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

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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

YSIN DD *

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HEAT LOSS

HEAT GAIN

a.

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

	<^0l
000	-005	■001
-00H		-OOH

" 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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*- 200 X i-		■SEAS ZONE			\ '
Q. U Q		! i			\
300		1	1	\

FIGURE 9. TYPICAL TEMPERATURE, SALINITY, AND DENSITY STRUCTURES IN THE SUBTROPIC REGION [after Tully 1964].

76

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SEASONAL CYCLE

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J U_i l__J I L

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JAN		NOV		7i
			^SEP-^ ; i i i
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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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-i — i — ( — i — > — i — i — i — i — i — f — i — »- JFMAMJJASONDJ

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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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

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DEVIATION Of SEA SURFACE TEMP IT) FROM lOKG Tt»«i MEAN BATCHED AREAS COLDER N 964

%jhjk. (after Renner 1964)

• ' V V

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FIGURE 58. COMPARISON OF SURFACE ANOMALY CHART WITH THE ASSOCIATED SUBSURFACE THERMAL STRUCTURE FOR MAY 1964. SHADED AREAS ON BT's INDICATES WARMER THAN NORMAL WATER.

125

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DEVIATION OF SEA SUBFACE TEMP PF1 ' »0M LONG Tf«M gtas MATCHED »»l«S COLDCK IN I9«3

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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

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0Evi»TiON Of 5E« Su»f»CE TEMP If ) FROM LONG TEOM UE1M HATCHED »«E»S COlOtO IN IM7

t(after Rentier 1967)

Tlfc> •

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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^^

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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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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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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

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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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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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MAY-AUG (p)

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SEP-DEC (a)

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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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SST Anomaly (°C)

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+

FIGURE 73. CORRELATION PLOT OF SST ANOMALY VERSUS HEAT CONTENT -ANOMALY AT STATION N FROM 0-91M. (R=C0RR. CORF.)

139

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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

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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 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.

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Security Classification

1-31408

Security Classification

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Sea Surface Temperature Anomalies Subsurface Temperature Anomalies Heat Content Northeast Pacific Ocean

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148

Security Classification

A- 3 I 409

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SHEIF BINDER

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Sea surface and related subsurface^ temperature anomalies at several posit ions ^ in the Northeast Paci- fic Ocean.

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Sea surface and related subsurface temperature anomalies at several positions in the Northeast Paci- fic Ocean.

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Sea surface and related subsurface tempe

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