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AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.
125
•A-
JUNE 1-30, 1965
DEVIATION OF SEA SUBFACE TEMP PF1
' »0M LONG Tf«M gtas MATCHED
»»l«S COLDCK IN I9«3
'-VQl^ \ "^"C (after Renncr 1965)
125J
FIGURE 59. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED
SUBSURFACE THERMAL STRUCTURE FOR JUNE 1965. SHADED
AREAS ON BT*s INDICATES WARMER THAN NORMAL WATER.
126
^J&y~-k^
APRIL 1-30. 1967
0Evi»TiON Of 5E« Su»f»CE TEMP If )
FROM LONG TEOM UE1M HATCHED
»«E»S COlOtO IN IM7
t(after Rentier 1967)
Tlfc> •
125
FIGURE 60. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED
SUBSURFACE THERMAL STRUCTURE FOR APRIL 1967. SHADED
AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.
12 7
SEPTEMBER 1-30, 1967
DEVIATION Or SEA SURFACE TEMP (*F I
FROM LONG TEAM UEAN HATCHED
AREAS COLDER IN 1967
\ \ \%
l.-A-^XlV-iafter Renner 1967)
3s tc^^S^^
125 J <*
FIGURE 61. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED
SUBSURFACE THERMAL STRUCTURE FOR SEPTEMBER 1967. SHADED
AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.
128
JULY 1-31, 1968
ocvution of se» surface temp rr
FROM LONG TERM MEAN M4TCME0
»R£»S COLOER IN !»»•
'vSf-^ (after Renner 1968)
12sJ ^
FIGURE- 62. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED
SUBSURFACE THERMAL STRUCTURE FOR JULY 1968. SHADED
AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.
129
125J
FIGURE 63. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED
SUBSURFACE THERMAL STRUCTURE FOR FEBRUARY 1969. SHADED
AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.
130
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. x X- Pos. Anomaly
0-10 10-20 20-40 40-60
Depth (m)
60-80 80-100 100-120
FIGURE 66. PLOT OF DEPTHS TO WHICH THE SURFACE ANOMALY
EXISTED VERSUS THE PERCENTAGE OF THE TOTAL
OBSERVATIONS FOR ALL STATIONS.
133
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135
FIGURE 69.
PLOT OF THE MAGNITUDE OF THE
SURFACE ANOMALY THAT EXISTED
40M VERSUS THE PERCENTAGE OF THE
TOTAL OBSERVATIONS FOR ALL
STATIONS.
0-5 .51-1.0 1.1-1.5 1.6-2.0 2.1-2.5 2.6-3.0 >3.0
Magnitude of Anomaly
-o — o
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Neg . Anomaly
Pos. Anomaly
FIGURE 70. PLOT OF MONTH OF OCCURRENCE FOR SURFACE ANOMALIES
THAT EXISTED TO 40M VERSUS THE PERCENTAGE OF THE
430 TOTAL OBSERVATIONS FOR ALL STATIONS.
M
M J J A
Month of Occurrence
136
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SST Anomaly (°C)
Y = .06 + 2.86X
R = .97
6^
FIGURE 71. CORRELATION PLOT OF SST ANOMALY VERSUS HEAT CONTENT
ANOMALY AT STATION N FROM 0-30M. (R=C0RR. COEF.)
137
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JAN-APR (+)
Y = .05 + 2.98X
R = 1.00
MAY-AUG (p)
Y = .14 + 2.70X
R = .93
SEP-DEC (a)
Y = .05 + 2.92X
R = 1.00
FIGURE 72. CORRELATION PLOT BY SEASON OF SST ANOMALY VERSUS HEAT
CONTENT ANOMALY AT STATION N FROM 0-30M. (R = CORR. COEF.)
138
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+
104
.151
+
+
*
+
4-
+
y
+
+
-4
s
+
+
+
+
4 -;t h 4
.5 T 1.0 1.5
SST Anomaly (°C)
Y - 0.0 + 5.95X
R - .82
+
FIGURE 73. CORRELATION PLOT OF SST ANOMALY VERSUS HEAT CONTENT
-ANOMALY AT STATION N FROM 0-91M. (R=C0RR. CORF.)
139
w « 3q4
c o
a
o ^
C_> rH
CO
*J B
rt O
K <
20
T
10+
■*4
-3
-2
-a
A'
i
+
1
x
-10^-
-20
—At 1 "
1 2
SST Anomaly (°C)
1 . JAN- APR (+)
Y - .47 + 9.02X
R - .99
2 . MAY- AUG (a)
Y - -.22 + 4.32X
R * .64
3. SEP-DEC (a)
Y - .09 + 4.91X
I -■ .83
301
FIGURE 74. CORRELATION PLOT BY SEASON OF SST ANOMALY VERSUS HEAT
CONTENT ANOMALY AT STATION N FROM 0-91M. (R=C0RR. COEF.)
140
6-
c o
<D ^!
c
o >-,
CJ .H
CO
*-> &L
ctj O'
<U C
33 <
4-
I — \~
f
-1.5
10
+
+
+
-±-
f
f
\
+ --5
2t
; f-
f i +
t
*-+
2 +
f
f
t
f f
"f f h
.5 1.0
SST Anonaly ( C)
4-
+
1.5
•4i
Y
R
-.07 + .95X
40
-6-
FIGURE 75. CORRELATION PLOT OF SST ANOMALY VERSUS HEAT CONTENT
ANOMALY AT STATION N FROM 91-I22M. (R=CORR. COEF.)
141
LIST OF REFERENCES
Bathen, K. H. , "Heat Storage and Advection in the North Pacific Ocean-,"
J. Geo. Res, , v. 76, no. 3, p. 676-687, January, 1971.
Burrows, J. B., The Sub -Thermoc line Duct, Master's Thesis, U. S. Naval
Postgraduate School, 61 pp., December, 1968.
Clark, N. E., Report on an Investigation of Large-Scale Heat Transfer
Processes and Fluctuations of Sea-Surface Temperature in the North
Pacific, Ph.D. Thesis, MIT, 148 pp., May, 1967.
Dietrich, G. , General Oceanography, Wiley, 1963, 588 pp.
Evans, M. W. , Schwartzlose, R. A., and Isaacs, J. D. , "Data From Moored
Instrument stations," Scripps Inst, of Ocean., SIO Ref. 68-17,
June, 1968.
Giovando, L. F. and Robinson, M. K. , "Characteristics of the Surface
Layer in the Northeast Pacific Ocean," Fish. Res. Bd. Canada Rept.
No. 205, v. 21, no. 5, 1965.
Holly, R. W. , Temperature and Density Structure of Water Along the
California Coast, Master's Thesis, U. S. Naval Postgraduate School,
204 pp., December, 1968.
Isaacs, J. D., "The North Pacific Study," J. of Hydronoautics, v. 3, no. 2,
p. 65-72, April, 1969.
Laevastu, T. , "Synoptic Scale Heat Exchange and Its Relation to Weather,"
FNWC Tech. Note No. 7, February, 1965.
La Fond, E. C, "Factors Affecting Vertical Temperature Gradients in the
Upper Layers of the Sea," Sci. Monthly, v. 78, p. 243-253, April, 1954.
LaViolette, P. E. and Seim, S. E. , Monthly Charts of Mean, Minimum, and
Maximum Sea Surface Temperature of the North Pacific Ocean, U. S. Naval
Oceanographic Office, 1969.
Leipper, D. F. , "Summary of North Pacific Weather Station Bathythermo-
graph Data, 1943-1952," Navy Dept. Tech. Rept. No. 7, January, 1954.
Muromtsev, A. M. , Atlas of Temperature, Salinity and Density of Water in
the Pacific Ocean, Academy of Sciences USSR, Moscow, 1963.
Murray, R. and Ratcliffe, R. A. S., "The Summer Weather of 1968: Related
Atmospheric Circulation and Sea Temperature Patterns," Met. Mag. , v. 98,
p. 201-219, 1968.
142
Namias, J., "Large-Scale Air-Sea Interactions Over the North Pacific From
Summer 1962 Through the Subsequent Winter," J, Geo. Res. , v. 68,
no. 21, p. 6171-6186, November, 1963.
Namias, J., "Long-Range Forecasting of the Atmosphere and Its Oceanic
Boundary - An Interdisciplinary Problem" Calif. Mar. Res. Comm. ,
CalCOFI Rept., v. 12, p. 29-42, January, 1968.
Namias, J., "Seasonal Interactions Between the North Pacific Ocean and
the Atmosphere During the 1960's," Mon. Wea. Rev. , v. 97, no. 3,
p. 173-192, March, 1969.
Panfilova, S. G., "Latitude-Mean Values of Water Temperature and Salinity
in the Pacific," Okeanologiga, v. 8, no. 5, p. 60-63, 1968.
Pattullo, J. G. , Burt, W. V., and Kulm, S. A., "Oceanic Heat Content Off
Oregon: Its Variations and Their Causes," Limn, and Ocean., v. 14,
no. 2, p. 297-287, March, 1969.
Pyke, C. B. , "On the Role of Air-Sea Interaction in the Development of
Cyclones," Bull. Am. Met. Soc, v. 46, no. 1, p. 41-15, January, 1965.
Reid, J. L. , "On the Geostrophic Flow at the Surface of the Pacific Ocean
with Respect to the 1000 Decibar Surface." Tellus, v. 13, no. 4,
p. 490-502, 1961.
Renner, J. A., "Sea Surface Temperature Charts, Eastern Pacific Ocean,"
California Fishery Market News Monthly Summary, U. S. Dept. of Commerce,
National Marine Fisheries Service, Fishery-Oceanography Center,
La Jolla, Calif., 1963-1969.
Robinson, M. K. , "Long-Term Mean Sea Temperatures at the Surface, 100,
200, 300, and 400 Feet for the North Pacific," (Unpublished).
Saur, J. F. T. , "A Study of the Quality of Sea Water Temperatures Reported
in Logs of Ship's Weather Observations," J. Appl. Meteorol., v. 2, no. 3,
p. 417-425, 1963.
Sette, 0. E. , Eber, L. E. , and Saur, J. F. T. ,. Monthly Mean Charts Sea
Surface Temperature North Pacific Ocean 1949-62, U. S. Dept. of Commerce,
National Marine Fisheries Service, Circ. 258, June, 1968.
Tully, J. P., "Oceanographic Regions and Assessment of Temperature
Structure in the Seasonal Zone of the North Pacific Ocean," J. Fish. Res.
Bd. Canada, v. 14, no. 2, p. 279-287, 1964.
U. S. Naval Oceanographic Office, World Atlas of Sea Surface Temperatures,
H. 0. Pub. No. 225, Washington, D. C. 1944.
Wolffe, P. M., Carstensen, L. P., and Laevastu, T. , "Analysis and Fore-
casting of Sea-Surface Temperature (SST)," FNWC Tech. Note No. 8,
February 1965.
143
Wyrtki, K. "The Average Heat Balance of the North Pacific Ocean and Its
Relation to Ocean Circulation," J. Geo. Res. , v. 70, no. 18, p. 4547-
4559, September 1965.
144
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Security Classification
DOCUMENT CONTROL DATA -R&D
[Security classification ol title, bodv of abstract and indexing annotation nust be entered when the overall report is classified)
Originating activity ( Corpora te auth or)
Naval Postgraduate School
Monterey, California 93940
2«. REPORT SECURITY CLASSIFICATION
Unclassified
26. GROUP
REPOR T TITLE
Sea Surface and Related Subsurface Temperature Anomalies at Several Positions in
the Northeast Pacific Ocean
I DESCRIPTIVE NOTES (Type ol report and, inclusive dates)
Master's Thesis (March 1971)
> iUTMORcSi (FifSI nam«, middle initial, last name)
Conrad Lucien Beland
REPOR T DATE
March 1971
T. TOTAL NO. OF PAGES
148
76. NO. OF RE FS
30
l«. CONTRACT OR GRANT NO.
6. PROJEC T NO
9a. ORIGINATOR'S REPORT NUMBER(S)
96. OTHE1 REPORT NO(SI (Any other numbers that may be ma signed
this report)
0 DISTRIBUTION STATEMENT
Approved for public release; distribution unlimited.
II SUPPLEMENTARY NOTES
12. SPONSORING MILITARY ACTIVITY
Naval Postgraduate School
Monterey, California 93940
ABSTRACT
Sea surface temperature (SST) anomalies from previous sources have been
related to subsurface temperature anomalies obtained from BT's at six positions
in the Northeast Pacific. In this manner some understanding of the value of SST
anomalies as indicators of ocean energy states is achieved. Results show that
for about 507, of the time, the SST anomaly generally extended to depths of 100
meters or more. November through April were found to be the months most favorable
for the occurrence of these deeply penetrating anomalies. Summertime SST
anomalies were determined to be shallow features of less than 40 meters and were
not indicative of subsurface heat content. A close linear relationship was
observed year round between SST anomalies and heat content anomalies in the top
30 meters of the ocean. There was little correlation between SST and heat
content anomalies in the 91-122 meter layer.
)D
• nov es I *♦ / O
/N OlOt -607-681 1
(PAGE 1)
147
Security Classification
1-31408
Security Classification
key wo R OS
Sea Surface Temperature Anomalies
Subsurface Temperature Anomalies
Heat Content
Northeast Pacific Ocean
DD,fr.M473
LINK C
BACK
/N 0101 -807-682 1
148
Security Classification
A- 3 I 409
C/aylorc/ ^=
SHEIF BINDER
jjj^S Syracuse, N. Y.
„^__ Stockton, Calif.
25700
Be land
Sea surface and
related subsurface^
temperature anomalies
at several posit ions ^
in the Northeast Paci-
fic Ocean.
126360
Be land
Sea surface and
related subsurface
temperature anomalies
at several positions
in the Northeast Paci-
fic Ocean.
thesB358
Sea surface and related subsurface tempe
3 2768 002 12964 5
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