Sea Temperatures Illustrated in Fig

Home , Chatham Sound, Dixon Entrance, Fitz Hugh Sound

CAN 54

FISHERIES RESEARCH BOARD OF CANADA

ANNUAL REPORT

of th<

PACIFIC OCEANOGRAPHIC GROUP

NANAIMO, B.C.

:•

1963 1S2J}

^AN30J964

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December 31, 1963 Restricted

FISHERIES RESEARCH BOARD OF CANADA

ANNUAL REPORT

of the

PACIFIC OCEANOGRAPHIC GROUP

NANAIMO, B.C.

1963

December 31, 1963 CONTENTS

Pages

Annual Report, 1963 1- 4

Sea Operations 5

Cooperations and Liaisons 6- 8

Technical Services 8- 9

Staff List 9-10

Publications, Manuscript Reports and Special Reports 11-14

Summary Reports of Research Projects 15-71

North Pacific Ocean 17-42

Coastal Waters 43-67

Special or Support Projects 68-71

Restricted

This is a private document. It may not be quoted as a scientific reference. Further information or reference material may be obtained from the publications listed on pages 11-14, or by correspondence with:

Oceanographer in Charge Fisheries Research Board of Canada Pacific Oceanographic Group Nanaimo, B. C.

December 31, 1963 Figure 1.

y FISHERIES RESEARCH BOARD OF CANADA PACIFIC OCEANOGRAPHIC GROUP

ANNUAL REPORT, 1963

The Pacific Oceanographic Group is a section of the Biological Station, Nanaimo, B.C., of the Fisheries Research Board of Canada. Under this direction and in cooperation with the Canadian Committee on Oceanography, the Group carries out research and coordinates all possible resources to fulfill the national requirements for oceanography in the Pacific area of interest (north of Lat. 40°N, and east of Long. 180°).

The requirements are to solve the oceanographic aspects of fisheries, military and industrial problems. In turn, these require the definition of the oceanographic conditions in all parts of the area and provision for their continuous assessment and forecasting.

Oceanographic conditions are defined by the properties and structure of the water. These vary from place to place and from time to time. In the present state of the art, they are observed by shipborne oceanographic surveys which are slow, tedious and costly. It is economically impossible to main tain comprehensive surveys in all areas all the time. It is only possible to survey limited areas at seasonal intervals. Such data, by themselves, are not adequate to monitor the oceanographic situations. However, with the aid of theory and analogues (hydraulic models) they can be made to reveal the sequences of oceanographic events and their relation to readily observed features such as shore and bottom, weather, runoff, tide and daily surface seawater observations at convenient, fixed positions. Other government agencies provide adequate descriptions and monitoring of all except the oceanographic features. Hence, the procedure is to define the properties and structures in each locality from a minimum of oceanographic surveys, define their relations to the readily observed features, and so provide simple, economic systems of monitoring, assessment and forecasting.

Since 1930 repeated surveys have been made in successive seasons, through a few years, in each locality. Also, daily observations of surface properties and structure have been made at as many fixed locations as possible. These data have been catalogued and published.

Descriptive oceanography

From time to time, as sufficient data became available, descriptive models of oceanographic behaviour were deduced. These models define the oceanographic environment in terms of water types, structures and their behaviour. They define how the structures are created, maintained and changed. They define the relation of the structures to weather, runoff,tide and the daily seawater observations. They made it possible to apply oceanography to fisheries, military and industrial problems and to provide an oceanographic information and forecasting service. Significant progress* has been made in all these aspects.

During the past year a considerable proportion of the effort has been devoted to finalizing and reporting researches on additional models. - 2 -

The recently completed behaviour model of the growth and decay of the seasonal thermocline in the Subarctic Pacific Ocean is the culmination of the research on the heating and cooling, and wind mixing and convection pro cesses. It allows assessment and forecasting of temperature structure in the seasonal zone (0-100 m depth).

The thermocline model has been extended to define the structure and behaviour in seven oceanographic climatic regions from the Equator to the Arctic in the North Pacific Ocean. These models define the different methods of assessing and forecasting oceanographic conditions in each region but allow the conclusions to be presented in a universally consistent and comprehensible manner. They provide for a mu'ch needed systematization in the presentation of oceanographic parameters.

Below the limit of seasonal variation (about 100 m depth) the pro perties and structure do not change rapidly and, in the eastern Subarctic Pacific, they may be monitored by occasional observations at judiciously chosen points. Evidently the annual synoptic surveys are no longer necessary. They may be replaced by very simple lines of monitoring observations.

The region along the ocean coast (the Coastal Domain, Fig. 1) has been shown to be transitional between the coastal estuarine region and the oceanic region, and is influenced by both. In these ocean coastal waters, the seasonal sequence of structures have been defined. With the aid of theory, the influence of wind on them has been described. This model is being extended to define the structures in terms of observed winds and runoff, and relate it to the daily seawater observations. This includes the structure and behaviour of the near surface and bottom waters on the continental shelf and slope.

In the near ocean there is an annual intrusion of waters from the Sub- tropics northward past the west coast of Vancouver Island. Occasionally this becomes extreme, as in 1958. This behaviour is being monitored by daily seawater observations, and the line of observations every six weeks between the coast and Ocean Station "P".

The studies in the inland seaways are nearing fruition. With the aid of the hydraulic model of the Hecate region the data accumulated since 1937 have been assessed. The oceanography of Dixon Entrance has been solved and is being prepared for publication. It is a complex estuarine system in which the oceanographic structures and domains are primarily determined by the tidal mechanisms and the flushing is determined by winds. There is good evidence that oceanographic conditions can be monitored by a marginal expan sion of the daily seawater observations and mean sea level data. This power ful technique is being extended to Hecate Strait and Queen Charlotte Sound, where a conclusion is expected during the coming year.

Monitoring

There are three major monitoring systems in operation now. Daily observations of surface seawater temperature and salinity are made at 14 positions (mostly at lightstations) (Fig. 1) along the ocean coast and the inland seaways. This program has been in operation for more than thirty years and, when interpreted in the light of the oceanographic behaviour models, it provides calendars of events in the waters over the continental shelf which - 3 -

can be correlated with statistical fisheries history. Ocean Station "P" (Lat. 50°N, Long. 145°W) in the Central Subarctic Domain (Fig. 1) is occupied during alternate six-week periods by two weatherships (C.C.G.S. "St. Catharines" and "Stonetown"). Both ships make twice daily bathythermo graph observations. One ship, C.C.G.S. "St. Catharines", carries an oceanographer who makes comprehensive observations from surface to bottom while the ship is "on station". These data monitor conditions in the eastern Central Subarctic Domain. A sequence of oceanographic observations, from surface to bottom, are made from this ship en route to and from Ocean Station "P". This sequence (Line "P", Fig. 1) provides a monitor through the Coastal, Transition and Central Subarctic Domains every six weeks. These monitoring systems are operating with classical equipment and procedures. The data are published immediately, and atlases showing useful analyses have been prepared. These (MS) reports form the bases for analytical studies and correlation with fisheries.

In addition, weather, sea surface temperature and some bathythermograms are observed by transitting ships, fisheries vessels, Picket and Weatherships. These data are collected and made available to an oceanographic information service created in the Naval and Air Force Weather Services. In these centres the forecasters receive the temperature data daily, analyse it according to the oceanographic models and provide regular assessments of structure and forecasts. These results are distributed to all agencies by mail (weekly) and to some agencies by radio facsimile (daily). The accumulation of these charts provides historical records of temperature structures.

These monitoring systems and the information service are limited by the existing classical equipment and procedures. There is an immediate need for new high-speed monitoring and interpretation techniques. To this end a philosophy of analysis of continuous records of sea surface temperature, to reveal many features of structure in the seasonal zone (0-100 metres depth) has been derived. Sophisticated airborne radiation thermometers have been designed and built with some financial assistance from the RCAF. This equip ment is to be carried by Maritime Air Command during regular daily routine patrols off the Canadian coast. These will provide much needed daily input of data to the Information Service.

The Pacific Naval Laboratory has supported this effort by designing and building corresponding continuous recording equipment for ships. These units are being installed in the exploratory fishing vessels ("G.B. Reed", etc.)

Fisheries oceanography Having arrived at a state of relative competence in the knowledge and monitoring of the environment, it is now expedient to apply the skills and correlate the information with fisheries. During the spring, oceanographers joined the expedition to study the seaward migration of young pink salmon in Burke Channel. They were able to provide a skilled appreciation of the environment for ecological studies of these fish migrations. - 4 -

Also, a number of senior ecologists and biologists have been transferred to the Group since October. They are examining the existing information by a "yes, maybe, no" technique to define what correlations exist, do not exist, and where and why they are indefinite. This procedure defines the present state of knowledge and the course of future research.

It is anticipated that, as the Marine Sciences Branch of the Department of Mines and Technical Surveys accepts responsibility for the national require ments in oceanography, the Pacific Oceanographic Group will devote increasing effort to fisheries oceanography.

Liaisons

Oceanographic research requires correlation of the locally observed structure with data from other parts of the oceans and with tides, weather, runoff, etc., which are observed by other agencies. Hence it is necessary to have wide liaisons to obtain and exchange data. These have been cultivated assiduously and successfully with all agencies, domestic and foreign, operating in the area of interest.

It has been noted that close to the Canadian coast there is a northward extension of the Transitional Domain (Fig. 1). The advance and retreat of this extension is of particular interest because it may affect the homing migration of salmon and the occurrence of albacore in the area, and was con sidered worthy of repeated surveys to determine its behaviour. This is being accomplished by liaison with the University of Washington. They are conducting regular surveys southward of Line "P" to determine the extent of the "plume" of discharge from the Columbia River. Data from those surveys, combined with the regular observations from the Line "P" monitoring are providing the required information.

In furtherance of this project there have been two combined expeditions in which C.N.A.V. "Oshawa", partly manned by oceanographers from P.O.G., has joined the sea operation. All data are exchanged.

Data collection

The Pacific Oceanographic Group has no ships. Observations are made from ships provided by the Royal Canadian Navy, the Department of Transport and the Department of Mines and Technical Surveys, and from aircraft provided by the Royal Canadian Air Force. The more sophisticated observations are made by P.O.G. personnel borne in these carriers, but many standard observa tions are made by the crews of the vessels and aircraft. Also daily seawater observations are made by local observers at 14 coastal positions (12 lightstations) and from the weatherships (Department of Transport) at Ocean Station "P" (Lat. 50°N, Long. 145°W).

J.P. Tully, Oceanographer in Charge. - 5 -

Table I. SEA OPERATIONS, 1963

Duration Senior Scientific Dates Ship (days) Scientist Party

Ocean Station "P"

Jan 15-Mar 4 48 C.C.G.S. "St. Catharines" D.G. Robertson 1 Apr 9-May 27 48 C.C.G.S. "St. Catharines" R.B. Tripp 1 Jun 25-Aug 5 41 C.C.G.S. "St. Catharines" R.G. Tippett 1 Sep 10-Oct 29 49 C.C.G.S. "St. Catharines" A.J. Stickland Z Dec 3-Jan 16, 44 C.C.G.S. "St. Catharines" R.B. Tripp 1 1964

Eastern Subarctic Pacific Region

Jul 15-Jul 23

Coastal

Apr 16-Jun 5 51 M.V. "Remora" A.J. Dodimead (Burke Channel) Aug 8-Aug 18 10 C.H.S. "Ehkoli" H.J. Hollister (visit to lightstations)

Oceanographic Support

Apr 1-Apr 9 8 C.N.A.V. "Oshawa" A.J. Stickland (offshore Vancouver Island with P.N.L.) May 20-Jun 12 23 C.N.A.V. "Oshawa" A.R. Stanley-Jones (Columbia River Plume and Transitional Domain with Univ. of Washington) Aug 22-Sep 10 20 C.C.G.S. "John A. H.J. Hollister Macdonald" (Prince Regent Inlet with P.N.L.) Dec 2-Dec 6 4 C.N.A.V. "Oshawa" R.H. Herlinveaux (offshore Vancouver Island with P.N.L.) Dec 9-Dec 21 13 C.N.A.V. "Oshawa" A.R. Stanley-Jones (Columbia River Plume and Transitional Domain with Univ. of Washington) -.6 -

COOPERATIONS AND LIAISONS

This Group coordinates all possible resources, domestic and foreign, to serve Canadian requirements for oceanography in the Pacific.

Fisheries Research Board: provides laboratories, staff, funds, adminis tration and direction, and technical services in the Biological Station at NanaimO.

Pacific Naval Laboratory (Defence Research Board): provides working liaison with the Navy and Air Force, engineering and shop service. It receives oceanographic support for sea operations and oceanographic data for defence research. The Group provides assistance, along with other agencies, to the P.N.L. operations listed as follows:

Ice Pack 1. Polar Continental Shelf Project, D.M.&T.S..(logistics) 2. R.C^A.F. Transport Command 3. D.O.T. (ships)

Underwater 1. I.O.U.B.C. (geology and scattering Weapons Range layer investigations) 2. F.R.B. (fishing vessel for scattering layer investigation - M.V. "A.P. Knight")

Oceanic Turbulence 1. R.C.N.

Directorate of Scientific Information Service: provides library, translation, and abstracting services.

Royal Canadian Navy: provides and operates the oceanographic vessels C.N.A.V. "Oshawa" and C.N.A.V. "Whitethroat". Department of Mines and Tech nical Surveys operates C.H.S. "Ehkoli". These ships are used jointly by Pacific Oceanographic Group, Pacific Naval Laboratory and the Institute of Oceanography of the University of British Columbia. Their use is coordinated by a Ships1 Schedule Panel of the West Coast Working Group of the Canadian Committee on Oceanography.

Royal Canadian Navy: calibrates and repairs all Canadian bathythermo graphs used in the Pacific. The bathythermograph calibration service is established in H.M.C. Dockyard.

Naval Weather Service: in the Royal Canadian Navy operates the Oceano graphic Service for Defence (Oceanographic Information Service) which collects, analyses, collates and distributes bathythermograph and surface temperature data from ships and aircraft. Pacific Oceanographic Group provides research and scientific support to this service.

Royal Canadian Air Force: The Maritime Air Command #407 Squadron (Comox) provides and operates aircraft for test of airborne equipment. Their requests for specific oceanographic information are being incorporated into the Oceanographic Information Service. - 7 -

Meteorological Service (Department of Transport): provides meteorological data and special analyses, and gives research support and encouragement to the studies of heating, cooling and evaporation in the ocean. Pacific Oceano graphic Group operates a pyroheliometer at Departure Bay.

Marine Services (Department of Transport): provides facilities for daily seawater observations at 12 lightstations; bathythermograph observa tions from C.C.G.S. "Stonetown" and C.C.G.S. "St. Catharines" on Ocean Station "P"; and accommodation and assistance for two oceanographers on C.C.G.S. "St. Catharines".

Air Services (Department of Transport): provides radio communication with the lightstations and the weatherships and facilities at Cape St. James Radio Beacon for daily seawater observations.

Hydrographic Service (Division of Marine Sciences, Department of Mines and Technical Surveys): provides regular and special charts, plotting sheets and special reproductions.

Canadian Oceanographic Data Centre (Department of Mines and Technical Surveys): Machine processes and publishes the oceanographic data.

International Pacific Salmon Fisheries Commission: requires analyses and timely information of oceanographic conditions that may affect the well- being and migration of salmons which migrate through Juan de Fuca Strait.

Department of Fisheries: are continuing to observe daily water temper atures in the Fraser River. They have installed bathythermograph winches on three of their patrol vessels to cooperate in data collection for the Infor mation Service.

Department of Public Printing and Stationery, Esquimalt Unit: provides exceptional service in printing data records and manuscript reports, and in providing other printing services.

United States Weather Bureau: the Extended Forecast Division provides monthly summaries of the barometric pressure distribution over the northern oceans. These are the basis of the monthly transport computations (discon tinued 1 June 1962).

Scripps Institution of Oceanography (La Jolla): seawater samples are taken monthly at Ocean Station "P" in containers provided by the Institution and are returned to them for radioactivity analyses.

University of Washington: C.N.A.V. "Oshawa" with oceanographic equip ment and two oceanographers took part in oceanographic surveys of the Transitional Domain and Columbia River plume. Additional personnel were pro vided by the University. Also, they processed the data and provided copies to P.O.G. - 8 -

Data and data records are regularly exchanged with:

U.S. Fish and Wildlife Service: Bureau of Commercial Fisheries Biolog ical Laboratory, San Diego, California; the North Pacific Fisheries Explora tion and Gear Research, Seattle, Washington; and the Biological Laboratory, Seattle, Washington.

I.G.Y. World Data Center A, Washington, D.C.

Scripps Institution of Oceanography, La Jolla, California.

U.S. Naval Oceanographic Office, Washington 25, D.C.

Japanese Hydrographic Office, Tokyo, Japan.

Department of Oceanography, University of Washington, Seattle, Wash.

Institute of Oceanography, University of British Columbia, Vancouver, B.C

U.S. Naval Postgraduate School, Monterey, California.

TECHNICAL SERVICES

A staff of sea technicians provide the assistance required for the collection and processing of data at sea and ashore.. These people assist as required under direction of the professional research staff.

In addition there are a number of functions that require full time and/or trade skills. The Group is not large enough to afford or fully occupy people in every function; rather, some people have several tasks, others are pooled with the technical services of the Biological Station.'

Technical services in the Pacific Oceanographic Group:

Data records (editing) H.J. Hollister

Library R.H. Herlinveaux

Equipment (procurement, maintenance, etc.) J.A. Stickland

Secretaries Mrs. D.M. Holmberg Miss J.E, Trevor

Cooperative services with the Biological Station (B.S.)

Electronics* M. Pirart (B.S.) J.D. Carswell (P.O.G.) D. Oliver (P.O.G.)

Engineering (civil) L.D.B. Terhune (P.O.G.)

Instrument making, machining R. Cagna (P.O.G.) - 9 -

Welding, machine shop work K. Sutherland (B.S.)

Photography C.J. Morley (B.S.)

Chemistry laboratory supervision, K.V. Stephens (P.O.G.) instrument maintenance (salinometers, photocolorimeters, etc.)

Services provided by Pacific Naval Laboratory:

Winches (design and maintenance), E.P. Fleischer (P.N.L.) liaison with R.C.N, and C.N.A.V. ships

STAFF LIST

J.P. Tully, M.B.E., Ph.D. Principal Scientist Oceanographer in Charge W.E. Johnson, Ph.D. Senior Scientist Fisheries Ecology (from October 1, 1963) A.J. Dodimead, M.Sc. Senior Scientist North Pacific (Fisheries) W,P. Wickett, M.A. Senior Scientist Fisheries Ecology (from November 1, 1963) L.F. Giovando, Ph.D. Associate Scientist North Pacific (Defence) S. Tabata, M.A. Associate Scientist (leave of absence from March 30, 1962) P.B. Crean, M.A.Sc. Associate Scientist Coastal R. Lebrasseur, M.A. Associate Scientist Fisheries Ecology (zoo- (from November 1, 1963) plankton) W.H. Bell, B.A.Sc. Assistant Scientist Hecate Model F.W. Dobson, M.Sc. Assistant Scientist Coastal, Marine Physics (to September 24, 1963) H.J. Hollister Technician 6 Chief Technician Daily Seawater Observations Data Processing, Records R.H. Herlinveaux Technician 5 PNL Support L.D.B. Terhune Technician 5 Model Laboratory K.V. Stephens Technician 4 Chemistry Laboratory (from November 1, 1963) J.A. Stickland Technician Supply and Maintenance D.G. Robertson, B.Sc. Technician Ocean Station "P" J.D. Carswell Technician Electronics H.W. Wilke, B.Sc. Technician Sea Technician (from October 1, 1963) J.H. Meikle Technician 2 Sea Technician (to July 15, 1963) R. Cagna Technician 2 Machinist J. Wong, B.Sc. Technician 2 Sea Technician (from July 15, 1963) A.R. Stanley-Jones, B.Sc. Technician 2 Sea Technician (from May 10, 1963) W.F. Pinckard Technician 2 Sea Technician (to September 30, 1963) - 10 -

R.B. Tripp Technician 1 Sea Technician H.H. Dobson Technician 1 Sea Technician (to March 1, 1963) M.C. Cairns (Miss) Asst. Technician 3 Flexowriter operator, (to May 31, 1963) Computations technician J.E. Trevor (Miss) Clerk 2 Assistant Secretary (from July 22, 1963) M.M.N. Sherry (Mrs.) Stenographer 3 Administrative Secretary (to March 1, 1963) D.M. Holmberg (Mrs.) Stenographer 3 Administrative Secretary (from March 18, 1963)

Seasonal and Term Employees

D.A. Oliver Technician 2 Electronics (ART) N.E.J. Boston M.Sc. Associate Scientist Hecate Model J.A. Gow, b.a! Student Assistant Sea Technician R.G. Tippett Student Assistant Sea Technician R.F. Wickett Student Assistant Sea Technician

Complement

Full time 27 Professional 12 Technical 13 Clerical 2

Seasonals 5

Personnel attached for training

From Department of Mines and Technical Surveys:

R.H. Loucks, M.A. Scientific Officer From Jul 15, 1963 M.E. Best .. Student Assistant From May 6 to Sep 11, 1963 B.R. Olund .. Student Assistant From May 6 to Sep 11, 1963 H.G. Andersen, B.Sc. Student Assistant From May B to Sep 13, 1963

Associated Research Scientists

A. Acara, Ph.D. (University of Istanbul, Turkey) National Research Council (from 31 January, 1961) Fellowship G.H. Jung, Ph.D. (U.S. Naval Postgraduate School, Monterey, California) (from May 31, 1963 to July 26, 1963) I.P. Bergeron, B.A.Sc. (Aviation Electric Limited, Montreal, Quebec) (from March 25 to May 30, 1963) -. 11 -

PUBLICATIONS

Acara, A. On the vertical transport velocity on Line "P" in the eastern Subarctic Pacific. Ocean., MS (13 pp^ ,5. Fig'.),; -Submitted for publication J. Fish. Res. Bd. Canada.

*Dodimead, A.J., F. Favorite, T. Hirano. A review of the oceanography of the Subarctic Pacific Region. Bull. 13, Int. North Pac. Fish. Comm., 195 pp.

Giovando, L.F. The Canadian Oceanographic Information Service. National Oceanographic Data Center, No. 2-63, pp. 1-2.

Lane, R.K. A model of seawater structure near the west coast of Vancouver Island, British Columbia. J. Fish. Res. Bd. Canada, Vol. 20, No. 4, pp. 939-967.

Tully, J.P. Oceanographic regions and assessment of structure in the North Pacific Ocean. MS (22 pp. 25 Fig.). Submitted for publication J. Amer. Soc. Limnology and Oceanography.

Tully, J.P. Oceanographic regions and processes in the seasonal zone of the North Pacific Ocean. MS (22 pp. 18 Fig.). Submitted for publication Hidaka Anniversary Volume, Geophys. Inst., Univ. of Tokyo, Tokyo.

Tully, J.P. Oceanography 1963. American Peoples Encyclopedia 1963 Yearbook, Grolier Incorporated (1 pp.) (in press).

Tully, J.P., and L.F. Giovando. Seasonal temperature structure in the eastern Subarctic Pacific Ocean. Marine Distributions. The Royal Society of Canada, Spec. Pub. No. 5. Edited by M.J. Dunbar, F.R.S.C, Univ. of Toronto Press, pp. 9-36.

Uda, M. Oceanography of the Subarctic Pacific Ocean. J. Fish. Res. Bd. Canada, Vol. 20, No. 1, pp. 119-179.

MANUSCRIPT REPORTS AND CIRCULARS

Andersen, H.G. Some small considerations of the effect of cloud on an Airborne Radiation Thermometer. Fisheries Research Board of Canada, Pacific Oceanographic Group Circular, No. 1963-2, 8 pp., 4 figs.

Bell, W.H. Reproduction of estuarine structure and current observation techniques in the Hecate Model. MS Rept. Oceanogr. and Limnol., No. 158, 24 pp., 13 figs.

Crean, P.B., H.H. Dobson, H.J. Hollister. Oceanographic data record. Monitor project, September 19 to October 9, 1962. MS Rept. Oceanogr. and Limnol., No. 142, 203 pp.

*This item was listed as MS submitted for publication in last year's report. It is listed here for exact reference. The pages are not included in the total of this year's production. - 12 -

Dodimead, A.J. Oceanographic conditions in the eastern Subarctic Pacific, January to March 1963. Fisheries Research Board of Canada, Pacific Oceanographic Group Circular, No. 1963-3, 2 pp., 7 figs.

Fofonoff, N.P., and F.W. Dobson. Transport computations for the North Pacific Ocean, 1950. MS Rept. Oceanogr. and Limnol., No. 149, 5 pp., 84 figs.

Transport computations for the North Pacific Ocean, 1951. MS. Rept. Oceanogr. and Limnol., No. 150, 5 pp., 84 figs.

Transport computations for the North Pacific Ocean, 1952. MS Rept. Oceanogr. and Limnol., No. 151, 5 pp., 84 figs.

Transport computations for the North Pacific Ocean, 1953. MS Rept. Oceanogr. and Limnol., No. 152, 5 pp., 84 figs.

Transport computations for the North Pacific Ocean, 1954. MS Rept. Oceanogr. and Limnol., No. 153, 5 pp., 84 figs.

Transport computations for the North Atlantic Ocean. Annual means and standard deviations, 1950-1961. MS Rept. Oceanogr. and Limnol., No. 156, 5 pp., 72 figs.

Transport computations for the North Atlantic Ocean, 1950-1959. 10-year means and standard deviations by months. MS Rept. Oceanogr. and Limnol., No. 162, 5 pp., 144 figs.

Transport computations for the North Pacific Ocean, January-May, 1962. MS Rept. Oceanogr. and Limnol., No. 164, 5 pp., 30 figs.

Transport computations for the North Atlantic Ocean, January- May, 1962. MS Rept. Oceanogr. and Limnol., No. 165, 5 pp., 30 figs.

Transport computations for the North Pacific Ocean, 1950-1959. 10-year means and standard deviations by months, wind stress and vertical velocity annual means 1955-1960. MS Rept. Oceanogr. and Limnol., No. 166, 5 pp., 84 figs., 6 tables.

Froese, C. Computation of mass transport in the ocean from atmospheric pressure data, FORTRAN I program for IBM 1620 computer. MS Rept. Oceanogr. and Limnol., No. 163, 16 pp.

Herlinveaux, R.H. Oceanographic observations in the Canadian Basin, Arctic Ocean, April-May, 1962. MS Rept. Oceanogr. and Limnol., No. 144, 25 pp.

Data record of oceanographic observations made in Pacific Naval Laboratory underwater sound studies, November 1961 to November 1962. MS Rept. Oceanogr. and Limnol., No. 146, 101 pp.

Hollister, H.J. Seawater temperatures along the British Columbia coast, October, November, December, 1962. Fisheries Research Board of Canada, Pacific Oceanographic Group Circular, No. 1963-1, 4 pp. - ,13 -

Seawater temperatures along the British Columbia coast, January to June 1963. Fisheries Research Board of Canada, Pacific Oceanographic Group Circular, No. 1963-5, 7 pp.

Data record of bathythermograms observed in the northeast Pacific Ocean during the Gulf of Alaska Salmon Tagging Program, April to July 1962. MS Rept. Oceanogr. and Limnol., No. 143, 74 pp.

Observations of seawater temperature and salinity on the Pacific coast of Canada, Volume XXII, 1962. MS Rept. Oceanogr. and Limnol., No. 161, 95 pp.

Pike, G.C., and L.F. Giovando. Whales and dolphins of the west coast of Canada. Fisheries Research Board of Canada, Cir. No. 68, 15 pp., 19 figs.

Robertson, D.G. Oceanographic observations from weatherships C.C.G.S. "St. Catharines", Cruise P-63-2, April 9-May 27, 1963 and C.C.G.S. "Stonetown", May 21-July 1, 1963. Fisheries Research Board of Canada, Pacific Oceano graphic Group Circular, No. 1963-4, 2 pp., 7 figs.

Oceanographic observations from weatherships C.C.G.S. "St. Cath arines", Cruise P-63-3, June 25-August 5 and C.C.G.S. "Stonetown", July 30-September 16, 1963. Fisheries Research Board of Canada, Pacific Oceanographic Group Circular, No. 1963-6, 2 pp., 7 figs.

Robertson, D.G., F.W. Dobson, H.J. Hollister. Oceanographic data record Ocean Weather Station "P", August 1, 1962 to January 18, 1963. MS Rept. Oceanogr. and Limnol., No. 154, 155 pp.

Tabata, S., and L.F. Giovando. The seasonal thermocline at Ocean Weather Station "P" during 1956 through 1959. MS Rept. Oceanogr. and Limnol., No. 157, 7 pp., 20 figs.

SPECIAL REPORTS

Crean, P.B. Oceanographic mechanisms in Dixon Entrance, B.C. Fisheries Research Board of Canada, Pacific Oceanographic Group Report. I.U.G.G. Conference, 15 pp., 27 figs.

Dodimead, A.J. Canadian oceanographic research in the eastern Subarctic Pacific Region during 1963. International North Pacific Fisheries Commission Annual Meeting, 4 pp., 7 figs.

Giovando, L.F. A case for the Shipborne Recording Thermometer. Fisheries Research Board of Canada, Pacific Oceanographic Report to the Scientific Adviser, Chief of Naval Staff, 10 pp., 9 figs.

The Shipborne Recording Thermometer: continuous recording of sea-surface temperature for fisheries studies. Fisheries Research Board of Canada, Pacific Oceanographic Group Internal Report, 12 pp., 10 figs. - 14 -

Tully, J.P. An Oceanographic Information Service on the Pacific coast of Canada. Fisheries Research Board of Canada, Pacific Oceanographic Group Report. Third Tripartite Naval Operational Research Symposium, Esquimalt, B.C., 23 pp., 27 figs.

Climate and weather in the ocean. Fisheries Research Board of Canada, Pacific Oceanographic Group Report. American Association for the Advancement of Science, California, 22 pp., 20 figs.

Oceanographic domains and assessment of structure in the North Pacific Ocean. Fisheries Research Board of Canada, Pacific Oceano graphic Group Report. Tripartite Symposium on Military Oceanography, Washington, 17 pp., 40 figs.

Requirements for a Military Oceanographic Information Service. Fisheries Research Board of Canada, Pacific Oceanographic Group Report Tripartite Symposium on Military Oceanography, Washington, 7 pp.

Table II. Summary of Publications and Reports, 1963

Text Figure Total T f*PTTI.Q Pages Pages Pages

Scientific Journals 8 178 48 226 MS Reports (0 & L) 19 765 838 1,603 Circulars (POG) 6 25 25 50 Other Reports 9 110 140 250

Totals (1963) 42 1,078 1,051 2,129 Totals (1962) 65 3,844 - 15 -

SUMMARY REPORTS OF RESEARCH PROJECTS

Title Reported by Pages

North Pacific Ocean

Climate in the sea J.P. Tully 17-20 Program and results of oceanographic D.G. Robertson 20-25 observations at and en route to and from Ocean Station "P" during 1963 A space-time bathythermograph survey R.H. Loucks 25-29 The Canadian Oceanographic Information L.F. Giovando 30-31 Service An assessment of oceanographic conditions R.H. Loucks 31-32 along Line "P" in late summer On the vertical transport velocity on Line A. Acara 33-35 "P" in the eastern Subarctic Pacific Ocean On the intermediate water of the North A. Acara 36-42 Pacific Ocean

Coastal Waters

Daily Seawater Observations H.J. Hollister 43-47 Oceanography of Dixon Entrance P.B. Crean 47-50 Hecate Model W.H. Bell 50-56 Early sea life of pink salmon A.J. Dodimead and 57-67 R.H. Herlinveaux

Special or Support Projects

Oceanographic support for Pacific Naval Laboratory projects Oceanic turbulence R.H. Herlinveaux 68 Operation ICEPACK IV H.J. Hollister 68-69 Scattering layer R.H. Herlinveaux 69-70 Correspondence of slicks and water R.H. Loucks 71 temperatures in Juan de Fuca Strait Cloud interference - ART W.H. Bell 71

- 17 -

NORTH PACIFIC OCEAN

Climate in the sea - J.P. Tully

An analogy may be drawn between weather and climate in the atmosphere and in the North Pacific Ocean. The ocean basin may be regarded as an inert, impervious bowl containing sea water whose properties can be changed only by surface processes such as heating, cooling, precipitation, evaporation and wind mixing. At the surface, the waters react to these processes in a few hours. The time lag increases with depth, daily, weekly to annually at 120 to 150 meters depth. This is the seasonal zone in which the climate is the sum total of ambient weatherlike variations. Below these depths the changes are small, slow and non-seasonal. The regional differences of pro perties and structure vanish between 1500 and 2000 meters where the tempera ture is 1.68°C, and the salinity is 34.67&.

Seven climatic regions have been defined in the seasonal zone (0 to 150 meters depth) of the North Pacific Ocean (Fig. 2). In general there is a gradient of climate in the sea from constant warm conditions in the Tropics to an extreme cycle of heating and cooling in the Arctic. Water masses are generated in the Tropics, Subtropics, Subarctic and Arctic where the pro perties and structure of the waters are determined by local surface processes in accord with the local atmospheric weather and climate. Kuroshio and Oyashio are western boundary streams in the ocean which transport waters from the extreme climatic regions towards the mid-latitudes more rapidly than they can adjust to the changing climate. These waters meet and mingle in the Confluence Region and are dissipated in the slow eastward trans-ocean drift.

In the Tropics daytime heating equals nighttime cooling throughout the year. In general precipitation slightly exceeds evaporation. Mixing is due entirely to wind. Hence, there is very little seasonal variation. The waters are warm (27° to 29°C), moderately saline (34.6-34.8&), and mixed to homogeneity to about 30 meters depth. Below this there is a thermocline separating the warmed and unwarmed waters and its depth remains constant through the year.

In the Subtropics there is a seasonal cycle of heating and cooling which increases northward. From the spring to the autumn Equinox daytime heating generally exceeds nighttime cooling. Heat accumulates in the sea so that the waters are warmest in September. Cooling is dominant during the remainder of the year so that the waters are coldest at the end of March. The annual range of temperature increases northward from zero in the Tropics to a maximum of 8 C° between 40° and 45°N Lat.

At the end of the cooling season the waters are isothermal to about 150 meters depth. Soon afterwards at the beginning of the heating season a thermocline is formed between 40 and 60 meters depth separating the warmed and unwarmed waters. As the upper waters are warmed the temperature dif ference through the thermocline (magnitude) grows while its depth (position) remains nearly constant. During the cooling season the upper waters cool, the thermocline is eroded and sinks (decays) to the limit of the seasonal zone (150 meters). In the Subtropics these waters never become as cold as the deep non-seasonal waters. Hence, there is a deep permanent thermocline in the non-seasonal zone (below 150 meters). •"*-•»" """«

Figure 2. - 19 -

In the Subtropics evaporation exceeds precipitation. Fresh water is continually being removed from the surface leaving the salt in the sea. Hence, the salinity is greatest at the surface and decreases with depth to a minimum below 200 meters depth. This situation is stabilized by the temperature gradient in the thermocline.

However, the waters above the seasonal thermocline are always homo geneous. Because of evaporation the salinity of the surface waters increases and despite the warming they become more dense and sink through and mix with the immediately underlying water. This convective mixing extends below the depth of simple wind mixing, but is limited by the density stability inherent in the thermocline.

The Subarctic is distinguished by excess precipitation, which creates a distinctive structure. The accumulated fresh water from precipitation is contained in an upper, near isohaline zone, from the surface to about 100 meters depth. Below this, between about 100 and 200 meters depth there is a halocline in which the salinity increases about ]$, to 33.£^». This zone marks the limit of surface seasonal effects. Below this the salinity increases into the abyss. There is no salinity minimum in the Subarctic or Arctic.

At the end of the cooling season the waters are homogeneous to the halocline (about 100 meters depth). In April a thermocline forms between about 25 and 50 meters depth, and its magnitude increases as the surface waters are warmed. Because of the excess precipitation there is no convec tion, hence the depth of the mixed layer above the thermocline is determined by wind mixing alone.

From September, during the cooling season, the thermocline decays; is eroded and sinks. It finally vanishes in the top of the halocline during January or February. Thereafter these upper waters are homogeneous and may continue to cool depending on the severity of the winter. In the nor thern parts of the region they frequently become colder than the waters in the halocline.

The Arctic regions in the Pacific are in the northern Bering and Okhotsk Seas where ice forms during winter. These are the coldest parts of the Subarctic region where the annual temperature range straddles the freezing temperature of sea water (-1.7°C). These regions are subject to excess precipitation and there is a halocline in the salinity structure.

As elsewhere warming commences in April but the heat is expended in melting the ice. Because sea ice contains little or no salt, this process releases fresh water which forms a shallow brackish layer. Warming does not commence until the ice vanishes about mid-summer. Thereafter, during the long Arctic days warming is rapid and the water temperature rises to more than 7°C at the end of the heating season in September. The thermocline remains shallow, coincident with the marked shallow seasonal halocline.

The heat is lost and the thermocline vanishes during the first few months of the cooling season. It cannot sink because it is stabilized in the shallow brackish layer of ice-melt water. As winter advances freezing occurs. The formation of ice removes fresh water from the sea leaving the salt in the residual water. Its salinity increases; it becomes more dense - 20 - than the underlying water and convective mixing occurs. Because there is excess precipitation the freezing process is never adequate to remove all the fresh water. Hence the residue of the seasonal halocline sinks. These residues from successive annual cycles accumulate in a deep permanent halocline, which in these regions extends from 100 to 500 meters depth. In the zone between the ice and the permanent halocline the waters are homo geneous at the freezing temperature.

Along the western boundary of the ocean Kuroshio is an ocean stream flowing northward from the vicinity of the Philippine Islands past Japan, at speeds of 25 to 50 miles per day. It carries water from the southern to the northern part of the Subtropic Region. Although it loses heat en route it does not become fully adjusted to the changing climate. It is always warmer than the surrounding water. Hence, it is a warm current.

Oyashio is a corresponding cold current flowing southward from the Arctic Regions in the Western Bering and Okhotsk Seas. This current carries cold water past the Kurile Islands to the limit of the Subarctic region off the north coast of Japan.

There the two currents meet and turn eastward in a region of confluence. In this region of confluence there are marked fronts between the cold and warm waters. In general the sea surface temperature changes about 15 C° in less than 200 miles. However, there is large-scale turbulence in the region. Eddies (boluses) of water break off from one stream and are occluded in the other. There are local situations where the surface temperature change is as great as 10 C° in ten miles. These eddies drift eastward, rotating and mixing with surrounding waters, and lose their identity in a few hundred miles.

This eastward drift (called the West Wind Drift) is slow (2 to 4 miles per day). In such a situation it requires only one season (heating or cooling) for the waters to become adjusted to the local climate and erase the last vestiges of their transported properties. Thus they become Subtropic or Subarctic waters in a few hundred miles from the Confluence Region.

The coastal waters, close along the shores of the continents are subject to the same surface processes as the ocean waters. In addition there are appreciable land effects which provide local restraints (i.e., harbours) and tidal currents which provide local transport and mixing. Each of these localities may be regarded as a sub-division (domain) of a principal clima tic region.

Program and results of oceanographic observations at and en route to and from Ocean Station "P" during 1963 - D.G. Robertson

Two Canadian weatherships, C.C.G.S. "St. Catharines" and C.C.G.S. "Stonetown" alternately, every six weeks, occupy Ocean Weather Station "P" (Fig. 1) (Lat. 50°00'N, Long. 145°00'W). Since 1952, oceanographic observa tions in the form of surface seawater temperatures and twice-daily bathythermograms at Ocean Station "P" and a series of bathythermograms every six weeks on a line between Swiftsure Bank and Ocean Station "P" have been made from aboard these vessels. In 1956 one of the ships, C.C.G.S. "St. Catharines", took on oceanographers from the Pacific Oceanographic Group to obtain serial - 21 - observations of temperature, salinity and other chemical properties, plankton and productivity measurements during alternate six-week periods.

The present purpose of the oceanographic observations from the weather ships is to maintain time-series observations to monitor the character of the water of the eastern Central Subarctic Domain.

The current oceanographic program is:

C.C.G.S. "Stonetown"

1. En route to and from Ocean Station "P" series of eight 125-meter bathythermograph casts at six different positions.

2. At Ocean Station "P" (a) series of eight 125-meter bathythermograph casts three times a week; (b) twice-daily bathythermograph casts; (c) daily collection of a surface salinity sample.

C.C.G.S. "St. Catharines"

1. En route to and from Ocean Station "P" (a) ten oceanographic stations along Line "P" (Fig. 1); (b) bathythermograph casts between and at the above oceanographic stations and the collection of surface salinity samples.

2. At Ocean Station "P" (a) weekly oceanographic casts to 400 and 2000 meters depth and from 2000 to 4200 meters depth three times during the six-week period. On all these casts serial observations of temperature, salinity and dissolved oxygen content were taken; (b) bathythermograph and surface salinity observations were taken as on the C.C.G.S. "Stonetown"; (c) productivity observations which included surface plant pigment and photosynthetic rate measurements every second day and serial observations with depth every second week; (d) zooplankton observations consisted of i) daily 150-meter vertical hauls; ii) two 1200-meter vertical hauls; iii) nine 10-minute horizontal evening surface tows.

Oceanographic conditions at Ocean Station "P" during 1963

The monthly mean surface sea temperatures illustrated in Fig. 3 are consistently higher in 1963 than the 1952-61 ten-year mean and alternate above and below the monthly means of 1962. In August, the monthly mean temperature was well above average and higher than in 1962.

The temperature (°C) and salinity (&), for the first seven months of 1963, are shown in Fig. 4. Seasonal warming commenced toward the end of April, about two to three weeks later than usual. With the development of the thermocline in May, a secondary halocline, coincident with the thermo cline, formed. Surface salinities remained relatively low at Ocean Station "P" JAN. FEB. MARCH APRIL MAY JUNE JULY AUG. SEPT. OCT. NOV. DEC

14 MONTHLY MEAN SURFACE SEA TEMPERATURE (°C) AT STATION "P"

12 (Lat 50°N. Long.l45°W)

<_>

S K)

UJ a. 2E H 8

Figure 3, 20 JANUARY, 1963 25 FEB, 1963 10 APRIL, 1963 -2IMAY.I963 t -JULY, 1963

HALOCLINE HALOCUNE

INVERSION INVERSION

TEMPERATURE CO TEMPERATURE CO TEMPERATURE CO AT OCEAN STATION "p" AT OCEAN STATION "P* AT OCEAN STATION "P"

20 JANUARY, 1963- -25 FEBRUARY. 1963 B APRIL, 1963 21 MAY,1963 I JULY,1963-

SALWITY (%J SALINITY (%.) SALINITY (%J

AT OCEAN STATION V AT OCEAN STATION V AT OCEAN STATION V

Figure 4. MOiauMUKia

XI 4-1 Q* (U •o

00 Vi 4J a) a

o i-H

•P CO

>» 4J 1-1 a •r< iH (0 00

•o a CO • en •"> vO u o\ 0 r-t N-/ 1 en a) m ^ ON 3 •-I 4J CD •V n 5 a) Ph Ou 2 B Ctf 92 4-1 a tH cl) •-) O CO 00 m C n o 3 l-i CO cd

• m

0) P d W)

fa - 25 -

A noteworthy feature in 1963 is the presence of 3.5 C° water between 150 and 300 meters depth from the first of April till the beginning of July. This is the coldest water that has occurred at these depths since serial oceanographic observations were started at Ocean Station "P" in 1956. It is most probably an eastward extension and expansion of subhalocline water from the western Subarctic Pacific.

Oceanographic conditions en route to and from Ocean Station "P" during 1963.

Figure 5 shows the surface observations of temperature (°C) and salinity <%,) from January 1959 to July 1963 along Line "P". The temperature chart was drawn from continuous Taylorgraph records of the C.C.G.S. "St. Catharines". The salinity chart was obtained from 10-meter salinity values at stations taken along the line. This method of presentation shows both the seasonal and yearly variations at any point along Line "P".

During this period, the lowest surface salinities occurred during the latter part of 1962 and during 1963. Surface temperatures were highest during August and September, 1963.

A space-time bathythermograph survey - R.H. Loucks From previous researches it is anticipated that transient thermoclines will occur in the potential layer depth during heating situations, which are most prevalent in late summer. An expedition was undertaken in late July to observe their character and distribution in the vicinity of Ocean Station "P". Unfortunately, heating conditions did not materialize. However, the observa tions were made as planned and the data were analysed for the character of internal waves. Two surveys were made in which C.N.A.V. "Oshawa" cruised at 8 knots along parallel lines, 8 miles long and two miles apart, covering 80 square miles during mid-day hours. Position was controlled by reference to the weathership which kept station by an anchored buoy. Bathythermographs were observed every 5 minutes (about 1/2 mile). Later the weathership, working alone, made a similar survey. There were two thermoclines. The depths of the top and bottom of the upper thermocline were plotted and contoured, assuming synopticity, as shown in Figs. 6, 7, and 8. These data suggest that the waves were flat-crested with narrow troughs They also suggest that there was some coherence (most evident in Fig. 6) and some randomness (most evident in Fig. 8). A statistical analysis was made (Table II). The average distances separating neighbouring crests/troughs, which differed from the mean by more than one Standard Deviation, were determined. These wave lengths varied from 1.6 to 26 km. This is the first time such a package of data has been obtained. It is being examined further to determine its significance, and if possible, to define some of the features of oceanic internal waves. TOPOGRAPHY OF TOP OF UPPER TKERMOCUNE

Station P, July 19,1963

Dtpths h mttiw

Contour hbrvd-l m«tm

TOPOGRAPHY OF BOTTOM OF UPPER THERMOCLINE

Station P, July 19, 1963

Ovpttts In iiictru

Contour ttervol - I metro

Figure 6. Depth (m) of seasonal thermocline in the vicinity of Ocean Station "P", July 19, 1963. TOPOGRAPHY OF TOP OF UPPER TKERMOCUNE

Sfctfcn P, Jtiy 20,1963 Mptns n cnttrM Oonlov WotqI"! cnttra

TOPOGRAPHY OF BOTTOM OF UPPER THERMOCUNE

Station P, July 20,1963 D^rths In metres

Contour ktfnvo)"l (intra

—SCN.-

Figure 7. Depth (m) of seasonal thermocline in the vicinity of Ocean Station "P", July 20, 1963. TOPOGRAPHY OF TOP OF UPPER THERMOCLME

Station P, July 2L1963 Depths In metres Contour Werwl-1 metre

scru.—

I4S*W

MtmcM. mua

TOPOGRAPHY OF BOTTOM OF UPPER THERMOCUNE

Station P, July 21,1963

Contour interval - I m. Depths in metres

SO^Nr

W5« W.

motion, win ? I t

Figure 8. Depth (m) of seasonal thermocline in the vicinity of Ocean Station "P", July 21, 1963. - 29 -

Table IH

Date •r % C V

July 19, 1963 23.2 2.9 9.3 t 0.8

19 28.4 3.3 5.1 t 0.8

July 20, 1963 25.4 3.2 7.7 t 0.8

20 29.3 3.0 6.9 t 0.8

July 21, 1963 24.9 2.5 6.4 t 0.8

21 27.8 2.6 3.5 t 0.8

IL is the average depth in meters of the top of the upper thermocline.

"n is the average depth in meters of the bottom of the 6 upper thermocline.

/" is the standard deviation in meters of the depth of the top/bottom of the upper thermocline.

"T is the average crest-to-crest separation, in kilometers, 6 of the larger 32% of the wave crests.. - 30 -

The Canadian Oceanographic Information Service - L.F. Giovando

The Canadian Oceanographic Information Service established to fulfill the oceanographic requirements of both fisheries and the military completed its third year of operation on the West Coast. It is officially termed Oceanographic Services for Defence (OSD). The headquarters of the Service, Maritime Headquarters Forecast Office, HMC Dockyard, Esquimalt, continued to produce the weekly series of OCEAN charts assessing the temperature structure above 300 feet. Four were issued each week: surface temperature, layer depth (top of the seasonal thermocline), bottom of this thermocline, and magnitude of the thermocline. These constitute adequate monitoring of the temperature structure in the Canadian area of interest in the Pacific. The charts are passed to the various users by mail (weekly) or by facsimile (daily) transmission. In addition, both the Centre at Esquimalt and that at the Aviation Forecast Office, RCAF, Comox, issued forecasts of layer depth and other features for use in exercises conducted by the RCN and the RCAF. These were, on the whole, found to be accurate and useful. Thus, the validity of the oceanographic principles underlying the OCEAN system of assessment was further demonstrated. A comprehensive outline of these principles has been completed and published.

Minor improvements, in the light of operational experience, have been made in the procedures of the Service. All aspects are kept under constant review. Early in 1964, the present OCEAN chart format will be replaced by a version of a new basic Canadian Weather Service Map. This will provide uniformity of output by the Information Centre (which deals in both meteoro logy and oceanography), and should aid in the studies of air-sea interactions.

The relationship of and the utility of Information Services to the military users of their output have undergone extensive and critical examina tions at several high-level meetings during the past year. OSD (West Coast) has contributed two lengthy reports which, it is hoped, will help to resolve at least some of the problems encountered.

Reference charts

The first phase of a joint project with Scripps Institution of Oceanography has been virtually completed. This involves the preparation of monthly "guess sheets" of layer depth (top of the thermocline) as inter preted by the OCEAN system of assessment. About 40,000 BT's have been examined. These have been obtained in the Subarctic region and the northern part of the Subtropics (above Lat. 35°N) over the past several years. The corresponding treatment for the bottom of the thermocline will commence shortly. The relationship between wind characteristics and layer depth, developed at POG and of great value in forecasting, has been further refined. A report dealing with the basis of this relationship will be issued shortly.

The data input to the Service remains, unfortunately, at a low level over the area of interest generally. The loss of data occasioned by the termination of the POG North Pacific and Coastal surveys has only partially been compensated for by the increased exploratory fishing surveys conducted by the Biological Station, Nanaimo. The input from fixed stations (Ocean Weather Station "P" and the USN Picket Ships) continues to be excellent. - 31 -

Internal waves

BT data from a special field study in the vicinity of Ocean Station "P" were utilized in an attempt to obtain some measure of the lengths of internal waves in the open ocean. It appears from this study that significant wave lengths, at the depths associated with the seasonal thermocline, ranged from 3 to 10 kilometers.

Shipborne recording thermometer

Further field trials have been conducted, in C.N.A.V. "Oshawa" with the SRT (shipborne recording thermometer) developed on the West Coast. The instrument seems capable of indicating the presence of internal waves. It also appears that the position of the instrument may affect the reliability of the output. Yawing of a ship, even that occurring under normal careful steerage, can cause surface water from the bow to be carried under the after part of the hull. This water may be of markedly different temperature from that at or below sensor depth (e.g., a thin, warm surface layer present on a hot, calm day). Mixing of this water with that below (at sensor depth) can supply fluctuating temperature readings (^ 0.5 F°). Thus the sensor, if mounted aft, would indicate variability, whereas water at or below sensor depth might at the time possess a high degree of uniformity. Thus operational decisions based on such "tactical" reading could be adversely affected. No effect occurs under uniform conditions brought about, say, by pronounced wind mixing; this fact appears to bear out the foregoing explanation. Thus a sensor mounting near the bow would appear to be the most logical one.

An assessment of oceanographic conditions along Line "P" in late summer - R.H. Loucks

A shipborne recording thermometer (SRT), designed by Mr. D.S. Street of the Pacific Naval Laboratory, was operated during daytime during a cruise from Esquimalt to Ocean Station "P" (50°N, 145°W) and return, in July, 1963, on the C.N.A.V. "Oshawa". The SRT.temperatures recorded, from the engine cooling water intake of the "Oshawa", westbound on July 15-18 and eastbound on July 21-23, are shown replotted in Figure 9. In addition, Figure 9 shows the Taylorgraph continuous temperature record from the engine cooling water intake of the weathership en route from Ocean Station "P" to the coast, August 1-5, 1963, together with the temperature structure defined by bathythermograms and oceanographic observations from the weathership.

The changes in temperature structure along Line "P" between July 15 and August 5, revealed by the continuously recording thermometers, are interpreted as manifestations of general heating and of increased currents in the neighbourhood of Long. 131°W. The currents are thought to have been initiated by clockwise winds. The wind stress would lead to converging Ekman flow and, thus, to convergence. This convergence would change the potential vorticity of the water column inducing barotropic flow southward. Convergence would also produce a "density trough" and, hence, baroclinic flow northward on the west and southward on the east. The data seem to support this suggested mechanism. B7 B6 B^W 134 LONOTUDE

Figure 9. - .33 -

On the vertical transport velocity on Line "P" in the eastern Subarctic Pacific Ocean - A. Acara

A general equation has been developed relating the vertical transport velocity in the sea to the meridional transport, which may be computed from oceanographic observations at two close stations when the depth of no-net horizontal motion is known. Starting with the continuity and geostrophic equations, the derived vertical transport velocity (WT) is:

WTl = ± v.^.z <3» S AD •Z •

where. § «2f (Rossby parameter) "P =s2(oSin^(Coriolis parameter)

V = mean meridional velocity

^5 = mean density Ty = meridional transport AD = D^ - D^ = difference between dynamic heights at two stations A and B

L = distance between A and ^ The vertical transport is dependent upon the parameter :jjr which varies from 0 at the poles to infinity at the Equator, and on the meridional transport (Ty ) which is a function of the curl of the surface wind stress. If only the earth's rotation is considered, the upwelling and sinking regions should be located at the lower and higher latitudes respectively. Further, the transport in the sea is proportional to the curl of the wind stress which creates regions of convergence and divergence, and hence causes vertical transports in the sea.

This method has been applied to Line "P". The bottom of the halocline has been assumed to be the depth of no-net horizontal motion. The calculated meridional transports (Ty ) and vertical transport velocity (\AJT ) in the halo cline layer along the line are shown in Fig. 10 and 11 respectively. North ward meridional transport is associated with upward vertical transport while southward transport is associated with downward transport. The upward and downward transports indicated divergent and convergent situations respectively. The magnitude of the meridional transport (Ty ) is 104 to 105 cm3/sec (Fig. 10); the vertical transport velocity (wT) varies from 10~5 to 10"4 cm/sec (Fig. 11) in the halocline layer along Line "P". I i i i i i i i i l VI i l '" I "I LINE UnU

Ocean StatTon'-

raciflc'ac/'fic Oceanoca

W! H6lHl.N1 135 MERIDIONA L TRA NSPOR T 3 .4 ( Cm/Sec x 10 ) W5WI5W.••• | ••.•135rfV ,,, , ,,,, 125y ffPW I35,,,,,. ttJ° 1959 ^16 14 i i i—| i i i • | | • ' ' ' I I I '"-r^r-r 1 I I I I I r Seot.18 __ -"SOUTHWARD I IM I I | I I I I I I I I IBigl I I NORTHWARD i i i i i i I i i i i I 1961 1J0T1I9i i i i I i i i "i 08,TTi i i i | i i i i

May 30 March 5 i 'f| • • ' ' ' | ' • ' ' I I i i i i l i i i i I i

May 31 „L7„ "FT i i qTi i-I—] i i '• • • i • i i mil Apr12 IP, 4"WPi \(\ i i'T i i i i i i i i i i i i i i i i i i i i i

,A;n™ gifr I i i i i I i i i i r~i i i i I i I i i I i i i i r—i i i i I Alh^23 MQV27 Jfii ' ii.ii feept.231 i i i b^e,28l""'"g ' piii i I i i I I I I I I I I' | i i • " | i i i i | •• i i MM Mi"]

Juh/3 IIHI ''aST' "' Dec.6 I i i i I I I I I I I I I I I ITT i I Dec.8I I I I lUUMMMUal I I I I I I ''I I I I I I Aug. 3' :• ... I n' ' I ' ' ' ' I ' ' ' ' 1962 Jon.21 1I •'• • • | • • '• » | I «HD | "TT-T-I

145 W 135 125 45W 135 125 1 ' » • • ' •••• I • • •• I •••• I i • i i i i i i i i i i •• i i • i i i j

Figure 10. LINE

^cean Station

Pacific W 451!! fi VERTICAL TRANSPORT VELOCITY ( Cm/Sec x 10 )

145 W 135 125 145 W 135 J25 I I I I I [ I I I I I I I I I I I ™f i " i i i " TTTfTTT 1959 Apr.16 A^4. 1 .. i i | i i ii i i i I i i i i I I111-Pfrr i i I i i i i i ISept" 13i i I i i i i | i i i 'bttffi|' UPWARD -*- DOWNWARD \ 1961 Jon 19 Apr17^^ 1—*" 1 i i i I I I I 'f PTI I | | i i I I | i i i I March 5 I i i i i | i i i i | i h May 30 I i i i i I•^^^nsp- i i i I i i i i V!ay3l 7A "i I,'.Jo1 ' | ' ' i I | \mA m- TT Apr12 \hmi^ i? T-r-rr-nr i i i I I i i i i I i i i i | '* Aug.22 | i i I i i •••••• i i i i i i 1 I I I I I I I I 1 I Aug.23 Mov27 ^ i i l i i 4* FT WA' I ""' r i i i I I i i i i •I i i i I ' ' ' • | ' ' I" I I I | I I I I fW ffl I I I I I I I ItttttMi T

145 W , , , 135 »f*5W • . l?5 . .,, ,,,,125 i i i i i i i i i i i i i i i i i. i i i |?5

Figure 11. - 36 -

On the intermediate water of the North Pacific Ocean - A. Acara

In the oceans, relatively low salinity water spreads at intermediate depths from the subpolar boundary regions towards the Equator, resulting in a layer of water (minimum salinity layer) of salinity less than that above and below in the Subtropic regions. The densities along the cores of the minimum salinity layer are almost identical (C^ « 27.25) in the Atlantic, South Pacific and Indian Oceans (Fig. 12). In the North Pacific there are two salinity minimum layers. The core of the primary layer is associated with a density surface of G£ = 26.75 1* 0.16 while that of the secondary salinity minimum layer is associated with a density surface of ^ = 25.31 - 1.10,

The primary salinity minimum layer in the Subtropic Region of the North Pacific Ocean occurs at depths of 100 to 200 meters in the vicinity of the Subarctic Boundary (Fig. 1) and between 500 and 700 meters at lower latitudes. Off the coast of Japan, it is found between depths of 750 and 900 meters (Fig. 13). The temperature in this layer lies between 6° and 8°C (Fig. 14).

The secondary salinity minimum layer occurs between depths of 30 and 300 meters, but is only observed east of Longitude 150°W (Fig. 13). The temper ature lies between 12° and 16°C (Fig. 14).

Formation of primary salinity minimum layer

The continuity of the isopycnal surface of G"^ =» 26.75 from the Sub arctic halocline layer southward through the Subtropic Region indicates that the formation of the salinity minimum layer occurs throughout the year in the halocline near the Subarctic Boundary. Furthermore, in winter, in the western Pacific, it can be formed by cooling and sinking of the surface waters from the Sea of Okhotsk and the Bering Sea.

Mechanism

Figure 15 shows the circulation at 400 meters relative to 1000 meters depth south of the Subarctic Boundary. From this circulation pattern, the southern limit of the isohaline of 34.0$, was determined (Fig. 16B). A near linear relationship between the southern extent of water of this salinity and the Subarctic boundary was obtained (Fig. 16C). It is shown that there is a pumping mechanism within the boundary region which generates and main tains the southward flow of the water in the salinity minimum layer. The energy required for this mechanism is supplied by the wind.

The calculated southward transport in the salinity minimum layer (26 T 13 x 10"m3/sec) agrees well with the calculated northward transport of the Pacific deep water (20 ± 5 x 106m3/sec) and observed transports. These results indicate that the transport in the salinity minimum layer depends on the rate of generation of the halocline water in the Subarctic Region. A schematic diagram of the features and circulation of these waters is shown in Fig. 17. The mean velocity in the salinity minimum layer is 2.8 t 1.4 cm/sec. T-S DIAGRAM OF IN TERMEDIA TE WA TERS ALL OCEANS

15-

ui K

335 340 345 350 SALINITY (%•)

THE NORTH PACIFIC OCEAN WESTERN EASTERN

a. I

Figure 12. 3 2 5 3 5 3

o •ri U-l •r-J O CO &4

X! •U u o z

(U -c

d •ni

ti o ft •u 3

>^ 4J

d •r-4 iH

3 CJO 1-1 Figure14. Temperature(°C)distributionin the NorthPacific Ocean. Figure 15. .• .J '.I 1. ••

40»N

40°N

SUBARCTIC c . «.rr,«r «*« BOUNDARY

35 40 LATITUOE «N SUBARCTIC BOUNDARY

Figure 16. (A) Schematicof circulationat 400 metres depth, (B,C) position of Subarctic Boundary and southern tip of isohalineof 34.0&, (D) relation between position of isohalineof 34.0%, and SubarcticBoundary, in the North Pacific Ocean, summer 1955. Figure 17. Schematic diagram of the circulationin the North Pacific Ocean. - 43-

COASTAL WATERS

Daily seawater observations - H.J. Hollister

Daily observations of surface seawater temperatures and the collection of samples for salinity determination were made at 13 locations on the B.C. coast in 1963 (Fig. 18). The majority of the sampling locations are situated at lightstations, and the observations are made by the lightkeeper. Daily water temperature observations of the Fraser River are made also at New West minster, B.C., by Department of Fisheries personnel.

This program is a simple means of providing data that reflect the annual and seasonal variations of surface oceanographic conditions in major regions of commercial fisheries importance o^ the B.C. coast. The records from several individual stations, when used as a group, will indicate variations that have occurred in the oceanographic conditions in the contiguous coastal ocean.

Seawater temperature conditions during 1963

i The monthly mean seawater temperatures during 1963 are presented in Table IV , along with the differences from the 1962 temperatures, and the anomaly classification indices. Each index represents the number of % stan dard deviation units there are in the difference of the monthly mean from the 10-year monthly mean. A positive index indicates a warm anomaly; a negative index a cold anomaly. Indices of 0 to 2 represent average conditions; indices greater than 2 represent anomalous conditions. This classification index system provides a standardized graduation of variable-sized anomalies, and as indices of the same scale have the same statistical significance, the anomalies at different locations can be readily compared.

The large number of positive classification indices for all the Stations reported in Table IV show that there was a predominately higher-than-average trend in the B.C. coastal seawater temperatures during the first 10 months of 1963. This warm anomalous condition was first noticed in the records from most of the Stations in October 1962, and has continued steadily since then, with only a few regional departures. An early peak in this warmer-than-average trend occurred in February and March. During the following 3 months the warm anomaly was still evident but no so great. In July, seawater temperatures were average, and at some locations in the Strait of Georgia, they were slightly lower than average. However, seawater temperatures increased rapidly in August and the warmer-than-average trend that was re-established in that month continued and increased into September and October.

As mentioned earlier, the data from the coastal observations can some times be used to recognize variations in conditions in the coastal ocean. The comparisons are easier to make when the conditions are considerably different from normal. Monthly sea surface temperature charts published by the U.S. Bureau of Commercial Fisheries at San Diego showed that in the first 10 months of 1963 the coastal ocean temperatures were 2 to 4 F° greater than the long-term mean. This is reflected in the warmer-than-average classification indices reported for the ocean coast stations at Langara I., Cape St. James, Kains I.., and Amphitrite Point. Also, when the coastal ocean temperature anomalies were at their largest in February, March, and September, so the Stations' indices were greatest. '»•! *?*L "4* "** »»»* '»'* '»o* '»»* '»«* '»** 'g» 124* 128* 122*

DAILY SEAWATER OBSERVATIONS

PACIFIC OCEAN

lll« >S4> lIV- 111* 111' 180" l»t>* 124* I2T* 124* 186* 124* 128* 122*

Figure 18. Location of stations making daily seawater observations. Table IV . Monthly mean seawater temperatures observed during 1963 at B.C. coastal stations

Station Jan Feb Mar Apr May Jun Jul Aug Sep Oct

Langara I. °F 44.8 45.5 44.9 45.8 48.5 50.5 52.9 53.5 54.2* 53.5* Class'n +1 +3 +2 +1 +2 +2 +2 +2 +2 +4 A1963-1962 F° +1*4' +2.8 +2.3 +1.3 +2.5 +1.8 +1.3 +2.0 +1.7

Triple I. °F 45.5 45.5 45.0 46.2 48.9 52.2 55.1 Class'n +1 +2 +2 +1 +1 +0 +1 A1963-1962 F° +3.0 +3.8 +3.2 +2.3 +2.7 +2.3 +2.4

Bonilla I. °F 44.5 45.6 45.3 46.6 50.0 52.2 52.9 53.6* 55.1* 53.4* A1963-1962 ; F° +2.4 +3.2 +3.6 +1.9 +2.4 +1.7 +1.4 +0.3 +2.7 +2.5

Mclnnes I. °F 45.2 45.7 45.6 46.8 50.1 52.9 56.0 56.9 A1963-9 yr avge F° +1.5 +1.9 +1.8 +1.0 +0.9 +0.5 +1.1 +0.5 A1963-1962 F° +2.3 +2.8 +3.1 +2.0 +2.3 +1.3 +2.2 +0.9

Cape St. James °F 46.5 46.5 46.4* 46.6 48.8 50.9 54.3 56.9 54.0 52.3* Class'n +1 +2 +2 +2 +3 +0 +0- +2 +0 +3 A1963-1962 F° +1.9 +2.4 +3.2 +2.0 +2.2 +1.8 +2.3 +3.5 -0.1 +2.8

Kains I. °F 47.4 47.4 46.8 48.6 51.6 53.1 55.5 57.2 59.9 56.7* Class'n +2 +2 +1 +1 +2 +0 +1 +2 +4 +5 A1963-1962 F° +2.7 +2.1 +1.5 +0.8 +2.1 +0.2 +1.3 +2.0 +6.0 +4.1

Pine I. °F 46.5 46.3 46.0 47.0 48.9 49.5 50.2 50.8 51.5 53.8* Class'n +2 +2 +1 +2 +2 +1 +1 +1 +3 +5 A1963-1962 F° +1.9 +1.4 +1.6 +1.3 +1.7 +1.1 +0.2 +1.0 +2.6 +3.4

Amphitrite Pt. °F 46.6 47.8 47.4 50.2 53.5 52.4 56.3 57.6* 57.8* 56.3* Class'n +0 +1 +1 +2 +2 -0 +0 +2 +3 +4 A1963-1962 F° +1.8 +1.7 +1.7 +1.2 +2.4 +0.5 +4.1 +2.0 +2.3 +1.4

Cape Mudge °F 45.9 46.4 47.2 48.3 51.3 54.7 58.6 58.5 57.8 53.1 Class'n +2 +1 +3 -0 -1 -1 +1 +2 +4 +4 A1963-1962 F° +1.8 +0.7 +1.2 +0.6 -0.6 +0.1 +2.0 +1.1 +4.2 Table IV (cont'd.)

Station Jan Feb Mar Apr May Jun Jul Aug Sep Oct

Chrome I. °F 44.7 46.0 46.4 48.5 54.2 58.8 60.2 64.0 58.7 52.8 A1963-1962 F° +0.5 +1.1 +1.9 +1.1 +0.7 +0.6 -3.5 +4.9 -0.3 +1.4

Entrance I. °F 43.1 45.5 46.6 48.8 55.8 60.0 61.9 64.2 61.3 54.5 Class'n -2 +2 +2 +1 +1 +1 -0 +1 +4 +4 A1963-1962 F° -0.4 +1.3 +1.9 +0.5 +2.7 +1.3 -0.9 +4.3 +2.1 +2.9

Departure Bay °F 43.1 44.9 45.8 49.0 55.3 59.7 62.4 63.7 60.0 53.6 Class 'n -0 +2 +2 +0 +0 +0 -1 +0 +2 +3 A1963-1962 F° +0.2 +0.9 +1.5 +0.4 +2.4 +0.2 -0.8 +2.9 +0.2 +2.5

East Point °F 45.8 45.8 46.3 47.2 49.7 51.6 53.4 53.6 52.8 50.7 Class'n +1 +2 .+3 +1 +1 +1 +0 +1 +1 +1 A1963-1962 F° +0.2 +0.4 +1.3 +0.5 +1.2 +0.4 +0.1 +0.8 -0.3 +0.3

Race Rocks °F 45.6 45.6 46.2 47.3 49.4 50.4 50.9 51.5 51.1 50.6* -p* Class'n +0 +0 +1 +0 +1 +0 -0 +0 +1 +3 A1963-1962 F° +0.6 +0.4 +0.9 +0.2 +0.6 +0.3 +0.1 +0.6 ±0.0 +0.5

Fraser River °F 37.7 39.5 40.8 44.7 51^2 55.6 60.1 64.4 62.6 53.9 Class'n -0 +1 +0 +0 +1. +0 -0 +1 +4 +4 A1963-1962 F° -0.5 +0.4 +1.6 +0.0 +1.8 +1.2 +0.9 +2.6 +3.8 +1.9

* Preliminary data, subject to revision - 47 -

Comparisons of anomalies in B.C. coast air temperatures must necessarily be considered when examining variations in coastal seawater temperatures. There was considerable similarity in the trends of air temperature variations and those of the seawater temperatures, .especially when the comparisons were made by geographic regions. Air temperatures were well above normal in February, and this is reflected in the significant increase in the seawater temperature anomaly for that month. The slightly lower-than-average seawater temperature conditions that were confined to the Strait of Georgia region during July occurred when air temperatures in that particular climatic region were lower than normal. A recovery to higher air temperatures in August was paralleled by a return to higher-than-average seawater temperatures in the same region. The considerably higher-than-average seawater temperatures in September are comparable to a 4 F° warm anomaly in air temperatures.

The anomalous warm conditions that prevailed during the first 10 months of 1963 are reflected also in the comparisons with 1962 conditions. Seawater temperatures during this period in 1962 were average or slightly lower-than- average, so the 1963 temperatures were appreciably higher than the previous year's. One significant exception to this general warmer-than-1962 trend was in July at the Strait of Georgia Stations, where a colder-than-1962 anomaly was observed for that one month. The stations in the northern coast region reported a greater warm anomaly than did those farther south.

Seawater salinity conditions during 1963

During the first 7 months of 1963, there were few significant departures from normal in the surface salinity conditions at most of the daily seawater stations. It was difficult even to recognize any common trend in the conditions at stations located in similar oceanographic and geographic regions. A few stations did record short periods of abnormal salinity conditions. The salinity at Langara I. during July and August was significantly higher than average, which could be attributed to a large deficiency in the precipitation amounts for that region during these two months. Much farther south, higher- than-average salinities were observed at East Point during the 4 months of April to July, and at Race Rocks during the months of July to September. Lower-than-average salinity conditions were observed at Entrance I. in January and February, but nowhere else in the Strait of Georgia region was this anomaly observed at the same time.

Oceanography of Dixon Entrance - P.B. Crean

Oceanographic and meteorological data from Dixon Entrance and its general environs have been examined with the object of determining oceanogra phic characteristics and associated causal sequences. Aided by experiments in a hydraulic analogue, a general model of oceanographic behaviour has been developed in terms of estuarine, tidal, wind and heat transfer mechanisms.

Figure 19 shows the geopotential topography of the surface of Dixon Entrance relative to the 125 decibar surface. This serves to illustrate two major features of water movements in the area. There is a net northward flow from Chatham Sound, which receives the major freshwater discharge affecting Dixon Entrance, past Dundas Island and into the southern part of Clarence Strait. Much of this flow moves seaward around Capes Chacon and Muzon. Part of this flow is retained in Dixon Entrance and recirculated in a large vortex w- -58*

LAT.

LONGITUDE I32» W.

Figure 19. Geopotential topography of Dixon Entrance, September- October, 1962. - 49 -

located approximately midway between Cape Chacon and Rose Spit. This vortex results from strong tidal movements in the northern Hecate Strait, adjacent to Rose Spit. It has been confirmed in the Hecate Model.

An annual cycle in the depths of isohalines and isotherms has been observed throughout Dixon Entrance, and is attributed to the annual cycle of prevailing winds over the offshore waters. Strong winds, predominantly from the southeast, restrict the estuarine discharge from Dixon Entrance, resulting in a depression of the isohaline surfaces in Dixon Entrance. In summer, predominantly northwest winds move*surface waters offshore enhancing the movement of brackish water out of Dixon Entrance. The isohalines rise during such periods of increased flushing.

Regularly monitored features in the region include observations of sea surface temperature and salinity, sea-level, river discharge and meteorological factors. These define four seasons 'in the oceanographic conditions and processes.

Winter

From November to March, the region is dominated by strong southeast winds which tend to hold surface waters in Dixon Entrance and onshore along the mainland coast. Monthly mean sea levels attain their highest values at this time of year (maximal conditions of wind and sea level occur in early winter, decreasing gradually later). Runoff is small and stems primarily from such precipitation as avoids retention in the mountain snow-fields. The seaward flushing of brackish water is weak and the amount of fresh water retained in Dixon Entrance is large. Isohaline surfaces are deep. This reten tion of brackish water constitutes the most important oceanographic feature of Dixon Entrance during the winter. Throughout this period, the sea is losing heat and by late winter near uniformity of temperature with depth exists throughout Dixon Entrance.

Spring

Through April and May, southeast winds decrease, and the winter accumu lation of brackish water is flushed seaward and isohaline surfaces rise sharply. Sea levels fall. The discharge from the major rivers increases rapidly. Heat flux at the sea surface is small as the period of winter cooling gives way to that of summer heating.

Summer

From June to August northwest winds' become predominant over the offshore waters, enhancing the movement of brackish water seaward. The major rivers attain full freshet. By late summer the surface salinities are least in Dixon Entrance and sea levels at Prince Rupert are at their lowest. The major flushing process, characteristic of the previous period, is much reduced and isohaline surfaces are shallowest. Throughout this period the sea is gaining heat and a marked thermocline exists. - 50 -

Autumn

Through September and October there occurs a marked increase in southeast winds. Monthly mean sea levels rise sharply. The depth of isohaline surfaces in Dixon Entrance increase as the seaward flushing of brackish water is reduced. Heat flux at the sea surface is minimal as the period of summer heating gives way to that of winter cooling,

The problem arises as to the definition of normal and abnormal conditions. A useful index of anomalous behaviour is available in the occurrence of unusual values in the daily observations of sea surface temperature and salinity which are available for various locations in the vicinity of Dixon Entrance over a period of several years. Also, the observed values of sea level at Prince Rupert may be used as an index of flushing in Dixon Entrance. In the present instance, fluctuations in sea level are largely accounted for by the wind and can be related to inverted barometric and steric effects (increased sea levels result from decreased barometric pressures and decreased mean densities of the water column, the latter occasioned by the onshore retention of brackish water under the influence of concomitant southeast winds). It would thus appear that daily observations of sea level, suitably averaged, would afford an approximate indication of unusual flushing conditions in Dixon Entrance.

Hecate Strait

Preliminary studies of data from Hecate Strait indicate that a dominant feature throughout the year is the retention of brackish water along the eastern shores and the continuity of more saline water northward, from Queen Charlotte Sound to Dixon Entrance, in the western part of the Strait. This appears attributable to the predominance of southeast winds in this area throughout the year. In winter, these winds are funnelled to great strength between the mountains of the Queen Charlotte Islands and the Coast Mountains of the mainland, leading to substantial transports of surface water into Dixon Entrance.

Hecate Model - W.H. Bell

The Hecate Model was built to study the relationship of tidal circula tion to the oceanographic structure and, subsequently, to derive the conse quences to the distribution and success of groundfish in the region.

Previously, tidal calibration of the model was made. Then, a two- fluid system was developed to give density gradients similar to those observed in nature. A comparison of model and prototype density structures is shown in Figure 20 . Suitable gradients were obtained after the model had been in operation for about 3 hours. These gradients were maintained for at least an additional 4 hours.

Because suitable density gradients were obtained for such a lengthy period, it was concluded that natural flushing of the region was unimportant compared to the effect of tides and basin geometry. Thus, it was not neces sary to install a complex plumbing arrangement to duplicate flushing. Siqmo-t units c—i—i—n-

COMPARISON OF PROTOTYPE AND MODEL

DENSITY STRUCTURES

E 9>

O 0-

1001— #o

o o

• Prototype (January 15, 1962) O Model (mixing in progress for 200 minutes)*

1000t

Figure 20. - 52 -

The foregoing experiments set the scene for making observations of sur face currents in the model. These were made by taking time-exposure photo graphs of confetti particles on the water surface. The water in the model was dyed red, and a blue filter was used on the camera. This provided excel lent contrast between the white confetti particles and the background. In shallow areas, where the depth of the dyed water was not sufficient to absorb all the blue light, the bottom was painted black. The confetti was 1/4-inch diameter loose-leaf punchings. The camera was fitted with a wide-angle lens and was located about 15 feet above the water surface. The aperture setting was f:4 for Tri-X film with illumination provided by a 1000-watt mercury vapour lamp. The shutter was tripped by a device using a rotating cam. This provided constant exposure times for a series of photographs and constant film transport times between photographs. Each photograph represents slightly more than one hour in prototype time. Flow directions could be determined by shielding the camera aperture for a short period of time just after the beginning of an exposure (causing a break in the streak on the film), or by following specific particles in successive photographs (with the aid of a tracing paper overlay). This latter method was also used to obtain resultant current vector patterns. An example of a velocity field photograph is shown in Fig. 21. It also clearly illustrates the convergence of the tides from the Dixon Entrance and Queen Charlotte Sound approaches. This convergence in the model is in excellent agreement with the co-phase lines found in the prototype.

Complete photographic coverage of the model required eight camera positions. Adjacent pictures overlapped one another by various amounts. A total of 16 consecutive photographs, similar to Figure 21 , was taken at each position to provide coverage over a complete tidal day. Both spring and neap tide sequences were used. Similar tidal amplitudes for each position were chosen on the basis of tide table predictions and verified later from the model tide records. The resultant surface currents for a spring tide are shown in Figure 22 .A great degree of similarity existed between the resul tant current patterns for both spring and neap tides, again suggesting that basin geometry is a governing factor in this region.

A large gyral circulation pattern can be noted in Figure 22 in the Dixon Entrance area. This feature was verified in prototype current and density structure data. A study to determine the probable driving mechanism was made. The flow was restricted by sandbags at various locations. Some results of this experiment are shown in Figure 23. With sandbags completely isolating Dixon Entrance from Hecate Strait, the resulting flow in Dixon Entrance is small. Shallow openings were made in the sandbags both east and west of Rose Spit, as indicated in the middle view of Figure 23. Flow through these openings generated gyral patterns, as shown. Complete removal of the sandbags (bottom view) indicated that the resulting Dixon Entrance gyre, which overrides the other rotational features, is driven by the stream of water flowing north past Rose Spit from the Hecate Strait banks.

The determination of sub-surface water movements was difficult because of the three degrees of freedom involved. Several suggested methods were rejected. Dye patches diffused too rapidly to be of much use. Neutral- buoyancy oil drop mixtures, when used in a model as large as the Hecate Model, were considered to be too difficult to distribute properly and, especially, to remove after an experiment. Sub-surface drag vanes attached to a surface float suffered the disadvantage of rapidly running aground near Figure 21. Time exposure showing surface water movements in Hecate Strait. LU Q O Ui o z « < q: a E

c 0) UJ O u. 15 o O LU o LU o -J X X < O UJ CO 2

UJ LU X o o H -J LU z > CO UJ Q Q O tr LU CM if) a. CM

LU z O f-l X (X4 I en to q: CL CM c/) o

LU LU > o o z CM LU q:

LU C/) a: O ' <

CO LU z -I < O § CO CO LU LU O 3 c/) UJ CO rr r ^ or vat cticnRaMvtzBi

SURFACE TRAJECTORIES IN DIXON ENTRANCE FOR VARIOUS FLOW RESTRICTIONS

USING A SINGLE FLUID AND A 15-DAY PERIOD

Figure 23. - 56 - the regions of particular interest in the model, as well as giving only two components of the fluid motion.

It was finally decided that ping-pong balls would make useful sub surface floats when adjusted for neutral buoyancy at some appropriate depth. The balls first had a 3/8-inch hole drilled in them. This was covered by gluing on a 1/32-inch piece of sheet rubber of suitable area. Then, by inserting a hypodermic needle through the rubber, the balls were filled with fresh water. The rubber provided for expansion and contraction due to temperature changes. If the changes were very large, inspiration or expira tion could take place through the small puncture. It was also found useful to use fresh water which had been filtered and chlorinated and to "strip" the water of dissolved gases by running it through a column of Berl saddles under a high vacuum. Final density adjustments were made by suspending a length of fine wire (#26 Cu) from a loop of thread glued to the bottom of the ball. Incremental changes in density were made by cutting off small pieces of the wire. The method of suspension of the wire prevented the float from running aground since, as soon as the end of the wire touched bottom, the effective density of the ball was reduced. The floats were acclimatized before use by storing them in a container of fresh water immersed in the model.

The major problem encountered in the use of neutrally-buoyant floats was that of recording positions or movements without resorting to elaborate photographic techniques. If only horizontal movements are of interest, these can be recorded on film by a camera suspended above the model. However, it is not possible to distinguish between vertical and horizontal movements of sub-surface floats in such photographs. Refraction reduces the error in horizontal measurements due to vertical movements (by reducing the apparent distance over which motion takes place), but introduces an error of its own which depends on the depth of the float and the horizontal distance of the float from the camera centre-line. Corrections can be made for this latter error. Thus, this method was useful for observations in regions where vertical movements were small. Where both vertical and horizontal movements were important, the simplest technique available appeared to be that of graphically recording visual observations. A relatively small portion of the model, con taining only a few floats, was viewed by several observers at the same time. These observers sketched motions in the three component directions by referring them to previously established reference points; e.g., cork floats anchored to the bottom with string which was knotted at intervals.

The results of the above experiments have been used in the interpre tation of data from past cruises in the Dixon Entrance region and as an aid in the exposition of the oceanography of the area. - 57 -

Early sea life of salmon - A.J. Dodimead and R.H. Herlinveaux

Intensive studies of young salmon in their coastal environment have been made in Burke Channel, Fitz Hugh Sound, Nalau Passage and vicinity, in the central British Columbia coast (Fig. 24). A prime purpose of this work is to determine the mortality of young salmon from the time they first enter salt water until they leave the coastal waters; how the mortality changes within a season and from season to season; and what external and internal factors are detrimental to or favour their survival. This investiga tion is under the direction of Dr. R. Parker of the Biological Station, Nanaimo, B. C.

The principal stock in this region, and the one currently under investi gation, is the pink salmon run of the Bella Coola River which flows in at the extreme head of Burke Channel (North Bentinck Arm). These fish first enter salt water about mid-April. During the latter part of this month they are abundant in North Bentinck Arm. From here they quickly spread down Burke Channel and across Fitz Hugh Sound to Nalau Passage but do not appear to penetrate, in significant numbers, into Fisher or Dean Channels, nor do they follow the east shores of Fitz. Hugh Sound. By mid-June most of these fish have passed through Nalau Passage into the open waters of Queen Charlotte Sound.

When the fish first enter the sea, they quickly form schools. Initially they are in close contact with the shores, and generally are found along the eastern shores of islands and points of Burke Channel and on the eastern shores of Fitz Hugh Sound and Fisher Channel, but not far removed from the mouth of Burke Channel. Shortly thereafter, the affinity for the shore is lost and schools are commonly sited in centre channel as well as along boundaries. This change in behaviour is associated with a general exodus of pink salmon from the enclosed waters into Queen Charlotte Sound. Throughout the period spent in enclosed waters, the juveniles appear to occupy only the immediate surface layer (2-3 fathoms).

Based on these general patterns of movement and behaviour (2 years of observations), an oceanographic program was undertaken this year (1963) for the purpose of instituting and developing the ecological aspects of the studies of this stock.

Oceanographic program

The oceanographic program consisted mainly of measurements of tempera ture, salinity and currents, particularly in the surface waters, at the same time as the biological studies on this stock.

The base of operations was a barge (125' x 75'). This platform pro vided excellent living and laboratory facilities. From this base camp, sea operations were carried out from aboard three vessels, "Melibe", "Noctiluca" and "Remora", all about 30 feet in length. These vessels were either built or adapted for specific tasks in the operation. Most of the oceanographic measurements were made'from aboard the "Remora", a 26-foot research gillnet boat, adapted for this phase of the work. Surface observations were obtained from the other two vessels during the time they were being used to scout and sample the schools of fish. 128° 127"

Figure 24. - 59 -

From April 12 to May 12, the base camp was anchored in Whiskey Bay, North Bentinck Arm (Fig. 24). Oceanographic observations were started on April 18. During this period, oceanographic observations from aboard the "Remora" were confined to the area from the head of Burke Channel (North Bentinck Arm) to and in Labouchere Channel.

On May 12, the barge was shifted from Whiskey Bay to Nalau Passage (Fig. 24) to carry out the next phase of the operation. Surface samples were obtained during the passage down Burke Channel. Operating from the base camp in Nalau Passage, oceanographic observations were made in the lower part of Burke Channel, Fitz Hugh Sound, Nalau Passage and adjacent areas. These observations were terminated on June 5.

Although no detailed oceanographic observations were made in the central portion of Burke Channel, a monitor of surface conditions was obtained through out the length of the Channel on May 12 and May 27. Observations were also made by the Institute of Oceanography, University of British Columbia (May 16-19).

In addition to these observations, surface and one-meter samples were obtained at the time of fish surveys and sampling.

From these combined data it is possible to define the oceanographic environment (salinity, temperature and currents) at the time the young fish were inhabiting these coastal waters.

Results

In some areas, the tidal and residual currents appear to be the dominant factor determining the distribution and movement of the small fish.

A. Burke Channel

Burke Channel is a typical estuarine system, as a result of the large fresh water runoff into the head of the channel. The net-circulation and water structure of such a system has been deduced. There is a net-seaward motion in the surface water which is a consequence of the discharge of fresh water into the head of the Channel. Being light, it overruns the sea water and as it moves seaward gains in volume by entrainment of saline water from below. To compensate for the entrainment of saline water into the outflowing surface layer, there is a net-subsurface inflow. The principal features of the salinity structure are an upper zone of brackish water, a marked halocline, and a lower zone. However, because of such factors as tides, variable winds and runoff, the circulation pattern and salinity structure and its distribution vary considerably over short periods of time.

Burke Channel can be divided into 3 distinct oceanographic areas, designated Area I, II and III (Fig. 24). This division is based on the salinity and/or temperature features of the surface waters. The longitudinal distribution of surface temperature and salinity for Burke Channel for three different periods in May is shown in Fig. 25. From its head to Labouchere Channel, there was a fairly marked salinity gradient (salinity increasing to seaward). Temperature gradients were also common over most of this area which is defined as Area I. Area II extends from Labouchere to the vicinity of Restoration Bay. Within this area surface salinity and temperature / f // / / 4 JST ;?

LONGITUDINAL DISTRIBUTION OF SURFACE SALINITY

(from Bella Coola to Edmund Point)

AREA 3 -AREA 2 •AREA I

/ / <£/ Ob 4* /

LONGITUDINAL DISTRIBUTION OF SURFACE TEMPERATURE I6°-| C. (from Bella Coola to Edmund Point)

I4e

I2e

I0C

AREA 3 AREA 2 -AREA I

Figure 25. - 61 - changes were relatively small. Area III is again associated with fairly marked surface gradients which are a result of mixing because of the pronounced sill near the mouth of Burke Channel (Fig. 24). The sill depth is approx imately 37 fathoms.

Windy Bay. Early in the season, large concentrations of pink salmon were observed in Windy Bay, particularly along the shores. Current observations suggest that surface waters from as far as mid--channel may be directed onshore in Windy Bay during certain phases of the tide. Furthermore, a clockwise gyre can form which tends to conserve some of the surface waters in this area. This latter feature is apparent in Fig. 26 which shows the results of one- meter current observations during the ebb and flood tide. Some of the waters moved out to mid-channel and presumably moved down-channel on the following ebb tide. Thus, the tidal currents in this area offer a means of concentrating the young fish along the shore and also of maintaining some of them in Windy Bay.

Junction of North and South Bentinck Arm. The results of surface and one-meter floats released on the ebb tide are shown in Fig. 27. Near the northern shore the movement was down-channe1. Floats released in mid-channel moved across the mouth of South Bentinck Arm and directly onto the southern shore of Burke Channel. Floats released near the southern shore started across the mouth of South Bentinck Arm and then up the centre of the Channel. How ever, wind was a dominant factor in this latter movement. The following day, under conditions of no wind, the surface movement from near the southern shore was directly across the mouth of South Bentinck Arm. This flow was in the form of a jet stream directed onto the southern shore of Burke Channel. These ebb tidal currents offer a means of transporting the fish across the mouth of South Bentinck Arm and onto the southern shore of Burke Channel where large concentrations of fish have been observed in the vicinity of Menzies Point.

Junction of Burke and Labouchere Channels. In the southern portion of Labouchere Channel, the near surface flow, during the flood tide, was south ward into Burke Channel (Fig. 28). Furthermore, south of the junction, the flow from the central to the western side of Burke was towards the mouth of the Channel. Further up Labouchere, in the vicinity of Deas Point, the surface flow during the ebb tide was toward Burke Channel. It appears from the results of these current observations, that there is a pronounced net southerly movement out of Labouchere into Burke Channel. As a result, Burke Channel surface waters do not penetrate into Dean Channel. It is postulated that these currents restrict the Bella Coola pink salmon to the Burke Channel system.

B. Fitz Hugh Sound

Previously, no detailed oceanographic investigations had been carried out in this area. During the present investigation, sufficient observations were made to define some of the principal oceanographic features of this area.

Temperature and salinity sections were taken across Fitz Hugh Sound during mid-flood and ebb tide periods on consecutive days (Fig. 29). These sections show that on the ebb tide, surface salinities were lowest along the western shore. The slope of the isohalines and isotherms in the upper 20 NORTH BENTINCK ARM

AVERAGE VELOCITY 0.3 KNOTS 0.3 KNOTS 0.2 KNOTS

TIME (hours) 12 18 I I I | I i i I I | I i I I I

CURRENT OBS. AT

I METRE DEPTH 52!20'

TIDE CURVE (Bello Bello) '•''•'''»'•'•'•APRIL 29,1963

TALLHEO PI 126° 59* 126° 55' 126° 51' Figure 26. o SURFACE *> -a | METRE

TIDE CURVE (Bella Bella)-MAY I, 1963 i i i 1 i i i i i I • i •• i I i t i i i

127°Oftl101 126° 57'

Figure 27, 52? 22'

127° 13' 127° 09'

Figure 28. Figure 29. - 66- meters infer a marked cross-channel velocity gradient on both phases of the tide. Also there is a reversal in the slope of these lines from.mid-ebb to the mid-flood tide. The configuration of the isohalines and isotherms below the halocline suggest that during the mid-flood period, the movement is north ward along the eastern side of Fitz Hugh Sound and southward along the western side. In part of the water column this flow was reversed on the ebb tide. Thus, these sections suggest a net or continuous southward movement on the western side and a net northward movement on the eastern side of the Sound. This circulation pattern is confirmed in the current observations. Drogues at one-meter depth were released at the start of the ebb tide at three posi tions across the mouth of Burke Channel. The drift of these floats is shown in Fig. 30. The drogue released in the centre of the Channel moved in a south west direction across Fitz Hugh Sound during the ebb tide and then continued southward, during the flood tide. The initial direction of the float released near the northern shore was first influenced by the ebb movement down Fisher Channel. However, once it encountered the central part its movement was similar. The float released near the southern shore moved southwestward on the ebb tide, but reversed direction on the change of the tide and moved back to the central part of Burke Channel. Presumably, on the following ebb tide it would move across Fitz Hugh Sound, similar to the other two floats. The flow in the central part of the mouth of Burke Channel appears to be in the form of successive jets across Fitz Hugh Sound.

This flow offers a mechanism by which surface water at the junction of Burke Channel and Fitz Hugh Sound may be moved to mid-Channel and subsequently carried across Fitz Hugh Sound. This mechanism is consistent with the observed distribution of fish in the vicinity of Burke Channel. Furthermore, they are again observed on the western side of Fitz Hugh Sound. 128*00' I27°50'

£%•« (}j

$ B% King Island

Jtir

#« V

TIDE CURVE (Bella BeBo) MAY 20,1963 i • • I . • • • t I • i i • i I i li I

Figure 30. - 68 -

SPECIAL OR SUPPORT PROJECTS

Oceanographic support for Pacific Naval Laboratory projects

Oceanic turbulence - R.H. Herlinveaux

The oceanic turbulence studies, under Dr. H,.L. Grant's direction are a continuation of the studies carried out last year. The chief purpose of the work is to measure the temperature spectrum under a number of oceanographic conditions. Specially designed equipment mounted on an underwater vehicle is used to measure the water velocity and associated temperature micro-fluctua tions at selected depths. The oceanographic observations, taken by Pacific Oceanographic Group personnel, are used to monitor the whole profile and indicate the range and amplitude of the large-scale variations. Two operations, in the ocean waters off Vancouver Island, were supported.

Operation ICEPACK IV - H.J. Hollister

The purpose of this operation was to measure the variations of under water explosive-sound transmission under an extensive ice-cover, in water depths of 1000 fms. The survey party of 5, including an oceanographer from P.O.G., was under the direction of Mr. J.R. Brown of the Pacific Naval Laboratory, Esquimalt, B.C. The party joined the Department of Transport ice-breaker C.C.G.S. "John A. Macdonald" at Resolute Bay, N.W.T., on August 31. A suitable sheet of ice, 6 feet thick, was eventually located on September 3 in Prince Regent Inlet, although the depth of the water was only 200 fms. The P.N.L. team set up the equipment on the ice-pack and underwater acoustics experiments were conducted for 3 days, September 4, 5, and 6. During that time, the oceanographer made a daily serial oceanographic cast,.and . hourly bathythermograph casts during the daytime whilst the acoustics exper iments were underway.

The oceanographic observations were made from the drifting ship, which was hove-to approximately 5 miles distant from the acoustics camp on the ice-pack. During the 3 days, the ice-pack in Prince Regent Inlet drifted in a southwest direction, and the depth of the water decreased from 200 fms to 150 fms (365 to 275 m). The oceanographic stations and BT observations were made along a 35-mile line!parallel to and approximately 10 miles distant from the eastern shore of Somerset Island.

Oceanographic conditions

The surface seawater temperature was generally -1° to +2°C throughout the 3-day operational period. The temperature structure observed in the 30 bathythermograms obtained during this period showed a very slight positive gradient of about 0.3 C° (sometimes reaching 0.5°) extending from the surface to a maximum temperature located between 15 and 30 m depth. This shallow temperature maximum was followed by an equally slight negative gradient to a depth between 65 to 80 m. From about 75 m to the maximum BT depth of 275 m, the temperature increased to about 0.9°C at 250 m depth. - 69 -

Surface salinity samples were obtained along the line of observation at the same time as the hourly BT casts. Throughout the 3-day period, the salinity varied from 28.7 to 29.8 %>• The salinity structure obtained from the oceano graphic station data showed the top of the halocline at 18 m and the bottom at 30 m, with the salinity values at the lower depth ranging from 31.5 to 32.0 #o. The salinity then increased gradually to an average value of 33.9$, at 250 m.

Sound velocity conditions

Sound velocity data were computed from the oceanographic station data by the Canadian Oceanographic Data Centre, Ottawa, Ontario. The slight positive and then negative temperature gradients to 75 m depth did not create any sig nificant duct or channel in the sound velocity field, and in effect the temperature structure in this upper zone could be considered isothermal. The sound velocity structure showed an overall positive gradient from the surface to the deepest sampling depth of 300 m. There was an increase from 1436 m/sec at the surface to 1439 m/sec at 30 m, followed by an iso-velocity structure to 100 m. This shallow positive gradient is due largely to the appreciable change of salinity from the surface to the bottom of the halo cline. Below 100 m, the sound velocity increased regularly to 1440 m/sec at 250 m.

The oceanographic observations indicated that a fairly stable water mass was present, especially below 30 m, in the area of acoustics operations, and it could be considered that a constant sound velocity field prevailed throughout the three-day experiment.

Scattering layer - R.H. Herlinveaux

A preliminary study of. the acoustic response of various materials and objects was carried out during the period February 14-18, 1963, in conjunction with scattering layer investigations. The importance of fish air sacks in the signal strength return from fish was also investigated.

The echo sounder used was a Kelvin Hughes model 29F mounted in the hull of C.G.S. "A.P. Knight". This echo sounder operates at 30 kilocycles.

Numerous targets of various material were attached to a BT wire and lowered over the side into the sounder beam path. They were then lowered in steps of 3 fathoms until all targets had disappeared except a reference target..

The results of this work are shown in Table ".V . This table shows that the air sacks in fish had no effective signal strength. Yet a plastic bag filled with air gave a better signal than one filled with saline water. A hollow aluminum float gave a better signal than a hollow glass ball. A flat steel surface gave a better signal return than a styrofoam target of similar size and shape.

It is realized that the physical features such as shape and density through the target are important, yet the hardness and firmness of the reflecting surface is also very important - even more important than an encased air cavity. Table V

Inside Depth Object Shape Dimensions Medium Observable

(fms.)

Plastic solutions bag saline water sphere 8" diam 30-40 Plastic solutions bag air sphere 8" diam (surf.) 50-60 Hollow aluminum float air sphere 8" diam >75 Hollow glass float air sphere 7" diam 40-50 Tank, steel air disc 8" diam 4" deep >100 Tank, steel water disc 8" diam 4" deep >100 Solid, styrofoam disc air pockets disc 8" diam 4" deep 100 o Fish - hake flesh and air sack 3 fish 18" long 3" thick 80 Fish - hake flesh and air sack 3 fish 18" long 3" thick 80 Fish - whiting flesh and air sack 3 fish 18" long 3" thick 80 Rockfish flesh and air sack 3 fish 13" long 3" thick >50 Dogfish flesh and no air 3 fish 13" long 2j" thick >50 sack - 71 -

Correspondence of slicks and water temperatures in Juan de Fuca Strait - R.H. Loucks

It was noticed, in Juan de Fuca Strait, on July 23, 1963, that the SRT was recording widely varying temperatures and that the warmer temperatures occurred in slicks while the colder temperatures occurred in ruffled areas. These alternate patches of warm water (slicks) and cold water (ruffled areas) are interpreted as indicating the presence of random internal waves whose energy is extracted from the tides.

Cloud interference - ART - W.H. Bell

Experience has shown that undercast clouds interfere with the sea's black body radiation so that the airborne equipment records a low temperature. An analysis of the interference factors and their effect have been made.