Bedford Instituteof Oceanography

The Bedford Institute of Oceanography (BIO) is the principal oceanographic institutionin Canada; it is operated within the framework of several federal government de-partments; its staff, therefore, are public servants.

BIO facilities (buildings, ships, computers, library, workshops, etc.) are operated bythe Department of Fisheries and Oceans, through its Director-General, Ocean Scienceand Surveys (Atlantic). The principal laboratories and departments are:

Department of Fisheries and Oceans (DFO)= Canadian Hydrographic Service (Atlantic Region)= Atlantic Oceanographic Laboratory= Marine Ecology Laboratory= Marine Fish Division

Department of Energy, Mines and Resources (DEMR)= Atlantic Geoscience Centre

Department of the Environment (DOE)= Seabird Research Unit

BIO operates a fleet of three research vessels, together with several smaller craft. Thetwo larger scientific ships, Hudson and Baffin, have global capability, extremely longendurance, and are Lloyds Ice Class I vessels able to work throughout the CanadianArctic.

BIO has four objectives:(1) To perform fundamental long-term research in all fields of the marine sciences (and

to act as the principal Canadian repository of expertise).(2) To perform shorter-term applied research in response to present national needs, and

to advise on the management of our marine environment including its fisheries andoffshore hydrocarbon resources.

(3) To perform necessary surveys and cartographic work to ensure a supply of suitablenavigational charts for the region from George’s Bank to the Northwest Passage inthe Canadian Arctic.

(4) To respond with all relevant expertise and assistance to any major marine emergen-cy within the same region

W.D. Bowen - Chief, Marine Fish Division, DFO

M.J. Keen - Director, Atlantic Geoscience Centre, DEMR

A.J. Kerr - Director, Atlantic Region, Canadian Hydrographic Service, DFO

K.H. Mann - Director, Marine Ecology Laboratory, DFO

G.T. Needler - Director, Atlantic Oceanographic Laboratory, DFO

D.N. Nettleship - Seabird Research Unit, Canadian Wildlife Service, DOE

On the cover:

An engraving of “The Glacier of Sermiatsialik, Greenland” from:Adams, William Henry Davenport. 1876. The Arctic World: Its Plants,Animals, and Natural Phenomena, with a Historical Sketch of ArcticDiscovery down to the British Polar Expedition, 1875-76. London:T. Nelson & Sons: p. 129.

Climate change and variability is the theme of our BIO Review this year. The peren-nial ice cover in polar regions has a profound effect on our world’s climate and,among oceanographic institutes, BIO is particularly active in carrying out researchand survey work at high latitudes. Many of the examples of our climate-relatedwork included herein are based on data collected on ship voyages to the CanadianArctic and adjoining areas.

change and variability

I n the southern winter of 1982, unusually strong southerlywinds developed in the Tasman Sea extending from southernNew Zealand nearly to the equator. These winds were thefirst evidence of the global weather disasters of the twosubsequent years. They initiated unusual westerlies in thetropical Pacific that then led to the strongest El Niño of thecentury; soon we read and heard of floods and storms inCalifornia and western South America, droughts in southernAfrica, Indonesia, and China, and failure of the monsoon inIndia.

It also quickly became common knowledge that all theseevents, which cost many lives and hundreds of millions ofdollars in property damage, were in some way caused by amajor change in ocean circulation in the tropical Pacific,itself connected with global changes in our weather patterns.If it did not become a household word, at least very manypeople now knew about El Niño and its consequences. Herein eastern Canada, 1982-1983 became known as the winter-that-wasn’t with quite important consequences for energy-consumption, and a lot of frustrated skiers. For the first timein decades, the coastal deserts of Peru were carpeted withflowers.

Since 1982, the ocean science community has been hard atwork trying to piece together exactly what did happen. Aswell as being the most important event of its kind this century,it was also the best studied because both oceanographers andmeteorologists have had El Niño studies as an important partof their agenda for several decades now. It is clear today that,associated with the events in the tropical Pacific, anomalousconditions in the ocean existed as far away as the Gulf ofAlaska and over much of the Atlantic.

Not only was the changed pattern of ocean circulationassociated with changed weather patterns, but it also hadimportant consequences for life in the ocean and for fisheriesresources. Sea lions and marine iguanas suffered in theGalapagos, seabirds failed to breed on many Pacific islands,and the great fisheries of the Humboldt Current suffered yetanother major change: anchovy, sardine, scallop, and bonitofisheries were all affected, for better or worse, and in severalparts of the ocean distant from the eastern Pacific accounts arebeginning to accumulate of northerly or southerly shifts inspecies’ ranges.

Perhaps coincidentally, perhaps because we were allsensitized by these events to the possibility of instabilitiesin our environment, public awareness began to grow duringthe same period about a much longer term process likely tochange the global climate: unlike El Niño, this change willbe caused by us. Again, the ‘greenhouse effect’ is not yet ahousehold word, but it is already well known by many peoplethat our industrial, agricultural, and transportation industrieshave directly contributed to increasing concentrations ofcarbon dioxide in the atmosphere in the last century since thestart of the industrial revolution; we expect this apparentlyirreversible trend will raise global temperatures over the nextcentury enough to shift climatic and agricultural regions,modify sea level, and wreak other havoc.

As with the El Niño phenomena, it is now widelyunderstood by the general public that the ocean has animportant role to play in determining how fast the‘greenhouse effect’ will change our climate: to an importantextent, the rapidity with which the ocean absorbs carbondioxide from the atmosphere, either by simple solution or byincorporation in the marine food chain, will determine howrapidly this gas and others, which also trap heat in theatmosphere, will in fact build up.

Now firmly in the public consciousness, this arrayof problems has preoccupied meteorologists and

Alan Longhurst.

1

oceanographers for at least a century. About 100 years ago,the meteorological service of India began seeking statisticalcorrelations between failure of the Indian monsoon, causingthe catastrophic famine of 1877, and other indices of weather- such as surface air pressure in distant parts of the Indo-Pacific region. By the early 1900s, the Director-Generalof Observatories for India, Gilbert Walker, had in factdiscovered the basic mechanism that drives El-Niño events.We now know that part of the global El-Niño event is oftendrought - or failure of the monsoon - in the Indiansubcontinent. In a listing of the occurrence of El Niño in thehistorical record, it is no surprise to find that of 1877-1878listed as one of the 14 greatest of the last 200 years.

What has all this to do with Canada, and Canadianoceanography? If you are a farmer in southern Saskatchewanin the great dry summer of 1984, you may wonder if what youare suffering, and what may well drive you off your landbefore the year is out, was predictable so that you could haveso ordered your farm business as to ease the shock. If you arean inshore fisherman off Nova Scotia during the samesummer, you may well wonder if the plague of southerndogfish, useless to market yet preventing your normal fishing,are brought by changes in ocean circulation this year and - ifso - could the event have been predicted? You may not knowthat what ails you may have its roots in processes studied andbeginning to be understood by oceanographers, includingthose of your Department of Fisheries and Oceans, but youknow that something is wrong.

It seemed natural, then, in place of the regional survey towhich we expected to devote our BIO Review ‘84, instead todevote it to discussing some of the ways this Institute is, andhas been, studying the difficult scientific problems that haveto be solved before we can usefully and operationally predictthe kinds of events that plagued us in 1982-1983, or that weexpect to influence the lives of our children. BIO does nothave a climate research programme as an organizationalcomponent of its work: rather, the problems of variability inthe marine environment are studied as components of almostall oceanographic, some geological, and some hydrographicprojects.

The range of climate-related activities at BIO is very large,from studies of how, and how fast, carbon dioxide passes

between air and sea water at the surface of the ocean to theconsequences of between-year differences in arctic ice coverfor shipping in the Northwest Passage. The variability ofancient climates as recorded in the strata in cores of deep-seasediments is studied by geologists, and the influence ofbetween-year variability on the reproduction of fish stocks inthe Northeast Atlantic is studied by biologists. Staff of BIOare active in planning for various components of the nationaland international climate research programmes that are veryactively being put together in response to our new perceptionsof how ocean variability impacts on our national economySome projects actually produce long-term data, on inshoreseawater temperatures and coastal sea levels for instance,which will serve as basic information about changes as theyoccur. Other programmes, such as a routine trans-Atlantictemperature section from Halifax to Europe, will soon beinitiated to provide some Canadian content to such data beingcollected actively by many nations.

The individual contributions in this Review are notintended comprehensively to cover all climate-related workat BIO; for this, the reader is referred to our regular list ofindividual project descriptions of all of our activities. Theprincipal descriptive chapters provide only a selected samplerof the whole.

The final chapters of BIO Review ‘84 comprise our nowfamiliar annual survey of relevant information about theInstitute: publications, voyages, research and survey projectsare all listed, as are the statistics of some of the facilitiesavailable at the Institute.

It is no coincidence that our Review this year contains anote on the 1984 Huntsman Award presentation to anoceanographer who has been investigating our planet’spaleoclimates and who spoke at the award ceremonies onhow analysis of these past climates is useful in interpretingpresent-day changes and predicting the likely future changesin our climate.

- A.R. LonghurstDirector-General

Ocean Science and Surveys, Atlantic RegionDepartment of Fisheries and Oceans

2

Contents

CLIMATE CHANGE AND VARIABILITY . . . . . . . . . . . . . . . . . . . . . 1

1. PALEOCLIMATOLOGY - PAST STATES OF THE OCEAN . . . 5

Climate and the geologic record by C.T. Schafer,P.J. Mudie, and J.N. Smith . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 6

Paleoclimatic models from fossil records:A case history in Lake Melville, Labrador by G. Vilks . . . . . . . . . . . . . . . 9

2. OCEAN CIRCULATION AND CLIMATE CHANGE - THE NORTHATLANTIC OCEAN . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 13

Gulf Stream studies by R.M. Hendry . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 13

Towards a world climate research programmeby F.W. Dobson and S.D. Smith . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 16

Sea-surface temperature trends and patterns in thenorthwest Atlantic by R.W. Trites . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 18

3. THE INFLUENCE OF THE ARCTIC . . . . . . . . . . . . . . . . . . . . . . . 21

Arctic run-off in the North Atlantic Oceanby J.R.N. Lazier . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 21

Sea ice as an indicator of climate changeby G. Symonds . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 24

Climatic change and the exploration of theCanadian Arctic by sea by A.J. Kerr and K. MacDonald . . . . . . . . . . . . . 26

4. BIOLOGICAL FEEDBACK AND EFFECTS . . . . . . . . . . . . . . . . . 30

Carbon dioxide and the biological cycle of the oceanby A.R. Longhurst, W.G. Harrison, and T. Platt . . . . . . . . . . . . . . . . . . . 30

Climate, freshwater run-off, and fisheriesby K.F. Drinkwater . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 33

Breeding of Arctic seabirds in unusual ice years:The Thick-billed Murre Uria lomvia in 1978 by D.N. Nettleship,T.R. Birkhead, and A.J. Gaston . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 35

5. CHARTS AND PUBLICATIONS . . . . . . . . . . . . . . . . . . . . . . . . . . . . 39

6. 1983 SHIP VOYAGES . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 49

7. ORGANIZATION AND STAFF . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 57

8. PROJECT LISTING . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 61

BIO Review is published annually by theBedford Institute of Oceanography.Change of address notices and other corre-spondence concerning this publicationshould be sent to:

Publication ServicesBedford Institute of OceanographyP.O. Box 1006Dartmouth, Nova ScotiaCanada B2Y 4A2

International Standard Serial No.(ISSN) 0229-89 IO

Cat. No. Fs75-203/1984EISBN 0-662- 12444-8

Une version française est aussi disponible.

@Minister of Supply and ServicesCanada 1984

BIO Review ‘84:

Editor -Michael P. LatremouilleProduction Co-ordinator -Susan Scale

Tvpesetter -Graph Comp Design,OttawaPrinter -Kromar Printing Ltd.,Winnipeg

3

HUNTSMAN AWARD RECIPIENTS

Wolfgang Berger. Reuben Lasker.

Dr. Wolfgang Berger of the Scripps Institution of Oceanography was the 1984 recipient ofthe A.G. Huntsman Medal for Excellence in the Marine Sciences. He was recognized for hiscontributions to the understanding of the carbonate preservation and dissolution cycles in deep-sea sediments. Dr. Berger developed the concept of the lysocline, a level or ocean depth atwhich the rate of solution of calcium carbonate just exceeds its combined rate of deposition andprecipitation. He described how the lysocline varied in the past and related these variations tochanges in global climate.

Dr. Reuben Lasker of the National Marine Fisheries Service at La Jolla, California, receivedthe 1983 Huntsman Medal for his sustained research into the problem of the ‘critical period’ inlarval fish and the determination of year-class strengths. Over 15 years, Dr. Lasker and hiscolleagues used both experimental and field observations to elucidate the mechanism thatdetermines year-class strength in the California anchovy population.

The A.G. Huntsman Award honours those who have had and continue to have a significantinfluence on the course of marine scientific thought. Established by the Bedford Institute ofOceanography and supported by the petroleum industry, government, and fisheries- and ocean-related industries, the award honours the memory of Archibald G. Huntsman (1883-1972), apioneer of Canadian oceanography and fisheries biology. Nominations for the award comefrom the entire Canadian community of marine scientists. Past recipients include ChristopherJ.R. Garrett, Ramon Margale,. Dan P. McKenzie, Henry M. Stommel, and J. Tuzo Wilson. Theaward is presented annually in one of three categories (except in its inaugural year, 1980. whenrecipients were honoured in all categories): marine geosciences, physical and chemicaloceanography, and marine biology.

4

Paleoclimatology -past states of the ocean

T he oceans as we know them are dominated by water only a fewdegrees above the freezing point. Today, the polar seas are partly ice-covered, and a very thin layer of warm water lies above their coldinterior: in tropical seas, only a few hundred metres below the surface,the water temperature approaches that of the Labrador Sea in summer.But, the oceans have not always been so. For long periods during thePaleozoic and Mesozoic eras, the polar seas were almost as warm as theGulf Stream off eastern Canada is now, there were no ice caps, and thethen-tropical oceans resembled the Red Sea. Over much shorter timeperiods, at the peak of the most recent glaciations, the oceans wereeven colder than today, the extent of warm surface water was much less,and enough water was bound up in the polar ice caps that sea level wasas much as 100 m below today’s stand.

Climatic changes appear to be mediated by a variety of mechanisms,but perhaps most importantly by the amount of carbon dioxide in theatmosphere. By reducing the earth’s outgoing radiation, this gaseffectively makes our planet a ‘greenhouse’ whose temperature will riseas more radiation arrives from the sun. This appears to be the drivingforce on both long- and short-term time scales, and it is itselfdetermined by the balance - still very improperly understood - betweenthose forces that release the gas into the atmosphere such as volcanicactivity, the decay of forest biomass, and the alteration of the oceanecosystem and those forces that remove it such as the weathering ofnew mountain chains and the accumulation of biomass as coal or oil.

Faced with the problem of predicting where the clearly observablepresent-day rise in atmospheric carbon dioxide will take our globalclimate - both in the atmosphere and oceans - the reaction of the oceanto past changes is our chief guide. Both at BIO and at other majorocean science institutes, we are probing the history of the oceans to tryto understand how these mechanisms actually caused the changes weknow occurred. From such studies we can hope to learn how rapidlychanges can occur, whether the new climate will be highly or slightlyvariable, and where sea level is likely to stand on our grandchildren’sseashores. What follows are two examples of this line of research.

5

Climate and the geologic recordC.T. Schafer, P.J. Mudie, and J.N. Smith

Proxy signals of past climate conditions can be derived from textural evidence inmarine sediments on a scale of years and from lithological and paleontologicalevidence on a scale of thousands to millions of years.

C limate research at the AtlanticGeoscience Centre (AGC) is concernedwith interpreting indirect climaticinformation imprinted on the geologicalrecord. Instrumental data necessary forpredicting the local impact of hemisphere-wide climate variations have been recordedin Canada for only about the last 100 y.These data reveal the links betweeninterannual or seasonal changes in weatherand variations in atmospheric circulation,but they cover too short a span to identifylonger term, low frequency changes. Forexample, to make a quantitative study ofclimate variations that take place over 50 yintervals, a record ten times as long (i.e.,500 to 1000 y) is required. The evaluationof extreme events like storms requires evenlonger records in order to reliably estimatetheir probability of recurrence. The proxysignals imprinted in the geological recordare one of the few sources of long recordsof climate information in Canada. Thesesignals are in the form of marinemicrofossil and fossil pollen abundances,and in the grain-size characteristics ofdiscrete sediment layers that occur in coresamples (see first figure). Working withproxy signals from locations throughoutthe country can help unravel the effect ofrecent global climate variations on thedifferent parts of Canada’s landmass, flora,

and marine environments, and permit us toassess the impact of long-term climaticchanges on local conditions.

A paleohydrologic study presentlyunderway in the Saguenay fjord, Quebec,is aimed primarily at describing thevariations in climate that modulated thespring river-discharge intensity of theSaguenay River before the 20th century.Investigation of sediments depositedduring the 20th century in a basin near thehead of the fjord has shown a directrelationship between the proportion ofcoarse sediment particles deposited eachyear during the 20th century and theintensity of the annual spring freshet of theriver. One major factor controlling theintensity of the freshet is the precipitationthat accumulated as snow during theprevious winter. Studies of the relationshipbetween snow cover, an important factorin the Canadian climate story, and airtemperature suggest that relatively warmmoist air flowing northward into Canadaover snow about 15 cm deep loses its heatby conduction, and cools by 4-5°C per day.Similarly, warming during the early springmonths is usually most rapid when snowcover is minimal or absent.

Interpretation of the proxy climaterecord for the Saguenay area depends onaccurate dating of subsamples from cores

Charles Schafer, Peta Mudie, and John Smith examine X-ray photographs of sedimentcores.

6

that contain a 400-y-long record ofsediment deposition. Geochronologicalinvestigations have been undertaken usingthe naturally-occurring radionuclide.Pb-210, whose half-life of 22 y makes thisisotope an appropriate radioactive tracerfor sediment dating over the past 100-150 y(see second figure). Radionuclides such asCs-137 and Pu-239 and 240, introducedinto the environment initially as a result ofnuclear weapons’ tests in the late forties,can also be used as time-stratigraphicmarkers to date specific horizons in recentsediments. Once the core has been datedprecisely using radionuclide tracers, otherdocumented anthropogenic or naturalphenomena are employed to extend thedating methodology back in time.

The precise dating of distinctive texturalchanges observed in older sediments. andknowledge of the river discharge ratesrequired to produce these changes, provideone means of reconstructing a proxyhistorical record of winter precipitationand temperature in the Saguenay area overthe past few hundred years.

Analysis of many core samples fromthe Saguenay fjord reveals a generalrelationship between the modal grain sizeof sediment layers and the magnitude ofthe annual-maximum mean-monthly riverdischarge. One such relationship wasestablished in the following manner. Thegrain size distribution of the sand fractionwas measured in 2-cm thick sedimentintervals that were dated to the nearest yearusing the Pb-210 method. The historicalrecord of river discharge was thencompared to determine the maximummean-monthly discharge during the yearof deposition of each associated sedimentinterval. This discharge level was plottedagainst the modal diameter of the sand foreach sediment interval (see third figure).The plot suggests a direct relationshipbetween modal sediment size and riverdischarge: thus, the deposition ofcomparatively coarse sand particles nearthe head of the fjord increases as theannual-maximum mean-monthly river-discharge level increases. Samplescontaining clay pellets identify sedimentinputs that are associated with landslides.and/or with anthropogenic activities suchas excavation of dam sites along the mainchannel of the Saguenay River during thefirst half of the 20th century.

The longer term climatic variationsthat are reflected by the major glacialand interglacial intervals observed in the

North American geologic record poseseveral important questions forpaleoclimatologists. Of current interestis the timing of changes in oceans, icesheets, and atmosphere during theapproach to a glacial climatic stage.Scientists agree that a global data baseis required to assess the tempo of thesechanges and to understand the changesin large-scale atmospheric circulationreflected in the proxy record contained inmarine sediments.

Deep-sea sediments provide long

An X-ray photograph of a sedimentcore showing annual deposits ofcomparatively coarse sediment (thedark layers) that are carried into a basinnear the head of the Saguenay fjordduring the annual spring freshet.

Pb-210 activities and river discharge intensity plotted as a function of core depth andyear of deposition in a core (3111) collected near the head of the Saguenay fjord. ThePb-210 is associated with fine sediment particles and its activity level at a particulardepth interval of the core is proportional to the time of deposition of the associatedsediment layer.

(100,000 to 750,000 y). continuousrecords of oceanographic responses toclimatic change. Proxy climatic data arederived from fossil plankton, such asforaminifera, coccoliths, and diatoms,which make up the bulk of the sediments.Statistical analysis of the planktondeposited at the seabed, in a sampling gridextending from the tropics to the polarregions, shows that the fossils recordmodern surface- and bottom-watertemperature conditions with an accuracyof about 1°C. If it is assumed that thetemperature response of the fossil planktonhas not changed significantly in onemillion years, then temperature-calibratedmodern fossil data can be applied to thelong sediment records in order to obtaingraphs of ocean temperature changes forprehistoric times, including the last ice agewhen most of Canada was covered by anice sheet l-3 km thick.

The method, known as paleoecologicaltransfer function analysis, has been usedsuccessfully by the international CLIMAPProject (Climate/Long-range InvestigationMapping and Prediction) to constructsynoptic maps of ocean circulation in theNorth Atlantic during the last glacialinterval ( 18,000 y ago), and during thetransition to interglacial conditions. whichhave existed for about the past 10,000 y.CLlMAPdata show that the Gulf Stream

off Greenland was about 1600 km furthersouth during the ice-age maximum whensummer ocean surface water aroundIceland was 7°C colder than at present.

Changes of this magnitude could have amajor effect on ocean productivity andclimate in eastern Canada. In 1982,therefore, a study was started at AGC andDalhousie University to analyze the proxyclimatic record in sediments from deepbasins on continental shelves off Labrador,Newfoundland, and Nova Scotia.Paleoecological transfer functions havebeen obtained for a 20,000 y record offHamilton Inlet, Central Labrador (seefourth figure). These data show that: ( 1 ) thesummer temperature of the LabradorCurrent was only about 2-4°C lower at theglacial maximum; (2) bottom water wasabout 1°C higher than at present during thewarmest interglacial interval, about 7000to 3000 y ago; and (3) there has been anaverage temperature decrease of 1-2°Cduring the past 3000 y.

In order to specify the ocean-atmosphere temperature relations thatcharacterize the onset of an ice age,however, it is necessary to examine proxyclimatic records that span several glacial-interglacial transitions (i.e.. that provide acontinuous record for at least the past350,000 y ). Therefore, we are nowstudying cores from Davis Strait that

7

The modal grain diameter of suspendedsediments increases in direct proportionto river discharge intensity becauserelatively coarse sediments are carriedin suspension farther offshore duringthe spring freshet before settling to thebottom of the fjord basin.

The slow sedimentation rates (2.5cm/ 1000 y) observed in cores from DavisStrait do not allow us to define the

contain a 300,000 y sediment record.Abundances of fossil foraminifera anddinoflagellates are being used to analyzethe history of ocean temperature andproductivity; pollen assemblages fromthese cores are also being analyzed toobtain proxy data that reflect climatechange and wind trajectories over theNorth American continent. Initial resultsindicate that the northern Labrador Seawas warmer than at present during earlierglacial stages due to a stronger northwardadvection of southern cyclonic air massesalong the margins of expanding ice sheetsover Greenland and Canada. Thiscirculation pattern also explains theincreased moisture required to maintainrapid ice-sheet growth.

characteristic features of climaticconditions during the onset of glaciationbecause sediment mixing by bioturbatingorganisms and from other causes limits theresolution of proxy climatic signals tobetween 2000 and 5000 y. Therefore, weare now pursuing various means of deepdrilling to obtain long geological recordsfrom ocean areas with high sedimentationrates in which the effects of bioturbationare substantially reduced. In the summerand fall of 1985, the Ocean DrillingProgram is scheduled to drill several long(500 m) boreholes in the Labrador Seabasin. Cores from these holes shouldprovide geological samples that willimprove the resolution of proxy climaticrecords for eastern Canada and thus extendthe paleoclimatic record back at least threemillion years.

Quantitative estimates of changes in the salinity andtemperature of the Labrador Current during the past 25,000 y(right) were determined from factor analysis of benthicforaminifera in a sediment core (left): paleoecological transferfunctions describe the relation between modern foraminifera(e.g., Nonion labradorica, E. excavatum) and present seawatertemperature/salinity.

8

Paleoclimatic models from fossil records:A case history in Lake Melville, southeastern

LabradorG. Vilks

Evidence of the fluctuations in the glacial and postglacial conditions in the LakeMelville area is preserved in the local sediments. Early fluctuations were due toan influx of glacial meltwater, later ones to shallowing of sill depths at theentrance to the lake.

B uilding paleoclimatic models fromfossil faunas is a developing science whoseaim is to improve our knowledge of pastclimates, age dating, and prediction ofclimate change. Stable isotope ratios,such as the 13C/12C and 18O/16O ratios inforaminiferal carbonates. have beensuccessfully used in studying offshoresediments and transfer functions have beencalculated so as to statistically estimatepaleotemperatures and paleosalinitiesfrom microfossil assemblages in sedimentcores. In marginal marine environmentssuch as Lake Melville, which is not a truelake at all, the offshore methods are notalways applicable, and we are still trying toestablish their usefulness. Along thezone of land-sea interactions, majorenvironmental changes have a tendency tofluctuate to greater extremes than regionaland global changes. Therefore, aframework of 14C ages is often the onlyway to correlate nearshore, offshore, andglobal paleoclimatic events reliably.Insufficient amounts of carbon areavailable for conventional dating methodsin our area and so 14C ages are too few tomake accurate correlations. The newlydeveloped mass spectrometer method forreliable 14C dating can handle samples 100times smaller and promises to overcomethis shortcoming soon.

In Lake Melville, foraminiferaare useful for paleo-oceanographic/paleoclimatic studies once their ecology issufficiently understood. Then a particularspecies assemblage found in subsurfacesediment can be linked, for example, to itsmost likely paleosalinity range, whichcould be linked to the LabradorCurrent and thus to a possible paleo-oceanographic/paleoclimatic settingthat existed during the time when theforaminifers were living on the sea floor.

I study foraminifera in Lake Melvillesediments to infer changes in

paleoenvironment during the last 10,000 y.a time span when continental glaciersretreated from southeastern Labrador inresponse to major changes in climate andoceanography

Lake Melville, a fjord on thesoutheastern Labrador coast, containsup to 300 m of unconsolidated deposits(Grant, 1975). Sediments in piston coresshow a series of well-defined lithologicand faunal boundaries that reflect changesin marine environments and sedimentaryprocesses from the late glacial to recenttimes. Thus we see sedimentary structuresthat were formed along the last glacial icemargins and faunas that were living duringthe early postglacial marine maximum andduring the Holocene changes in sea level.The preserved marine record of fossils andsediment lithology can provide proxyinformation on major changes inpaleoclimate.

Studies of terrain and soils around LakeMelville suggest a complex history ofglacial-deglacial events (Fulton and

Gus Vilks.

Hogdson, 1979). To the north of LakeMelville, the Late Wisconsinan iceextended to the sea; to the south, the MealyMountains may have obstructed some ofthe seaward flow and the ice may havestopped short of the present shoreline(Rogerson, 1977). Drawdown may havetaken place in the Lake Melville Basin,which most likely acted as a calving bayfor the glacial ice.

Since deglaciation, relative sea level haschanged as a result of isostatic rebound ofthe terrain. The initial marine flooding wasfollowed by sea-level regression at faster

Location map of Lake Melville showing its bathymetry and the core stations occupied.

9

rates inland than at the coastline. Thus, thedeposits of the marine maximum are found150 m above the present datum at GooseBay and 120 m above that at the Narrows(Andrews, 1973).

The salinity and temperature of the waterin Lake Melville are a function of riverrun-off and the marine contribution fromthe Labrador Sea. During August, thewarm and fresh river water is present as athin surface layer almost throughout theLake, but during October the surfacecooling promotes mixing. The shallowchannel leading to the Lake prevents theentrance of relatively saline and coldsubsurface waters into the Lake and, as aresult, the bottom waters of Lake Melvilleare less saline than waters at correspondingdepths outside it. Because of the relativelylow bottom salinities, the exchange ofwater in the basin is at least annual. Thus,the dissolved oxygen in bottom water ofLake Melville is at the level of saturation.

The sediments collected in piston coresare basically olive brown muds thatbecome silty to sandy towards the bottomof the cores. The fine sediment structuresare best seen in x-radiographs taken

through longitudinally split cores. Themost prominent and diagnostic features arethe bioturbated surface layers underlain bylaminated sediments towards the bottom.The laminae are due to fine layers ofslightly coarser sediment. Within thebioturbated zone, x-radiographs also showpyritized structures of biogenic origin andworm burrows. Dropstones are pebblesthat have been released by melting sea iceand occasionally show evidence of havingsunk through layers of mud. The gasfissures of Core 111 formed after the coreswere collected and are most likely due tomethane gas coming out of solution.

The presence of foraminifera insediment cores is closely related to x-raystratigraphy. Foraminifera are commononly in the bioturbated zone of the coresand occur in small numbers or are totallyabsent from the sharply laminatedsediments (third figure). Basically twotypes of foraminifera are present in thefossiliferous zone. The upper layers of thecores are dominated by agglutinatedspecies below which there is a zonedominated by calcareous species. A fewmolluscan shells are also found in the

bioturbated zone in addition to evidenceof other macrobenthos, such as wormburrows.

Faunal changes in sediment coresstrongly suggest major changes in themarine environment through time. Pollenprofiles in Core 111 and 13C datesof organic matter indicate averagesedimentation rates on the order of 2 mper 1000 y in the deep basins (Vilks andMudie, 1983) and less than 1 m per 1000 yon the ridges. Since all sample intervalswere 5 cm thick, the time resolution ineach sample is not better than about 25 y inthe basins and 50-100 y on the ridges.

Foraminifera are directly affected bywater salinity and temperature, availabilityof food through primary and secondaryproduction rates, and dissolved oxygen.Sediment sources in combination withsedimentary environment govern the typeof sediment available as substratum (e.g.,some species prefer muddy sediments andothers sandy). These primary factors arelinked to a series of secondary factors thateventually lead to the climate.

Foraminifera living on the sea floor atthe present time are adjusted to the bottom

The Narrows lead into Lake Melville in southeastern Labrador. contains generally deep waters comparatively free of shoalsThe lake, which is tidal, has a maximum width of 32 km and except in the western part of the main section.

10

salinity of 28 parts per thousand, thetemperature of 0.5°C, and the mainlymuddy sediment. The average freshwaterinflux through river run-off is 58 km3/y;dissolved oxygen levels in the bottomwater are between 7-8 ml per litre; and seaice is present from November until May.The minimum water depth in the channel,which is 2.8 km wide and 22 km long, is30 m. Any major changes in these primaryfactors would lead to changes inforaminiferal assemblages on the sea floor.

Studies of foraminiferal ecology inestuarine environments suggest thatsalinity is one of the important factorsinfluencing the distribution of species. Inthe most thoroughly studied core, 111, theeurysaline cold-water agglutinated speciesat the surface are replaced by calcareousspecies about 400 cm downcore. Thecalcareous interval contains an upperfaunal zone dominated by Islandiellahelenae and a lower zone dominatedby Elphidium excavatum f. clavata. Apaleosalinity range of 32-34 parts perthousand was estimated for the I. helenaezone on the basis of the known salinitytolerance ranges of species within the zone(Vilks and Mudie, 1983; Mudie,et al., 1984). These same studies suggesta warmer paleotemperature range ofbetween 0°-2°C. The I. helenae zone isbetween 5000 BP and 8000 BP old.

Higher bottom salinities could be dueto: (1) greater paleosill depths at theentrance to Lake Melville; (2) lowervolumes of fresh water added to thesystem; (3) saltier water entering the Lake;or a combination of the three alternatives.Pollen profiles in Core 111 do not suggestan extensive dry period since deglaciation;thus, reduced run-off is unlikely. Raisedmarine deposits at certain areas around theLake and in the Narrows indicate greaterpaleodepths in Lake Melville and in theNarrows. Since the sill surface is in thepycnocline, slight changes in its depthswill determine the type of water enteringthe Lake from outside. Deepening of thesill, and thus widening of the channel. willallow the entrance of more saline water inaddition to reducing tidal mixing. Thus,higher paleosalinities could easily beexplained by a deeper channel withoutchanging the characteristics of the innershelf Labrador Current.

The paleosalinities of the E. excavatumf. clavata zone towards the bottom of thecore are 31-33 parts per thousand. a lowerrange than for the I. helenae zone of the

Temperature and salinity profiles in Hamilton Inlet, Labrador.

younger sediments. The extrapolated 14Cage for the top of the E. excavatum zone isabout 8000 y BP and within the time of theearly postglacial marine maximum inHamilton Inlet. The sill depth may thenhave been close to 130 m and if theestuarine circulation were similar to thepresent, bottom salinities should have been

in the order of 33-34 parts per thousand.The predicted lower paleosalinitiesindicate that fresher water from glacial run-off may have been present at greater depthsin the Hamilton Inlet area.

Elphidium excavatum f. clavat ispresent in recent sediments in a variety ofenvironments ranging from estuaries to

11

The stratigraphy in Lake Melvillesediment cores as determined fromexamination of X-ray photographs.

References

ANDREWS, J.T. 1973. Maps of the maximumpostglacial marine limit and rebound for the formerLaurentide Ice Sheet (the National Atlas of Canada).Arctic and Alpine Research 5: 41-48.

FULTON, R.J. and HODGSON. D.A. 1979.Wisconsin glacial retreat. southern Labrador. InCurrent Research. Part C. Geological Survey ofCanada. Paper 79-1C: 17-21.

GRANT, A.C. 1975. Seismic reconnaissance of LakeMelville. Labrador. Can. J. Earth Sci. 12: 2103-2110.

MUDIE, P.J., KEEN, C.E., HARDY, I.A.. andVILKS, G. 1984. Multivariate analysis andquantitative paleoecology of benthic foraminiferain surface and Later Quaternary shelf sediments,northern Canada. Marine Micropaleontology 8:283-313.

ROGERSON, R.J. 1977. Glacial geomorphologyand sediments of the Porcupine Strand area.Labrador. Canada. Unpubl. PhD. thesis. MacQuaricUniversity. Eastwood. Sydney. Australia: 277 p.

VILKS. G. and MUDIE. P 1983. Evidence forpostglacial paleoccanographic and paleoclimaticchanges in Lake Melville, Labrador. Arctic andAlpine Research 15: 307-320.

continental slopes. In older sediments offEastern Canada and Scandinavia, thespecies is persistently dominant in lateglacial deposits and is one of the majorspecies found in sediments facing atidewater glacier in Spitzbergen. Thereis, therefore, a distinct possibility that theE. excavatum zone found in all corescollected in Lake Melville represents adistal glacial margin environment duringthe time when glaciers were melting in theuplands to the west of Lake Melville.

12

Below the zone of the distal glacialsediments are laminated sediments devoidof faunal remains. These may have beendeposited in a proximal glacialenvironment dominated by the presence ofglacial ice and large volumes of glacialmeltwater. Below the sampling depth ofpiston corers, the high resolution Huntecdeep tow seismic profiles also showstratified sediments that lie on top ofacoustic structures interpreted as tills.

Ocean circulationand climate change -The North Atlantic Ocean

A s the global climate changes either naturally on various time-scales or as the carbon-dioxide ‘greenhouse’ effect begins to bite, theconsequences will not simply be a uniform warming, with all otherweather patterns remaining as we know them today. The global windpatterns will shift their location and climate belts marked by certainlevels of rainfall will shift not only north and south, but also east andwest.

Such changes can be predicted with a degree of certainty already, butwe are very far from being able to do the same thing for the changes inocean-current patterns that will undoubtedly also occur. Yet such areprobably the most important effects: what if, for instance, the GulfStream departs from the North American coast not at Cape Hatteras,but at Cape Cod or Nantuckett Shoals, which is certainly notimpossible? How will it then impact on the coastline and continentalshelf of eastern Canada‘? Will it strengthen or weaken the transport ofcold arctic water along our coasts by the Labrador Current?

These are the kinds of questions to which the three studies discussedin this chapter are addressed.

Gulf Stream studies

The Gulf Stream exerts a major influence on the climate of the North AtlanticOcean and adjacent land areas by transporting large amounts of heat poleward.Understanding the dynamics of this system is an important goal of present-dayphysical oceanographic research.

T he Gulf Stream is a major feature of theworld ocean circulation. Beginning withthe Florida Current off the southeast coastof the United States, it grows into theeastward flowing Gulf Stream proper southof Nova Scotia, and rounds the GrandBanks to continue as the North AtlanticCurrent flowing across the northern NorthAtlantic Ocean towards Europe. To thephysical oceanographer, the Gulf Streamis a fascinating dynamical puzzle. It is amid-ocean jet with water transport equal to10,000 St. Lawrence Rivers, constantlytwisting and meandering as it goes, casting

off eddies that entrain up to 15,000 km-3 ofwater and can persist for months or evenyears. To the climatologist, the GulfStream is the northern and westernboundary of an immense pool of warmwater that is a source of heat and moisturefor the overlying atmosphere and plays avital role in determining the regionalclimate. Changes in the position of thisboundary and changes in the temperatureof the warm pool will inevitably bereflected in changes in the regionalclimate. A long-term goal of the physicaloceanographer studying the Gulf Stream

R.M. Hendry

Ross Hendry.13

to understand the dynamics of the system

who encountered the Florida Current in1513 in the course of his exploration of

so as to be able to predict such changes.

the New World. It was relatively familiarto American mariners in 1770 whenBenjamin Franklin, then Deputy

According to Professor Henry Stommel

Postmaster General for the American

in his well-known monograph “The Gulf

Colonies, had a chart prepared showing the

Stream”, the first mention of this majorcurrent system comes from Ponce de Leon

30°N, in a broad band running northeast

the net heat transfer from the atmosphere

from the Gulf of Mexico all the way to theNorwegian Sea, the ocean releases heat to

to the North Atlantic Ocean averaged over

the atmosphere over an annual cycle. Thistransfer is partly sensible heat, or energy

the annual cycle. South of approximately

associated with molecular motions, but thedominant component is the latent heat of

30°N. relatively cool surface waters gainheat from the overlying air as well as fromthe direct influence of the sun. North of

The net heat transfer from the atmosphere to the North Atlantic Ocean over the annualcycle. Contours are in watts per square metre.

course of the Gulf Stream to encouragemail packets from England to NewEngland to avoid the strong eastwardcurrents in the Stream and thus speed theirpassage. As late as 1942, Sverdrup couldwrite in his classic oceanographic textbookthat most meteorologists of the dayneglected the effect of ocean currents suchas the Gulf Stream in transporting heatfrom lower to higher latitudes. Sverdruphimself showed by example that oceanictransports could be significant in someregions, but he felt that the atmosphereplayed the dominant role in the overallprocess. In fact, modern studies haveshown that the ocean circulation is vitalin the global climate system, actuallycarrying more heat poleward in tropicallatitudes than the atmospheric circulationitself.

We can refer to the first figure to begin adiscussion of the influence of the GulfStream and ocean circulation in general onthe climate of the North Atlantic Oceanand adjacent land areas. This figure shows

14

evaporation associated with the changeof state from liquid ocean water to watervapour picked up by the moving air. Thetwo areas of greatest oceanic heat loss arefound just east of the United States near35°N and just east of Newfoundland near45°N. where relatively cool and dry windsblowing off the North American continentfirst encounter the warmer ocean waters.The maximum rate of heat transfer foundis about 250 Wm-2 of ocean surface. Bycomparison, the annual mean surplus ofradiation from the sun at the surface of theearth near the equator, after allowing forreflection of incoming short wave radiationand long wave back radiation, is only about150 Wm-2.

The heat energy absorbed by theatmosphere over the mid-latitude NorthAtlantic is carried to the east by theprevailing westerly winds and helps shapethe temperate climate of northwesternEurope. Most of the heat must be releasedby condensation and subsequentprecipitation of the water vapour carried

by the winds, giving a somewhat dampclimate to these European countries as anunavoidable companion of their moderateannual range of temperature.

Referring again to the first figure, theocean waters immediately adjacent tonorthwestern Europe release relativelysmall amounts of heat to the atmospherecompared to the areas near the NorthAmerican coast, and the ocean-wideatmospheric circulation is a vital link inthis coupled regional climate system. TheGulf Stream does not really bathe theshores of Europe as is sometimes naivelysuggested. Some readers might wonderwhy Canadian oceanographers should beso concerned with the climate of Europe,but it must be recognized that the studyof large-scale ocean and atmosphericcirculation is truly an international effort.Japanese oceanographers studying asimilar system of large air-sea heatexchange associated with the KuroshioCurrent in the western Pacific Ocean arecontributing to the understanding offactors shaping the maritime climate ofcoastal British Columbia! To return to thebasic theme of this article, just what is therole of the Gulf Stream in this large-scaleprocess and how can fluctuations in oceancurrents change our climate?

A moment’s thought will make it clearthat if certain areas in the North Atlanticare losing great quantities of heat to theatmosphere without cooling drastically,then heat must also be being supplied tothese areas from some other source. Oceancurrents accomplish this by transportingheat from tropical regions that enjoy a netsurplus of solar energy input over a year.The maximum average poleward heattransfer by ocean currents in the NorthAtlantic has been estimated at about3 x 1015W near 20°N. just at the upstreamend of the Gulf Stream System. Thepoleward ocean heat-transport decreases tothe north as the ocean-borne heat isreleased to the atmosphere. The GulfStream, and its continuation as the NorthAtlantic Current, carry relatively warmwaters to the north. In a steady state, anequal southward transport of water mustoccur somewhere in the ocean to maintainmass continuity. A net heat transportresults because the southward flowingcurrents generally carry cooler water thanthe northward flowing currents. Onecomponent of the return flow is the coldLabrador Current, which flows southwarddown the eastern coast of Canada. Other

return flows take place at abyssal depths.The three-dimensional structure of theNorth Atlantic circulation is the focus ofstudy for oceanographers from manynations. The dynamical balances thatcontrol the circulation and maintain thedistinctive warm-water gyres associatedwith the Gulf Stream and the NorthAtlantic Current are only partlyunderstood. Specific mechanismsby which oceanic heat-transport isaccomplished are also being activelystudied. One question still to be answeredis the importance of time-dependent oceaneddies in the large-scale transport of heat.

The warm Gulf Stream currents areimportant in determining ocean conditionsin Eastern Canadian waters as well as inshaping the large-scale patterns of climate.An economically important region calledthe Slope Water is found north of the GulfStream between eastern continental NorthAmerica and the Grand Banks. This SlopeWater is formed mainly of a mixture ofwarm water from the Sargasso Sea south ofthe Gulf Stream and cold Labrador Currentwater. It is separated from the warmerwaters to the south by the Gulf Streamitself, which acts as a dynamical but partlypermeable boundary. We will return to theSlope Water in the concluding paragraph.

The Atlantic Oceanographic Laboratoryhas been and continues to be involved inthe international effort to understand thephysics of deep-ocean circulation, and hasexpended a considerable effort in studiesof the Gulf Stream System. The secondfigure shows the locations of some ofthe moorings instrumented with currentand temperature sensors that have beendeployed in such studies by the AtlanticOceanographic Laboratory over the pastdecade. Several of the individualexperiments were conducted in co-operation with scientists at the WoodsHole Oceanographic Institution andsome of their mooring positions are alsoindicated in the figure to give an idea of thescope of the combined effort. Many ofthese studies have been frankly exploratoryin nature, designed to answer very basicquestions.

How energetic are Gulf Stream eddies atdifferent locations? We have helped to mapout the answer to this question by showingthat the current fluctuations decrease inmagnitude but have longer temporalperiods on moving downstream in thesystem. How do the currents change withdepth in the Gulf Stream’? A two-year

Instrumented moorings deployed by the Atlantic Oceanographic Laboratory tostudy the Gulf Stream. Also shown are some of the moorings deployed by the WoodsHole Oceanographic Institution ( = = ) for the same purpose.

study begun in 1983 is seeking the answerto this very question. How important arecut-off Gulf Stream rings in transferringheat across the Stream between the warmSargasso Sea and the cooler Slope Waterwith its Labrador Current influence? Thereare hints that such processes may be a verysignificant part of the total transfer, but thefinal answer has yet to be found.

In the introductory remarks, Imentioned the possibility of climatechange. The third figure gives an exampleof the type of long-term variability actuallyobserved in the North Atlantic Ocean. Itshows the trend in annual mean sea-surfacetemperature during the first part of thepresent century in a 5° by 5° square centred

in the Slope Water south of Nova Scotiaand Newfoundland. There is convincingevidence of a net warming of these watersby at least 2°C over the 40 y of data.Explanations for this phenomenon arelargely speculative, but one suggestion isthat the warming was due to increasedmixing with warm water from the SargassoSea as a result of more frequent andenergetic meandering and eddy productionby the Gulf Stream. The Stream itself isdriven by the large-scale North Atlanticwind system. Changes in sea-surfacetemperature and the resulting changes inair-sea heat exchange affect the large-scaleatmospheric circulation. The resultingfeedback loop is typical of the entire global

Time series of annual sea temperature anomalies (°C) in the Slope Water south of NovaScotia (40-45°N, 55-60°W). (After Bjerknes, J.B. 1964. Atlantic air-sea interaction. InAdvances in Geophysics 10: p. 36. )

15

climate system. By seeking to understand Stream and its eddies, we hope tothe fundamental dynamics of the Gulf contribute to the eventual understanding

Towards a world climate research programmeF.W. Dobson and S.D. Smith

As a result of our participation in the “CAGE” study of the feasibility ofmeasuring the poleward heat transport of the North Atlantic Ocean, we areinvestigating the accuracy of extant formulae for estimating sea-surface heatexchanges. We have found substantial discrepancies between our results andestablished wisdom; this promises an exciting future for the World ClimateResearch Programmes.

T he World Climate ResearchProgramme, established in 1980 by theWorld Meteorological Organization, isdesigned to investigate the variability ofthe earth’s climate on three time scales:roughly speaking, months, years, anddecades. The goal is to explain andeventually predict the variations. Theoceans are involved at all three time scales:they store heat locallyon a monthly time scale; year-to-yearvariability in sea-surface temperature andoceanic heat-storage rate is the immediatecause of the El Niño events; and it is theability of the great ocean currents plusglobal exchange processes that will, overthe long term, determine the response ofour climate system to man-made changesin the carbon-dioxide content of theatmosphere (the ‘greenhouse’ effect). Theinternational efforts now getting underwayare reflected in some BIO researchprogrammes.

Clarifying the roles of the atmosphereand the ocean and the many ways in whichthey interact is crucial if progress is tobe made in the modelling and eventualprediction of the earth’s climate. We beginby describing an internationally sponsoredinvestigation of the feasibility of makingan accurate measurement of the amount ofheat carried poleward annually by theNorth Atlantic Ocean (the CAGE study).We then outline our current work, much ofwhich resulted from the CAGE study, andfinish by describing the ‘state of the art’ inclimate-scale air-sea interaction research,and ramifications for the upcoming WorldClimate Research Programme.

In June 1980, the Committee on ClimateChange in the Ocean set up a small group,which included one of us (Dobson), toreport on the feasibility of making animportant measurement: the amount of

16

heat annually transported poleward by theNorth Atlantic Ocean, to an accuracy of20%. The idea was to surround the ocean,theoretically, with a ‘Cage’, measure allthe heat entering and leaving the sides andtop of the cage, and thus discover howmuch heat was being transported by theocean within.

This heat transport had already beenestimated by three different techniques.First, in 1974 Andrew Bunker estimatedthe amount of heat transferred annuallythrough the surface of the North Atlanticusing empirical formulae relating theair-sea heat transfers to quantities suchas wind speed, air-sea temperaturedifferences, humidity, and cloud coverfrom millions of archived ship-reports.The heat given up annually by the NorthAtlantic Ocean to the atmosphere(relatively little heat leaks into the ArcticOcean) must be made up by polewardtransfer within the ocean. Bunker’sestimate was 1.1 x 1015 W (one petawatt),equivalent to the output of one 300 MWpower station every nautical mile along theequator, from one side of the Atlantic to theother!

Second, in 1976 Abraham Oort andThomas Vonder Haar used a variant of the‘Cage’ idea: they estimated, for 10° latitudebands, the heat entering the top of theatmosphere from satellite-based solarradiation measurements, the heattransported poleward in the atmospherefrom archived radiosonde-measurementsof wind, temperature, and humidity, andthe rate at which heat is stored by the oceanfrom archived sea-temperature data.Knowing that the system is in equilibrium(we are not warming up or cooling downmeasurably, over long time-averages), theyobtained a poleward transfer of 2.2 x1015 W by the North Atlantic and North

of this complicated system.

Fred Dobson and Stuart Smith.

Pacific combined, which seems to be inreasonable agreement with Bunker’sresult, if it is assumed that the Atlantictransports half of the total.

Third, in 1980 Harry Bryden and MindyHall used oceanographic data only.Noting that the depth-averaged oceantemperatures along 24°N (roughly Miamito Dakar) remained very constanteverywhere on the line, and knowing theamount of heat transported polewardacross 24°N by the Gulf Stream as it flowsthrough the Florida Strait, they estimatedfrom the heat balance at that latitude thatthe ocean gives up 1.1 x 1015 W to theatmosphere, a figure close to thatcomputed by Bunker.

The Committee on Climate Change inthe Ocean believed there was a goodchance that, given updated and moreaccurate formulae for computing the heattransported through the sea surface fromships’ meteorological observations, givenmore accurate and carefully planned-satellite measurements of the incomingsolar radiation and reasonableaugmentations of the existing WMOradiosonde and sea-temperature reportingnetworks, and given some oceanographicwork at 24°N specifically tuned to measurepoleward oceanic heat transport (Brydenand Hall used existing data), it should bepossible to measure the poleward transportof heat by the North Atlantic Ocean to

± 20%. when averaged over a five-yearperiod.

The ‘Cage’ Group studied the issue withsome care. Their conclusions werestartling and disconcerting: of the threetechniques proposed for determiningthe meridional heat flux, only theoceanographic determination appearedfeasible.

The estimation of the transport of heatthrough the sea surface was deemed theleast accurate with errors of 30-50%. Thebudget technique pioneered by Oort andVonder Haar was investigated using newlyobtained more accurate satellite data, thebest available meteorological data set, andthe best current numerical forecast model.The global heat transport budget showedunexplained yearly imbalances in Eurasiaof ±40 Wm-2 (±20% in the North Atlanticis 10 Wm-2). For the oceanographictechnique, new ways of estimating theheat transport were attempted, a newprogramme was undertaken for measuringthe heat transport of the Gulf Stream, and astudy of how best to estimate heat storagein the entire ocean showed it could be donewith seven lines of expendable temperatureprobes, dropped every 175 km by merchantships on regular runs five times per year,and reaching depths of 1200 m. Anothermajor finding was that the heat transportappears to vary by less than 20% of itsmean value from year to year. On the basisof this evidence, the CCO decided that the‘Cage’ experiment would not be pursuedas an entity; rather, those parts thatappeared feasible would be done one byone as part of the World Ocean CirculationExperiment.

Having dedicated large parts of ourcareers to upgrading the formulae forvertical heat transport through the seasurface, we were challenged by the CAGEfindings to determine and, when possible,reduce the error bounds of each of theformulae. Heat is transported through thesea surface by four different means:(1) Incoming solar radiation (heats the sea

surface);(2) Infrared radiation (cools the sea

surface);(3) Turbulent heat transport (heats or cools

the surface depending on whether theair is warmer or cooler than the sea;wind-speed dependent); and

(4) Turbulent water-vapour transport(usually cools the sea surface; wind-speed dependent).

Our first efforts (Smith, 1981) centredon a careful review of our ownmeasurements, and of the literature, totabulate evaporation and heat transportusing the best formulae. These transportswere typically 20-30% less than Bunker’svalues.

We compared (Dobson) meteorologicalmeasurements by trained observers withcalibrated instruments on Ocean WeatherStations against the same quantitiesreported by non-professional observers onships within 2° in latitude and longitude ofthe Ocean Weather Stations. The passingships produced identical climatologies; theworst error was a 6% underestimate of totalcloud amount.

radiation formula used by Budykooverestimates the rate of cooling of theocean by as much as 30% in tropicalregions. We hope that others will join us inthe search for a better formula.

Our recently published study of thelocal heat budget at Ocean Weather StationBravo, in the middle of the Labrador Sea(Smith and Dobson, 1984) shows thatBunker’s method overestimates the netcooling of the sea surface by about 50%.By comparing the incoming heat with therate of storage of heat at Bravo, usingoceanographic data originally studied byJohn Lazier, we estimated how much heatwas moved into or out of the region byocean currents. From month to month, the

Oceanic heat transport (in units of 1013 W) from Hastenrath (1980). The dashed linesshow how the southern ocean was divided: the stippled areas indicated regions ofmaximum export of heat by ocean currents.

We tested existing formulae against15-20 y time-series of solar radiationmeasurements at Ocean Weather StationsP in the North Pacific, at A, I, J, and K inthe eastern North Atlantic, and at SableIsland, N.S. The most widely usedformula (Bunker for instance used it),developed in Russia by Budyko andBerliand, estimates clear-sky radiant heatinput to within 2%, but underestimatessolar heating on cloudy days by 30% ormore. Other less well known formulae dobetter, but we decided to optimize theprocedure to model the observations withformulae that allow for what we regard tobe the important physics. We can modelthe mean solar radiation to within about5%, and we cannot do better because theradiometers used presently on theweatherships are no better!

We know already that the infrared

amount of heat stored differed wildly fromthat crossing the surface, while over thelong term the amounts were roughly equal.Since the oceanography of the areaindicates little movement of heat, theconclusion is not inconsistent with ourversions of the heat transport formulae.

One of our colleagues, Professor L.Hasse of the University of Kiel in WestGermany, and a student have acquiredwhat was still available of Bunker’scomputed monthly averages of the variousmeteorological variables in the NorthAtlantic, and they are re-computing, withthe most modem formulae, the distributionof the heat transports through the seasurface over time and space. We havediscussed the formulae with them, andreached general agreement on which touse. (Theirs are not exactly the same asours - what two scientists will agree - but

17

they are close.) Even before the work iscompleted, it is clear that the Bunkerestimate of 1015 W for the mean annualpoleward transport of heat by the NorthAtlantic across 24°N is too high. Thequestion is: by how much? Our guess isabout 50%. Because most existingestimates, by whatever technique, giveabout 1015 W, the new results will call allthe old ones into question.

Calling the results into question for awell-studied ocean like the North Atlanticis a matter of great concern to those whowish to understand the global climatesystem and eventually to predict it. Theaccompanying figure, from a paper byStefan Hastenrath (1980), indicates howthe heat transport of the various oceans isinterconnected, with the North Atlanticbeing a major contributor. Rearranging the

balance to fit a new, smaller estimate forthe North Atlantic heat transport will notbe a simple matter. Since the ocean andatmosphere are strongly coupled, theatmospheric contribution to the polewardtransport of heat must also bereconsidered. The resolution of theresulting arguments will not be easy; webelieve our surface heating formulae arecorrect now at least to within 20%. Thescience of climate-scale air-sea interactionpromises to be an exciting one over thenext few years.

References

BRYDEN, H.L. and HALL, M.H. 1980. Heattransport by currents across 25°N in the AtlanticOcean. Science 207: 884-886.

BUNKER, A.F. 1976. Computations of surfaceenergy flux and annual air-sea interaction cycles of

Sea-surface temperature trends and patternsin the Northwest Atlantic

R.W. Trites

Studies of sea-surface temperature in the northwest Atlantic reveal both year-to-year and decadal-scale changes. Evidence is mounting that the large-scalemeteorology is of primary importance in producing the observed variability.

The twice-daily observations of sea- On a 30-y basis, the 1951 to 1980 periodsurface temperature (SST) begun in 1921 was 0.6°C warmer than the 1921 to 1950at St. Andrews, New Brunswick, are the period. The rather large year-to-yearlongest continuous series of water variations in temperature revealed in thetemperature data for one site along the records (up to 1.8°C) make up a sizableCanadian Atlantic coast. Annual mean fraction of the maximum change (2.7°C)temperatures for 1921 to 1983 as compared between the coldest year, 1923, and theto the 7°C average for the total period were warmest, 1951.below normal from the early twenties to The water temperature at any giventhe mid forties; from about 1945 to 1960, coastal site is the result of both localvalues were above the 60-y mean. processes (heat exchange across the seaSubsequently no clear trends are apparent. surface and mixing) and advection

Mean annual sea-surface temperature at St. Andrews, New Brunswick, from 1921 to1983. The annual average for the total period is 7°C.

18

the North Atlantic Ocean. Monthly Weather Review104: 1122-1140.

DOBSON, F.W., BRETHERTON, F.P.BURRIDGE, D.M., CREASE, J., KRAUS, E.B.,and VONDER HAAR, T.H. 1982. The CAGEExperiment: A feasibility study Report WCP-22,World Meteorological Organization, Geneva: 95 p.

HASTENRATH, S. 1980. Heat budget of tropicalocean and atmosphere. Journal of PhysicalOceanography 10: 159-170.

LAZIER, J.R.N. 1980. Oceanographic conditions atOcean Weather Ship Bravo, 1964-1974. Atmosphere-Ocean 18: 227-238.

OORT, A.H. and VONDER HAAR, T.H. 1976. Onthe observed cycle in the ocean-atmosphere heatbalance over the northern hemisphere. Journal ofPhysical Oceanography 6: 781-800.

SMITH,S.D. 198l. Coefficients for sea surface windstress and heat exchange. Bedford Institute ofOceanography, Report Series, BI-R-81-19: 31 pp.

SMITH, S.D. and DOBSON, F. W. 1984. The heatbudget at Ocean Weather Station Bravo. Atmosphere-Ocean 22: l-22.

operating on a range of geographic scales.For any given month (or even year),temperature anomalies at sampling sitesseparated by as little as a few tens ofkilometres may be of different magnitudeand sign. When averaged over severalyears, however, the mean anomaliesusually become comparable. In fact, thereis evidence mounting that large-scaleprocesses operate over distances ofperhaps several thousand kilometres toproduce coherent temperature shifts.

Plots of 3-year equally weighted meansof the annual air-temperature averagesat Eastport, Maine; Fredericton, NewBrunswick; Ottawa, Ontario; and SableIsland, Nova Scotia.

To appreciate the geographic scale ofthese longer term temperature changes, itis useful to study air temperatures firstbecause they have been more oftenrecorded and at more sites than watertemperatures. Doing so, one finds thatyear-to-year variability in air temperature iscorrelated over relatively wide geographicareas. For example, the relatively closecorrelation between the 3-y running meansof the annual averages of air temperaturefor Ottawa, Fredericton, Eastport, andSable Island is readily apparent. Similarly,

the correlation between air and coastalwater temperatures is usually good whenrunning means over several years are used.

For the Northwest Atlantic as a whole,the largest SST data base is derivedprincipally from records of the intaketemperature of the cooling water onmerchant vessels; these temperatures arereported in radio weather messages toshore stations and in log books transmittedto the National Climatic Center in North Surface water temperature at St. Andrews, New Brunswick, and air temperatures atCarolina. When analyzed in quadrangles Sable Island and Halifax, Nova Scotia. Ten-year moving averages of the annual meanof one-degree latitude and longitude, this temperatures are credited to the last year of the period.

Chart showing the areas over which sea-surface observations have been averaged monthly.

1 9

The distribution of annual sea surface temperature anomalies from 1972 to 1983 bysubarea (see previous chart) relative to the means for the 1972-1980 base period. (A‘+‘ or a ‘-’ symbol represents an anomaly that exceeds 0.15°C: a ‘ = = ’ symbol representsan anomaly with a magnitude of less than 0.15°C.) Only anomalies exceeding 0.15°Chave been used in constructing the contours.

data base typically displays relatively highspatial and temporal variability.Undoubtedly, some of this variabilityis real but some is the result ofundersampling. However, large-scalecoherence and shifts can be identified bygrouping the data for the NorthwestAtlantic into a number of subareas, whichcoincide with fishing banks or with majorwater masses (e.g., the Labrador Current,Gulf Stream, Sargasso Sea). A time-spaceplot of annual sea-surface temperatureanomalies in the 1972 to 1983 period isreasonably constant usually over 1000to 20 km for several years. From 1972to 1975, the northern and shelf waters

from the Labrador coast to the Gulf ofMaine were relatively cold, while thetemperatures of the southern and offshoreGulf Stream and Sargasso Sea were abovenormal. In 1976, the situation appears tohave been in the process of reversing. From1977 to 1983, annual mean temperatureswere usually above normal in the northernregions and below-normal in the southern.The largest positive anomalies for the 12-yperiod occurred in 1983 in the GrandBanks - Scotian Shelf region.

Not surprisingly there are goodindications that the sea-surfacetemperature anomaly pattern and the large-scale meteorology (air temperature and

Ron Trites.

pressure patterns) are closely linked. It isnoteworthy that during 1982 and 1983, thestrongest El Niño Southern Oscillation(ENSO) in over 100 y was recorded. ElNiño refers to anomalously warm water inthe eastern tropical Pacific but has beenshown recently to be part of a much largerocean-atmosphere interaction. The effectsare felt almost worldwide and it appearslikely that the anomalous sea-levelatmospheric pressure pattern over theNorth Atlantic is at least partially related tothe atmospheric response associated withthe El Niño event, but the nature of anyrelationship needs further research.

20

The influence of the Arctic

T he global thermal machine that determines our climate, and whosevariability is the subject of this Review, acts principally to redistributeheat - received mostly at the surface of the planet in the tropics - overthe whole planetary surface into the pattern of warm and cold areaswith which we are all familiar, and which drive our industry,agriculture, and forestry.

It is the redistribution of heat that drives the wind systems, both atthe surface and at high altitudes, and the surface and deep currents ofthe oceans. In eastern Canada and in the North Atlantic Ocean, thetransport of heat to high latitudes by warm surface currents of theocean, and the return of cold water southwards from the arctic, eitherat the surface as the Labrador Current or at depth from the centres offormation of deep water in the Labrador and Norwegian seas,dominates these processes. Variability in this heat transport affectsnot only the arctic itself, and life there, but also the oceanography ofthe whole region, and is the subject of the studies we discuss in this

chapter.

Arctic run-offin the North Atlantic Ocean

J.R.N. LazierFreshwater run-off in the Arctic helps control important physical processes inthe North Atlantic Ocean such as winter-time convection in the Labrardor Seaand transport in the boundary currents. Two programmes designed to investigatethe freshwater's role are described.

The 80,000 or so tons of fresh water that detail how the water gets into the middle ofmake their way every second into the North the ocean so we can better understand howAtlantic Ocean from the large Arctic rivers the processes work and interact with eachin Canada and the USSR such as the other.MacKenzie and Yenisey significantlyinfluence the climate and structure of the

Fresh water enters the ocean as riverrun-off, rain, snow, or melted ice. It thenmixes into the ocean waters, which areabout 3.5% salt. The fresh water doesn’tstay completely fresh but graduallybecomes saltier and may be traced in theocean as flows of water with less salt thanthe open ocean water.

ocean.During the past few years. we have

begun to discover some of the highlights ofthis association. We first learned of the roleof fresh water in the winter mixing byconvection down into the ocean that occursin the Labrador Sea, then we saw howchanges from year to year in the freshwaterflow can control the depth of thisconvection, and now we are working to

The Arctic is the freshest of the worlds’oceans, partly because it receives theoutflows from the large Arctic rivers andpartly because the permanent ice cover

John Lazier.

prevents evaporation of fresh water out ofthe ocean. Arctic water comes into theNorth Atlantic through the Canadian

21

Archipelago and Denmark Strait betweenGreenland and Iceland. A smallercontribution of fresh water also comesfrom Hudson Bay through Hudson Strait.

The influence of the fresher Arctic waterin the North Atlantic is illustrated in themap of salinity at 30-m depth shown in thefirst figure. Next to Greenland, BaffinIsland, and Labrador are bands of lowsalinity water (less than 33.0 ppt or 3.3%salt) marking the southward flows ofthe Arctic water in the East- and West-Greenland, Baffin-Island and Labradorcurrents. The effect of the outflow from theSt. Lawrence River is also evident inthe low salinity water in the Gulf ofSt. Lawrence and seaward of Nova Scotia.The highest salinities due to highevaporation rates are found in the middle ofthe ocean at the latitude of southernFlorida. In the middle of the Labrador Sea.south of Greenland and east of Labrador,there is an area of the deep ocean with a

lower salinity than anywhere else. This isthe flow that is important to the LabradorSea.

The influence of this flow on the climateof the ocean was first realized when thedata from the Ocean Weather Ship Bravowere examined. This ship was stationedat 56°30’N, 51°W in the middle of theLabrador Sea between 1945 and 1974, andcollected oceanographic data for the finalten years. The salinity at various depths atthe Bravo position is shown for the tenyears in the second figure. The bottom linerepresents the salinity near the surface and,because the lines never cross, the lowestsalinity is always at the surface. Every yearthis line shows the salinity decreasing insummer and increasing in winter- theannual cycle. The summer decrease occursbecause of the spring and summer increasein run-off and ice melt, while the increasein winter comes when the run-off slowsdown in autumn at the same time that

cooling and more violent storms stir thelow salinity water down into the watercolumn and bring higher salinity water upnear the surface. The climatic signal inthese salinity values is the change to lowervalues, in addition to the annual signal,from the late sixties to early seventies. Thischange at Bravo was one manifestation of awidespread phenomenon that shortenedthe growing season in England in the latesixties and put more ice than usual north ofIceland: the effects are still being observedin, for example, the mid-North Atlanticat the 1500-m depth. The reason for thesalinity decrease was traced by Dicksonet al. (1975) to an abnormally highatmospheric pressure system thatremained over Greenland for a number ofyears. Air moves clockwise around highpressure regions and in this case producedabnormally strong and persistent windssouth along the east coast of Greenland.Ice and cold low-salinity Arctic water were

The salinity in parts per thousand at a depth of 30 m in the North Atlantic Ocean.

22

thereby forced south of Denmark Strait inlarger quantities.

In the middle of the Labrador Sea, thelayer of abnormally fresh water made thewater column abnormally stable in the latesixties thereby increasing the heat lossrequired to convectively mix the waterto a given depth. This is an importantconsideration because the Labrador Sea isone of the few places in the world wherethe water is overturned in winter to greatdepths via convection. This is how some ofthe deep waters are created or renewed inthe ocean. In an exceptionally cold year,such as 1976, the water can be mixed downto 2000 m but in mild years, such as 1969or 1970, extra fresh water adds buoyancyto the surface layer and the mixed layermay only get to a depth of 200 m. Thisdifference in depth of winter mixing can beroughly deduced from the salinity plot(second figure). In winter, the water ishomogeneous at depth if the figure’s linesrun together. If they stay apart, there isstill a salinity gradient with depth. Theend of the mild winters that seemed toaccompany the abnormally low salinitywater ended abruptly in the severe winterof 1971-1972. Convection proceeded thatyear to 1500 m and probably beyond.

To recap, an abnormally highatmospheric pressure over Greenlandproduced higher than normal winds southalong the east coast of Greenland, whichforced more Arctic water into the Atlanticthan usual. This Arctic water,characterized by a lower salinity than theAtlantic, created a low buoyancy cap ontop of the Labrador Sea, which helped toreduce the depth to which deep convectionoccurred in the winters of 1969-1971.

A large climatic signal such as this is ofgreat interest in itself because it showswhat changes do occur and illustratessome of the important connectionsbetween the physical processes in theocean. Understanding this chain of eventsand the magnitude of its impacts will be avery powerful economic tool.

Now that one significant change in theocean climate has been observed, it isimportant to know how often suchphenomena occur, what if any effect theyhave on the atmospheric climate, and whateffect they have on the Newfoundlandfisheries. To look a bit further, aprogramme was begun in 1978 to monitorthe flow of the Labrador Current nearHamilton Bank, Labrador. The current

meters used to measure water velocity for and change the current is increased.9 to 12 months at a time are moored at three The renewal of the water filling the toppositions: one at the 1000 m isobath in the 500 m or so of the Labrador Sea is anotherfastest part of the current and the other two process currently being investigated atin the shallower water to the west of the BIO. We are reasonably certain all thisBank. Because icebergs are numerous in water is created by mixing some Labradorthe area, the meters are near the bottom or Current water and some Gulf Stream water

The monthly averages of salinity for 11 depths at station Bravo from 1964 to 1973.

no shallower than 500 m, which is too badbecause the strongest part of the currentis near the surface, and probably anysignificant changes from one year tothe next will be observed with greatestamplitude near the surface.

A number of equipment problems havebeen encountered in this program, thestrangest being the very high andunexpected rates of corrosion in the middleof the Labrador Current that caused theloss of four instruments. Two of these wereeventually recovered with good data: onein Ireland and one in the Azores. Icebergsand/or fishing trawlers have taken anotherthree moorings but by changing themooring design, using improvedequipment, and trying to moor in the‘safe’ spots, the success rate was greatlyimproved.

The data so far show many interestingfeatures such as a seasonal change in thestrength of the main part of the current, andunexplained midwinter surges in flow overthe inner shelf, but it is probably too earlyto know if we are observing any significantclimate changes. Meantime, a lot is beinglearned about the weekly to seasonalchanges in the temperature, salinity,and velocity, and consequently ourunderstanding of the processes that control

together, but how or where this mixingoccurs is still unknown. The most likelyarea seems to be east and northeast ofFlemish Cap where water from theLabrador Current flows off the shallowcontinental shelves toward the north just tothe west at the strong northerly flow of themost northerly branch of the Gulf Stream.The Labrador water, cold and relativelyfresh beside the warm salty water fromthe south, makes for larger horizontalgradients of temperature and salinitythroughout the area. Mixing or stirring ismore likely in areas of large horizontalgradients than in areas of small gradientspartly because these regions are moreenergetic with large horizontal and verticalvelocity gradients associated with the largetemperature and salinity gradients. Thelarge horizontal velocity gradients oftenbecome unstable, breaking the frontalregions up into smaller eddies that tend tostir the different water types together. Bymapping the temperature and salinityin the area, and by analysing paths ofsatellite-tracked drifters and water-velocitydata, the processes that cause the waters tomix before they move into the middle of theLabrador Sea are being understood a littlebetter.

23

In summary, one intriguing climaticsignal has been found in the salinity values(which decreased in the late sixties) of themiddle of the Labrador Sea. This lowsalinity layer helped to limit the depth ofdeep convective mixing in winter andslightly altered the temperature andsalinity characteristics of the upper

waters of the Labrador Sea. Two fieldprogrammes are presently underway tofurther our understanding of the processesthat bring Arctic water south, mix it withthe southern waters, and cause changes inthe heat or salt content from one year to thenext.

Reference

DICKSON, R.R., LAMB, H.H., MALMBERG,S.-A., and COLEBROOK, J.M. 1975. Climaticreversal in the northern North Atlantic. Nature ,256:479-482.

Sea ice as an indicator of climate changeG. Symonds

Fluctuations in sea-ice extent recorded from 1963 to I969 are closely correlatedto contemporaneous variations in both atmosphere and ocean. Also, thepresence of sea ice increases atmospheric and possibly oceanic variability.Thus, sea ice has both a passive and an active effect on local and global climate.

From global glaciations to local year-to-year fluctuations, sea-ice extent is asensitive indicator of climate variability.This sensitivity is enhanced throughatmosphere-ice-ocean interactionswhereby sea ice responds to climatefluctuations and can in turn feedback to influence climate variability.Understanding the factors affecting thedistribution of sea ice can therefore providesome insights into factors affecting climatevariability.

The general circulation of theatmosphere is driven by the globaldistribution of heat absorbed by theatmosphere. In general the amount of heatabsorbed depends on: (1) the amount ofsolar radiation incident on the upperatmosphere; (2) the composition of theatmosphere; and (3) the reflective andabsorption characteristics of the earth’ssurface.

The atmosphere readily allows short-wave radiation (solar energy) to passthrough it to be absorbed or reflected at theearth’s surface. The energy absorbed isradiated back into the atmosphere as long-wave radiation, the main source of heat forthe atmosphere. A measure of the amountof energy absorbed and hence the heatingof the earth is provided by the albedo of thesurface-the ratio of reflected to incidentshort-wave radiation. The albedo liesbetween zero and one and the higher thealbedo, the higher the reflectivity and thelower the absorption. For flat ground androck it is 0.12-0.15, for snow and ice 0.70- 0.80. The high albedo of snow and iceleads to the positive feedback mechanismthrough which a global decrease in

24

temperature will cause an increase inice extent, which in turn decreasestemperature even more (due to the higheralbedo of ice), and thus further increasesice extent. Similarly, with increasingtemperatures and decreasing ice coverage,the associated decrease in albedo leads tofurther warming. In addition to the albedoeffect, ice also effectively insulatesthe atmosphere from the ocean. Bytransporting heat from low latitudes, theoceans provide a significant source of heatto polar regions. The presence or absenceof ice significantly affects the ocean-atmosphere heat flux and surface airtemperatures.

During the winter months, Arctic sea-ice covers an area of approximately14 x 106 km2 while in the summer thecoverage is reduced to 7 x 106 km2. In thenorthern hemisphere 7 x 106 km2 ofocean are alternatively ice covered and icefree during the course of a year. In additionto the seasonal cycle over one year, the areacovered by ice may vary by 0.3 x 106 km2

over time scales of 10 y. These figures arebased on an average over the period1953-1977 (Walsh and Johnson, 1979).Over geological time, the extent of sea icehas varied from extreme glaciationsextending as far south as 40°N to entirelyice-free periods. Fluctuations in sea-iceextent are one result of the complex air-sea-ice interaction processes and are inherentlycoupled with climatic variations.

In the northern hemisphere today, theregions where the ice cover varies greatlyfrom winter to summer and from year toyear are the seas adjacent to the ArcticOcean. In the Greenland and Labrador

Graham Symonds.

seas, Baffin Bay, and Davis Strait, theArctic outflow transports sea ice and low-salinity surface water southward along theeastern coasts of Greenland, Baffin Island,and Labrador. Because of this surfaceoutflow of water near the freezing point,sea ice forms in winter throughout this areayet melts and retreats in summer because ofthe strong solar heating at these latitudes.A similar low-salinity surface-layer allowsice to grow southward within the BeringSea. However, in the Barents Sea north ofNorway there is an inflow into the ArcticOcean of warm salty Atlantic water, whichreplaces the outflow of cold low-salinitywater from the Arctic. This provides asource of heat at these high latitudes thatkeeps parts of the Barents Sea ice freethroughout the year, and melts ice overmuch of the rest of the area in summer.Thus, ocean currents play a large role indetermining ice distribution in thenorthern hemisphere.

The extent of ice in any season in thesemarginal seas varies from year to year.When such variations persist over a

number of years and over a large area, theymay play a significant role in modifying theglobal climate. While their global effectsare still speculative, regional changes inice distributions have had profound effectson the climate of adjacent coastal areas aswell as on the local fisheries. The firstfigure shows the distribution of sea ice offLabrador and Newfoundland for Marchaveraged over the period 1963-1978. The0.5 contour represents the limit of theregion covered by ice for at least 50% ofthe period 1963-1978. This regionrepresents the average conditions forLabrador and Newfoundland. Also shownin the figure are the minimum andmaximum extremes for March (indicatedby the 1.0 and 0.1 contours respectively).During summer. the region shown in thefigure is entirely ice free. The fluctuationsin sea ice extent, both seasonally and yearto year, can be expected to affect the localclimate and in turn reflect large-scaleclimatic variations.

The atmosphere-ice-ocean coupling isillustrated in the second figure. At the topis a time series of departures from themean, or anomalies, for ice extent offNewfoundland and Labrador duringMarch from 1963-1978. Below this is theanomaly of water temperature in Marchaveraged over the upper 200 m of the watercolumn at station 27 just off St. John's.Newfoundland (see first figure). Alsoshown are the anomalies of air temperatureand westerly wind velocities in the vicinityof Battle Harbour, Labrador (see firstfigure). Obvious similarities exist betweeneach of the four series shown in the secondfigure. Warmer than normal watertemperatures are associated with belownormal ice extent and vice-versa. Both theair temperature and water temperature varyin much the same way in spite of theirspatial separation and the fact that thewater temperature is averaged over theupper 200 m of the ocean. The variationin ice extent with both air and watertemperatures is as one might expect whilethe variation with westerly wind requiressome explanation. Firstly, a westerly windblows cold air from the Canadian interiorinto the Labrador Sea; hence the inverserelationship with air temperature asshown in the second figure. Secondly, thecombination of increased wind speed andcold temperatures increases the air-sea heatflux and lowers the water temperature,which makes conditions more conduciveto ice formation. Finally, the westerly windmoves the ice offshore (approximately 30°

Sea-ice extent for March expressed as the probability of occurrence of ice determinedfrom the period 1963 to 1978. Mean, minimum, and maximum extents are representedby the 0.5, 1.0, and 0.1 contours, respectively.

March anomalies of ice extent (top) measured as the area covered by ice in the regionshown in the first figure. Corresponding anomalies of water column temperature, airtemperature, and westerly geostrophic wind illustrate atmosphere-ice-ocean coupling.

25

to the right of the wind direction) thusincreasing the offshore extent of ice and atthe same time producing areas of openwater along the coast where new ice mayform.

In addition to having important localimplications there is evidence that thevariability shown in the second figureoccurs on a much larger climate scale. AtOcean Weather Ship Bravo, in the centreof the Labrador Sea, the same signal intemperature and salinity has been observed(Lazier, 1980), which indicates variabilityon a scale that includes the Labrador Sea.Other evidence in the literature suggeststhat the variability shown in the secondfigure may be associated with large-scalefluctuations in atmospheric circulationaffecting Greenland and Northern Europe(Dickson et al., 1975). Greater thannormal sea-ice extent in the Norwegian-Greenland Seas has been related to an

intensification in a high pressure cell overGreenland and an associated increase inthe northerly wind component. In turn,heavy ice years in the Norwegian-Greenland Sea tend to be associated withlight years in Baffin Bay/Davis Strait.Furthermore, it has been well documentedthat winter temperatures tend to be lowover northern Europe when they are highover Greenland and the Canadian Arctic,and vice-versa (Van Loon and Rogers,1978). This temperature pattern has beenassociated with well-defined pressureanomalies over most of the northernhemisphere.

The fundamental outstanding problemis to separate cause from effect. Thepreceding discussion has illustrated thecoupling and feedback processes involvedin atmosphere-ice-ocean interaction,but has given no indication as to whatthe driving mechanisms are and what the

Climatic changeand the exploration of theCanadian Arctic by sea

A.J. Kerr and K. MacDonaldLooking back over a thousand years of exploration of the Canadian Arctic itappears that complex geography has had as much to do with the movement of seaice as have climatic changes. This is not to say that climatic research is not anessential feature in developing economic marine transportation as the Sovietshave shown in developing their Northern Sea Route over the last 50 years.

Much of the early exploration of ourCanadian Arctic was carried out by seaand, although air transportation has nowlargely replaced travel by ship and dogsled, an ability to move ships freelythrough Arctic waters remains important toCanada. Obviously, sea ice significantlyinhibits the movement of ships in polarregions with rough weather and evenicebergs being less important. Sea-icecover is to some extent influenced byclimatic trends, both year-to-year andlonger term. It is important, therefore, thatwe develop an understanding of howvariability of sea-ice cover has affectedArctic navigation in the past and may do soin the future.

Today in the Arctic we are interested inthe possibility of exporting large reservesof oil and natural gas, and already ore isbeing shipped from mines well above the

26

Adam Kerr and Kirk MacDonald.

response is to these processes. Anunderstanding of these processes isnecessary before we can hope to predictboth local and global variations in climateand how this climate might be modified byman’s intervention. Identifying the majordriving mechanisms is the subject ofongoing research within the AtlanticOceanographic Laboratory.

References

DICKSON, R.R., LAMB, H.H., MALMBERG,S.A. and COLEBROOK, J.M. 1975. Climatereversals in the northern North Atlantic. Nature 256:479-482.

LAZIER, J.R.N. 1980. Oceanographic conditions atOcean Weather Ship BRAVO. 1964-1974.Atmosphere-Ocean 18: 227-238.

VAN LOON, H. and ROGERS, J.C. 1978. The see-saw in winter temperatures between Greenland andnorthern Europe. Part I: General description. MonthlyWeather Review 106: 296-310.

WALSH, J.E. and JOHNSON, C.M. 1979. Ananalysis of Arctic Sea ice fluctuations. 1953-1977.Journal of Physical Oceanography 9: 580-591.

Arctic Circle. The epic voyages of thesupertanker Manhattan through theNorthwest Passage in 1969 and the SovietArktika to the North Pole in 1977demonstrated that very large ships cantravel in ice-infested waters throughout thewhole year. However, the environmentalimpact of the traffic and the design ofthe ships are not fully worked out. Inaddressing these concerns we must notonly provide answers for today but mustpredict the situation in the future when theclimate may be different. In particular, wemust attempt to predict the presence of ice

and whether it will pose an increasingdifficulty to the exploitation andexportation of hydrocarbons.

Can we relate periods of climatic changein the past with what we know of thehistory of arctic navigation? As early as330 B.C., Pypheus, a Greek navigator-astronomer, sailed from near the present-day Marseilles out into the Atlantic andthen northwards to a frozen ocean wherehis exploration was halted. This voyageoccurred during a period of climaticdeterioration with cool moist conditionsbut since neither Pypheus nor we know justwhere he was stopped by ice, we can sayno more than that this appears to be theearliest recorded arctic voyage. However.we do know that the period 950-1200 A. D.was relatively warm and that this clearlyhad a very significant effect on themovement of people into Iceland andGreenland and subsequently into theCanadian Arctic. It was during this periodthat those hardy seafarers, the Vikings,first found their way to Iceland, then tosouthern and southwestern Greenland, andfinally across the northwestern Atlantic toBaffin Island, the Labrador Coast, and to atleast one settlement in Newfoundland.From the sagas and archaeologicalevidence we know that southwestGreenland at that time was fertile and therewere many farms. Most importantly for us,regular trade was carried out betweenGreenland and Norway that later becameimpossible due to the presence of sea icearound Iceland. During this period, whenNorse adventurers travelled freely to thenortheastern shores of North America, seaice must have retreated well to the north inBaffin Bay.

From about 1200 onwards the climate ofthe northern hemisphere progressivelydeteriorated, culminating in the period1650-1750, the “Little Ice Age”. Therewas an increase in the amount of sea ice inthe northern Atlantic, and particularlyaround Greenland and Iceland, resulting inthe abandonment of the shipping routesfrom Greenland to Europe from the earlyfifteenth century until the 1720s and theeventual death of the Norse colonies.The sea-ice situation around Icelandwas particularly serious at the end ofthe sixteenth century. However, it was atthe very peak of this period (1576-1578)that Martin Frobisher, an Elizabethannavigator, made his voyages to the baynamed after him in southern Baffin Island.John Davis, another Elizabethan sailor,

This engraving depicts Edward Parry’s ships, the Hecla and Fury, wintering at WinterIsland in 1819-1820. (From: Adams, W.H.D. 1876. The Arctic World: Its Plants,Animals, and Natural Phenomena with a Historical Sketch of Arctic discovery down tothe British Polar Expedition, 1875-76. London: T. Nelson & Sons.)

managed to penetrate north of 70° latitudeinto Baffin Bay in 1587. His track up thewest coast of Greenland and then westacross Baffin Bay indicates that theinfamous “middle pack”, an area of heavypack ice in the northern part of the bay wellknown to later navigators, barred his wayfurther north. In 1616, Henry Baffin madea remarkable circumnavigation of the baynamed after him, a voyage that was onlymatched by John Ross, who followed in hisfootsteps two centuries later. Thus at thevery nadir of the Little Ice Age, Europeansailing ships were able to make their firstrecorded penetration of this easternarchipelago.

The latter half of the Little Ice Age wasnot a period of significant exploration bysea in the Canadian Arctic, thoughapparently the four voyages made intoHudson Bay then were not unduly impededby ice. At the end of the eighteenth centurythere were considerable fluctuations intemperature in northern Europe with aperiod of relative cold extending intothe first half of the nineteenth century.This was significant in terms of Arcticexploration because it coincided with theBritish Navy’s great interest in this part ofthe world. In 1818, John Ross made amajor voyage of discovery into northernBaffin Bay. On board with him as officerswere men who later would becomefamous: Edward Parry, John Franklin.George Back, Edward Sabine. and JamesClark Ross. Ross failed to recognize the

entrance to Lancaster Sound and it was leftto his second-in-command, LieutenantParry, to make a year later that truly mostremarkable of Arctic voyages across thelength of Parry channel to Winter Harbouron Melville Island. The success of thisvoyage indicates that low temperatures atleast as recorded in northern Europe are notnecessarily a good criterion for heavy icecover in the Canadian Arctic islandchannels. Parry’s voyage was followed notlong after by the ill-fated Franklin voyageand the many voyages that searched forhim subsequently. Franklin’s ships we nowknow were beset by heavy ice in PeelSound, but this was not related to unusualice or climatic conditions. Heavy iceaccumulations in Parry Channel tend topress southward through the channels tothe south becoming at times heavilyconsolidated and even barring the passageof modern icebreakers.

The final decades of the nineteenthcentury saw another cold spell in northernEurope that did not let up until after 1910,so Amundsen’s first transit of theNorthwest Passage in the little sailingvessel Gjoa from 1903-1906 may beattributed perhaps to sheer persistence.as well as skill in avoiding ice. Certainly,Joseph Bernier aboard the Arctic in1910-1911 did not find ice conditions light:he met heavy packs in Barrow Strait and.although he did manage to reach southwestMelville Island, he found - like almostall explorers before and after him - that

27

M’Clure Strait was impenetrable.Unusually warm summer temperatures

dominated the northern hemisphere fromthe 1920s to the 1940s, perhaps thewarmest era since that of the Norseexplorers: some writers have related thesuccessful transits of the RCMP vesselSt. Roche to this climatic change, butthis relationship can be questioned. Thewarming trend faltered in the fifties, a timeof considerable shipping activity in Arcticwaters. A major component of thisexpanded activity was the establishment ofthe Dewline. While warming trends mayhave been a bonus, the use of powerfulicebreakers guaranteed the success ofthese operations. The voyage of theManhattan, particularly its transit of theNorthwest Passage in 1969, contributedanother element to icebreaking technologyby reinforcing the arguments about usingmass to break up ice in congestedchannels. It became clear that very largevessels, suitably strengthened andpowered, could force their way throughalmost any kind of ice condition.Nonetheless, the Manhattan, even withthe escort of the John A. MacDonald andLouis St. Laurent. Canada’s largesticebreakers, could not penetrate themultiyear polar ice of M’Clure Strait.

In the last decade in spite of one or twoparticularly severe ice years such as thesummer of 1972, some yachts andpassenger vessels have made remarkablevoyages right through the NorthwestPassage. Because average temperaturesapparently declined during this period,these voyages are all the more remarkable.The availability of detailed icereconnaissance and short-term forecasts(a few days) was certainly a powerful factorin these arctic navigations.

Apart from the influence of majorclimatic trends the presence of ice appearsto be controlled as much by complexgeography as by variations in wintertemperature. The overall pattern ofsummer ice distribution is well known,but short-term movements are oftendifficult to predict.

In Baffin Bay, a tongue of open waterextends up the west coast of Greenland andduring the summer links up with the openNorth Water in the northern part of the bay.The latter feature is the most extensivepolynya in the Canadian Arctic. On thewestern side of the bay. the ice tends toaccumulate as the “middle pack”. anarea that proved extremely hazardous to28

CSS Hudson steams through ice inViscount Melville Sound during itscircumnavigation of the Americas in1970.

the whalers during the last century. InLancaster Sound, open water extendswestwards during the summer from theNorth Water as far as Barrow Strait. To thenorth of Devon Island, the open waterduring the summer extends into JonesSound and in most summers it extendsfurther up the west side of Ellesmere Islandacross Norwegian Bay and into EurekaSound.

To the north and west lie the QueenElizabeth Islands, where ice seldombreaks up in the summer and the channelsare usually inaccessible even to today’sicebreakers. Resolute, because of itsrelatively easy access at the western end ofLancaster Sound, has become a centralshipping point while Eureka has becomethe northernmost station regularly servedby Coast Guard icebreakers. In contrast tothe well-developed ports and even townsthat exist on the Greenland coast, the coastof Baffin Island is hazardous and

frequently beset by ice. To go westwardsfrom Resolute, the mariner has twochoices: to continue westwards viaViscount Melville Sound and Prince ofWales Strait into the Beaufort Sea, or toproceed southwards through Prince RegentInlet or Peel Sound and thence throughVictoria Strait and Coronation Gulf intothe Beaufort Sea. The northern of these tworoutes is deeper and is the only route thatwould be available to supertankers, but it isan area of heavy multiyear ice forced downthrough M’Clure Strait. The southern routeis usually easier with respect to ice, but it isrelatively shallow.

The presence of ice in either thenorthern or southern routes to the westcannot be attributed solely to climaticchanges, although an abnormally coldsummer will undoubtedly slow the break-up. In a normal year, one-year ice inViscount Melville Sound will break up andthe southward setting currents throughByam Martin Channel and McDougallSound will give open water along the northside. This was the open lead which allowedParry, Bernier, and later explorers to reachMelville Island. If the summer becomeswarmer than usual, the ice in the QueenElizabeth Islands to the north will break upand heavy multiyear ice will move south toblock Viscount Melville Sound. Some ofthis may drift even further south, blockM’Clintock channel completely, and makenavigation through Peel Sound difficult ifnot impossible. On these occasions shipswith shallow enough drafts will take aroute through Prince Regent Inlet andthen through Bellot Strait. A particularlydevastating set of circumstances can occurwhen after a warmer than usual summerthere is a cold winter that freezes themultiyear ice solidly into the new iceacross Viscount Melville Sound.

The Beaufort Sea is probably directlyinfluenced by climatic trends asanomalously low temperatures extend thelimits of the Arctic Ocean pack ice. PointBarrow is the key to unlock the BeaufortSea to ships that have not wintered in, as anextension of the Arctic pack may seal offthe Beaufort Sea completely by groundingagainst Point Barrow. The situation in theBeaufort Sea is similar to that faced in 1983by the Soviets on their Northern Sea Routewhen many ships, including icebreakers.were trapped by ice. It was the need tounderstand climatic fluctuations on thisroute that led them to initiate a majorprogram of research on the Arctic Ocean

The Canadian Arctic showing the major locations discussed in the text.

sea ice in the 1930s. Evidently, there is still hydrocarbons in the Arctic islands and themuch to be learned. Beaufort Sea that focussed our attention on

Since the establishment of the Polar ice dynamics. Practical problems of theContinental Shelf Project in 1958, Canada day include not only the study of icealso has paid more attention to increasing applied to the needs of shipping but also toits scientific knowledge of the Arctic. such problems as the construction of iceHowever, it was the search for platforms from which to operate drilling

rigs. Clearly, long-term climatic trends area factor that must be considered in many ofthese studies and research in that area is ofgreat importance for future Canadiandevelopments in the North.

29

Biological feedbackand effects

Until very recently our concerns with biology related to climatechange were restricted entirely to the consequences that climatevariability might have on our fisheries resources and wildlife. Today,our concerns are widening as we and other research groups comeincreasingly to understand that, even with regard to such processes asthe balance of carbon dioxide between atmosphere and ocean, wecannot view the oceans simply as physical and chemical systems.

We now understand, from our studies of past oceans, that the ocean’splants and animals play a key role in determining how oceans mediateclimate change. The studies reviewed in this chapter address themselvesto the consequences for animals of climate change in the ocean, butalso to the manner in which ocean plants may cause the changes tooccur in particular ways.

Carbon dioxide and the biological cycleof the ocean

A.R. Longhurst, W.G. Harrison, and T. PlattThe growth of planktonic marine plants may play an important role incontrolling the amount of atmospheric carbon dioxide, and hence the‘greenhouse effect’, yet our level of understanding of the processes of plantproduction in the ocean is inadequate to quantify this role.

I nternational concern that increasingamounts of carbon dioxide in theatmosphere may cause significant changesin the global climate during the nextcentury is based on observations that levelshave risen over the last 120 y by about20%. Considerable disagreement existsabout how this happened, and a globalmass budget for carbon dioxide still hasmany major uncertainties - perhapsespecially on the role of the ocean as asink for atmospheric carbon dioxide(e.g., Hobbie et al., 1984; Walsh, 1984).

A very recent analysis of air trapped inglacial ice from Greenland has given thestartling result that atmospheric carbon-dioxide concentrations apparently doubled(or were reduced to one half) over periodsof only a couple of hundred years about30,000-40,000 y ago (Oeschger et al.,

30

1983). It is hard to see how such rapidchanges, which must have modified theclimate, could be due to the mechanismsthat we now think we understand: theremust have been a feedback mechanismbetween the upper ocean and theatmosphere other than by simple physicalprocesses. A possible mechanism isthrough production of plant material byphotosynthesis of phytoplankton in thelighted zone of the ocean, which causes a‘biological pump’ to transfer carbondioxide from the upper ocean to the deep-ocean sediments by the fall-out of plantmaterial whether digested or not. Analysisof this mechanism immediately brings oneup against a set of much bigger problems:the global, biochemical cycling not only ofcarbon but also of nitrogen, phosphorus,and oxygen.

Unfortunately, we do not know as muchas we need to about these cycles in theocean. Worse, it now seems that we do notknow as much as we previously thought.Understanding the biogeochemical cycleof an element requires a knowledge of howmuch there is, how it is distributed amongits different forms (organically bound,ionic, gaseous, and so on), and the rates ofchange among the various forms.

One of the most important geochemicalprocesses for carbon is that associated withphotosynthesis, by which carbon dioxideis converted to carbohydrate with acorresponding release of molecularoxygen. There has been little agreementabout the rate of this process in the ocean.In addressing this basic question, theMarine Ecology Laboratory is trying tomake a contribution to understandingworld climate and the ‘greenhouse’problem.

It used to be thought (see tabulation inPlatt and Subba Rao, 1975) that the averagerate of photosynthesis by phytoplankton inthe open ocean was 50-100 g carbon m-2

y-1 based on a compilation of data fromexperiments that used radioactivelylabelled carbon dioxide. Towards the endof the seventies, these figures began to bechallenged (see Kerr, 1983); someinvestigators now suggest that the annual

photosynthetic production figures for theopen ocean be increased by a factor of 5,or even 10, revisions that if valid are ofconsiderable significance in understandingthe ‘greenhouse’ effect.

One line of evidence that has been usedin support of this argument is based on thesummer accumulation of oxygen belowthe pycnocline (Shulenberger andReid, 1981). Oxygen is evolved inphotosynthesis, but its concentration in theocean’s surface layer is usually adjusted byexchange with the atmosphere. Diffusionof oxygen from below the mixed layerinto the atmosphere is impeded by thepycnocline so that a subsurface oxygenmaximum is developed, which representsthe cumulative primary production sincethe pycnocline was formed.

A comparison was made in the centralgyre of the North Pacific Ocean betweenthis technique and the instantaneousfixation of carbon dioxide as measuredby the 14C method at the depth of thesubsurface oxygen maximum.Unfortunately, the two methods measureprocesses on vastly different scales of timeand space (Platt et al., 1984). The 14Cmethod measures photosynthesis at aparticular depth over the time required todo the experiment (not more than 24 h).The oxygen accumulation method has anintrinsic time scale of about 100 days, forwhich the corresponding space scale isabout 1 x 106m.

Further possible problems with thecomparison have been discussed by Platt( 1984). Among the more important issampling variability in 14C measurements.When small-scale variability in theamplitude of the subsurface oxygenmaximum is considered, the purporteddiscrepancy between the oxygen andcarbon fluxes becomes much less certain.

Another recent study relevant to theopen-ocean production problem is that ofWilliams et al. (1983), who compared theevolution of oxygen with the fixationof carbon dioxide in independentmeasurements on the same sample. Herethe time-scales of the two methods weremuch better matched and gave similarresults. Nonetheless, interpreting theapparent agreements between the short-term oxygen and carbon fluxes asevidence that both are accurate may be anoversimplification of a complex problem(Smith et al., 1984).

Because the surface layer of the oceancan exchange gaseous components with

Glen Harrison, Alan Longhurst, and Trevor Platt.

the atmosphere, it has been suggested thatincreasing levels of carbon dioxide in theatmosphere due to man, which havereceived so much attention in the control ofworld climate, will modify the carboncycle in the ocean, in particular that part ofthe cycle associated with photosynthesis(e.g., Holm-Hansen, 1982). Butphotosynthesis in the ocean is apparentlyalmost never limited by availability ofcarbon. Other essential elements,especially nitrogen, are in very muchsmaller supply and more likely to limitphotosynthesis.

The absolute level of primaryproductivity in the ocean is, in fact,thought to be limited by the rate at whichnitrogen can be supplied from the abyssalreservoir. This has been termed ‘new’production in contrast with productivitymaintained by biological recycling oforganically-bound nitrogen in the upperocean or ‘regenerated’ production(Dugdale and Goering, 1967). Much aswith the controversy surrounding 14Cmeasurements, attempts at quantifying‘new’ and ‘regenerated’ production usingnitrogen tracers have come under similarcriticism (e.g., Harrison, 1983). and muchis still unclear regarding the biochemicalnitrogen cycle and how it affectsprimary production (Harrison. 1982).Notwithstanding these problems,increasing the availability of carbonatoms in the surface of the ocean or in theatmosphere above it, unless complementedwith a suitable increase in availability ofnitrogen atoms, will have no direct effecton the biological production cycle.

It has been suggested that the flux ofnitrogen from the abyss, and thus ‘new’production, must be generally balanced bya flux of carbon associated with organicparticles sedimenting from the surfacelayer (Eppley and Peterson, 1979). This hasled to considerable interest in the resultsobtained from sediment traps designed tointercept these particles as they fall. Suchmeasurements are showing, (e.g. Billet etal., 1983) that the rate of sedimentation(and by implication the rate ofphotosynthesis) is by no means as constantin time as was previously supposed.

Intermittency appears to becharacteristic of ocean productivity, asit is of so many ocean properties. Untilthis variability is fully described andunderstood, our picture of oceanproductivity will be incomplete. Thepresent picture, derived fromextrapolations of isolated measurements asif intermittency were not the rule, is farfrom adequate. It may turn out that themost cost-effective way to monitor andcharacterize variability in oceanproductivity is through a global network ofsediment traps.

In some of the more remote areas of theworld’s oceans, new measurements ofphotosynthesis are changing old ideas thatwere based on little data. This is certainlytrue in Arctic waters (Subba Rao and Platt,in press) where we now believe that annualprimary production is more than an orderof magnitude higher than estimated tenyears ago. During a CSS Hudson voyagein August 1983 to Jones Sound in theCanadian Arctic. we measured more

31

Primary production rates during the development and decline of a photoplankton‘bloom’ in Jones Sound, eastern Canadian Arctic. Carbon and oxygen productivitiesare shown.

primary production in one day than hadpreviously been thought to occur in theArctic basin in one year (see figure). Alarge part of the reason for this is thatArctic productivity is strongly seasonal,and ignoring this can produce a verydistorted picture.

A similar conclusion can be reached byexamining nitrogen cycles, as was donerecently in the Antarctic by Jennings et al.(1984). They inferred, from the seasonaldepletion of nitrate, a rate of primaryproduction four times higher than previousestimates from isolated 14C experiments.They attributed the discrepancy not toa fundamental inadequacy of the 14Cmethod but rather to the difficulties ofextrapolating results over space and timein an intensely intermittent system.

Thus our understanding of the oceaniccarbon dioxide cycle, perhaps intimatelylinked with the atmospheric cycle andtherefore with the question of climatechange, is now developing in a way thatadmits of higher levels of plant productionin the ocean than was previously thoughtpossible. Where this new understanding, towhich various MEL research projects havecontributed significantly over the last fewyears, will lead us is still hard to see. It isremarkable that after so many years ofstudy, we are still unable to approach asimple global mass budget for carbon-dioxide cycling that satisfactorily accountsfor what we know of biological processes

32

in the ocean. As the inexorable rise ofcarbon dioxide and other ‘greenhouse’gases in the atmosphere continues to beobserved by our monitoring stations,biological oceanographers willincreasingly be under pressure to developinternational programmes to address theissue. Indeed, such are planned already bythe Committee for Climate Changes inthe Ocean of SCOR and WMO, and theMarine Ecology Laboratory expects tocontinue to be intimately involved in thisactivity in the coming years.

References

BILLETT, D.S.M., LAMPITT, R.S., RICE, A.L.,and MANTOURA, R.F.C. 1983. Seasonalsedimentation of phytoplankton to the deep-seabenthos. Nature 302: 520-522.

DUGDALE, R.C. and GOERING, J.J. 1967. Uptakeof new and regenerated forms of nitrogen in primaryproductivity. Limnology and Oceanography 12:196-206.

EPPLEY, R.W. and PETERSON, B.J. 1979.Particulate organic matter flux and planktonic newproduction in the deep ocean. Nature 282: 677-680.

HARRISON, W.G. 1982. Nitrogen nutritionofmarine phytoplankton: open questions. In BIOReview ‘82; Ed. M.P. Latremouille. Bedford Instituteof Oceanography, Dartmouth, Nova Scotia: 25-28.

HOBBIE, J.. COLE. J.. DUNGAN. J..HOUGHTON. R.A.. and PETERSON. B. 1984.Role of biota in global CO2 balance: The controversy.BioScience 34: 492-498.

HOLM-HANSEN, O. 1982. Effect of increased CO2

on ocean biota. In Environmental and SocietalConsequences of a Possible CO2 - Induced ClimateChange: Office of Energy Research. Washington.D.C. Vol. II: 1-22.

JENNINGS, J.C., Jr., GORDON, L.I.. andNELSON, D.M. 1984. Nutrient depletion indicateshigh primary productivity in the Weddell Sea.Nature 309: 51-54.

KERR, S.R. 1983. Are the ocean’s deserts blooming?Science 220: 397-398.

OESCHGER, H. et al. 1983. Non-anthropogenicchanges in atmospheric CO2. In Summary Report,Committee on Climatic Changes and the Ocean.UNESCO: 23-25.

PLATT, T. and SUBBA RAO, D.V. 1975. Primaryproduction of marine microphytes. Photosynthesisand productivity in different environments 3:249-280.

PLATT, T., LEWIS, M.R., and GEIDER, R. 1984.Thermodynamics of the pelagic ecosystem:Elementary closure conditions for biologicalproduction in the open ocean. In Flows of Energyand Materials in Marine Ecosystems: Theory andPractice; Ed. M.J. Fasham. Plenum Press. London:49-84.

PLATT, T. In press. Primary Productivity in theCentral North Pacific: Comparison of oxygen andcarbon fluxes.

SHULENBERGER, E. and REID, J.L. 1981. ThePacific shallow oxygen maximum, deepchlorophyllmaximum. and primary productivity reconsidered.Deep-Sea Research 28A: 901-919.

SMITH,R.E.H.,GEIDER,R.J.,and PLATT,T. Inpress. Microplankton productivity in the oligotrophicocean.

SUBBA RAO, D.V. and PLATT, T. In press. PrimaryProduction of Arctic Waters. In Polar Biology.

WALSH, J.J. 1984. The role of ocean biota inaccelerated ecological cycles: A temporal view.BioScience.

WILLIAMS, P.J. LEB,. HEINEMANN, K.R.,MARRA. J.. and PURDIE. D.A. 1983.Phytoplankton production in oligotrophic waters:Measurements by the 14C and oxygen techniques.Nature 305: 49-50.

Climate, freshwater run-off,and fisheriesK. F. Drinkwater

Effects of freshwater run-off on the physical characteristics of the continentalshelf waters of eastern Canada extend thousands of kilometres from where therivers enter the sea. They can in turn influence the survival of certain fish in theirearly life stages. Thus, there are correlations between fish abundance and riverrun-off: examples from the Gulf of St. Lawrence, Gulf of Maine, and LabradorShelf are discussed.

Marine fish populations respond tochanges in ocean climate. These can berather dramatic as in the case of the tenfolddecrease in the anchovy catches off Perufollowing the cessation of upwellingcaused by the El Niño event in 1972 orthe threefold increase in cod catches offwestern Greenland following the warmingtrend in the fifties. Changes in climatecan bring about shifts in geographicaldistributions such as the alternation ofNorth Sea herring between the coasts ofNorway and Sweden during warm and coldperiods, respectively. The influence of thephysical environment on the fish andshellfish populations in the northeastAtlantic has been the subject of severalinvestigations (e.g., ICNAF. 1965) withsea temperatures the climatic factor mostoften considered. For example, duringcolder than normal years the number ofcod caught on Georges Bank increases(Martin and Kohler, 1965) but Gulf ofMaine lobster catches decrease (Dow,1969; Flowers and Saila, 1972). Over thelast decade scientists from the MarineEcology Laboratory have been studyingthe role of freshwater run-off on the majorcommercial species off eastern Canada.This article briefly describes some of theimportant findings from that research.

Sutcliffe (1972) in a study of a smallembayment along Nova Scotia’s Atlanticcoast observed a direct correspondencebetween fluctuations in the amount of localfreshwater run-off and the rate of primaryproduction. Lacking adequate statisticsfrom the embayment for testing long-termrelationships he turned his attention to theGulf of St. Lawrence. Not only are therelong time series records for the Gulf butthe freshwater run-off is very large. The St.Lawrence River system alone discharges424 km3/y of freshwater. a quantitygreater than the sum of the entire run-off(353 km3/y) along the eastern coast of the

United States from the Canadian boundaryto the southern tip of Florida (Sutcliffeet al., 1976). The influence of the St.Lawrence discharge is traceablethroughout the Gulf of St. Lawrence ontothe Scotian Shelf and as far south as theGulf of Maine (Sutcliffe et al., 1976).Year-to-year changes in the freshwaterdischarge or its seasonal pattern canproduce measurable effects on thesalinity and stratification of the watersdownstream. For example, the summersalinities in the surface waters of theMagdalen Shallows are determined by thespring run-off from the St. Lawrence River(Lauzier, 1957).

Sutcliffe (1972) investigated therelationship between fish abundance andSt. Lawrence River discharge. Quebeclandings of halibut, haddock, soft-shellclams, and lobster were all found to bepositively correlated with the annual run-off. The maximum correlation coefficientsoccur when the fish lags the riverdischarge. The lag time in years is speciesdependent and is approximately equal tothe age at maturity (i.e., the age it entersthe fishery). This indicates that run-offaffects the fish’s first year of life and isconsistent with other biological studiesthat suggest fish abundance is determinedin the egg and larval stages. Sutcliffeargued further that, if the St. LawrenceRiver is primarily influencing the first yearof life, then higher correlations may resultif run-off at critical months is used ratherthan annual means. This was subsequentlyshown to be correct with the springdischarge correlating most closely with thelagged fish abundance (Sutcliffe, 1973).The similarity in the lobster landings andApril run-off is shown in the first figure.As a result of the lag times between riverdischarge and fish, predictions of fishcatch can be made from the correlationswith run-off (Sheldon et al., 1982).

Ken Drinkwater.

It was originally thought that increasedfreshwater discharge causes nutrientenrichment of the surface layers throughestuarine circulation and mixing(Sutcliffe, 1973). The excess nutrients thenlead to increased biological productionthat enhances larval fish survival. Laterstudies showed that an important effect ofincreased freshwater flow is to intensifystratification downstream, which causesgreater heat retention near the surface (G.Bugden, personal communication). This,in part, accounts for the close resemblancebetween St. Lawrence River run-off andcoastal sea-surface temperature records(Sutcliffe et al., 1976).

The physical effects of the freshwaterdischarge from the St. Lawrence River arenot limited to the Gulf of St. Lawrence butextend beyond to the Scotian Shelf andthe Gulf of Maine (Sutcliffe et al., 1976).Therefore, investigations into the possibleeffects of the St. Lawrence River on Gulfof Maine fish stocks were undertaken.Catches of 10 out of 15 commercial marinespecies of fish and shellfish in the Gulf ofMaine showed significant correlation withthe St. Lawrence River run-off (Sutcliffe etal., 1977). As in the Gulf of St. Lawrence,maximum correlations occurred when thefish was lagged by a time approximatelymatching its age at commercial size. Whileover half of the species in the Gulf ofMaine were positively correlated withrun-off, four species were negativelycorrelated. Fish abundance was also related

33

Three-year running means of theQuebec lobster landings and thecombined April river discharge fromthe St. Lawrence, Ottawa and SaguenayRivers.

to coastal sea-surface temperatures, aresult that is not surprising given the highcorrelation between the sea-surfacetemperatures and the river discharge. Thepositively correlated species are generallyconsidered to be near the northern limitof their distributional range, while on theother hand many of the negativelycorrelated species are near their southernlimit. If temperatures are warm then it isgood for the warm-water species but not sogood for the cold-water species.

Having observed the large geographicarea over which the effects of St. LawrenceRiver are felt, Sutcliffe and coworkersinvestigated another important source offreshwater in eastern Canada - the run-offinto Hudson Bay. The total freshwaterdischarge into Hudson Bay and James Bayis 523 km3/y (Prinsenberg, 1980), anamount even larger than that of the St.Lawrence system. The peak monthly meandischarge in June can be traced as a salinityminimum down the Labrador Shelf,onto the Grand Banks (Sutcliffe et al.,1983), and apparently onto the southernNewfoundland Shelf (Petrie andAnderson, 1983). Sutcliffe et al. (1983)also related the abundance of Atlantic codstocks on the southern Labrador Shelf andnorthern Newfoundland shelf to changes insurface-layer salinity (see second figure).The correlations between cod and salinityare positive indicating high salinity (i.e.low run-off) promotes cod production.They argue that tidally-generated mixingwithin Hudson Strait increases thenutrients and the salinity in the surfacewaters. These waters are carried by theresidual circulation onto the northernLabrador Shelf where the nutrientspromote primary production. In the timerequired for a food chain to develop, thewater is advected southward by the

34

Labrador Current; this explains thesouthward increase in fish concentrationsalong the Labrador Shelf. In years of highfreshwater-outflow from Hudson Bay, theincreased stratification suppresses mixing,which reduces nutrients and lowers thesalinity of the water on the Labrador Shelf;less food is then available to the cod.

Future research will be directed towardsa further understanding of the actualmechanisms linking fish with run-off.These will include studies on the role offreshwater discharge on the physicaloceanography of the continental shelvesoff Canada’s east coast as well ascontinuing to relate environmentalfluctuations to changes in fish abundance.

The measured abundance of Atlanticcod in southern Labrador and northernNewfoundland and the abundancecalculated from correlations withsalinities.

References

DOW, R.L. 1969. Cyclic and geographic trends insea water temperatures to American lobster. Science164: 1060-1063.

FLOWERS, J.M. and SAILA, S.B. 1972. Ananalysis of temperature effects on the inshore lobsterfishery. Journal of the Fisheries Research Board ofCanada 29: 1221-1225.

ICNAF (International Commission for NorthwestAtlantic Fisheries). 1965. Special Publication No. 6.ICNAF Environmental Symposium. Rome. 1964:914 p.

LAUZIER, L.M. 1957. The St. Lawrence spring run-off and summer salinities in the Magdalen Shallows.Bulletin of the Fisheries Research Board of Canada111: 193-194.

MARTIN, W.R. and KOHLER, A.C. 1965.Variation in recruitment of cod (Gadus morhua) insouthern ICNAF waters. as related to environmentalchanges. ICNAF. Special Publication 6: 833-846.

PETRIE, B. and ANDERSON, C. 1983. Circulationon the Newfoundland continental shelf. Atmosphere-Ocean 21: 207-226.

PRINSENBERG, S.J. 1980. Man-madechanges inthe freshwater input rates of Hudson and James Bays.Canadian Journal of Fisheries and Aquatic Sciences37: 1101-1110.

SHELDON, R.W., SUTCLIFFE, W.H. JR., andDRINKWATER, K. 1982. Fish production inmultispecies fisheries. In Multispecies Approaches toFisheries Management Advice: Ed. M.C. Mercer.Canadian Special Publication of Fisheries andAquatic Sciences 39: 28-34.

SUTCLIFFE, W.H. JR. 1972. Some relationsof landdrainage. nutrients. particulate material and fish catchin two eastern Canadian bays. Journal of the FisheriesResearch Board of Canada 29: 357-362.

SUTCLIFFE, W.H. JR. 1973. Correlations betweenseasonal river discharge and local landings ofAmerican lobster (Homarus americanus) andAtlantic halibut (Hippoglossus hippoglossus) inthe Gulf of St. Lawrence. Journal of the FisheriesResearch Board of Canada 30: 856-859.

SUTCLIFFE, W.H. JR., LOUCKS, R.H., andDRINKWATER, K.F. 1976. Coastal circulation andphysical oceanography of the Scotian Shelf and theGulf of Maine. Journal of the Fisheries ResearchBoard of Canada 33: 98-115.

SUTCLIFFE, W.H. JR., DRINKWATER, K.F., andMUIR, B.S. 1977. Correlationsof fishcatches andenvironmental factors in the Gulf of Maine. Journalof the Fisheries Research Board of Canada 34:19-40.

SUTCLIFFE, W.H. JR., LOUCKS, R.H.,DRINKWATER, K.F. and COOTE, A.R. 1983.Nutrient flux onto the Labrador Shelf from HudsonStrait and its biological consequences. CanadianJournal of Fisheries and Aquatic Sciences 40:1692-1701.

Breeding of Arctic seabirdsin unusual ice years:

The Thick-billed Murre Uria lomvia in 1978*

D.N. Nettleship, T.R. Birkhead, and A.J. GastonUnusually severe ice conditions in Lancaster Sound during 1978 resulted inThick-billed Murres breeding three weeks later than normal: smaller eggs andchicks were produced, parental behaviour was abnormal, fledging successdeclined, and almost all chicks were lost immediately after fledging.

Total reproductive failure amongseabirds is unusual, particularly amongspecies breeding in temperate or arcticregions (Belopol’skii, 1957; Freuchen andSalomonsen, 1958; Salomonsen, 1972).Here we present, for the first time, adetailed account of the effect of unusuallysevere ice conditions on the breeding ofThick-billed Murres Uria lomvia.

The study was conducted in 1978 atPrince Leopold Island at the western endof Lancaster Sound, N. W.T., with someadditional observations near Cape Hay,Bylot Island, and at Cambridge Point,Coburg Island. Between 86,000 and160,000 pairs of Thick-billed Murresbreed at these colonies (see first figure).Detailed records of ice conditions in theregion have been kept since the late forties,and in all previous years ice in LancasterSound (west to Prince Leopold Island) hasremained open or broken up and moved outduring the spring or summer, usually bylate April. In 1978, however, PrinceLeopold Island remained ice-locked, andLancaster Sound was choked with largeice-pans throughout the summer. CapeHay was near the ice edge in 1978, andCoburg Island was ice-free throughout the1978 breeding season. We comparedfeatures of the breeding biology of Thick-billed Murres at Prince Leopold Island in1978 with data from 1975/1977 when iceconditions were relatively normal (Gastonand Nettleship, 1981) and fell within theaverages shown in the first figure. Allresults in the text refer to Prince LeopoldIsland unless otherwise stated.

The median egg-laying date in 1978(18 July) was approximately 18 days later

than in 1975-1977 (see second figure).Mean laying dates differed significantly(P<0.001) between years, and laying in1978 was significantly later (P<0.05) thanin any previous year. Counts of the totalnumber of eggs laid on four study plotsshowed that at least 97% of the 1975-1977population bred in 1978. The timing ofbreeding at Cape Hay in 1978 was similarto that at Prince Leopold Island;extrapolating from a small sample (n = 63)of hatching dates, the median laying date atCape Hay was 20 July

Thick-billed Murres produced relativelysmall eggs in 1978 in comparison withprevious years. Mean egg volumes differedsignificantly between years (F3.446 =15.6, P<0.001). In 1975 and 1976volumes were not significantly different,nor were those in 1977 and 1978 (all otherpair-wise comparisons were: Duncan’sMultiple Range Test, P<0.05). In additionthere were no significant differences in eggvolume between Prince Leopold Island,Cape Hay, and Cambridge Point in 1978(the size of breeding adults did not differbetween these colonies). This indicatesthat environmental conditions had very farreaching effects on food availability, andwere not restricted to birds breeding atPrince Leopold Island.

The mean egg volume at Prince LeopoldIsland in 1978 was not significantlydifferent from that in 1977 when laying wassignificantly later than in 1975 or 1976,although the difference in median layingdates was only four days (Gaston andNettleship, 1981). This suggests, first,that there might be a minimum viableegg volume of about 78-80 cm3 for

* This investigation is associated with the program ‘Studies on northern seabirds’. Seabird ResearchCanadian Wildlife Service. Environment Canada (Report No. 184).

Unit,

1Ambient temperatures were recorded each day at 0700 and 1900 local time, and the mean values determined.The chick-rearing period was here defined as from the start of hatching through to the median fledging date.Averagedaily temperatures: 1975: + 2.5°C. 1976: +0.7°C. 1977: + 2.5°C. and 1978: -1.0C.

David Nettleship.

Thick-billed Murres in Lancaster Soundpopulations. Second, it suggests that theremay be a trade-off between egg-volumeand timing of breeding, so that the birdsminimize the delay in laying by producingsmaller eggs. In 1978 feeding conditionsduring the period of egg formation musthave been considerably worse than in 1977since it took 18 days longer than normal toaccumulate sufficient food reserves toproduce even minimum-sized eggs.

Body weights of adult murres during theincubation period were not significantlylower in 1978 than in other years, andincubation proceeded normally in 1978,with the mean incubation period (32.1days) similar to that in previous years(Gaston and Nettleship, 1981).

Chick growth rates were lower in 1978than in previous years. The mean weight oftwo-day old chicks in 1978 was 66.0 g ± 1.72S.E. (n=21), 8% lower than in1975-1977 (70.8 - 72.2 g). By day 14 thepercentage difference in mean weightsbetween 1978 and previous years hadincreased to 17% (1978: 155.7 g,1975-1977: 204.5-221.5g). Thesedifferences could be due to chicks hatchingfrom relatively small eggs in 1978, areduction in calorific intake, or increasedenergy consumption due to changes inbrooding attentiveness of the adults or todifferences in air temperature. Mean airtemperatures during the chick-rearingperiod were slightly lower in 1978 1 and, inmarked contrast to previous years (Gastonand Nettleship, 1981) and other studies(Birkhead, 1976), some adult murres left

35

Distribution and concentration of ice in Lancaster Sound and fast ice edges (1.0 or 10/10 ice cover). Middle-shows areas ofvicinity in normal years and in 1978: hatched lines show close pack ice (0.8 or 8/10 ice cover) to compact or consolidatedboundaries between ice and water areas (double hatched: pack ice (1.0 or 10/10 ice cover). Late-shows areas of open packnormal years; single hatched: 1978). Early-shows locations of ice in 1978.

their chicks unattended for up to four hoursat a time, especially towards the end of theseason. Despite these marked differencesin growth patterns and behaviour, the meanduration of the chick-rearing period (2 Idays) did not differ between years. In a verylate season on the Murman coast (KolaPeninsula, U.S.S.R.), some adult murresabandoned eggs and chicks after mostchicks had fledged (Kartashev, 1960).

The breeding success of about 350 pairsof Thick-billed Murres was monitored ineach of the four years: the proportion ofeggs that hatched in 1978 (81.4%) wassimilar to l975-1977 (82.5 - 86.3%). butthe proportion of young that survived tofledge in 1978 (81.8% ) was low comparedwith 1975-1977 (90.9-91.9%):(combining data for 1975-1977: X2

1 =21.2, P<0.001). In 1978 several chickswere found dead at their sites, apparentlydue to starvation. No deaths fromstarvation were suspected in earlier years

36

(Gaston and Nettleship, 1981). Breedingsuccess was lower in 1978 (66.6%) than inany preceding year (74.9-79.3%).Evidence from fledging weights suggestedthat young murres in 1978 fledged at about20% below normal weight (Gaston andNettleship, 1981). Although there are nodata on the subsequent survival of murrechicks, it seems likely that very lightchicks would have less chance of survivingthan average or heavy chicks (Perrins etal., 1973).

Fledging chicks and theiraccompanying adults from Prince LeopoldIsland swim east out of Lancaster Sound.and then south to southwest Greenlandwhere they overwinter. In 1978 fledgingdid not proceed normally, and adultsattempted to encourage chicks less than15 days old (i.e.. below the minimumfledging age) to Hedge. During fledgingmost chicks managed to alight in openwater between pans of ice which

encompassed the island. Chicks appearedto have some degree of control over theirdescent and actively avoided the ice.Fledging chicks and adults wereconfronted with approximately 300 kmof heavy ice concentration includingenormous ice floes (5-10 km across).which separated them from open waternear the entrance to Lancaster Sound.Adults and chicks started to walk over theice, but virtually all chicks perished as aresult of exhaustion and/or exposure, and itseems likely that no chicks from PrinceLeopold Island survived in 1978. At CapeHay and Coburg Island, ice cover wasmuch less, so most chicks probablyfledged successfully. However, if they alsoHedged at very low body weights as a resultof breeding late, it seems likely that post-Hedging survival would be low.

The long-term effect of one year’sreproductive failure on the numbers ofThick-billed Murres must be considered in

Thick-billed Murres on section of east cliffs at PrinceLeopold Island, August 1978, showing density of breedingbirds and characteristics of the rock ledge habitat.

Thick-billed Murre and egg, a sea-cliff colonially breedingarctic seabird.

relation to their population dynamics.Thick-billed Murres exhibit low adultmortality with a breeding life of at least10 y and delayed onset of breeding(probably commencing in the 5th year) andlow annual productivity (Birkhead andHudson, 1977). However, a decrease inproductivity or juvenile survival in oneyear will have only a minor effect onsubsequent population size (Wooler andCoulson, 1977), particularly if juvenilemortality is density dependent. Thus, lowproductivity one year may be offset byincreased juvenile survival in the next.On the other hand, even a small increase

in adult mortality is likely to have asubstantial and long-lasting effect onpopulation size. For example, a specieswith a 95% annual adult survival rate needonly suffer a 5% decrease in survival todouble its mortality rate. This means thatseabird populations can readily withstanda ‘natural disaster’ such as the 1978 ice andassociated climatic conditions, whichaffects only productivity, because theirlife-history pattern has evolved to copewith such events. They are, however, muchless likely to recover from any factor (suchas oil pollution, gill-netting, and hunting)that increases adult mortality. Of all

seabirds breeding in Lancaster Sound,Thick-billed Murres are especiallyvulnerable to increased adult mortality,through man’s activities in arctic regions.Already, salmon gill-net fishing offsouthwest Greenland (the wintering areafor most of the Lancaster Sound Thick-billed Murre population) has causedmassive mortality (Tull et al., 1972;Nettleship, 1977). Now, in addition, thereis the threat of oil pollution as a result ofoffshore drilling (Milne and Smiley, 1978)and tanker transport.

37

Egg-laying dates of Thick-billed Murresat Prince Leopold Island in fourseasons. The heavy arrow indicatesthe median laying date. Studies for1975-1977 commenced on 18 May,7 May, and 1 June, respectively; studiesin 1978 were initiated on 21 July oncethe unusual ice conditions in LancasterSound were identified and reported.Laying dates for 1978 were extrapolatedfrom hatching dates using the meanincubation period (32 days) derivedfrom the 1975-1977 data. Thick-billed Murre breeding habitat - top of cliffs at Prince Leopold Island.

References

BELOPOL’SKII, L.O. 1957. Ecology of sea colonybirds of the Barents Sea. (Translated from Russian.1961.) Israel Program for Scientific Translations,Jerusalem: 346 p.

BIRKHEAD, T.R. 1976. Breeding biology andsurvival of Guillemots Uria aalge. Unpubl. D. Phil.thesis, University of Oxford, Oxford: 204p.

BIRKHEAD, T.R. and HUDSON, P.J. 1977.Population parameters for the Common GuillemotUria aalge. Ornis Scandinavica 8: 145-154.

FREUCHEN, P. and SALOMONSEN, F. 1958. TheArctic Year. G.P Putnam’s & Sons. New York: 438p.

GASTON, A.J. and NETTLESHIP, D.N. 1981. TheThick-billed Murres of Prince Leopold Island - astudy of the breeding ecology of a colonial high arctic

seabird. Canadian Wildlife Service MonographSeries No. 6, Ottawa: 350p.

KARTASCHEW, N.N. 1960. Die Alkenvogel desNordatlantiks. A. Ziemsen VerIag. Wittenberg.Luthesstadt: 154p.

MILNE, A.R. and SMILEY, B.D. 1978.Offshorcdrilling in Lancaster Sound - possible environmentalhazards. Institute of Ocean Sciences. CanadaDepartment of Fisheries and Oceans, Sidney. B.C. :95p.

NETTLESHIP, D.N. 1977. Seabird resources ofeastern Canada: status. problems and prospects.In Proceedings of a symposium on Canada’sEndangered Species and Habitats; Eds. T. Mosquin

and C. Suchal. Canadian Nature Federation SpecialPublication No. 6. Ottawa: 96-108.

PERRINS, C.M., HARRIS, M.P., and BRITTON,C.K. 1973. Survival of Manx Shearwaters Puffinuspuffinus. Ibis 115: 535-548.

SALOMONSEN, F. 1973. Zoogeographical andecological problems in arctic birds. Proceedings ofthe International Ornithological Congress 15: 25-77.

TULL, C.E., GERMAIN, P., and MAY, A.W. 1972.Mortality of Thick-billed Murres in the westGreenland salmon fishery. Nature 237: 42-44.

WOOLER, R.D. and COULSON, J.C. 1977. Factorsaffecting the age of first breeding of the KittiwakeRissa tridactyla. Ibis 119: 339-349.

38

Charts and Publications

CHART PRODUCTION

The Atlantic Region of the CanadianHydrographic Service has a cartographicstaff of 25, with the responsibility for 433navigational charts covering the regionfrom the Bay of Fundy to Prince of WalesStrait in the Arctic.

During 1983, 5 new charts, 3 standardnew editions, 25 new editions for Loran Cand/or Decca, 7 chart correction patches,and 43 Notices to Mariners were producedby C.H.S. Atlantic. In addition to this,21 new editions for Loran C were alsoproduced in the Atlantic Region bycommercial contract. Our headquartersoffice produced for the region 4 newcharts, 21 new editions (primarily toincorporate the new 1 ALA buoyagesystem), and 30 reprints. For the first timein the Atlantic Region, 14 charts wereprinted by contract in Halifax, N.S.

New Charts4000 Gulf of Maine to Baffin Bay4006 Newfoundland to Bermuda4245 Yarmouth Harbour and Approaches4277 Great Bras d’Or, St. Andrews

Channel4843 Head of St. Mary’s Bay5044 Cape Harrison to Dog Island5045 Dog Islands to Cape Makkovik7540 Bridport Inlet and Approaches7552 Bellot Strait and Approaches

New Editions and Reprints4001 Gulf of Maine to Strait of Belle Isle4010 Bay of Fundy Inner Portion4011 Approaches to Bay of Fundy4013 Halifax to Sydney4015 Sydney to Saint Pierre4016 Saint Pierre to Saint John’s4017 Cape Race to Cape Freels4021 Pointe Armour to Cape Whittle4022 Cabot Strait and Approaches4023 Northumberland Strait4128 Approaches to Saint John Harbour4154C Nactaquac Dam to Newbourg

Junction4145.1 Nactaquac Dam to Newbourg

Junction4145.2 Nactaquac Dam to Newbourg

Junction

4275431943434384439944034462446344644519

St. Peters Bay 7950Saint John Harbour and ApproachesFriar Roads

4520453045444545

Pearl Island to Cape LaHaveParrsboro Harbour and ApproachesEast Point to Cape BearSt. Georges BayCheticamp to Cape MabouCheticamp to Cape St. LawrenceMaiden Arm, Spring Inlet andApproachesOrange Bay to Cape BonavistaHamilton Sound, Eastern PortionDeer and St. James HarboursSmith and Random Sounds, EasternPortion

45754577

Cape Boyle to Renews HarbourOld Perlican and Winterton to HeartsContent

459845994611462246244625462646354700470347164730473147454771

Bay of Exploits Sheet IV North-EastLittle Bay Island to League PointGrand Bank and ApproachesCape St. Marys to Argentia HarbourLong Island to St. Lawrence HarbourBurin Peninsula to Saint PierreSaint Pierre and MiquelonCape Ray to LaPoile BayBelle Isle to Resolution IslandWhite Point to Corbet IslandChateau BayNain to Domino PointStrait of Belle Isle to Domino RunWhite Point to Sandy IslandEclipse Harbour to Cape WhiteHandkerchief

477547765001515052515391701170537065712671277170721773027404

Nain to Saglek BaySaglek Bay to Buttons IslandLabrador Sea

7430

White Bear Island to Ragged IslandPayne Bay and ApproachesDouglas Harbour and ApproachesHudson Strait to GrønlandPadloping Island to Clyde InletMill Island to Winter IslandCulbertson Island to FrobisherKoojeese Inlet and ApproachesExeter Bay and ApproachesScott Inlet to Pond InletLady Ann Strait to Smith SoundFrozen Strait, Lyon Inlet andApproachesRepulse Bay, Harbour Island toTalon Bay

7455 Igloolik and Approaches7465 Frustration Bay and Approaches7930 Hell Gate and Cardigan Strait

795480058007800880098010801180128013801480158046804780488049

Jones Sound, Norwegian Bay andQueens ChannelCape Stallworthy to Cape DiscoveryGeorges BankHalifax to Sable IslandBanquereau and Misaine BanksGrand Banks of NewfoundlandGrand Banks (Southern Portion)Grand Banks (Northern Portion)Flemish PassFlemish CapGrand Banks (North-East Portion)Funk Island and ApproachesButton Island to Cod IslandsCod Island to Cape HarrisonCape Harrison to St. Michael BaySt. Michael Bay to Gray Island

Large Corrections (Patches)4637 Burgeo and Ramea Island4703 White Point to Corbet Island4744 Approaches to Spotted Island

Harbour4745 White Point to Sandy Island4910 Miramichi5133 Domino Point to Cape North

PUBLICATIONS

We present below an alphabetical listingby author of BIO publications for 1983.Articles published in scientific andhydrographic journals, books, conferenceproceedings, and various series oftechnical reports are included. For furtherinformation on any publication listed hereplease contact: Publication Services,Bedford Institute of Oceanography,P.O. Box 1006, Dartmouth, Nova Scotia,Canada B2Y 4A2.

ABOU DEBS, C. et NIVAL, P. 1983. Etude dela ponte et du développement embryonnaire enrelation avec la temperature et la nourriture chezTemora stylifera Dana (Copepoda: Calanoida).Journal of Experimental Biology and Ecology72: 125-145.

ADDISON, R.F. 1983. PCB replacements indielectric fluids. Environmental Science andTechnology 17: 486A.

ADDISON, R.F., PATERSON, S., andMACKAY, D. 1983. The predictedenvironmental distribution of some PCB

39

replacements. Chemosphere 12 : 827-834.

AGTERBERG, F.P. and GRADSTEIN, F.M.1983. System of interactive computer programsfor quantitative stratigraphic correlation.Geological Survey of Canada, Paper 83-1A:83-87.

AKSU, A.E. and PIPER, D.J.W. 1983.Progradation of the Late Quaternary GeditzDelta, Turkey Marine Geology 54: 1-25.

ALZIEU, C., BEWERS, J.M., andDUINKER, J.C. 1983. Administrativesummary report of the ICES fifth roundintercalibration for trace metals in seawater(S/TM/SW). International Council for theExploration of the Seas, Report CM 1983/E: 28: 4p.

ANDERSEN, L.G., DYRSSEN, D.W.,JONES, E.P., and LOWINGS, M.G. 1983.Inputs and outputs of salt, freshwater, alkalinity,and silica in the Arctic Ocean. Deep-SeaResearch 30: 87-94.

ANDERSON, N.M. and KERR, A.J. 1983.Exploring Arctic seas - today and yesterday.Canadian Special Publication of Fisheries andAquatic Sciences 67: 78-84.

ANON. 1983. Bay of Fundy bibliography:Supplement III. Proceedings of the NovaScotian Institute of science 33: 101-105.

BARRON, J.L., DYRSSEN, D., JONES,E.P., and WEDBORG, M. 1983. Acomparison of computer methods for seawateralkalinity titrations. Deep-Sea Research 30:441-448.

BARSS, M.S. and WILLIAMS, G.L. 1983.Alphabetical listing of fossil dinocyst species.Canadian Technical Report of Hydrographyand Ocean Sciences No. 23: 48 p.

BATES, S.S., LETOURNEAU, M.,TESSIER, A., and CAMPBELL, P.G.C. 1983.Variation in zinc adsorption and transportduring growth of Chlamydomonas variabilis(chlorophyceae) in batch culture with dailyaddition of zinc. Canadian Journal of Fisheriesand Aquatic Sciences 40: 895-904.

BEARDSLEY, R.C., MILLS, C.A., SMITH,P.C., and BUTMAN, B. 1983. Mean Euleriansubsurface currents measured in the Gulf ofMaine and adjacent Scotian and New Englandshelf and slope regions, 1974-1980. WoodsHole Oceanographic Institution, ReportWHOI-83-44.

BENOIT, J.R. and MUNGALL, J.C.H. 1983.Proceedings of the 1982 Grand Banks CurrentWorkshop. Canadian Technical Report ofHydrography and Ocean Sciences 28: iv +43 p.

BERMAN, S.S., MYKYTIUK, A.P.,YEATS, P.A., and BEWERS, J.M. 1983.ICES fifth round intercalibration for trace40

metals in seawater, ICES S/TM/SW (Section 3)Preliminary Report. International Council forthe Exploration of the Seas, Report CM 1983/E:24:33 p.

BERNSTEIN, B.B., SCHROETER, S.C., andMANN, K.H. 1983. Sea urchin(Strongylocentrotus droebachiensis)aggregating behavior investigated by a subtidalmultifactorial experiment. Canadian Journal ofFisheries and Aquatic Sciences 40: 1975-1986.

BEWERS, J.M. 1983. Report of the ICESobservers to the meeting of the Ad HocScientific Group of the London Convention.In Observers’ Reports from CooperatingOrganizations. International Council for theExploration of the Seas, Paper CM 1983/GEN. 1: 6-7.

BEWERS, J.M. and DUINKER, J.C. 1983.Methods of assessing gross riverine dischargesof trace metals and organohalogens into themarine environment. In Report of the ICESAdvisory Committee on Marine Pollution(1982). International Council for theExploration of the Seas, Cooperative ResearchReport 120: 60-72.

BEWERS, J.M. and WINDOM, H.L. 1983.Intercomparison of seawater sampling devicesfor trace metals. In Trace Metals in Sea Water.Plenum Publishing Corp.: 143-154.

BEWERS, J.M. and YEATS, P.A. 1983. ICESfifth round intercalibration for trace metals inseawater (ICES S/TM/SW). Report ofSection 1: Comparison of filtration procedures.International Council for the Exploration of theSeas, Report CM1983/E:18: 21 p.

BEWERS, J.M. and YEATS, P.A. 1983.Transport of metals through the coastal zone.International Council for the Exploration of theSeas, Report 118: 146-163.

BEZANSON, D. and KRANCK, K. 1982.Near-bottom sediment suspensions measuredby sediment trap. In Report on Ocean DumpingResearch and Development, Atlantic Region,1980-81. Environment Canada, SurveillanceReport EPS-5-AR-82-1.

BIRKHEAD, T.R., JOHNSON, S.D. andNETTLESHIP, D.N. 1983. Extra-pairmatings, operational sex ratio and mateguarding in the Common Murre Uria aalge.Canadian Wildlife Service, “Studies onNorthern Seabirds,” Manuscript ReportNo. 168: 1-28.

BIRKHEAD, T.R., JOHNSON, S.D. andNETTLESHIP, D.N. 1983. A possible hybridmurre Uria allge x Uria lomvia. CanadianWildlife Service, “Studies on northernseabirds,” Manuscript Report No. 166: 1-6.

BIRKHEAD, T.R. and NETTLESHIP, D.N.1983. Alloparental care in the Common MurreUria aalge. Canadian Wildlife Service,“Studies on northern seabirds,” ManuscriptReport No. 167: 1-10.

BIRKHEAD, T.R. and NETTLESHIP, D.N.1983. Studies of alcids breeding at the GannetClusters, Labrador, 1982. Canadian WildlifeService, “Studies on northern seabirds,”Manuscript Report No. 149: 1-115.

BRODIE, P.F. and BECK, B. 1983. Predationby sharks on the grey seal (Halichoerus grypus)in eastern Canada. Canadian Journal ofFisheries and Aquatic Sciences 40: 267-271.

BROWN, B.E. and HALLIDAY, R.G. 1983.Fisheries resources of the Northwest Atlantic -some responses to extreme fishingperturbations. In Proceedings of the JointOceanographic Assembly 1982 - GeneralSymposia. Canadian National Committee/Scientific Committee on Oceanic Research,Ottawa, Ontario: 96-109.

BROWN, R.G.B. 1983. Birds and the sea.Oceanus 26 (1): 2-10.

BUCKLEY, D.E. and WINTERS, G.V. 1983.Geochemical transport through the Miramichiestuary. In Proceedings of the Conference onPollution in the North Atlantic Ocean; Eds.J.W. Farrington, J.H. Vandermeulen, and D.G.Cook. Canadian Journal of Fisheries andAquatic Sciences 40 (Supplement 2): 162-182.

BUJAK, J.P. and DAVIES, E.H. 1983.Fluorescence helps find oil. Geos 12: 5-8.

BUJAK, J.P. and DAVIES, E.H. 1983. Modernand fossil Peridiniineae. American Associationof Stratigraphic Palynologists, ContributionSeries 13: 203 p.

BURDIGE, D.J. and KEPKAY, P.E. 1983.Determination of bacterial manganeseoxidization rates in sediments using an in-situdialysis technique. Geochimica etCosmochimica Acta 47: 1907-1916.

BURKE, R. 1983. The Canadian HydrographicService (Atlantic) sweep program - A statusreport. Lighthouse 27.

CAMPANA, S.E. 1983. Feeding periodicityand the production of daily growth incrementsin otoliths of steelhead trout (Salmo gairdneri)and starry flounder (Platichthys stellatus).Canadian Journal of Zoology 61: 1591-1597.

CAMPANA, S.E. 1983. Calcium depositionand otolith check formation during periods ofstress in coho salmon, Oncorhynchus kisutch.Comparative Biochemistry and Physiology75(A): 215-220.

CAMPANA, S.E. 1983. Mortality of starryflounders (Plcrtichthys stellatus) with skintumors. Canadian Journal of Fisheries andAquatic Sciences 40: 200-207.

CARTER, L. and SCHAFER, C.T. 1983.Interaction of the western boundaryundercurrent with the continental margin offNewfoundland. Sedimenrology 30: 751-768.

CHASE, R., CLARK, J.I., SHIELDS, D.H.,McCANN, S.B., D’ANGLEJAN, B., PIPER,D.J.W., and PETERS, G.R. 1983. Marinegeoscience in universities. In: The Geosciencesin Canada; Part 1. Marine geoscience inCanada, a status report. prepared and edited bythe Marine Geoscience Committee. CanadianGeoscience Council. Geological Survey ofCanada. Paper 81-86 (Part I): 62-67.

CLARKE, R.A. and GASCARD, J.-C. 1983.The formation of Labrador Sea water. Part 1:Large-scale processes. Journal of PhysicalOceanogrccphy 13: 1764-1778.

COCHRANE, J.A. and DUNSIGER, A.D.1983. Remote acoustic classification of marinesediments with application to offshoreNewfoundland. Canadian Journal of EarthSciences 20: 1195-1211.

COTA, G.F. and HARRISON, W.G. 1983.Plankton dynamics in Bedford Basin. NovaScotia: Carbon flux in feeding experiments withmicro-and macrozooplankton from February13, 1978 to January 31, 1979. Canadian DataReport of Fisheries and Aquatic SciencesNo. 392.

CÔTÉ, B. and PLATT, T. 1983. Day-to-dayvariations in the spring-summer photosyntheticparameters of coastal marine phytoplankton.Limnology and Oceanogrctphy 28(2): 320-344.

CRANSTON, R.E. 1983. Chromium inCascadia Basin. northeast Pacific Ocean.Marine Chemistry 13: 109-125.

CRANSTON, R.E., STOFFYN, M.A., andBUCKLEY, D.E. 1983. Sedimentarygeochemistry of a potential radioactive wastedisposal site in the Nares Abyssal Plain.EOS64: 741.

DALE, C.E. and O’BOYLE, R.N. 1983. Abiological review of the status of the 4VWxflatfish stocks. Canadian Atlantic FisheriesScientific Advisory Committee. ResearchDocument 83/62.

DAVIES, E.H. 1983. The dinoflagellate Oppel-zonation of the Jurassic - Lower Cretaceoussequence in the Sverdrup Basin, Arctic Canada.Geological Survey of Canada, Bulletin 359:59 p.

DEN HARTOG, G., SMITH, S.D.,ANDERSON, R.J., TOPHAM, D.R., andPERKIN, R.G. 1983. An investigation of apolynyna in the Canadian Archipelago.

3. Surface heat flux. Journal of GeohysicalResearch 88: 2911-2916.

DICKIE, L.M. 1983. Frederick Ronald Hayes.1904-1982 (Obituary). Canadian Journal ofFisheries and Aquatic Sciences 40: 551-553.

DICKIE, L.M. 1983. Genetic structure ofmussel populations in eastern Canadian waters.Northwest Atlantic Fisheries Organization.Scientific Council Studies 6: 73-73.

DICKIE, L.M., DOWD, R.G., andBOUDREAU, P.R. 1983. An echo countingand logging system (ECOLOG) for demersalfish size distribution and densities. CanadianJournal of Fisheries and Aquatic Sciences 40:487-498.

DICKIE, L.M. and TRITES, R.W. 1983. TheGulf of St. Lawrence. ln Estuaries and EnclosedSeas; Ed. B.H. Ketchum. Amsterdam: ElsevierScientific Publication Company, Chapter 16:403-425.

DOBSON, D. and PETRIE, B. 1983. Long-term temperature monitoring program 1982.Scotia - Fundy, Gulf regions. Canadian DataReport of Hydrography and Ocean SciencesNo. 10.

DOBSON, D. and PETRIE, B. 1983. Long-term temperature monitoring program 1982.Newfoundland region. Canadian Data Report ofHydrography and Ocean Sciences No. 11.

DOBSON, F.W. 1983. Introductory physicaloceanography. In Air-Sea Exchange of Gasesand Particles; Eds. P.S. Liss and G.N. Slinn.The Netherlands; D. Reidel Publishing Co.:53-119.

DOBSON, F.W. 1983. The CAGE Experiment.Large-scale oceanographic experiments in theWCRP. Proceedings of JSC/CCCO StudyConference, Tokyo, 10-21 May 1983.WCRP- 1, 2, World MeteorologicalOrganization. Geneva: 419-436.

DOBSON, F.W., BRETHERTON, F.P.,BURRIDGE, D.M., CREASE, J., andKRAUS, E.B. 1982. The CAGE Experiment:A Feasibility Study. Report WCP-22. WorldMeteorological Organization. Geneva: 95 p.

DOEVEN, P.H. 1983. Cretaceous nannofossilstratigraphy and paleoecology of thenorthwestern Atlantic. Geological Survey ofCanada. Bulletin 356: 69 p.

DRINKWATER, K.F. 1983. Mooredcurrentmeter data from Hudson Strait. 1982. CanadianData Report of Fisheries and Aquatic SciencesNo. 381.

DRINKWATER, K.G., TAYLOR, G., andPETRIE. L. 1983. Temperature, salinity andSigma-t distributions in the southeasternMagdalen Shallows, eastern NorthumberlandStrait and St. Georges Bay during July 1981.Canadian Technical Report of Fisheries andAquatic Sciences No. 1144.

EATON, R.M., ANDERSON, N.M., andEVANGELATOS, T.V. 1983. The electronicchart. Canadian Special Publication ofFisheries and Aquatic Sciences 67: 188-195.

FADER, G.B. 1983. Sparker seismic reflectionprofiles; Bay of Fundy from Grand MananIsland to Chignecto Bay. Geological Survey ofCanada, Open File Report 898.

Mark Stoffynin thelaboratory.

41

FALKOWSKI, P.G., VIDAL, J., HOPKINS,T.S., ROWE, G.T., WHITLEDGE, T.E., andHARRISON, W.G. 1983. Summer nutrientdynamics in the Middle Atlantic Bight: Primaryproduction and utilization of phytoplanktoncarbon. Journal of Plankton Research 5:515-537.

FARROW, G.E., SYVITSKI, J.P.M., andTUNNICLIFFE, V. 1983. Suspendedparticulate loading on the macrobenthos in ahighly turbid fjord- Knight Inlet, BritishColumbia. Canadian Journal of Fisheries andAquatic Sciences 40 (Supplement 1): 273-288.

FARRINGTON, J. W., VANDERMEULEN,J.H., and COOK, D.G. (Editors). 1983.Proceedings of the Conference on Pollutionin the North Atlantic Ocean. CanadianJournal of Fisheries and Aquatic Sciences 40(Supplement 2): 362 p.

FASHAM, M. and PLATT, T. 1983.Photosynthetic response of phytoplankton tolight: a physiological model. Proceedings of theRoyal Society of London B 219: 355-370.

FODA, A., VANDERMEULEN, J.H., andWRENCH, J.J. 1983. Uptake and conversion ofselenium by a marine bacterium. CanadianJournal of Fisheries and Aquatic Sciences 40(Supplement 2): 215-220.

FORBES, D.L. 1983. Morphology andsedimentology of a sinuous gravel-bed channelsystem: Lower Babage river, Yukon CoastalPlain, Canada. In Modern and Ancient FluvialSystems; Eds. J.D. Collinson and J. Lewin.Oxford; Blackwell: 195-206.

FORDJOR, C.K, BELL, J.S., and GOUGH,D.I. 1983. Breakouts in Alberta and stress inthe North American Plate. Canadian Journal ofEarth Sciences 20 (9): 1445-1455.

FOWLER, G.M. and SMITH, S.J. 1983.Length changes in silver hake (Merlucciusbilinearis) larvae: Effects of formalin, ethanol,and freezing. Canadian Journal of Fisheriesand Aquatic Sciences 40: 866-870.

FRANK, K.T. and LEGGETT, W.C. 1983.Multispecies larval fish association: Accidentor adoption? Canadian Journal of Fisheriesand Aquatic Sciences 40: 754-762.

FRANK, K.T. and LEGGETT, W.C. 1983.Survival value of an opportunistic life-stagetransition in capelin (Mallotus villosus).Canadian Journal of Fisheries and AquaticSciences 40: 1442-1448.

FU, T. and POCKLINGTON, R. 1983. Marineorganic chemistry: Master reference list.Canadian Data Report of Hydrography andOcean Sciences 24: 89 p.

FU, T. and POCKLINGTON, R. 1983.Quantitative adsorption of organic matter fromseawater on solid matrices. Marine Chemistry13: 255-264.

42

GAGNE, J.A., CURRIE, L., and WAIWOOD,K. 1983. The offshore cod fishery in 4X: Abiological update. Canadian Atlantic FisheriesScientific Advisory Committee, ResearchDocument 83/43.

GAGNE, J.A. and O’BOYLE, R. 1983. Thetiming of cod spawning on the Scotian Shelf.Flødevigen rapportser 1: 501-517.

GAGNE, J.A., SINCLAIR, A.F, andCURRIE, L. 1983. Status of the 4V cod stock.Canadian Atlantic Fisheries Scientific AdvisoryCommittee, Research Document 83/56.

GALLEGOS, C.L., PLATT, T., HARRISON,W.G., and IRWIN, B. 1983. Photosyntheticparameters of Arctic marine phytoplankton:Vertical variations and time scales ofadaptation. Limnology and Oceanography 28:1231-1237.

GARTNER-KEPKAY, K.E., ZOUROS, E.,DICKIE, L.M., and FREEMAN, K.R. 1983.Genetic differentiation in the face of gene flow:A study of mussel ations from a single NovaScotian embayment. Canadian Journal ofFisheries and Aquatic Sciences 40: 443-451.

GASCARD, J.-C. and CLARKE, R.E. 1983.The formation of Labrador Sea water. Part 2:Meso and smaller scale processes. Journal ofPhysical Oceanography 13: 1779-1797.

GOUGH, D.I., FORBES, C.K., and BELL,J.S. 1983. A stress province boundary andtractions on the North American plate. Nature305: 619-621.

GORDON, D.C. JR. and DESPLANQUE, C.1983. Dynamics and environmental effects ofice in the Cumberland Basin of the Bay ofFundy. Canadian Journal of Fisheries andAquatic Sciences 40: 1331-1342.

GRADSTEIN, F.M. 1983. Cenozoicstratigraphy using agglutinated foraminifera. InProceedings of the Workshop on ArenaceousForaminifera (lst, Amsterdam, Netherlands,1981); Eds. J.G. Verdenius, J.E. Van Hinte, andA.R. Fortuin. Continental Shelf Institute,Trondheim, Norway: 247-249.

GRADSTEIN, FM., BERGGREN, W.A.,KAMINSKI, M.J., and MILLER, K.G. 1983.Paleobathymetry of Late Cretaceous -Paleogene agglutinated (flysch type) benthicforaminiferal faunas and a modem analog.American Association of Petroleum GeologistsBulletin 67: 473.

GRADSTEIN, F.M., MILLER, K., andBERGGREN, W.A. 1983. Depthindependence of flysch-type agglutinatedforaminifera. In Proceedings of the Workshopon Arenaceous Foraminifera (1st, Amsterdam,Netherlands, 1981); Eds. J.G. Verdenius, J.E.Van Hinte, and A.R. Fortuin. Continental ShelfInstitute, Trondheim, Norway: 57-58.

GRAVES, M. 1983. A survey of the publishedliterature on sampling and in-situmeasurements on physical properties in thevicinity of the ocean’s bottom. GeologicalSurvey of Canada, Open File Report No. 919.

GREENBERG, D.A. 1983. Modelling of themean barotropic radiation field of an eddy overa slope. Journal of Physical Oceanography 13:886-904.

GREENBERG, D.A. 1983. The effects oftidal power development on the physicaloceanography of the Bay of Fundy and Gulf ofMaine. In The Effects of the Proposed Tidal-Hydroelectric Project in the Bay of Fundy -Proceedings of the hearing of the U. S. SenateCommittee on Environment and Public Worksin Augusta, Maine, July 25, 1984. U.S.Government Printing Office, Washington.

GREENBERG, D.A. 1983. The effects oftidal power development on the physicaloceanography of the Bay of Fundy and Gulf ofMaine. Published in the Proceedings of theFundy Environmental Studies CommitteeMeeting on marine environmentalconsequences of tidal power developmentin the upper reaches of the Bay of Fundy,November 8-10, Moncton, N. S.

GREENBERG, D.A. and AMOS, C.L. 1983.Suspended sediment transport and depositionmodelling in the Bay of Fundy, Nova Scotia - Aregion of potential tidal power development.Canadian Journal of Fisheries and AquaticSciences 40 (Supplement 1): 20-34.

HACQUEBARD, P.A. 1983. Geologicaldevelopment and economic evaluation of theSydney Coal Basin, Nova Scotia. GeologicalSurvey of Canada, Paper 83-1A: 71-81.

HALLIDAY, R.G. 1983. Biological input ongroundfish management plan. FisheriesNews 3: 3-4.

HANSEN, P.-D., ADDISON, R.F., andWILLIS, D. W. 1983. Hepatic microsomal o-de-ethylases in cod (Gadus morhua): Theirinduction by Aroclor 1254 but not by Aroclor1016. Comparative Biochemistry andPhsyiology 74C: 173-175.

HARDING, G.C., DRINKWATER, K.F., andVASS, W.P. 1983. Factors influencing the sizeof American lobster (Homarus americanus)stocks along the Atlantic coast of Nova Scotia,Gulf of St. Lawrence, and Gulf of Maine: A newsynthesis. Canadian Journal of Fisheries andAquatic Sciences 40: 186-184.

HARRISON, W.G. 1983. The time course ofuptake of inorganic and organic nitrogencompounds of phytoplankton from the easternCanadian Arctic: A comparison with temperateand tropical populations. Limnology andOceanography 28: 1231-1237.

HARRISON, W.G. 1983. Uptake andrecycling of soluble reactive phosphorus bymarine microplankton. Marine EcologyProgress Series 10: 127-135.

HARRISON, W.G. 1983. Use of isotopes. InNitrogen in the Marine environment; Eds.E.T. Carpenter and D.G. Capone. New York;Academic Press: 763-807.

HARRISON, W.G., DOUGLAS, D.,FALKOWSKI, P., ROWE, G., and VIDAL, J.1983. Summer nutrient dynamics of the MiddleAtlantic Bight: Nitrogen uptake andregeneration. Journal of Plankton Research 5:539-556.

HAWORTH, R.T. and JACOBI, R.D. 1983.Geophysical correlation between the geologicalzonation of Newfoundland and the British Isles.ln Contributions to the Tectonics andGeophysics of Mountain Chains; Eds. R.D.Hatcher Jr., H. Williams, and I. Zietz.Geological Society of America. Memoir 158:25-32.

HEAD, E.J.H. and CONOVER, R.J. 1983.Induction of digestive enzymes in Calanushyperboreus. Marine Biology Letters 4:219-231.

HERMAN, A.W. and PLATT, T. 1983.Numerical modelling of die1 carbon productionand zooplankton grazing on the Scotian Shelfbased on observational data. EcologicalModelling 18: 55-72.

HILL, P.R. 1983. Detailed morphology of asmall area on the Nova Scotian continentalslope. Marine Geology 53: 55-76.

HILL, P.R. and BOWEN, A.J. 1983. Modernsediment dynamics at the shelf-slope boundaryoff Nova Scotia. In The Shelf Break; CriticalInterface on Continental Margins; Eds. D.J.Stanley and G.T. Moore. Society of EconomicPaleontologists and Mineralogists, SpecialPublication 33: 265-276.

HILL, P.R., PIPER, D.J.W., and NORMARK,W. R. 1983. Pisces IV submersible dives on theScotian Slope at 63°W. Geological Survey ofCanada, Paper 83-1A: 65-69.

HOGANS, W.E., BRATTEY, J., UHAZY,L.S., and HURLEY, P.C.F. 1983. Helminthparasites of swordfish (Xiphias gladius L.) fromthe northwest Atlantic Ocean. Journal ofParasitology 69: 1178-1179.

HUNT, J.J. 1983. Herring gonadosomatic indexin relation to maturity stage. Canadian AtlanticFisheries Scientific Advisory Committee,Research Document 83/53.

HUNTE, W. and MAHON, B. 1983. Howimportant are migratory patterns of pelagicfishes in the Caribbean. Food and AgricultureOrganization of the United Nations, FisheriesReport No. 278. Supplement: 165-175.

The Atlantic Geoscience Centre recently established a thoroughly modern core samplerepository and curation facility that currently holds over 7000 samples from easternCanadian and Arctic offshore regions. Above, Joe Younger and Iris Hardy split asediment core: one half will be archived while the other ‘working’ half will besubsequently subsampled and analyzed. Below, Donna Holt retrieves the working halfof a core from the repository.

HUNTE, W. and MAHON, R. 1983. Lifehistory and exploitation of Macrobrachiumfaustinum in a tropical high gradient river.Fishery Bulletin 81: 654-660.

HURLEY, P.C.E., COREY, S., and ILES, T.D.1983. Distributional patterns of chaetognaths inthe Bay of Fundy Canadian Journal of Zoology61: 2257-2265.

HURLEY, P.C.F. and ILES, T.D. 1983. Ageand growth determination of Atlantic bluefintuna (Thunnus thynnus) using otoliths. In

Proceedings of the International Workshop onAge Determination of Oceanic Pelagic Fishes:Tunas, Billfishes and Sharks; Eds. E.D. Princeand L.M. Pulos. National Marine FisheriesService 8, National Oceanic and AtmosphericAdministration Technical Report: 71-75.

HURLEY, P.C.F. and O’BOYLE. R.N. 1983.An evaluation of the current 5Z populationcharacteristics during 1960-82 with yieldprojected to 1984. Canadian Atlantic FisheriesScientific Advisory Committee. ResearchDocument 83/77.

43

IRWIN, B., CAVERHILL, C., SUBBA RAO,D.V., CARVER, C., and PLATT, T. 1983.Primary productivity measurements in thechlorophyll maximum in the vicinity of theMid-Atlantic Ridge, west of the Azores, from8 July to 25 July 1982. Canadian Data Report ofFisheries and Aquatic Sciences No. 402.

IRWIN, B., HARRIS, L., DICKIE, P.,LINDLEY, P., and PLATT, T. 1983.Phytoplankton productivity in the easternCanadian Arctic during July and August 1980.Canadian Data Report of Fisheries and AquaticSciences No. 386.

IRWIN, B., HARRIS, L., HODGSON, M.,HORNE, E., and PLATT, T. 1983. Primaryproductivity and nutrient measurements innorthern Foxe Basin, N. W.T., from August 27to September 7, 1981. Canadian Data Report ofFisheries and Aquatic Sciences No. 385.

IRWIN, B., HARRISION, W.G., and PLATT,T. 1983. Plankton dynamics in Bedford Basin,Nova Scotia: Phytoplankton productivityexperiments and nutrient measurements fromFebruary 13, 1978 until March 14, 1979.Canadian Data Report of Fisheries and AquaticSciences No. 272.

IRWIN, B., LINDLEY, P., GALLEGOS,C.L., and PLATT, T. 1983. Phytoplanktonproductivity experiments on the Scotian Shelffrom April 18 to May 2, 1979. Canadian DataReport of Fisheries and Aquatic SciencesNo. 384.

IRWIN, B., PLATT, T., LINDLEY, P.,FASHAM, M.J., and JONES, K. 1983.Phytoplankton productivity in the vicinity of afront southwest of the Azores during May 1981.Canadian Data Report of Fisheries and AquaticSciences No. 400.

JACKSON, H.R. 1983. Rotation poles for theeastern Arctic and implications for Nares Strait.In International Union of Geodesy andGeophysics General Assembly (18th, 1983,Hamburg, Germany), IUGG InterdisciplinarySymposia, Hamburg, v. 2: 211.

JACKSON, H.R. and REID, I. 1983. Oceanicmagnetic anomaly amplitudes: Variation withsea-floor spreading rate and possibleimplications. Earth and Planetary ScienceLetters 63: 368-378.

JONES, E.P. 1983. Tracers in the sea.Canadian Journal of Fisheries and AquaticSciences 40: 1846-1847.

JONES, E.P., COOTE, A.R., and LEVY,E.M. 1983. Effect of sea-ice meltwater on thealkalinity of seawater. Journal of MarineResearch 41: 43-52.

JONES, H.W., EATON, R.M., andWILSON, J. 1983. UHF syledis for coastalsurvey positioning. Proceedings of the U.S.National Ocean Science Conference (April1983).44

JOSENHANS, H.W. 1983. Evidence of pre-Late Wisconsinian glaciations in the LabradorShelf-Cartwright Saddle region. CanadianJournal of Earth Sciences 20: 225-235.

KAMPP, K. 1983. The Thick-billed murres inGreenland: movements, mortality and hunting- an analysis of 35 years of banding.(Translation from Danish by R.G.B. Brown.)Science Candidate Thesis, KobenhavnsUniversitet. Canadian Wildlife Service,“Studies on northern seabirds,” ManuscriptReport No. 170: 1-167.

KEEN, C.E. 1983. Salt diapirs and thermalmaturity: Scotian Basin. Bulletin of CanadianPetroleum Geology 31: 101-108.

KEEN, C.E., BEAUMONT, C., andBOUTILIER, R. 1983. A summary ofthermomechanical model results for theevolution of continental margins based on threerifting processes. In Studies in ContinentalMargin Geology; Eds. J.S. Watkins and C.L.Drake. American Association of PetroleumGeologists Memoir 34: 725-728.

KEEN, C.E., PIPER, D.J.W., and KEEN,M.J. 1983. Canada - Its role in internationalmarine geoscience. In The Geosciences inCanada, 1980; Part 1. Marine Geoscience inCanada, A status report; prepared and edited bythe Marine Geoscience Committee, CanadianGeoscience Council. Geological Survey ofCanada, Paper 81-6 (Part I): 53-55.

KEEN, C.E., REID, I., and EWING, J. 1983.Continuity of oceanic crust across a riftedcontinental margin and the role of partialmelting in the rifting process. In InternationalUnion of Geodesy and Geophysics GeneralAssembly (18th, 1983, Hamburg, Germany),Inter-Union Commission on the Lithosphere,Hamburg: 60.

KEEN, M.J. 1983. International phase of oceandrilling: Canadian participation. In TheGeosciences in Canada, 1980; Part 1. MarineGeoscience in Canada, A status report,prepared and edited by the Marine GeoscienceCommittee, Canadian Geoscience Council.Geological Survey of Canada, Paper 81-6(Part I): 55-58.

KEEN, M.J. 1983. Ocean drilling program:Producing geological maps of the seabed.Northern Miner 69: B1-B2.

KEEN, M.J. 1983. Practical problems andissues and the earth sciences offshore.Geological Survey of Canada, Paper 83-8: 1.

KEEN, M.J. 1983. The federal environmentalassessment review process. In The Geosciencesin Canada, 1980; Part 1. Marine Geoscience inCanada, A status report; prepared and edited bythe Marine Geoscience Committee, CanadianGeoscience Council. Geological Survey ofCanada, Paper 81-6 (Part I): 48-50.

KEEN, M.J., SLY, PG., HYNDMAN, R.D.,and LEWIS, C.P. 1983. Marine geosciences inthe government of Canada. In The Geosciencesin Canada, 1980; Part 1. Marine Geoscience inCanada, A status report, prepared and edited bythe Marine Geoscience Committee, CanadianGeoscience Council. Geological Survey ofCanada, Paper 81-6 (Part I).

KENCHINGTON, T.J. 1983. Comment on“Meristic variation in beaked redfishes,Sebastes mentella and S. fasciatus, in thenorthwest Atlantic. Canadian Journal ofFisheries and Aquatic Sciences 40: 1532-1533.

KENCHINGTON, T.J. 1983. Morphologicalcharacteristics of Scotian Shelf redfish(Sebastes spp.) and rosefish (Helicolenusdactylopterus). Canadian Manuscript Report ofFisheries and Aquatic Sciences No. 1707.

KEPKAY, P.E. 1983. Kinetics of bacterialmanganese oxidation and trace metal binding.In Selected papers from the 6th InternationalSymposium on EnvironmentalBiogeochemistry. Van Nostrand Rheinhold,New York.

KERR, S.R. 1983. Fisheries studies infreshwater and their relevance to marinesystems. Northwest Atlantic FisheriesOrganization, Scientific Council Report83/1X/86.

KERR, S.R. 1983. Review of “MarineFisheries Ecosystem: Its QuantitativeEvaluation and Management,” edited by T.Laevastu and H. A. Larkins. Canadian Journalof Fisheries and Aquatic Sciences 40: 386-387.

KOELLER, PA. 1983. Update on 4VWXargentine. Canadian Atlantic FisheriesScientific Advisory Committee, ResearchDocument 83/39.

KOELLER, P.A. and SMITH, S.J. 1983.Preliminary analysis of A.T. Cameron -LadyHammond comparative fishing experiments1979-81. Canadian Atlantic Fisheries ScientificAdvisory Committee, Research Document83/59.

KULKA, D. and WALDRON, D. 1983. TheAtlantic Observer Program - A discussion ofsampling from commercial catches at sea. InSampling Commercial Catches of MarineFish and Invertebrates. Canadian SpecialPublication of Fisheries and Aquatic Sciences66: 255-262.

LADLE STUDY GROUP (WHITMARSH,R.B., KEEN, C.E., STEINMETZ, L.,TOMBLIN, J., DONEGAN, M., LILWALL,R.C., LONCAREVIC, B.D., NICHOLS, B.and SHEPARD, J.). 1983. A lithosphericseismic refraction profile in the western NorthAtlantic Ocean. Geophysical Journal of theRoyal Astronomical Society 75: 23-69.

LAWRENCE, D.J. and TRITES, R.W. 1983.Surface oil spill trajectory modelling forGeorges and Browns Banks. CanadianTechnical Report of Hydrography and OceanSciences No. 29.

LEGGETT, W.C., FRANK, K.T., andCARSCADDEN, J.E. 1983. Estimating year-class strength in capelin (Mallotus villosus)from abiotic variables. Northwest AtlanticFisheries Organization, Scientijc CouncilReport 83/VI/52 (Series N170): 19 p.

LEVY, E.M. 1983. Background levels ofvolatile hydrocarbons and petroleum residuesin the waters and sediments of the Grand Banks.Canadian Journal of Fisheries and AquaticSciences 40 (Supplement 2): 23-33.

LEVY, E.M. 1983. Baseline levels of volatilehydrocarbons and petroleum residues in thewaters and sediments of the Grand Banks.Canadian Journal of Fisheries and AquaticSciences 40 (Supplement 2): 23-33.

LEVY, E.M. 1983. Commentary: What impactwill the oil industry have on seabirds in theCanadian Arctic? Arctic 36: 1-4.

LEWIS, M.R., CULLEN, J.J., and PLATT, T.1983. Phytoplankton and thermal structure inthe upper ocean: Consequences of non-uniformity in chlorophyll profile. Journal ofGeophysical Research 88: 2565-2570.

LEWIS, M.R., CULLEN, J.J., and PLATT, T.1983. Relationship between vertical mixing andphoto-adaption of phytoplankton: Similaritycriteria. Marine Ecology Progress Series 15:141-149.

LEWIS, M.R. and SMITH, J.C. 1983. A smallvolume, short-incubation time method formeasurement of photosynthesis as a funciton ofincident h-radiance. Marine Ecology ProgressSeries 13: 99-102.

LI, W. K.W. 1983. Consideration of errors inestimating kinetic parameters based onMichaelis-Menten formalism in microbialecology Limnology and Oceanography 28:185-190.

LI, W.K.W., SUBBA RAO, D.V.,HARRISON, W.G., SMITH, J.C.,CULLEN, J.J., IRWIN, B., and PLATT, T.1983. Autotrophic picoplankton in the tropicalocean. Science 219: 292-295.

LIVELY, R.R. 1983. Avalon Channel-Newfoundland temperature, salinity, andsigma-t sections. Canadian Technical Report ofHydrography and Ocean Sciences No. 24.

LOCK, A.R., CURRIE, T., and BROWNLIE,J. 1983. A census of tern colonies on theAtlantic coast of mainland Nova Scotia.Canadian Wildlife Service, “Studies on northernseabirds,” Manuscript Report No. 171 : 1-7.

LOCK, A.R., CURRIE, T., and BROWNLIE,J. 1983. Cormorant colonies on the Atlanticcoast of mainland Nova Scotia. CanadianWildlife Service, “Studies on northernseabirds,” Manuscript Report No. 172: 109.

LONCAREVIC, B.D. 1983. Ocean bottomseismometry. In CRC Handbook ofGeophysical Exploration at Sea. Boca Raton,Florida: CRC Press, Inc. : 219-263.

LORING, D.H., RANTALA, R.T.T.,MORRIS, A.W., BLAKE, A.J., andHOWLAND, R.J.M. 1983. Chemicalcomposition of suspended particles in anestuarine turbidity maximum zone. CanadianJournal of Fisheries and Aquatic Sciences 40(Supplement I): 20, Hydrography and OceanSciences No. 4.

LORING, D.H., RANTALA, R.T.T., andSMITH, J.N. 1983. Response time of SaguenayFjord sediments to metal contamination.Environmental Biogeochemistry and EcologyBulletin 35: 59-72.

LOUIS, J.P., PETRIE, B.D., and SMITH, P.C.1982. Observations of topographic Rossbywaves on the continental margin off NovaScotia. Journal of Physical Oceanography 12:47-55.

LOUIS, J.P. and SMITH, PC. 1982. Thedevelopment of the barotropic radiation field ofan eddy over a slope. Journal of PhysicalOceanography 12: 56-73.

MacLEAN, B. and WILLIAMS, G.L. 1983.Geological investigations of the Baffin IslandShelf in 1982. Geological Survey of Canada,Paper 83-1B: 309-315.

MACNAB, R. 1983. Multiparameter mappingoff the east coast of Canada. Geological Surveyof Canada, Paper 83-1A: 163-171.

MACNAB, R. 1983. Multiparameter surveysin the offshore: Broadening the dimensions ofhydrography. Canadian Special Publication ofFisheries and Aquatic Sciences 67: 149-156.

MACNAB, R. 1983. Shipac: A softwarepackage for the shipboard processing of marinegeophysical survey data. Geological Survey ofCanada, Paper 83-1B: 327-330.

MACNAB, R., WOODSIDE, J., andLONCAREVIC, B. 1983. Rebuilding a largeinventory of marine geophysical survey data:A case study. In International Union of Geodesyand Geophysics General Assembly (18th,1983, Hamburg, Germany), IUGGInterdisciplinary Symposia, Hamburg: v. I :250.

MAHON, R. 1983. The long-term effects ofdecreased fishing mortality on the age/sizecomposition and variability of catch of 4VWhaddock. Canadian Atlantic Fisheries ScientificAdvisory Committee, Research Document83/65.

MAHON, R., SIMPSON, P., andWALDRON, D.E. 1983. Eastern Scotian Shelfhaddock (4VW): Stock status in 1982 andprojections to 1984. Canadian AtlanticFisheries Scientific Advisory Committee,Research Document 83/47.

MAHON, R. and WHITE, G.N. 1983. Theeffect of temporal trends in size-at-age on F0,1 ,for 4VW haddock. Canadian Atlantic FisheriesScientific Advisory Committee, ResearchDocument 83/48.

MALLETT, A.L. and HALEY, L.E. 1983.Effects of inbreeding on larval and spatperformance in the American oyster.Aquaculture 33: 229-235.

MALLETT, A.L. and HALEY, L. E. 1983.Growth rate and survival in pure populationmatings and crosses of the oyster Crassostreavirginica. Canadian Journal of Fisheries andAquatic Sciences 40: 948-954.

McGLADE, J., ANNAND, C., andKENCHINGTON, T. 1983. Electrophoreticidentificaton of Sebastes and Helicolenus inthe northwestern Atlantic. Canadian Journal ofFisheries and Aquatic Sciences 40: 1861-1870.

McGLADE, J.M., BEANLANDS, D., andANNAND, M.C. 1983. Stock status of pollockin NAFO Division 4VWX and Subarea 5.Canadian Atlantic Fisheries Scientific AdvisoryCommittee, Research Document 83/34.

McGLADE, J.M. and SMITH, S.J. 1983.Principal component methods for exploratorydata analysis of commercial length-frequencydata. In Sampling Commercial Catches ofMarine Fish and Invertebrates; Eds. W.G.Doubleday and D. Rivard. Canadian SpecialPublication of Fisheries and Aquatic Sciences66: 235-239.

METUZALS, K.I. and HURLEY, P.C.F.1983. Preliminary analysis of the CanadianAtlantic Bluefin tuna fishery during 1982.International Commission for the Conservationof Atlantic tunas, Collective Volume ofScientific Papers XVIII(2): 434-442.

MILLER, R.O., MACNAB, R., AMOS, C.L.,and FADER, G.B. 1983. Canadian east coastmultiparameter surveys, 1982. GeologicalSurvey of Canada, Paper 83-1B: 331-334.

MOORE, R.M., LOWINGS, M.G., and TAN,F.C. 1983. Geochemical profiles in thecentralArctic Ocean: Their relation to freezing andshallow circulation. Journal of GeophysicalResearch 88: 2667-2674.

MUDIE, P.J. and HELGASON, J. 1983.Palynological evidence for Miocene climaticcooling in eastern Iceland about 9.8 millionyears ago. Nature 303: 689-692.

45

NEEDLER, G.T., BEWERS, J.M., andHAGEN, A. A. 1983. Oceanographic modeland radiologic basis for control of radionuclidereleases. International Atmospheric EnergyAgency, International Conference onRadioactive Waste Management, Seattle,Washington, May 16-20, 1983.

NEILSON, J.D. and BANFORD, C.E. 1983.Chinook salmon (Oncorhynchus tshawytscha)spawner characteristics in relation to realphysical features. Canadian Journal of Zoology61: 1524-1531.

NORMARK, W.R., PIPER, D.J.W., andSTOW, D.A.V. 1983. Quaternary developmentof channels, levees, and lobes on the middleLaurentian Fan. American Association ofPetroleum Geologists Bulletin 67: 1400-1409.

O’BOYLE, R.N. 1983. An evaluation of the5Ze haddock population characteristics duringthe 1963-1982 period with yield projected to1984. Canadian Atlantic Fisheries ScientificAdvisory Committee, Research Document83/76.

O’BOYLE, R.N., CLEARLY, L., andMcMILLAN, J. 1983. Determination of thesize composition of the landed catch ofhaddock from NAFO Division 4X during1968-1981. In Sampling Commercial Catchesof Marine Fish and Invertebrates; Eds. W.G.Doubleday and D. Rivard. Canadian SpecialPublication of Fisheries and Aquatic Sciences66: 216-234.

O’BOYLE, R.N., WAIWOOD, K., andMcMILLAN, J. 1983. An evaluation of the 4Xhaddock population characteristics during1962-1982 with yield projections to 1984.Canadian Atlantic Fisheries Scientific AdvisoryCommittee. Research Document 83/34.

OGG, J.G., ROBERTSON, A.H.F., andJANSA, L.F. 1983. Jurassic sedimentationhistory of site 354 (western North Atlantic) andof the Atlantic-Tethys seaway In Initial Reportsof the Deep-Sea Drilling Project; R.E.Sheridan, FM. Gradstein, et al. Washington,D.C., U.S. Government Printing Office, v. 76:829-884.

PEMPKOWIAK, J. 1983. C13 reversed-phasetrace enrichment of short and long-chain(C2-C8-C20) fatty acids from dilute aqueoussolutions and sea water. Journal ofChromatography 258: 93-102.

PEMPKOWIAK, J. and POCKLINGTON, R.1983. Phenolic aldehydes as indicators of theorigin of humic substances in marineenvironments. In Aquatic Terrestrial HumicMaterials (Chapter 18); Eds. R.F. Christmanand E.T. Gjessing. Ann Arbor; Ann ArborScience Publishers: 538 p.

PETRIE, B. 1983. Current response at the shelfbreak to transient wind forcing. Journal ofGeophysical Research 88: 9567-9578.46

PETRIE, B. and ANDERSON, C. 1983.Circulation on the Newfoundland ContinentalShelf. Atmosphere-Ocean 21(2): 207-226.

PLATT, J.E and NETTLESHIP, D.N. 1983.Diving depths of four alcids in Newfoundland.Canadian Wildlife Service, “Studies onnorthern seabirds,” Manuscript Report No.129: 1-13.

PIPER, D.J.W. and NORMARK, W.R. 1983.Turbidite depositional patterns and flowcharacteristics, Navy Submarine Fan,California Borderland. Sedimentology 30:681-694.

PIPER, D.J.W., SPARKES, R., FARRE, J.A.,and SHOR, A. 1983. Mid-range sidescan and4.5 kHz subbottom profiler survey of mass-movement features, Scotian Slope at 61°40’W.Geological Survey of Canada, Open File Report938.

PLATT, T. and HERMAN, A.W. 1983. Remotesensing of phytoplankton in the sea: Surfacelayer chlorophyll as an estimate of water-column chlorophyll and primary production.International Journal of Remote Sensing 4:343-351.

PLATT, T., SUBBA RAO, D.V., and IRWIN,B. 1983. Photosynthesis of picoplankton in theoligotrophic ocean. Nature 300: 702-704.

PLATT, T., SUBBA RAO, D.V., SMITH,J.C., LI, W.K.W., IRWIN, B., HORNE, E.,and SAMEOTO, D.D. 1983.Photosynthetically-competent phytoplanktonfrom the aphotic zone of the deep ocean.Marine Ecology Progress Series 10: 105-110.

PRINSENBERG, S.J. 1983. Effects of thehydroelectric developments on theoceanographic surface parameters of HudsonBay. Atmosphere-Ocean 21: 418-430.

QUON, C. 1983. Convection induced byinsulated boundaries in a square. Physics ofFluids 26: 632-637.

QUON, C. 1983. Effects of grid distribution onthe computation of high Rayleigh numberconvection in a differentially heated cavity InNumerical Properties and Methodologies inHeat Transfer; Ed. T.M. Shih. New York;Springer-Verlag and Berlin; HemispherePublishing Corp. : 261-281.

RADTKE, R.L. and HURLEY, P.D.F. 1983.Age estimation and growth of broadbillswordfish (Xiphias gladius), from thenorthwest Atlantic based on external features ofotoliths. In Proceedings of the InternationalWorkshop on Age Determination of OceanPelagic Fishes: Tunas, Billfishes and Sharks;Eds. E.D. Prince and L.M. Pulos. NationalMarine Fisheries Service 8, National Oceanicand Atmospheric Administration TechnicalReport.

REID, I., KEEN, C.E., and EWING, J. 1983.Continuity of oceanic crust beneath a riftedcontinental margin and partial melting in therifting process. EOS 64: 757.

RULLKOTTER, J., VUCHEV, V., HINZ, K.,WINTERER, E.L., BAUMGARTNER, PO.,BRADSHAW, M.J., CHANNELL, J.E.T.,JAFFREZO, M., JANSA, L.F., LECKIE,R.M., MOORE, J.M., SCHAFTENAAR, C.,STEIGNER, T.H., and WIEGAND, G.E.1983. Potential deep-sea petroleum sourcebeds related to coastal upwelling. In CoastalUpwelling: Its sediment record. Part B:Sedimentary Records of Ancient CoastalUpwelling; Eds. J. Theide and E. Suess. NewYork: Plenum Press: 467-483.

RYDER, R.A. and KERR, S.R. 1983.Reducing the risk of fish introductions: Arational approach to the management ofintegrated coldwater communities. EuropeanInland Fisheries Advisory Committee,Symposium on Stock Enhancement in theManagement of Freshwater Fisheries,Budapest, Hungary: 24 p.

RYNN, J.M.W. and REID, I.D. 1983. Crustalstructure of the western Arafura Sea from oceanbottom seismograph data. Journal of theGeological Society of Australia 30 (l/2): 59-74.

SAMEOTO, D.D. 1983. Euphausiddistribution in acoustic scattering layers and itssignificance to surface swarms. Journal ofPlankton Research 5: 129-143.

SAMEOTO, D.D. 1983. Micronektonsampling using a new multiple-net sampler,the Bioness, in conjunction with a 120 kHzsounder. In SCOR Symposium on Methods ofSampling Micronekton: Ed. W.G. Pearcy.Crane, Russak and Company, Inc., U.S.A.Biological Oceanography 2: 179-198.

SCHAFER, C., COLE, F., and CARTER, L.1983. Paraecology of bathyal zone arenaceousForaminifera genera and species assemblagesoff northeast Newfoundland. In Proceedings ofthe Workshop on Arenaceous Foraminifera(lst, Amsterdam, Netherlands, 1981); Eds.J.G. Verdenius, J.E. Van Hinte, and A.R.Fortuin. Continental Shelf Institute,Trondheim, Norway: 133-145.

SCHAFER, C.T. and SMITH, J.N. 1983. Riverdischarge, sedimentation and benthicenvironmental variations in inner MiramichiBay. Canadian Journal of Earth Sciences 20:388-398.

SCHWINGHAMER, P. 1983. Generatingecological hypotheses from biomass spectrausing causal analysis: a benthic example.Marine Ecology Progress Series 13: 151-166.

SCHWINGHAMER, P., TAN, F.C., andGORDON, D.C. JR. 1983. Stable carbonisotope studies on the Pecks Cove mudflat

ecosystem in the Cumberland Basin, Bay ofFundy. Canadian Journal of Fisheries andAquaticSciences (Supplement I): 262-272.

SCOTT, D., GRADSTEIN, E, SCHAFER,C., MILLER, A., and WILLIAMSON, M.1983. The Recent as a key to the past: Does itapply to agglutinated foraminiferalassemblages? In Proceedings of the Workshopon Arenaceous Foraminifera (1st, Amsterdam,Netherlands, 1981); Eds. J.G. Verdenius, J.E.Van Hinte, and A.R. Fortuin. Continental ShelfInstitute, Trondheim, Norway: 147-157.

SCOTT, D.B. and GREENBERG, D.A. 1983.Relative sea-level rise and tidal development inthe Fundy tidal system. Canadian Journal ofEarth Sciences 20: 1554-1564.

SCOTT, J.S. 1983. Canadian Research Reportto NAFO, Section II. Northwest AtlanticFisheries Organization, Scientific CouncilSummary Document 83/VI/II: 9-13.

SCOTT, J.S. 1983. Inferred spawning areas andseasons of groundfishes on the Scotian Shelf.Canadian Technical Report of Fisheries andAquatic Sciences No. 1212.

SCOTT, J.S. 1983. Program of research byCanada (Scotia-Fundy Region) in the NAFOarea for 1983. Northwest Atlantic FisheriesOrganization, Circular Letter 83/38.

SHIH, K.G., DOHERTY, F., and MACNAB,R. 1983. A fast polynomial approximation ofthe international geomagnetic reference fields.Geological Survey of Canada, Paper 83-1A:486.

SHIH, K.G. and MACNAB, R. 1983. Agravity map of the Canadian east coast offshore:A demonstration of computer techniques for theconstruction of regional contour maps fromlarge data sets. Geological Survey of Canada,Paper 83-1B: 429-431.

SHIH, K.G. and MACNAB, R.F 1983.Computer contouring of marine survey data:Choosing the best technique for gridding inputdata. Geological Survey of Canada, Paper83-1A: 173-178.

SHOTTON, R. 1983. Linearity of echoresponse from herring schools. InternationalCouncil for the Exploration of the Sea C.M.1983/B:33: 20 p.

SILVA, A.J., MORAN, K., and ACKERS,S.A. 1983. Stress-strain-time behavior of deepsea clays. Canadian Geotechnical Journal 20:517-531.

SILVERT, W. 1983. Ecological modelling withelectronic spreadsheets. CanadianMathematical Society, Applied MathematicsNotes: 1-8.

SILVERT, W. 1983. Is dynamical systemstheory the best way to understand ecosystemstability? In Population Biology; Eds. H .E.

Freedman and C. Strobeck. Springer-VerlagLecture Notes in Mathematics 52: 366-371.

SILVERT, W. 1983. Review of energectics andsystems. Transactions of the AmericanFisheries Society 112: 230-232.

SILVERT, W. 1983. Teaching ecologicalmodelling with electronic spreadsheets.Collegiate Microcomputer 2 : 129-133.

SIMON, J. and STOBO, W.T. 1983. The1982-1983, 4Vn herring biological update.Canadian Atlantic Fisheries Scientific AdvisoryCommittee, Research Document 83/49.

SINCLAIR, A., HAMOR, T.,SCIOCCHETTI, R., VAN HELVOORT, G.,and WALDRON, D. 1983. Conversion factorsfor silver hake on four Soviet trawlers fishing in1981. Canadian Atlantic Fisheries ScientificAdvisory Committee, Research Document83/2.

SINCLAIR, M., MAGUIRE, J.J., KOELLER,P.A., and SCOTT, J.S. 1983. Trophic dynamicmodels in the light of current resource inventorydata and stock assessment results. Rapports etProcès - Verbaux des reunions, ConseilInternational pour 1’Exploration de al Mer 183:269-284.

SINCLAIR, M., O’BOYLE, R., and ILES,T.D. 1983. Consideration of the stable agedistribution assumption in “analytical” yieldmodels. Canadian Journal of Fisheries andAquatic Sciences 40: 95-101.

SINCLAIR, A., SCIOCCHETTI, R., andTUCKER, H. 1983. Cod fillet conversionfactors from French vessels in 1983. CanadianAtlantic Fisheries Scientific AdvisoryCommittee, Research Document 83/41.

SMITH, J.C., PLATT, T., and HARRISON,W.G. 1983. Photoadaptation of carboxylatingenzymes and photosynthesis during a springbloom. Progress in Oceanography 12 :425-459.

SMITH, J.N., ELLIS, K., and BISHOP, E J.1983. Pre-operational environmentalmonitoring report for the Point Lepreau, N.B.,nuclear generating station- 1981. CanadianTechnical Report of Hydrography and OceanSciences No. 4.

SMITH, P.C. 1983. Eddies and CoastalInteractions. In Eddies in Marine Science(Chapter 20), Berlin and Heidelberg; Springer-Verlag: 447-480.

SMITH, P.C., CHAMPAGNE, V.E.,BENNETT, A.S., and HERMAN, A.W. 1983.Batfish sections near the edge of the ScotianShelf. Canadian Technical Report ofHydrography and Ocean Sciences No. 1.

SMITH, R.E.H. and KALFF, J. 1983.Competition for phosphorus among co-occurring freshwater phytoplankton.Limnology and Oceanology 28: 448-464.

SMITH, S.D., ANDERSON, R.J., DENHARTAOG, G., TOPHAM, D.R., andPERKIN, R.G. 1983. An investigation of apolynya in the Canadian Archipelago.2. Structure of turbulence and sensible heatflux. Journal of Geophysical Research 88:2900-2910.

SMITH, R.E.H. and KALFF, J. 1983. Samplepreparation for quantitative autoradiography ofphytoplankton. Limnology and Oceanology 28:383-388.

SMITH, S.D. and BANKE, E.G. 1983. Theinfluence of winds, currents, and towing forceon the drift of icebergs. Cold Regions Scienceand Technology 6: 241-255.

SMITH, S.D., KATSAROS, K.B., and OOST,W. A. 1983. HEXOS - Humidity exchange overthe sea: Scientific plan. Canadian TechnicalReport of Hydrography and Ocean SciencesNo. 21 .

SMITH, S.J. 1983. Biological update of theinshore cod stock in Subdivision 4Vn(May-December) for 1982. Canadian AtlanticFisheries Scientific Advisory Committee,Research Document 83/44.

SMITH, S.J. and MacGUIRE, J.J. 1983.Estimating the variance of length compositionsamples. In Sampling Commercial Catches ofMarine Fish and Invertebrates; Eds. W.G.Doubleday and D. Rivard. Canadian SpecialPublication of Fisheries and Aquatic Sciences66: 165-170.

SRIVASTAVA, S.P. 1983. Davis Strait:Structures, origin and evolution. In Structureand development of the Greenland-ScotlandRidge; New methods and concepts; Eds.M.H.P. Bott, S. Saxou, M. Talwani, andJ. Theide. New York; Plenum Press: 159-189,

STOBO, W.T. 1983. Report of the “ad hoc”Working Group on Herring Tagging. NorthwestAtlantic Fisheries Organization, ScientificCouncil Summary Document 83/VI/18: 41 p.

SUTCLIFFE, W.H., JR., LOUCKS, R.H.,DRINKWATER, K.F., and COOTE, A.R.1983. Nutrient flux onto the Labrador Shelffrom Hudson Strait, and its biologicalconsequences. Canadian Journal of Fisheriesand Aquatic Sciences 40: 1692-1701.

SYVITSKI, J.P.M. 1983. Q-mode factoranalysis. Geological Survey of Canada, OpenFile Report No. 965.

SYVITSKI, J.P.M. and BLAKENEY, C.P.1983. Sedimentology of Arctic fjordsexperiment: HU 82-031 data report, Volume 1.Canadian Data Report of Hydrography and

47

Ocean Sciences No. 12 (Also issued asGeological Survey of Canada, Open FileReport No. 960).

SYVITSKI, J.P.M., FADER, G.B.,JOSENHANS, H.W., MacLEAN, B.,and PIPER, D.J.W. 1983. Seabedinvestigations of the Canadian east coast andArctic using PISCES IV. Geoscience Canada10: 59-68.

SYVITSKI, J.P.M., SILVERBERG, N.,OUELETTE, G., and ASPREY, K.W. 1983.First observations of benthos and seston from asubmersible in the lower St. Lawrence Estuary.Géographie Physique et Quaternaire 38:227-240.

SYVITSKI, J.P.M. and SKEI, J.M. (Editors).1983. Sedimentology of fjords. SedimentaryGeology 36: 75-342.

TAN, F.C., DYRSSEN, D., and STRAIN,P.M. 1983. Sea ice meltwater and excessalkalinity in the East Greenland current.Oceanologica acta 6: 283-288.

TAN, F.C. and STRAIN, P.M. 1983. Sources,sinks and distribution of organic carbon in theSt. Lawrence Estuary, Canada. Geochimica etCosmochimica Acta 47: 125-132.

TANG, C.L. 1982. A model for frontalupwelling. In Hydrodynamics of Semi-Enclosed Seas. Amsterdam; Elsevier ScientificPublishing Co.: 329-348.

TRITES, R.W. 1983. Overview ofoceanographic conditions in NAFO Subareas2, 3 and 4 during the 1970-1979 decade.Northwest Atlantic Fisheries Organization,Scientific Council Studies 5: 51-78.

TRITES, R.W. 1983. Physical oceanographicfeatures and processes relevant to Illexillecebrosus spawning areas and subsequentlarval distribution. Northwest Atlantic FisheriesOrganization, Scientific Council Studies 6:39-55.

TRITES, R.W. and DRINKWATER, K.F.1983. Overview of environmental conditionsin 1982 within the NAFO convention area.Northwest Atlantic Fisheries Organization,Scientific Council Report 83/VI/23: 42 p.

TRITES, R.W. and GARRETT, C.J.R. 1983.Physical oceanography of the Quoddy Region.In Marine and Coastal Systems of the Quoddy;Ed. M.L.H. Thomas. Canadian SpecialPublication Fisheries and Aquatic Sciences 64:9-34.

TRITES, R.W., VANDERMEULEN, J.H.,and LAWRENCE, D.J. 1983. Modellingsurface water circulation from Cabot Straitusing KURDISTAN oil spill data. Atmosphere-Ocean

TOPHAM, D.R., PERKIN, R.G., SMITH,S.D., ANDERSON, R.J., and DEN

48

HARTOG, G. 1983. An investigation of apolynya in the Canadian Archipelago, 1,Introduction and Oceanography. Journal ofGeophysical Research 88: 2888-2899.

TUNNICLIFFE, V. and SYVITSKI, J.P.M.1983. Corals move boulders: An unusualmechanism of sediment transport. Limnologyand Oceanography 28: 564-568.

VANDERMEULEN, J.H. 1983. Long termissues in Puget Sound. In Proceedings of PugetSound Water Quality Conference, Sept. 30-Oct. 1, 1983, Seattle, Washington: 59-77.

VANDERMEULEN, J.H. and CAPUZZO, J.1983. Understanding sublethal pollutant effectsin the marine environment. In Ocean WasteManagement - Policy and Strategies.International Ocean Disposal Symposia Series.Special Symposium, University of RhodeIsland, May 2-6, 1983: 11 p.

VANDERMEULEN, J.H., SILVERT, W., andFODA, A. 1983. Sublethal hydrocarbonphytotoxicity in the middle unicellular algaPavlova lutheri. Aquatic Toxicology 4: 31-49.

VERSPOOR, E. 1983. A case of bigamy in theCommon Guillemot Uria aalge. CanadianWildlife Survey, “Studies on northernseabirds,” Manuscript Report No. 161: 1-6.

VERSPOOR, E., BIRKHEAD, T.R., andNETTLESHIP, D.N. 1983. Attendance andegg/chick brooding patterns of murres andRazorbills at the Gannet Clusters, Labrador,1982. Canadian Wildlife Survey, “Studies onnorthern seabirds,” Manuscript ReportNo. 150: 1-38.

VILKS, G. and HARDY, I.A. 1983. The 12thArctic Workshop. Geoscience Canada 10:125-127.

VILKS, G. and MUDIE, P.J. 1983. Evidencefor postglacial paleoceanographic andpaleoclimatic changes in Lake Melville,Labrador, Canada. Arctic and Alpine Research25: 307-320.

WAIWOOD, K.G. and MAJKOWSKI, J.1983. Food consumption and diet compositionof cod (Gadus morhua) inhabiting thesouthwest Gulf of St. Lawrence.Environmental Biology of Fishes 1: 63-78.

WALDRON, D.E. 1983. Factors influencingScotian Shelf finfish and squid interactions withspecial reference to silver hake (Merlucciusbilinearis). Northwest Atlantic FisheriesOrganization, Scientijic Council ResearchDocument 83/IX/92.

WALDRON, D.E., SINCLAIR, A.F, andHUNT, J.J. 1983. Population abundance ofScotian Shelf silver hake (Merlucciusbilinearis) in 1982 with projections to 1984.Northwest Atlantic Fisheries Organization,Scientific Council Research Document83/VI/59.

WANG, Y. 1983. The mudflat system of China.In Proceedins of the Symposium on theDynamics of Turbid Coastal Environments;Eds. D.C. Gordon Jr. and A.S. Houston.Canadian Journal of Fisheries and AquaticSciences 40 (Supplement I ): 160-171.

WHITE, G.N. 1983. Identification ofinfluential variables in yield per recruitanalysis. In: Sampling Commercial Catches ofMarine Fish and Invertebrates; Eds.Canadian Special Publication of Fisheries andAquatic Sciences 66: 130-140.

WHITE, G.N. and GAVARIS, S. 1983.Diagnosis for the multiplicative model.Canadian Atlantic Fisheries Scientific AdvisoryCommittee, Research Document 83/58.

WHITMAN, BEN & ASSOCIATES. 1983.Bedford Institute of Oceanography towingwinch investigation. Geological Survey ofCanada, Open File Report No. 933.

WILLIAMS, G.L. 1983. Pyroclasts.Geoscience Canada 10: 135.

WINTERS, G. V. 1983. Modelling suspendedsediment dynamics of the Miramichi Estuary,New Brunswick, Canada. Canadian Journal ofFisheries and Aquatic Sciences: 105-116.

YEATS, P.A. and BEWERS, J.M. 1983.Potential anthropogenic influences on tracemetal distribution in the North Atlantic.Canadian Journal of Fisheries and AquaticSciences 40 (Supplement 2): 124-131.

YEATS, P.A. and CAMPBELL, J.A. 1983.Nickel, copper, cadmium and zinc in theNorthwest Atlantic Ocean. Marine Chemistry12: 43-58.

ZWANENBURG, K. 1983. 1983 status reporton the 4VWx red fish. Canadian AtlanticFisheries Scientific Advisory Committee,Research Document 83/17.

ZWANENBURG, K.T. and SMITH, S.J. 1983.Comparison of finfish length-frequencydistributions estimated from samples taken atsea and in port. In Sampling CommercialCatches of Marine Fish and Invertebrates.Canadian Special Publication of Fisheries andAquatic Sciences 66: 189-193.

1983 Ship Voyages*

VOYAGEYEAR -

NUMBER

83-002

83-007

83-009

83-017Phase I

Phase II

83-019

83-021

VOYAGEDATES

Apr. 6 to 23

Apr. 23 to May 2

May 4 to 30

Jun. 7 to 21

Jun. 22 to Jul. 5

Jul. 8 to 15

Jul. 28 to Aug. 6

OFFICERIN

CHARGE

T. Platt, MEL

P.J. Ryall,Dalhousie Univ.

R.M. Hendry, AOL

K.S. Manchester, AGC

B.D. Loncarevic, AGC

G. B. Fader, AGC

J.R. Lazier, AOL

C.S.S. HUDSON

= The C.S.S. Hudson is a diesel-electric driven ship designedand used for multidisciplinary oceanographic research. Theship is owned and operated by the federal Department ofFisheries and Oceans.

= Principal Statistics-Lloyds Ice Class I hull . . . built in 1963. . . 90.4 m overall length . . . 15.3 m overall beam . . . 6.3 mmaximum draft . . . 4870 tonne displacement . . . 3721 grossregistered tons . . . 17 knot full speed . . . 13 knot cruisingspeed in Sea State 3 . . . 80 day endurance and 23,000 n. milerange at cruising speed . . . scientific complement of 26 . . .205 m2 of space in four laboratories . . . two HP 1000 compu-ter systems . . . heliport and hangar . . . twin screws and bowthruster for position holding . . . four survey launches

* Abbreviations used here include: AGC Atlantic Geoscience Centre: AOL Atlantic Oceanographic Laboratory; CHS Canadian Hydrographic Service; DFO Department ofFisheries and Oceans: FESD Fisheries Environmental Sciences Division: GIROQ Groupe interuniversitaire de recherches ockanographiques du Québec; IMPD Invertebratesand Marine Plants Division; NAFO Northwest Atlantic Fisheries Organization: NSRF Nova Scotia Research Foundation.

AREAOF

OPERATION

Scotian Shelf/Sargasso Sea

St. Georges, Bermuda

Bermuda to Halifax

Scotian ShelfLaurentian FanGrand Banks

Same

Bedford Basin.Scotian Shelf and Slope

Hamilton Bank

VOYAGEOBJECTIVES

Series of biological oceanographicobservations on the pelagicecosystem at an oligotrophicstation

Deep water tests of rock core drill:sediment sampling; recover anddeploy moorings; obtain box coresamplesDeploy current meter moorings;CTD survey; heat flowmeasurements; navigation tests;collect rain samples for pollutionstudies

Test new deep tow equipment.CHIRP sonar system, CTD. andgravimeters; sediment sampling:acoustic survey; deploy currentmeter moorings; recovery anddeployment of OBSs

SameTest Seabed II mapping system:sidescan sonar survey; seabedsediment samplingRecover and deploy moorings: CTDsurvey

49

83-023

83-028

83-030

83-033

83-036

83-043

Aug. 6 to Sep. 17

Sep. 19 to Oct. 5

Oct. 5 to 26

Oct. 28 to Nov. 7

Nov. 9 to Dec. 7

Dec. 7 to 13

T. Platt, MEL

J.P. Syvitski, AGC

G. Vilks, AGC

G. Vilks, AGC

J.R. Lazier, AOL

A.E. Hay,Memorial Univ.

Eastern Arctic. north ofHudson Strait

Baffin Island fjords

Labrador Shelf.Lake Melville

Northeast Labrador Shelf,Grand Banks

Hamilton Bank

Fortune Bay.Baie d’Espoir. andHermitage Channel, Nfld.

VOYAGEYEAR -

NUMBER

83-008

83-035

83-042

VOYAGEDATES

May 2 to Oct. 28

Nov. 3 to 28

Dec. 1 to 7

OFFICERIN

CHARGE

V. J. Gaudet, CHS

G. W. Henderson, CHS

A.K. Malone, CHS

Study biological oceanography ofArctic

Climatology. sediment dynamics.animal-sediment relationships. andother studies

Sediment sampling and seismicsurveys; chemical study ofpetroleum related substances

Study paleoecology andstratigraphy of Quaternarysediments, and sediment stability

Replace moorings; CTD surveying;obtain Batfish sections; Polar Frontsurvey

CTD survey; deploy current meters;heat flow measurements; obtaingravity cores

C.S.S. BAFFIN

= The C.S.S. Baffin is a diesel driven shipdesigned for hydro-graphic surveying but also used for general oceanography.The ship is owned and operated by the federal Department ofFisheries and Oceans.

= Principal Statistics- Lloyds Ice Class I hull . . . built in 1956. . .87 m overall length . . . 15 m moulded beam . . . 5.7m max-imum draft . . . 4986 tonne displacement . . . 15.5 knot fullspeed . . . 10 knot cruising speed in Sea State 3 . . . 76 dayendurance and 18,000 n. mile range at cruising speed . . .complement of 29 hydrographic staff... drafting. plotting.and laboratory spaces provided . . . two HP 1000 computersystems . . . heliport and hangar . . . twin screws and bowthruster for position holding . . . six survey launches

AREAOF

OPERATION

Trinity Bay, Belle IsleStrait, Nfld.:Jones Sound. NWT

SW Nova Scotia

Scotian Shelf area

VOYAGEOBJECTIVES

Standard navigational charting

Multidisciplinary data collectionfor map productionTesting DOLPHIN. transducers.oceanographic winch. and launchlifting hooks

The NOAA ship Whiting sails outto sea after paying a courtesy callto BIO.

50

C.S.S. DAWSON

= The C.S.S. Dawson is a diesel-driven ship designed andused for multidisciplinary oceanographic research, hydro-graphic surveying, and handling of moorings in deep andshallow water. The ship is owned and operated by the federalDepartment of Fisheries and Oceans.

= Principal Statistics - built in 1967 . . . 64.5 m overall length. . . 12 m moulded beam . . . 4.9 m maximum draft . . . 1940tonne displacement . . . 1311 gross registered tons . . . 14 knotfull speed . . . 10 knot cruising speed in Sea State 3 . . . 45 day

endurance and 11,000 n. mile range at cruising speed . . . sci-entific complement of 13 . . . 87.3 m2 of space in four labora-tories . . . computer suite provided . . . twin screws and bowthruster for position holding . . . one survey launch

VOYAGEYEAR -

NUMBER

83-001

83-003

83-006

83-010Phase I

Phase II

83-012

83-014

83-018

83-020

83-022Phase I

Phase IIPhase III

83-024

83-026Phase I

VOYAGEDATES

Apr. 5 to 12

Apr. 12 to 18

Apr. 20 to May 3

May 17 to 18

May 18 to 23

May 5 to 13

Jun. 2 to 21

Jun. 22 to Jul. 5

May 23 to 30

Aug. 2 to 5

Aug. 5 to 9Aug. 12 to 19

Aug. 19 to 30

Jul. 7 to 12

OFFICERIN

CHARGE

PC. Smith, AOL

J.N. Smith, AOL

D.D. Sameoto, MEL

R. Hall, Dalhousie Univ.

T. Chriss, D. HuntleyDalhousie Univ.

D.E.T. Bidgood, NSRF

H.G. Miller,Memorial Univ.

S.D. Smith, AOL

K.T. Frank, MEL

I. Reid, AGC

L. Legendre, GIROQN. Silverberg, GIROQ

J.A. Elliott, AOL

C.L. Amos, AGC

AREAOF

OPERATION

SW Nova Scotia Shelf/Browns Bank

Point Lepreau/ Bay of Fundy

Scotian Shelf

Scotian Shelf

Emerald Basin area

Scotian Shelf and Slope

Nfld. Coast

Strait of Belle Isle

NAFO Division 4X

Mouth of Laurentian Channel

Northwest Gulf

Gulf of St. Lawrence

Edge of Scotian Shelf

Scotian Shelf area

VOYAGEOBJECTIVES

Recover Cape Sable moorings;deploy Browns Bank moorings;carry out dispersion study;hydrographic surveying

Collect samples for laboratoryradioactivity analysis

Test new sampling equipment;conduct acoustic/light experiment;collect zooplankton/ micronektonsamples

Identification of acoustic reflectors

Testing and collecting bottomturbulence data with newinstrumentation system; marinecopepod measurements; bottomstereophotography

High resolution seismic surveying;core samplingPhysical and biologicaloceanography; underwater gravitymapping; surficial geology; seabirdobservations

Collect data for a computer modelof iceberg drift; currentmeasurements; test“penetrometer” sediment corer

ichthyoplankton survey (SW NovaScotia Fishery Ecology Program)

Grand Banks microseismicityexperiment (recovery of OBSs)

General oceanography

Sampling for biogeochemicalevaluation of the benthic boundarylayer

Study the generation of highamplitude internal waves

Seismic surveying and coring forsediment studies

51

Phase II

83-027

83-029

83-031

83-032

83-034

83-037Phase I

Phase II

83-038

83-039

C.S.S. MAXWELL

Jul. 12 to 16

Sep. 26 to Oct. 10

Sep.7 to 21

Oct. 11 to 20

Oct. 24 to 29

Nov. 2 to 11

Nov. 14 to 21

Nov. 21 to 28

Nov. 30 to Dec. 7

Dec. 10 to 15

= The C.S.S. Maxwell is a diesel-driven ship designed andused for inshore hydrographic surveying. The ship is ownedand operated by the federal Department of Fisheries andOceans.

= Principal Statistics - built in 1962 . . . 35 m overall length . . .7.6 m moulded beam . . . 2.1 m maximum draft . . . 270 tonnedisplacement . . . 262 gross registered tons . . . 12.2 knot fullspeed . . . 10 knot cruising speed in Sea State 2 . . . 10 dayendurance and 2400 n. mile range at cruising speed . . . scien-tific complement of 7 . . . drafting and plotting facilities . . .two survey launches

K.T. Frank, MEL

D. Huntley, T. Chriss,Dalhousie Univ.

R.M. Hendry, AOL

D.L. McKeown, AOL

N.S. Oakey, AOL

PC. Smith, AOL

K.T. Frank, MEL

P. Schwinghamer, MEL

G.L. Budgen, AOL

K.S. Manchester, AGC

NAFO Division 4X

Emerald Basin off N.S.

Gulf Stream

Scotian Shelf/Slope;Emerald and Western banks

Edge of Scotian Shelf

Browns Bank off N.S.

NAFO Division 4X,(primarily Browns Bank)

SW Nova Scotia

Gulf of St. Lawrence

St. Margaret’s Bay, N.S.

Ichthyoplankton survey andzooplankton studies (SW NovaScotia Fishery Ecology Program)

Test. and gather data with, newbottom turbulence instrumentation;stereophotography of bottomroughnessCTD survey; acoustic profiling;water samplingTest Ametek current profiler andDatasonics multifrequency backscatter systemsTest Epsonde to 1000 m; studyturbulent mixing in mixed layer;study surface energy, heat flux, andwave generation

Recover and redeploy moorings;dispersion studies; WAVECdirectional-buoy testing;hydrographic survey

Ichthyoplankton survey andzooplankton studies (SW NovaScotia Fishery Ecology Program)Biological sampling of bottom; testbenthic camera system; respirationexperiments on benthic organisms

Quantify heat content and densitydistribution for seasonal iceforecasting; nutrient and oxygensampling; satellite buoydeployment.

Test Nordco underwater coringsystem; collect nearshoregeological samples for mapping

VOYAGEYEAR -

NUMBER

83-00483-011Phase IPhase II

83-04 I

52

VOYAGEDATES

Apr. 15 to May 2

May 9 to Jun. 10Jun. 14 to Oct. 28

Nov. 8 to 30

OFFICER AREAIN OF

CHARGE OPERATION

B.D. Loncarevic, AGC Mahone Bay, N.S. Evaluation of KSS-30 gravimeter

E.J. Comeau, CHS St. Mary’s Bay, N.S.E.J. Comeau, CHS Trinity Bay, Nfld.R.M. Eaton, CHS Mahone Bay, N.S.

VOYAGEOBJECTIVES

Standard navigational charting

Standard navigational chartingEvaluations of navigationalsystems

NAVICULA

VOYAGEYEAR -

NUMBER

83-005

83-015

83-016

OTHER VOYAGES

VOYAGEYEAR -

NUMBER&

VESSEL

83-025M.V.Sigma-T83-013M.V.Quest

VOYAGEDATES

Apr. 18 to May 27Sep. 6 to Oct. 28

Jul. 23 to 30Aug. 25 to 30

Jun. 2 to Aug. 23

VOYAGEDATES

OFFICER AREAIN OF

CHARGE OPERATIONVOYAGE

OBJECTIVES

Jun. 17 to Sep. 19 G.C.H. Harding, MEL St. Margaret’s Bay Larval lobster survey

May 25 to Jun. 7 C.E. Keen, AGC

OFFICER AREAIN OF

CHARGE OPERATION

D. Blaney, CHS

G.A. Packman,Environment Canada

T.C. Lambert, MEL

Nova Scotia Coast;Northumberland StraitStrait of Canso; ChedabuctoBay: Sydney Harbour. N.S.

St. Georges Bay. N.S.

= The Navicula is a wooden-hulled fishing vessel owned andoperated by the federal Department of Fisheries and Oceansand used for research in biological oceanography.

= Principal Statistics - built in 1968 . . . 19.8 m overall length. . . 5.5 m moulded beam . . . 110 ton displacement . . . 78 grossregistered tons

Continental Marginsouthwest of the GrandBanks; Laurentian Channel/Fan

VOYAGEOBJECTIVES

Chart revision; range surveys

Sediment studies related to oceandumping

Ichthyoplankton survey

Deploy OBSs; collect data fromOBS stations and seismic reflectionsystem; system assessment

NOTE: The Atlantic Region of the Canadian Hydrographic Service also had the use of the CCGS John A.McDonald on a non-dedicated basis and the CCGS Labrador on a dedicated basis (Aug. 13 to Oct. 5) primarilyfor survey work in the Arctic.

53

VOYAGENUMBER

H088.H089H090

H091

H092

H093

H094.H095

H096

H097

H098

H099

H100

H101.H102.H103

H104

H105

H106

H107H108

H109

H110

54

VOYAGEDATES

Jan 6 to 18

Jan. 29 to Feb. 5

Feb. 8 to 20

Feb. 21 to 26

Mar. 5 to 17

Mar. 21 to Apr. 15

Apr. 20 to 28

May 4 to 14

May 19 to 29

Jun. 1 to 14

Jun. 16 to Jul. 4

Jul. 8 to 29

Aug. 1 to 12

Aug. 15 to 17

Sep. 3 to 15

Sep. 23 to Nov. 6

Nov. 15 to 21

Nov. 24 to Dec. 8

OFFICERIN

CHARGE

R. Mahon/M. Buzeta

J. Reid

P. Hurley

P. Hurley, T. Koslow.Dalhousie Univ.

M. Fowler

S. Scott.N. McFarlane

P. Hurley, T. Koslow.Dalhousie Univ.

J. Reid

P. Hurley, T. Koslow.Dalhousie Univ.

P. Hurley

J. Anderson. DFO Nfld.

P. Perley, G. White

P. Koeller

J. Pringle, IMPD

D. Gascon.DFO Quebec

P. Rubec.DFO Gulf Region

J. Reid

J. McGlade

LADY HAMMOND

= The Lady Hammond. a converted fishing trawler. is char-tered by the Department of Fisheries and Oceans fromNorthlake Shipping Ltd. and used specifically for fisheriesresearch. Its main user is the Marine Fish Division. whichhas components at BIO and in St. Andrews, N.B. Except asotherwise noted below in the remainder of this chapter.“officers in charge” are affiliated with the Marine Fish Divi-sion.

= Principal Statistics-built in 1972 . . . 54 m overall length . . .11 m overall beam . . . 5.5 m maximum draft . . . 306 gross reg-istered tons . . . 13.5 knot maximum speed . . . 12 knot cruis-ing speed

AREAOF

OPERATION

NAFO Div. 4X

Bedford and Emerald basinsNAFO Div. 4X

NAFO Div. 4X

NAFO Div. 4X

Scotian Shelf, Bay of Fundy

NAFO Div. 4X

NAFO Div. 4X

NAFO Div. 4X

NAFO Div. 4X

NAFO Div. 4N

NAFO Div. 4V, 4W, and 4X

NAFO Div. 4X

St. Margaret’s Bay andapproaches

NAFO Div. 4R

NAFO Div. 4R and 4S

Bedford Basin

NW Atlantic

VOYAGEOBJECTIVES

Groundfish survey. SW Nova ScotiaFishery Ecology ProgramMININESS gear trials

Broadscale survey. SW Nova ScotiaFishery Ecology Program

Process studies. SW Nova ScotiaFishery Ecology Program

Broadscale survey, SW Nova ScotiaFishery Ecology Program

Spring groundfish survey

Process studies, SW Nova ScotiaFisheries Ecology Program

Broadscale distribution survey.SW Nova Scotia Fishery EcologyProgram

Process studies. SW Nova ScotiaFishery Ecology Program

Broadscale distribution survey.SW Nova Scotia Fishery EcologyProgram

Ichthyoplankton survey

Comparative fishing withM . V. Needler

Juvenile haddock survey

Lobster survey

Cod tagging

Shrimp and redfish abundancesurveyMININESS gear trials

Pollock survey

E.E. PRINCE

= The E.E. Prince is a steel stern trawler used for fisheriesresearch. and experimental and exploratory fishing. Theship is owned and operated by the federal Department ofFisheries and Oceans.

= Principal Statistics- built in 1966 . . . 39.9 m overall length. . . 8.2 m overall beam . . . 3.6 m maximum draft . . . 421 tondisplacement . . . 406 gross registered tons

VOYAGENUMBER

P282P283

P284

P285

P286

P287

P288

P289

P290

P291

P292

P293

P294P295

P296

P297

P298

P299

VOYAGEDATES

Jan. 7 to 25

Feb. 4 to 11

Feb. 15 to 23

Mar. 3 to 7

Mar. 9 to 11

Mar. 15 to 27

Apr. 6 to 21

May 6 to 13

May 16 to 26

Jun. 4 to 17Jun. 20

Jul. 11 to 22Aug. 1 to 26Aug. 29 to Sep. 2

Sep. 6 to 30

Oct. 18 to 26Oct. 31 to Nov. 14

Nov. 18 to 24

OFFICERIN

CHARGE

U. Buerkle

M. Etter, IMPD

L. Dickie, MEL

M. Strong

C. Morrison, FESD

G. Boutilier

P. Hurley

M. Etter, IMPD

G. Robert, IMPD

W. Squires, DFO Nfld.

B. Mercille, DFOGulf RegionJ. Pringle, IMPD

G. Robert, IMPDJ. Reid

D. Clay, DFO GulfRegionL. Dickie, MEL

M. Power

M. Etter, IMPD

AREAOF

OPERATION

Chedabucto Bay

Roseway Bank

NAFO Div. 4T

Emerald Basin

Halifax Harbour

Bay of Fundy

NAFO Div. 4X

NAFO Subdiv. 4Vn

Middle. Western. andBrowns banks; Germanand Lurcher shoalsNAFO Div. 3L

NAFO Div. 4T andSubdiv. 4Vn

Scotian ShelfGeorges BankNAFO Div. 4X

NAFO Div. 4T

Bancaro Bank

Bay of FundyScotian Shelf

VOYAGEOBJECTIVES

Herring-acoustics survey

Shrimpdistribution and abundance

ECOLOG testingPollock collection for meristic andelectrophoretic studiesLive fish collection

Larval herring survey

Broadscale distribution survey,SW Nova Scotia Fishery EcologyProgramShrimp distribution and abundance

Stock assessment survey on deepsea scallops

Snow crab survey

Mackerel egg and larval survey

Lobster larval survey

Lobster larval surveyMININESS gear trials

Groundfish survey

ECOLOG testing

Herring survey

Shrimp survey

CO-OPERATIVE VOYAGES

During 1983, the Marine Fish Division participated in co-operative voyages aboard the USSR’s research vessel Let Kievu (abbreviated as LK below)

VOYAGENUMBER

LK01 LK02

VOYAGEDATES

Oct. 17 to Nov. 24

OFFICERIN

CHARGE

B. Wood, M. Strong

AREAOF

OPERATION

Scotian Shelf

VOYAGEOBJECTIVES

Comparative juvenile silver hakesurvey

55

M.V. ALFRED NEEDLER

= The M.V.Alfred W.H. Needler is a diesel-driven shipownedand operated by the federal Department of Fisheries andOceans. and used for fisheries research.

= Principal Statistics- built in 1982 . . . 50.3 m overall length. . . 10.9 m beam . . . 925.03 gross registered tons . . . comple-ment of 10 scientific staff . . . equipped with up-to-date com-munication systems, electronics, navigational aids,research equipment, and fishing gear.

VOYAGENUMBER

N007

N008

N009

N010

N011

N012.N013.N014

N015

N016

N017.N018N019

N020

VOYAGEDATES

Jan. 7 to 17

Jan. 28 to Mar. 2

Apr. 22 to May 8

May 25 to Jun. 4

Jun. 20 to 30

Jul. 5 to 29

Aug. 3 to Sep. 9

Sep. 12 to 29

Oct. 3 to 27

Oct. 31 to Nov. 9

Nov. 16 to 30

OFFICERIN

CHARGE

G. Winters

T. Rowell (IMPD)E. Dawe

J. Baird, DFO Nfld.K. Waiwood

P.Koeller

P. Koeller

R. Mahon

J. Young. IMPD

S. Smith/K. Waiwood

D. Waldron

W.D. Smith

AREAOF

OPERATION

St. Pierre Bank

Halifax to Jacksonville,Florida

NAFO Subdiv. 3Ps and 3Pn

NAFO Division 4X

SW Nova Scotia

Scotian Shelf, Bay of Fundy

NAFO Division 4X

Scotian Shelf

Scotian Shelf

Scotian Shelf

Banquereau Bank

VOYAGEOBJECTIVES

Assessment of scallop stocks

Distribution of larval and juvenileIllex along the axis of the GulfStream

Groundfish survey

Groundfish survey (SW NovaScotia Fishery Ecology Program)

Juvenile haddock survey

Standard groundfish survey

Groundfish survey (SW NovaScotia Fishery Ecology Program)Distribution of squid

Fall groundfish survey

Silver hake stock discrimination

Redfish inventory

VOYAGES ABOARD THE CHARTERED VESSEL J.L. HART

VOYAGENUMBER

0S01

OFFICER AREAVOYAGE IN OF VOYAGEDATES CHARGE OPERATION OBJECTIVES

Aug. 2 to 27 M. Power, J.S. Scott

Mar. 31 to Apr. 9 W. Smith

Jul. 11 to 20 U. Buerkle

Sable Island. LaHave-Brownsbanks

NAFO Div. 4XBay of Fundy

Juvenile haddock survey,comparative day-night fishing

Haddock taggingHerring-acoustics survey

56

Organization and Staff

BIO is a research institute of theGovernment of Canada operated by theDepartment of Fisheries and Oceans(DFO), both on its own behalf and for theother federal departments that maintainlaboratories and groups at the Institute.Research, facilities, and services are co-ordinated by a series of special and generalcommittees.

BIO also houses the office of theNorthwest Atlantic Fisheries Organization(Executive Secretary- Captain J.C.E.

Cardoso); the analytical laboratories of theDepartment of the Environment’s (DOE)Environmental Protection Service(Dr. H. S. Samant); and the Atlanticregional office of the Canada Oil and GasLands Administration of the Departmentof Energy, Mines and Resources (DEMR).In leased accommodation at BIO are thefollowing marine-science related privatecompanies: Huntec Ltd., Wycove SystemsLtd., and Franklin Computers Ltd.

We present below the major groups at

BIO together with their managers and a listof Institute staff as at July 1984. Telephonenumbers are included in the first list: notethat Nova Scotia’s area code is 902 and theBIO exchange is 426. In the staff list, thegroup or division for which an individualworks is given in abbreviated formfollowing his/her name: the abbreviationsused are defined in the list of major groupsimmediately below.

OCEAN SCIENCE ANDSURVEYS, ATLANTIC (DFO)

CHS - Canadian Hydrographic Service(Atlantic Region)

ATLANTIC FISHERIES SERVICE,MARITIMES (DFO)

A.R. LonghurstDG - Director-General . . . . . . . . . . . . . 3492

OID - Ocean Information DivisionH.B. Nicholls, Head . . . . . . . . . . . . . . . . 3246

Public Relations

B.Bennett . . . . . . . . . . . . . . . . . . . . . . . . 3698

C.E.Murray,Manager . . . . . . . . . . . . . . 3251BIOMAIL Officer

MS - Management ServicesG.C. Bowdridge, Manager . . . . . . . . . . . 6166

Administrative ServicesM.C. Bond, Chief. . . . . . . . . . . . . . . . . . 7060Financial ServicesE. Pottie, Chief . . . . . . . . . . . . . . . . . . . . 7060Materiel Management ServicesR.J. Stacey, Chief . . . . . . . . . . . . . . . . . . 3487

P - Personnel ServicesJ.C. Feetham, Manager. . . . . . . . . . . . . . 2366

AOL - Atlantic OceanographicLaboratory

G.T. Needler, Director . . . . . . . . . . . . . . 7456

AOL - 1. Chemical OceanographyJ.M.Bewers,Head . . . . . . . . . . . . . . . . . 2371AOL - 2. Coastal OceanographyC.S. Mason, Head. . . . . . . . . . . . . . . . . . 3857AOL - 3. MetrologyD.L. McKeown, Head. . . . . . . . . . . . . . . 3489AOL - 4. Ocean CirculationJ.A. Elliott, Head . . . . . . . . . . . . . . . . . . 2502

A.J. Kerr, Director. . . . . . . . . . . . . . . . . . 3497

CHS - 1. Field SurveysT.B. Smith, Head . . . . . . . . . . . . . . . . . . 2432

S.T. Grant, Head . . . . . . . . . . . . . . . . . . . 3846

CHS - 2. Chart ProductionS. Weston, Head . . . . . . . . . . . . . . . . . . . 2432CHS - 3. Hydrographic DevelopmentR.G. Burke, Head . . . . . . . . . . . . . . . . . . 3657CHS - 4, NavigationR.M. Eaton, Head . . . . . . . . . . . . . . . . . . 2572CHS - 5. Planning and RecordsR.C. Lewis, Head . . . . . . . . . . . . . . . . . . 2477CHS- 6. Tidal

MEL - Marine Ecology LaboratoryK.H. Mann, Director . . . . . . . . . . . . .

MEL - 1. Biological OceanographyT.C. Platt, Head . . . . . . . . . . . . . . . . .MEL - 2. Environmental QualityR.F. Addison, Head. . . . . . . . . . . . . . .MEL - 3. Fisheries OceanographyS . R . K e r r , H e a d . . . . . . . . . . . . . . . . . .

IF - Institute FacilitiesR.L.G. Gilbert, Manager . . . . . . . . . . 3681

IF - 1. ShipsJ. Parsons, Head . . . . . . . . . . . . . . . . .IF - 2. Engineering ServicesD.F. Dinn, Head . . . . . . . . . . . . . . . . .IF - 3. Computing ServicesD.M. Porteous, Head . . . . . . . . . . . . .IF - 4. Library ServicesJ.E. Sutherland, Head . . . . . . . . . . . . .IF - 5. Publication ServicesM.P. Latremouille, Head . . . . . . . . . . .

7292

3700

2452

3675

5947

. 3696

. 3793

. 3279

. 3792

MFD - Marine Fish DivisionW.D. Bowen, Chief. . . . . . . . . . . . . . . . . 8390

CAFSAC - Canadian Atlantic FisheriesScientific Advisoy Committee - SecretariatD.Geddes . . . . . . . . . . . . . . . . . . . . . . . . 8390

CANADIAN WILDLIFESERVICE (DOE)

SRU - Seabird Research UnitD.N. Nettleship, Head . . . . . . . . . . . . . . 3274

GEOLOGICAL SURVEY OFCANADA (DEMR)

AGC - Atlantic Geoscience CentreM.J. Keen, Director. . . . . . . . . . . . . . . . . 2367

AGC - 1. AdministrationC.Racine, Head . . . . . . . . . . . . . . . . . . . 2111AGC - 2. Eastern Petroleum GeologyG.L. Williams, Head . . . . . . . . . . . . . . . 2730AGC - 3. Environmental Marine GeologyD.J.W. Piper, Head . . . . . . . . . . . . . . . . . 7730AGC - 4. Program SupportK.S. Manchester, Head . . . . . . . . . . . . . . 3411AGC - 5. Regional ReconnaissanceC.E.Keen, Head . . . . . . . . . . . . . . . . . . . 3448

57

STAFF LISTINGABRIEL, James AOL-1ACKER, Queenie MSADAMS, Al IF-1ADDISON, Richard MEL-2AHERN, Patrick MEL-2ALLEN, Lorraine MEL-3AMIRAULT, Byron AOL-1AMOS, Carl AGC-3ANDERSON, Bob AOL-4ANDERSON, Debbie MSANDERSON, George MSANNAND, Christine MFDANNING, Jeff MEL-1ARCHER, Barbara OIDARCHIBALD, Chris MSARMITAGE, Fred IF-2ARMSTRONG, Nancy MFDASCOLI, Piero AGC-2ASPREY, Ken AGC-3ATKINSON, Karen AOL-2ATKINSON, Tony AGC-4AVERY, Mike AGC-2AVEY, David BaffinAWALT, Garon IF-2

CALDWELL, Glen IF-2CAMERON, Ralph CHS-1CAMERON, Rose MSCAMPANA, Steve MFDCAMPBELL, Paul AGC-3CARR, Judy MFDCARSON, Bruce AOL-4CASEY, Deborah IF-3CASHIN, EImo IF-1

CASSIVI, Roger AOL-3CAVERHILL, Carla MEL-1CHAMBERLAIN, Duncan IF-1CHAPMAN, Borden AGC-4CHARLTON, Beverly MFDCHENIER, Marcel CHS-2CHIN-YEE, Mark IF-2CLARKE, Allyn AOL-4CLARKE, Tom IF-2CLATTENBURG, Donald AGC-3CLIFF, John BaffinCLOTHIER, Rodney BaffinCOADY, Vernon AGC-4COCHRANE, Norman AOL-3COLE, Flona AGC-3COLFORD, Brian MSCOLLIER, Kathie AOL-3COLLINS, Gary IF-3COMEAU, Ernest CHS-1CONNOLLY, Gerald AOL-3CONOVER, Bob MEL- ICONRAD, Bruce HudsonCONRAD, David AOL-1COOK, Gary AGC-2COOKE, Gary IF-2COSGROVE, Art IF-5COSTELLO, Gerard CHS-1COTA, Glenn MEL-1

Jackie Dale,

BACKMAN, Earl DawsonBAKER, Lloyd IF-1BARSS, Sedley AGC-2BASDEN, Kelly IF-1BASTIEN, Robert IF-3BATES, Steve MEL-1BEALS, Carol CHSBEANLANDS, Brian AOL-3BEANLANDS, Diane MFDBEAVER, Darrell AGC-4BECK, Brian MFDBECK, Vince IF-3BELANGER, Roger IF-5BELL, Bill DawsonBELLEFONTAINE, Larry AOL-2BELLEFONTAINE, Linda MSBENNETT, Andrew AOL-3BENNETT, Rick NaviculaBERKELEY, Tom CHS-3BEST, Neville HudsonBETLEM, Jan AOL-3BEWERS, Michael AOL-1BLAKENEY, Claudia AGC-3BLANCHARD, Elaine MSBLANEY, Dave CHS-1BLASCO, Steve AGC-3BONANG, Faye MSBONANG, Linda MS

58

BOND, Murray MSBOUDREAU, Gerry AOL-4BOUDREAU, Henri CHS-1BOUDREAU, Paul MEL-3BOWDRIDGE, Gordon MSBOWEN, Don MFDBOWEN, Eileen MSBOWMAN, Garnet CHS-1BOWSER, Mike IF-2BOYCE, Rick AOL-2BOYCE, Austin AGC-4BRANTON, Bob MFDBRINE, Doug IF-3BRODIE, Paul MEL-3BROWN, Dick SRUBUCKLEY, Dale AGC-3BUGDEN, Gary AOL-2BURGESS, Frank CHS-1BURHOE, Meg MSBURKE, Robert CHS-3BURKE, Walter CHS-1

FAULKNER, Pat MSFEETHAM, Jim PFENERTY, Norman IF-5FENN, Guy AGC-4FERGUSON, Carol IF-1FERGUSON John CHS-1FINDLEY, Bill IF-1

Bert Bennett,

COURNOYER, Jean IF-2COX, Brian BaffinCRANFORD, Peter MEL-2CRANSTON, Ray AGC-3CRAWFORD, Keith CHS-ZCREWE, Norman AOL-1CRILLEY, Bernard AGC-2CRONK, Suzanne AGC-5CROWE, Hubert HudsonCRUX Elizabeth CHS-2CUNNINGHAM, Carl AOL-1CUNNINGHAM, John CHSCURRIE, Randy IF-3CUTHBERT, Jim IF-3

DAGNALL, Joyce SRUDALE, Carla MFDDALE, Jackie MELDALZIEL, John AOL-/DANIELS, Marilyn IF-4D’APOLLONIA, Steve AGC-3DAS, Paddy BaffinDAVIES, Ed AGC-2DEASE, Ann MSDEASE, Gerry IF-2DeLONG, Bob IF-2DEMONT, Leaman IF-2DENNIS, Pat AGC-1D’ENTREMONT, Paul AOL-2DEONARINE, Bhan AGC-3DESCHENES, Mary Jean IF-3DESSUREAULT, Jean-Guy AOL-3DICKIE, Lloyd MEL-3DICKIE, Paul MEL-1DICKINSON, Ross DawsonDINN, Donald IF-2DOBSON, Des AOL-2DOBSON, Fred AOL-4DOLLIMOUNT, Ray HudsonDOWD, Dick MEL-3DRINKWATER, Ken MEL-3DUFFY, Sean CHS-1DUGAS, Theresa CAFCASDUNBRACK, Stu CHS-1DUNPHY, Paul AOL-4DURVASULA, Rao MEL-1

EATON, Mike CHS-4EDMONDS, Roy MELEDWARDS, Bob PEISENER, Don IF-2ELLIOTT, Jim AOL-4ELLIS, Kathy AOL-1ETTER, Jim IF-2

FADER, Gordon AGC-5FAHIE, Ted IF-2

Jeff McRuer, FANNING, Paul MFD

FITZGERALD, Bob AGC-3FLEMING, Dave CHS-2FODA, Azmeralda MEL-2FOOTE, Tom AOL-2FORBES, Donald AGC-3FORBES, Steve CHS-3FOWLER, George AOL-3FRANK, Ken MEL-3FRASER, Brian MEL-1FRASER, Jack MaxwellFRASER, Shardlyn PFREEMAN, Button MFDFREEMAN, Ken MEL-3FRICKER, Aubrey AGC-4FRIIS, Mike MSFRIZZLE, Doug CHS-2FROBEL, David AGC-3FROST, Jim MEL-3FULLERTON, Anne MEL-3

GALLANT, Celesta MSGALLANT, Roger IF-2GALLIOTT, Jim AOL-2GAMMON, Gary MSGAUDET, Victor CHS-1GEDDES, Dianne CAFSACGIDNEY, Betty CHS-2GILBERT, Reg IF

Keeping things together,

GILROY, Dave IF-2GIROUARD, Paul AGC-5GLAZEBROOK, Sherman AOL-4GOODWIN, Winston IF-2GOODYEAR, Julian CHS-1GORDON, Don MEL-2GORVEATT, Mike AGC-4GRADSTEIN, Felix AGC-2GRANT, Al AGC-2GRANT, Gary AGC-2GRANT, Steve CHS-6GREENBERG, David AOL-2GREGORY, Don AOL-4GREGORY, Doug AOL-2

GREIFENEDER, Bruno AOL-4GUILDERSON, Joan DGGUILBAULT, Jean-Pierre AGC-3

HAASE, Bob CHS-1HACQUEBARD, Peter AGC-2HALE, Ken IF-5HALLIDAY, James IF-1HALLIDAY, Ralph MFDHALVERSON, George IF-2HAMILTON, Jim AOL-3HAMILTON, Phyllis CHS-6HANTZIS, Alex CHS-2HARDING, Gareth MEL-2HARDY, Iris AGC-5HARGRAVE, Barry MEL-2HANKINSON, Doug BaffinHARMES, Bob AGC-3HARRIS, Cynthia MFDHARRIS, Jerry DawsonnHARRIS, Leslie MEL-1HARRISON, Glen MEL-1HARTLING, Bert AOL-2HARVEY, David AOL-3HAYDEN, Helen AOL-2HAYES, Terry AGC-1HEAD, Erica MEL-1HEFFLER, Dave AGC-4HEMPHILL, Milt CHS-1HENDERSON, Gary CHS-1HENDERSON, Terry AGC-1HENDRY, Ross AOL-4HENDSBEE, Dave AOL-4HENNEBERRY, Andy MEL-2HEPWORTH, Deborah CHS-2HERMAN, Alex AOL-3HILL, Phil AGC-3HILLIER, Blair AGC-4HILTZ, Ray AOL-1HILTZ, Sharon MSHINDS, Jim HudsonHODGSON, Mark MEL-1HOFFER, Darrell AGC-5HOGANSON, Joan MSHOLLAND, Len DawsonHOLMES, Wayne IF-2

JACKSON, Art AGC-2JACKSON, Ruth AGC-5JAMIESON, Steve PJANSA, Lubomir AGC-2JARVIS, Lawrence Hudson

Sheila MacHattie.

HORNE, Ed MEL-1HORNE, Jack IF-2HOUSSER, Debbie AGC-5HOWIE, Bob AGC-2HUBLEY, Susan AGC-4HUGHES, David CHS-1HUGHES, Mike AGC-4HUNTER, Leamond CHS-2HURLEY, Peter MFD

IRWIN, Brian MEL-1

Ken Freeman.

JAY, Malcolm CHS-2JENNEX, Rita MSJODREY, Fred AGC-4JOHN, Paulette MSJOHNSON, Sue SRUJOHNSTON, Larry AGC-4JOLLIMORE, Shirley IF-4JONES, Peter AOL-1JONES, Roger CHS-2JORDAN, Francis AOL-2JOSENHANS, Heiner AGC-5

KARG, Marlene IF-3KAVANAUGH, Anita IF-4KAY, William AGC-5KEARNEY, Carl DawsonKEDDY, Lil MSKEEN, Charlotte AGC-5KEEN, Mike AGCKEENAN, Pat AOL-2KEIZER, Paul MEL-2KELLY, Bruce IF-2KEPKAY, Paul MEL-2KERR, Adam CHSKERR, Steve MEL-3KIERSTEAD, Linda SRUKING, Donna MFDKING, Graeme CHS-5KING, Rollie IF-1KNOX, Don AOL-3KOELLER, Peter MFDKRANCK, Kate AOL-2

LAKE, Diana MSLAKE, Paul AGC-2LAMBERT, Tim MEL-3LAMPLUGH, Mike CHS-1LANDRY, Marilyn MEL-1LANGILLE, Neil NaviculaLAPIERRE, Mike IF-2LAPIERRE, Richard IF-1LAROSE, Jim CHS-2

LARSEN, Ejnar MEL-1LATREMOUILLE, Michael IF-5LAWRENCE, Don AOL-2LAZIER, John AOL-4LeBLANC, Bill AGC-3LeBLANC, Cliff MaxwellLeBLANC, Paul IF-2LEJEUNE, Diane MSLEJEUNE, Hans MSLEONARD, Jim AOL-1LEVY, Eric AOL-1LEWIS, Mary MEL-1LEWIS, Mike AGC-3LEWIS, Reg CHS-5LI, Bill MEL-1LISCHENSKI, Ed CHS-2LITTLE, Betty PLIVELY, Bob AOL-2LOCK, Stan BaffinLOCK, Tony SRULOCKE, Don AGC-4LOCKYER, Roy HudsonLODER, John AOL-4LONCAREVIC, Bosko AGC-5LONGHURST, Alan DCLORING, Douglas AOL-1LUTLEY, Judy MSLUTWICK, Graham CHS-6

MacDONALD, Al MEL-1MacDONALD, Barry MSMacDONALD, Gerry IF-2MacDONALD, Kirk CHS-5MacDONALD, Rose CHS-2MacGOWAN, Bruce CHS-1MacHATTIE, George IF-2MacHATTIE, Sheila PMacISAAC, Mary MFDMacKAY, Bob HudsonMacLAREN, Florence PMacLAREN, Oswald AOL-3MacLAUGHLIN, John IF-2MacLEAN, Brian AGC-5MacLEAN, Carleton BaffinMacLEOD, Grant CHS-2MacMILLAN, Bill AGC-2MacMILLAN, Linda CHS-1MACE, Pamela MFDMACNAB, Ron AGC-5MAHON, Robin MFDMALLET, Andre MEL-3MALONE, Kent CHS-1MANCHESTER, Keith AGC-4MANN, Ken MELMARTELL, Jim MSMARTIN, Bud MSMARTIN, Harold DawsonMASON, Clive AOL-2

Ray Hiltz.

MASON, Ralph MSMATTHEWS, Benny DawsonMATTHEWS, Gordon HudsonMAUGER, Fred HudsonMAZERALL, Anne IF-4McALPINE, Don AGC-2MCCARTHY, Cathy AGC-2MCCARTHY, Paul CHS-1McCORRISTON, Bert CHS-2MacFARLENE, Andrew SRUMcGINN, Pete CHS-6McGLADE, Jacquie MFDMcKEOWN, Dave AOL-3McMILLAN, Jim MFD

Herman Varma.

MCNEIL, Beverley CHSMcRUER, Jeff MEL-3MEHLMAN, Rick CHS-1MEIN, John BaffinMEISNER, Patsy CHS-2MELBOURNE, Ron CHS-2MIDDLETON, Cecilia AGC-3MILLER, Bob AGC-5MILLER, Frank CHS-2MILLETT, David BaffinMILLIGAN, Tim AOL-2MILNE, Mary AGC-2MITCHELL, Carol AGC-2MITCHELL, Michel AOL-3MOFFATT, John AOL-1MOORE, Bill IF-1MORAN, Kate AGC-3MUDIE, Peta AGC-3MUISE, Fred IF-2MUISE, Laura MSMURPHY, Bob AGC-4MURRAY, Ed OIDMYRA, Valerie MFDMYERS, Steven IF-1

NEEDLER, George AOLNELSON, Rick AOL-1NETTLESHIP, David SRUNEU, Hans AOL-2NICHOLLS, Brian OIDNICHOLS, Brian AGC-5NICHOLSON, Dale CHS- 1NICKERSON, Bruce AOL-3NICKERSON, Carol MSNICOLL, Michael IF-1NIELSEN, Jes AGC-4NORTON, Neil Baffin

OAKEY, Neil AOL-4O’BOY LE, Bob MFDO’NEIL, John AOL-4O’REILLY, Charles CHS-6O’ROURKE, Mike IF-2ORR, Ann MEL-3

59

PALMER, Nick CHS-2PALMER. Richard CHS-1PARANJAPE. Madhu MEL-1PARNELL, Cheryl AGC-1PARROTT, Russell AGC-3PARSONS, Art IF-2PATON, Jim MSPEER, Don MEL-2PELLERINE, Danny IF-1PENNELL, Charles HudsonPERROTTE, Roland CHS-2PETERSON, Ingrid AOL-4PETRIE, Brian AOL-2PETRIE, Liam MEL-3PHILLIPS, Georgina MEL-2PHILLIPS, Ted AOL-3PIETRZAK, Robert CHS-5PI PER, David AGC-3PLATT, Trevor MEL-1POCKLINGTON, Roger AOL-1POLSON, Carl IF-2PORTEOUS, Dave IF-3PORTER, Cathy AOL-4POTTIE, Dennis AOL-1POTTIE, Ed MSPOWROZ, William DawsonPOZDNEKOFF, Peter AOL-4PRIME, Wayne AGC-4PRINSENBERG, Simon AOL-2PRITCHARD, John AOL-2PROCTOR, Wally AOL-3PROUSE, Nick MEL-2PURDY, Phil MS

ROSSE, Ray MSROZON, Chris CHS-1RUDDERHAM, Dave MEL-1RUMLEY, Betty AOL-2RUSHTON, Laurie MEL-1RUSHTON, Terry IFRUXTON, Michael CHS-1RYAN, Anne CHS-1

SABOWITZ, Norman IF-4SADI, Jorge BaffinSAMEOTO, Doug MEL-1SANDSTROM, Hal AOL-4SAUNDERS, Jo-Anne IF-4SAVOY, Rachel1 PSCHAFER, Charles AGC-3SCHIPILOW, Catherine CHS-2SCHUTZENMEIER, Marion AOL-2SCHWARTZ, Bernie IF-2SCHWINGHAMER, Peter MEL-2SCOTNEY, Murray AOL-2SEIBERT, Gerald OIDSHATFORD, Lester AOL-3SHAY, Juanita IF-2SHELDON, Ray MEL-3SHERIN, Andy AGC-4SHIH, Keh-Gong AGC-5SHOTTON, Ross MEL-3SILVERT, Bill MEL-3SIMMONS, Carol MEL-2SIMMS, Judy AOL-1SIMON, Jim MFDSIMPSON, Pat MFDSINCLAIR, Alan MFDSLADE, Harvey IF-5SMITH, Alan CHS-2SMITH, Burt CHS-1SMITH, Bill MFDSMITH, Fred IF-1SMITH, John AOL-1SMITH, John MEL-1SMITH, Michelle SRUSMITH, Peter AOL-2SMITH, Steve MFDSMITH, Stu AOL-4SMITH, Sylvia MELSMITH, Ted IF-1SPARKES, Roy AGC-4SPENCER, Florence AGC-1SPENCER, Sid IF-2SPRINGETT, Joan MSSRIVASTAVA, Shiri AGC-5

J a c k H o r n e ,

QUON, Charlie AOL-4

RACINE, Carol AGC-1RAFUSE, Phil BaffinRAIT, Sue MSRANTALA, Reydo AOL-1RASHID, Mohammed AGC-3REED, Barry DawsonREID, Ian AGC-5REID, Jim MFDREIMER, Dwight MEL-3REINHARD, Harry MSREINIGER, Bob AOL-4REYNOLDS, Bill HudsonRICHARD, Wayne IF-3RIPPEY, Jim HudsonRITCEY, Jack BaffinROBERTSON Kevin AGC-3ROCKWELL, Gary CHS-1RODGER, Glen CHS-1ROOP, David CHS-1ROSE, Charlie IF-2ROSS, Charles AOL-4ROSS, Jim CHS-2

STEAD, Gordon CHS-2STEELE, Trudi AOL-4STEEVES, Gcorge IF-2STEPANCZAK, Mike AOL-3STEWART, Pat AGC-1STILO, Carlos BaffinSTIRLING, Charles CHS-1STOBO, Wayne MFDSTODDART, Stan HudsonSTOFFYN, Mark AGC-3STOFFYN, Patricia AGC-3STOLL, Hartmut IF-2STRAIN, Peter AOL-1STRUM, Loran HudsonSTUART, Al IF-2STUIFBERGEN, Nick CHS-4SUTHERLAND, Betty IF-4SWIM, Minard CHS-1SYMES, Jane PSYMONDS, Graham AOL-4SYVITSKI, James AGC-3

60

TAN, Francis AOL-1TANG, Charles AOL-2TAYLOR, Bill IF-3TAYLOR, Bob AGC-3TAYLOR, Gcorgc MEL-3

Harvey Slade,

TEE, Kim-Tai AOL-4THOMAS, Frank AGC-2TILLMAN, Betty PTOLLIVER, Deloros AGC-1TOMS, Elaine IF-4TOPLISS, Brenda AOL-2TOTTEN, Gary IF-1TRITES, Ron MEL-3

UNDERWOOD, Bob IF-2

VANDERMEULEN, John MEL-2VARBEFF, Boris IF-2VARMA, Herman CHS-1VASS, Peter MEL-2VAUGHAN, Betty IF-2VERGE, Ed AOL-2VETESE, Barb AGC-1VEZINA, Guy IF-2VILKS, Gus AGC-3VINE, Dick IF-2

WADE, John AGC-2WALDRON, Don MFDWALKER, Bob AOL-2WARD, Brian IF-2WARDROPE, Dick IF-2WARNELL, Margaret IF-3WATSON, Nelson MEL-1WEBBER, Shirley MSWENTZELL, Cathy PWESTHAVER, Don IF-2WESTON, Sandra CHS-2WHITE, George MFDWHITE, Joe MSWHITE, Keith CHS-3WHITEWAY, Bill AOL-3WHITMAN, John AOL-3WIECHULA, Marek IF-3WIELE, Heinz IF-5WILE, Bruce AOL-4WILLIAMS, Doug MSWILLIAMS, Graham AGC-2WILLIAMS, Pat AOLWILLIS, Doug EL-2WILSON, George IF-1WILSON, Jim IF-2WINTER, Danny IF-2WINTERS, Gary AGC-3WOOD, Bryan FDWOODHAMS, Lofty IF-2WOODSIDE, John AGC-SWRIGHT, Dan AOL-4WRIGHT, Morley IF-2WTTEWAAL, Joan IF-3

YEATS, Phil AOL-1YOULE, Gordon AOL-3YOUNG, Gerry MFDYOUNG, Scott AOL-3

ZEMLYAK, Frank AOL-1ZEVENHUIZEN, John AGC-5ZINCK Maurice MFL-2ZWANENBURG, Kees MFD

Bruno Greifeneder.

Project Listing

We present below a listing of theprojects (A,B,C, etc.) and individualinvestigations (1,2,3, etc.) beingundertaken by the four major componentsof the Bedford Institute of Oceanography;the Atlantic Oceanographic Laboratory,Marine Ecology Laboratory, AtlanticGeoscience Centre, and Atlantic Region ofthe Canadian Hydrographic Service. Thelisting was current at the end of December1983. For more information on theseprojects and those of other BIOcomponents, feel free to write toPublication Services, Bedford Institute ofOceanography, P.O. Box 1006,Dartmouth, Nova Scotia B2Y 4A2.

ATLANTICOCEANOGRAPHICLABORATORYA. SURFACE AND MIXED-LAYEROCEANOGRAPHY

1.

2.

3.

4.

5.6.7.

8.9.

10.

11.

12.

13.14.

15.

16.

17.

18.

Sea surface wind stress, heat flux, andevaporation (S.D. Smith, R.J. Anderson,F.W. Dobson)Arctic polynya experiment (S.D. Smith,R.J. Anderson)CO2 exchange at the air-sea interface(E.P. Jones, S.D. Smith)Surface heat flux at OWS Bravo (S.D. Smith,F.W. Dobson, J.R.N. Lazier)Wave growth studies (F.W. Dobson)Wave climate studies (H.J.A. Neu)Oil trajectory analysis (D.J. Lawrence,J.A. Elliott)Surface drifters (D. Gregory)Iceberg drift track modelling (S.D. Smith)Microstructure in the surface layers (N.S. Oakey,J.A. Elliott)Near-surface velocity measurements(N.S. Oakey)Comparison of long-term mean air-sea fluxesfrom historical data (F. W. Dobson, S.D. Smith)Studies of the Labrador ice edge (G. Symonds)Gulf of St. Lawrence ice studies (G. Symonds,G.L. Bugden)Atmospheric Fluxes - MIZEX, the Marginal IceZone Experiment (R.J. Anderson, S.D. Smith)Mean wind stress estimates from bulkaerodynamic formulas (D. Wright,K. Thompson, R. F. Marsden)Fronts at the edge of Gulf Stream rings(A.S. Bennett, D.J. Lawrence, C.L. Tang)Sea Ice Dynamics - MIZEX. the Marginal IceZone Experiment (G. Symonds)

B. LARGE-SCALE DEEP-SEAOCEANOGRAPHY

1.

2.

3.

4.

5.

6.

7.

8.9.

10.

11.

12.

13.14.

Labrador Sea water formation (R.A. Clarke,N.S. Oakey, J.-C. Gascard)Dynamics of the Labrador Sea (C. Quon,R.A. Clarke)Labrador Current variability (A. Allen,R.A. Clarke)Age determination in Baffin Bay bottom water(E.P. Jones, J.N. Smith, K. Ellis)Local-scale Gulf Stream variability(R.M. Hendry, R.F. Reiniger)Gulf Stream extension experiment(R.M. Hendry, R.F. Reiniger)Newfoundland Basin experiment (R.A. Clarke,R.M. Hendry, A.R. Coote)Stability problems in GFD flows (C. Quon)Northwest Atlantic atlases (R.F. Reiniger,R.A. Clarke, R.M. Hendry, D. Gregory)Norwegian/Greenland sea experiment(R.A. Clarke and others)Baseline hydrography and ocean heat flux(R.M. Hendry)Polar front or North Atlantic current(J.R.N. Lazier)Denmark Strait overflow (C.K. Ross)Geochemical tracer studies (G.T. Needler,D. Wright)

C. CONTINENTAL SHELF AND PASSAGEDYNAMICS

1.

2.

3.

5.

6.7.

8.

9.

10.

Cape Sable experiment (P.C. Smith,D. LeFaivre, K.-T. Tee. R.W. Trites)Shelf break experiment (P.C. Smith,B.D. Petrie, J.P. Louis)Strait of Belle Isle (B.D. Petrie, C. Garrett,B. Toulany, D.A. Greenberg)Tidally induced mixing (J.A. Elliott,H. Sandstrom)Batfish internal waves (A.S. Bennett)Dynamics of tidal rectification over submarinetopography (D. Wright, J. Loder)Dynamics of residual circulation in the Gulf ofMaine (D.A. Greenberg, J. Loder. P.C. Smith,D. Wright)Mixing and circulation on Georges Bank(J. Loder, D. Wright)Circulation and dispersion on Browns Bank(P.C. Smith)

D. CONTINENTAL SHELF AND PASSAGEWATER-MASS AND TRANSPORT STUDIES

1. Labrador shelf and slope studies (J.R.N. Lazier)2. Flemish Cap experiment (C.K. Ross)3. Long-term monitoring of the Labrador Current

at Hamilton Bank (J.R.N. Lazier)4. Data archiving (D. Gregory)5. Development of remote sensing facilities at the

Atlantic Oceanographic Laboratory(C.S. Mason, A.S. Bennett, B. Topliss)

6. Oceanography of the Newfoundland continentalshelf (B.D. Petrie)

7. Long-term temperature monitoring(B.D. Petrie, D. Dobson)

8. Eastern Arctic physical oceanography(C.K. Ross)

9. Water transport through and in the NorthwestPassage (S.J. Prinsenberg, B. Bennett)

E. OCEANOGRAPHY OF ESTUARIES ANDEMBAYMENTS

1.2.

3.4.

5.

6.

7.

8.

9.

10.

11.

12.

13.14.

15.

16.

17.

18.19.

20.

Saguenay fjord study (G.H. Seibert)Northwestern Gulf of St. Lawrence (C.L. Tang,A.S. Bennett)Gaspe Current studies (C.L. Tang)Gulf of St. Lawrence frontal study (C.L. Tang,A.S. Bennett)Seasonal and interannual variability in the Gulfof St. Lawrence (G.L. Bugden)Laurentian Channel current measurements(G.L. Bugden)The Gulf of St. Lawrence - Numericalmodelling studies (K.-T. Tee)Tidal and residual currents - 3-D modellingstudies (K.-T. Tee)Bay of Fundy tidal power - studies in physicaloceanography (D.A. Greenberg)Forced flows in the Strait of Canso(D.J. Lawrence, D.A. Greenberg)Physical behaviour of particulate matter andsediments in the natural environment(K. Kranck)Laboratory studies of particulate matter(K. Kranck)Bottom drifters (D. Gregory)Residual barotropic circulation in the Bay ofFundy and Gulf of Maine (D.A. Greenberg)Suspended sediment modelling(D.A. Greenberg, C.L. Amos)Winter processes in the Gulf of St. Lawrence(G.L. Bugden)Modelling historical tides (D.A. Greenberg.D. Scott, D. Grant)Storm surge (D.A. Greenberg, T.S. Murty)Tidal and wind mixing in the Gulf of Maine(D.A, Greenberg, J. Loder)Circulation and air/sea fluxes of Hudson Bayand James Bay (S. Prinsenberg)

F. SENSOR DEVELOPMENT1. Anemometers for drifting buoys

(J.-G. Dessureault)2. CTDs and associated sensors (A.S. Bennett)3. Thermistor chains on drifting buoys

(G.A. Fowler, J.A. Elliott)4. Towed biological sensors (A.W. Herman and

others)5. The dynamics of primary and secondary

production on the Scotian Shelf (A.W. Herman,D.D. Sameoto, T.C. Platt)

6. Vertical profiling biological sensors (A.W.Herman, M. Mitchell, S. Young, E. Phillips)

7. Zooplankton grazing and phytoplanktonproduction dynamics (A.W. Herman,A.R. Longhurst, D.D. Sameoto, T.C. Platt,W.G. Harrison)

8. Measurement of zooplankton variability(A.W. Herman, D.D. Sameoto)

9. Real-time data acquisition (A.S. Bennett)

61

10. CTD sensor time-constant measurements(A.S. Bennett)

11. Moored biological sensors (A.W. Herman,M. Mitchell, S. Young, E. Phillips)

12. Satellite estimations of primary productivity(B.J. Topliss)

13. Optical properties of Canadian waters

G. SURVEY AND POSITIONING SYSTEMDEVELOPMENT

1. Bottom referenced acoustic positioning systems(D.L. McKeown)

2. Ship referenced acoustic positioning systems(D L. McKeown)

3. Multifrequency acoustic scanning of watercolumn (N.A. Cochrane)

4. Digital echo sounding (N.A. Cochrane)5. Doppler current profiler (N.A. Cochrane)

H. OCEANOGRAPHIC INSTRUMENTDEPLOYMENT

1.

2.

3.

4.

5.

6 .

Engineering studies of stable platforms(S.D. Smith, R.J. Anderson, R.G. Mills)Mooring system development (G.A. Fowler,R.F. Reiniger, A.J. Hartling)Handling and operational techniques forinstrument cable systems (J.-G. Dessureault,R.F. Reiniger)Drill system improvement (G.A. Fowler,P.F. Kingston, P.J.C. Ryall)In-situ sampling of suspended particulate matter(D.L. McKeown, B. Beanlands, P.A. Yeats)Measurement of geotechnical properties(G.A. Fowler)

I. NEARSHORE ANDGEOCHEMISTRY

ESTUARINE

1.

2.

3.

4.

5.

6.

7.

8.

9.

10.

11.

12.

13.

Estuarine and coastal trace metal geochemistry(P.A. Yeats, D.H. Loring)Atmospheric input into the ocean (P.A. Yeats,J.A. Dalziel)Sediment geochronology and geochemistry inthe Saguenay Fjord (J.N. Smith, K. Ellis)Sediment transport and bioturbation studies inthe Bay of Fundy (K. Ellis, J.N. Smith,D. Wildish)Organic composition of the St. Lawrence River(R. Pocklington, F.C. Tan, D. Cossa.E. Degens)Physical-chemical controls of particulate heavymetals in a turbid tidal estuary (D.H. Loring,A. Morris)CO2 sinks in shelf and slope sediments(R. Pocklington, E. Premuzic)Arctic and west coast fjords (J.N. Smith,K. Ellis, C.T. Schafer, J.P.M. Syvitski)Chemical pathways of environmentaldegradation of oil (E.M. Levy)Climate variability in fjords (J.N. Smith,K. Ellis, C.T. Schafer)Plant degradation and coastal food web studiesby stable isotope methods (R. Stephenson,F.C. Tan, K.H. Mann)Isotope geochemistry of major world estuaries(F.C. Tan, J.M. Edmond)Review of chemical oceanography in the Gulf ofSt. Lawrence (J.M. Bewers)

J. DEEP OCEAN MARINE CHEMISTRY1. Nutrient regeneration processes in Baffin Bay

(E.P. Jones)2. The carbonate system and nutrients in Arctic

regions (E.P. Jones)3. Distribution of sea-ice meltwater in the Arctic

(F.C. Tan, P.M. Strain)4. Trace metal geochemistry in the North Atlantic

(P.A. Yeats, J.A. Dalziel)5. Sediment transport, deposition, and

bioturbation studies on the Newfoundland slope(J.N. Smith, K. Ellis, C.T. Schafer)

62

6. Natural marine organic constituents(R. Pocklington, J.D. Leonard)

7. Paleoclimatic studies (F.C. Tan, G. Vilks)8. Comparison of vertical distribution of trace

metals in the North Atlantic and North Pacificoceans (P.A. Yeats)

9. Carbon isotope fractionation studies in marinephytoplankton (F.C. Tan, P. Wangersky)

10. Extraction, identification, and analysis ofdissolved organic matter (R. Pocklington,F.C. Tan, T. Fu)

11. Radionuclide measurements in the Arctic(J.N. Smith, K. Ellis, E.P. Jones)

12. Chemistry of sea ice (E.P. Jones)13. Carbon isotope studies on particulate and

dissolved organic carbon in deep sea and coastalenvironments (F.C. Tan, P. Strain)

K. MARINE POLLUTION CHEMISTRY1.

2.

3.

4.

5.

6.

7.

8.

9.10.

11.

12.

13.

Dissolved low molecular weight hydrocarbonsin Baffin Bay (E.M. Levy)Petroleum hydrocarbon components(E.M. Levy)Petroleum residues in the eastern CanadianArctic (E.M. Levy)

2.

3.

4.

Large-scale oil pollution of the oceans 5.(E.M. Levy)Point Lepreau environmental monitoringprogram (J.N. Smith, K. Ellis, G.L. Bugden,J.M. Bewers, D. Scarratt)Canadian marine analytical chemical standards(J.M. Bewers, P.A. Yeats, J.A. Dalziel)International activities (J.M. Bewers,E.M. Levy, D.H. Loring)Joint Canada/FRG caisson experiments on metalexchanges between aqueous and sedimentaryphases (D.H. Loring, R. Rantala)Marine emergencies (E.M. Levy)Heavy metal contamination in a Greenland fjord(D.H. Loring)Background levels of petroleum residues andlow molecular weight hydrocarbons in theLabrador shelf and Hudson Strait regions(E.M. Levy)Intercalibration for hydrocarbons in the watercolumn and on the sea surface (E.M. Levy)Petroleum pollution monitoring in the Gulf ofSt. Lawrence (E.M. Levy)

L. TECHNOLOGY TRANSFER1. Seabed mosaics (J.-G. Dessureault)2. Ocean data systems (J.A. Elliott)3. Papa (J.A. Elliott)

MARINEECOLOGYLABORATORYA. PRIMARY PRODUCTION PROCESSES

1. Mathematical representation andparameterization of photosynthetic response tochanges in light intensity (T.C. Platt)

2. Dependence of photosynthesis-light parameterson environmental conditions (T.C. Platt andothers)

3. Significance and nature of aggregation anddispersion in phytoplankton productionprocesses (T.C. Platt)

4. Physiology and biochemistry of enzymes ofphotosynthesis (J.C. Smith, T.C. Platt)

5. Growth rates and protein synthesis byphytoplankton in relation to light intensity(W.K.W. Li and others)

6. Respiration, nutrient uptake, and regenerationin natural phytoplankton populations(W.G. Harrison and others)

7. Physical oceanography of selected features in

connection with marine ecological studies(E.P.W. Horne, T.C. Platt)

8. Physiology of marine micro-organisms(W.K.W. Li)

9. Patterns of phytoplankton photosynthesisassessed by radiocarbon distribution amongcellular polymers and metabolites (W.K.W. Li,T.C. Platt)

10. Role of picoplankton in the marine ecosystem(T.C. Platt and others)

11. Biological oceanography of the Grand Banks(E.P.W. Horne and others)

B. SECONDARY PRODUCTION PROCESSES1.

6.

7.

8.

9.

10.

Carbon and nitrogen utilization by zooplanktonand factors controlling secondary production(R.J. Conover)Ecology of microzooplankton in the BedfordBasin, Nova Scotia (M.A. Paranjape)Development of profiling equipment (BIONESSand LHPR) for plankton and micronekton(D.D. Sameoto)Use of acoustic techniques to measuredistribution of plankton and ichthyoplankton(D.D. Sameoto)Analysis of microdistribution ofichthyoplankton and zooplankton in upwellingecosystems (D.D. Sameoto)Nature and significance of vertical variability inzooplankton profiles (A.R. Longhurst)Investigation of the biochemical composition ofparticulate organic matter in relation to digestionby zooplankton (E. Head)Measurements of enzyme levels and their utilityin estimating physiological rates and indetermining physiological stages (E. Head)BIOSTAT program: zooplankton andmicronekton (D.D. Sameoto)Feeding studies on zooplankton grown in analgal chemostat (E. Head, R.J. Conover)

C. ATLANTIC CONSHELF ECOLOGY1.

2.

3.

4.

5.

6.

Scotian Shelf Resources and the ShelfIchthyoplankton Program: data acquisition overlarge spatial and long temporal scales(R.J. Conover)Seasonal cycles of abundance and distribution ofmicrozooplankton on the Scotian Shelf(M.A. Paranjape)Comparison of methods of calculation ofsecondary production estimates fromzooplankton population data (R.J. Conover)Significance of Yarmouth upwelling planktonproduction to the general productivity of ScotianShelf fish stocks (D.D. Sameoto)Vertical flux of living and nonliving particles inthe water column and nutrient-gas exchangeacross the seawater-sediment boundary on theScotian Shelf (B.T. Hargrave, G.C.H.Harding)Comparative studies of functional structure ofpelagic ecosystems (A.R. Longhurst)

D. EASTERN ARCTIC ECOLOGICAL STUDIES1. Physiology, production, and distribution of

marine phytoplankton (T.C. Platt and others)2. Distribution, growth, production, and the role of

diapause in Arctic zooplankton communities(R.J. Conover and others)

3. Zooplankton and micronekton of the easternArctic (D.D. Sameoto)

4. Arctic microzooplankton net samples(D.D. Sameoto)

5. Distribution and abundance ofmicrozooplankton in the Arctic(M.A. Paranjape)

6. Eco-physiological aspects of marine bacterialprocesses (W. K. W. Li)

7. Studies of epontic communities in BarrowStrait, 1983 (N. Watson and others)

E. ECOLOGY OF FISHERIES PRODUCTION1 . Acoustic analysis of fish populations and

development of survey methods (L.M. Dickieand others)

2. Genetic and environmental control ofproduction parameters (L.M. Dickie and others)

3. Geographic variations of production parameter\(L.M. Dickie and others)

4. Metabolism and growth of tishes (S.R. Kcrr)5. Mathematical analysis of fish production

systems ( W. L. Silvert )6 . Size-structure spectrum of fish production

(S.R. Kerr and others)7. Plankton growth rate in relation to size and

temperature (R. W. Sheldon)

8.9.

10.

11.

12.

Bioenergetics: Marine mammals (P.F. Brodie)Feeding strategies and ecological impact ofbivalve larvae (C. Abou Debs)Mathematical analysis of fish populationinteractions (S.R. Kerr, L.M. Dickie)Marine mammal - fisheries interactions(P. Brodie)Grand Banks ecosystem models (W.L. Silvertand others)

2.

3 .

4.

5.

6.F. ENVIRONMENTAL VARIABILITY EFFECTS:CLIMATIC AND ENVIRONMENTALCONTROLOF FISH POPULATION ABUNDANCE

1. Residual current patterns on the CanadianAtlantic continental shelf as revealed by driftbottles and seabed drifters (R. W. Trites)

7.

8.

9.

1 .

2.

3.

4.

5.

At top, a large set of herring (~150 tons) is pumped aboard the purse seiner MattunaMariner over German Bank, southwest Nova Scotia. Below, a biologist samples andmeasures the catch from the chute behind her that transfers the fish to the holds of theship.

Water type analyses for the NAFO areas(R.W. Trites, K.F. Drinkwater)Effects of Hudson Bay outflow on the LabradorShelf (K.F. Drinkwater)Larval transport and diffusion studies(R.W. Trites, T.W. Rowell)Current and transport in the George’s Bank -southwest Nova Scotia region in relation to theinshore/offshore lobster problem (R.W. Trites)Oil distribution in relation to winds and currentsfollowing the breakup of the Kurdistan(R.W. Trites and others)Halifax Section historical data(K.F. Drinkwater)Environmental variability -correlations andresponse scales (R. W. Trites)Climatic variability in the NAFO areas(R.W. Trites, K.F. Drinkwater)Baffin Island fjords (R.W. Trites)IO.

G. FISHERIES RECRUITMENT VARIABILITY

6.

7.

8.

9.

10.

11.

12.

13.14.

15.

16.

17.

IX

Steady-state model and transient features of thecirculation of St. George’s Bay(K.F. Drinkwater)The distribution. abundance. and recruitment oflobster larvae and their relation to stockrecruitment (G.C.H. Harding and others)Seasonal variability of planktonic particle sizespectrum (G.C.H. Harding and others)Nutrition and growth of micro-. macro-. andichthyoplankton (R.W. Sheldon and others)Vertical movement of plankton, suspendedmatter. and dissolved nutrients in the watercolumn (G.C. H. Harding and others)Characterization of water masses by particlespectra (R.W. Sheldon and others)Langmuir circulation and small scaledistribution of plankton (T. Lambert and others)Primary production dynamics (K.F. Drinkwaterand others)Coupling of pelagic and benthic productionsystems (P. Schwinghamer and others)Instrument development for surveys of particlesize distribution (R.W. Sheldon)Trophic relationships in nearshore kelpcommunities (K.H. Mann)Hydrography of the southern Gulf ofSt. Lawrence (K.F. Drinkwater)Fish reproductive strategies (T. Lambert)Recruitment of larval lobsters along southwestNova Scotia. the Bay of Fundy. and the Gulf ofMaine (G.C.H. Harding and others)Fine-scale measurements of larval survival(K.T. Frank)Dispersal strategies of marine fish larvae(K.T. Frank)Broad-scale spatial coherence of reproductivesuccess among discrete stocks of capelin(K.T. Frank and others)Southwest Nova Scotia fisheries ecology -Benthic production processes (P. Schwinghamerand others)

H. SUBLETHALCONTAMINATION EFFECTS1.

2.3.

4.

5.

6.

7.

MFO induction by PCBs and PCB replacements(R.F. Addison)Organochlorines in seals (R.F. Addison)Fate. metabolism. and effects of petroleumhydrocarbons in the marine environment(J.H. Vandermeulen)Organochlorine dynamics in the marine pelagicecosystem (G.C.H. Harding, R.F. Addison)Transfer of metalloids through marine foodchains (J.H. Vandermeulen)Hazard assessment of “new” environmentalcontaminants (R.F. Addison)“Calibration” of MFO systems in winterflounder as an ‘effects' monitoring tool(R.F. Addison)

63

I. BAY OF FUNDY ECOLOGICAL STUDIES1.

2.

3.

4.

5.

6.

7.

8.

9.

10.

Ice dynamics in the upper reaches of the Bay ofFundy (D.C. Gordon Jr. )Water chemistry and primary production in theBay of Fundy (D.C. Gordon Jr. and others)Concentration. distribution, seasonal variation.and flux of inorganic nutrients and organicmatter in shallow waters and intertidal sedimentsin the upper reaches of the Bay of Fundy(D.C. Gordon Jr. and others)Intertidal primary production and respirationand the availability of sediment organic matter(B.T. Hargrave and others)Microbial ecology of the Bay of Fundy(L. Cammen. P. Schwinghamer)Subtidal benthic ecology of the Bay of Fundy(P. Schwinghamer, D.L. Peer)Intertidal benthic ecology of the upper teaches ofthe Bay of Fundy (P. Schwinghamer and others)Zooplankton studies in Cumberland Basin. N.S.(N. Prouse)Production. export. and ecological importanceof the Bay of Fundy saltmarshes (D.C. Gordonand others)Modelling of Bay of Fundy ecosystems(D.C. Gordon and others)

J. DEEP OCEAN ECOLOGY1. Deep ocean benthic community studies

(P. Schwinghamer)2. Mobility of trace metals and radionuclides in

sediments (P. Kepkay)3. Activity of scavenging amphipods in transfer of

materials in the deep ocean (B.T. Hargrave)4. Vertical fluxes under the Arctic ice cap

(D.C. Gordon Jr. and others)

ATLANTICGEOSCIENCECENTREA. COASTAL PROGRAM

1.

2.

3.

4.

5.

6.7.

8.

Consulting advice on physical environmentalproblems in the coastal zone (R.B. Taylor)Coastal morphology and sediment dynamics.southeast and east Cape Breton Island, N.S.(R.B. Taylor)Morphology, sedimentology, and dynamics ofNewfoundland coast (D.L. Forbes)Coastal environments and processes in theCanadian Arctic Archipelago (R.B. Taylor)Sediment dynamics and depositional processesin thecoastal zone (D.L. Forbes)Beaufort Sea coast (D.L. Forbes)Permafrost processes in Arctic beaches(R.B. Taylor)Near-surface geology of the Arctic islandchannels (D.J. W. Piper)

B. COASTAL INLETS1.

2 .3.

4.

5.

6.

The physical behaviour of suspended particulatematter in natural aqueous environments(J.P.M. Syvitski)Sedimentology of fjords (J.P.M. Syvitski)Landsat calibration for suspended sedimentconcentration in marine coastal environments(C.L. Amos)Sediment dynamics - Head of the Bay of Fundy(C.L. Amos)Geochemical transformations and reactions oforganic compounds in Recent marine sediments(M.A. Rashid)Ocean dumping consultation and study(D.L. Forbes)

C. CONTINENTAL SHELFI. Ice scouring of continental shelves

(C.F.M. Lewis)

64

E. DEEP SEA1. Environmental geology of the deep ocean

(D.E. Buckley)2. Surficial geology of the Lomonosov Ridge.

Arctic Ocean (S.M. Blasco)3. Facies models of modem turbidites

(D.J.W. Piper)

Sonic anemeters set up near the polynyaat Dundas Island (near Devon Island) tomeasure heat flux and wind speed.

2.

3.

4.

Stability and transport of sediments oncontinental shelves (C.L. Amos)Engineering geology of the Arctic shelf(C.F.M. Lewis)Surficial geology and geomorphology.MacKenzie Bay/Continental Shelf(S.M. Blasco)

D. CONTINENTAL SLOPEI. Quaternary geologic processes on continental

slopes (D.J.W. Piper)

4. Temporal and spatial variation of deep oceancurrents in the western Labrador Sea(C.T. Schafer)

F. HOLOCENE1. The Recent paleoclimatic and paleoecologic

records in fjord sediments (C.T. Schafer)

G. PLEISTOCENE1. Pleistocene-Holocene sedimentation in

Hamilton Inlet and southeastern Labrador Shelf(G. Vilks)

2. Quantitative Quaternary paleoecology. easternCanada (P. Mudie)

H. SURFICIAL SEDIMENTS AND BEDROCKMAPPING

1. Bedrock and surficial geology. Grand Banks andScotian Shelf (G.B. Fader)

2. Eastern Baffin Island shelf bedrock and surficialgeology mapping program (B. MacLean)

3. Surficial geology. geomorphology, andglaciology of the Labrador Sea (H. Josenhans)

I. REGIONAL GEOPHYSICAL SURVEYS1. East coast offshore surveys (R.F. Macnab)2. Evaluation of KSS-30 gravimeter

(B.D. Loncarevic)3. An earth science atlas of the continental margins

of eastern Canada (S.P. Srivastava)4. Arctic Ocean seismic refraction and related

geophysical measurements (H.R. Jackson)

J. DEEP STRUCTURAL INVESTIGATIONS1. Comparative studies of the continental margins

of the Labrador Sea and of the North Atlantic(S.P. Srivastava)

Within sight of Baffin Island, Joseph Bray checks CSS Hudson’s gyrocompass bymeasuring the sun’s azimuth at noon.

The Sigma-T arriving at the BIO jetty.

2 . Seismic studies of continental margins andocean basins of the North Atlantic (LASE)(I. Reid)

3 . Surficial geology and crustal structure of theAlpha Ridge. Arctic Ocean (H.R. Jackson)

4 . Geology of the eastern margin of Canada andother parts of the Canadian offshore(G.L. Williams)

5 . Seismicity studies of the eastern Canadianmargins (I. Reid)

K. THEORETICAL MODELLING1. Rift processes and the development of passive

continental margins (C.E. Keen)

L. BASIN ANALYSIS AND PETROLEUMGEOLOGY

1..

2 .

3.

4.

5.

Regional subsurface geology of the Mesozoicand Cenozoic rocks of the Atlantic continentalmargin (J.A. Wade)Geological interpretation of geophysical data asan aid to basin synthesis and hydrocarboninventory (A.C. Grant)Compilation of geoscientific data in the UpperPaleozoic basins of southeastern Canada(R.D. Howie)Stratigraphy and sedimentology of theMesozoic and Tertiary rocks of the Atlanticcontinental margin (L.F. Jansa)Reconnaissance field study of the Mesozoicsequences outcropping on the Iberian Peninsula(L.F. Jansa)

M. RESOURCE APPRAISAL1. Hydrocarbon inventory of the sedimentary

basins of eastern Canada (J.S. Bell)2. Rank and petrographic studies of coal and

organic matter dispersed in sediments(P.A. Hacquebard)

3. Maturation studies (J.S. Bell)

N. BIOSTRATIGRAPHY1.

2.

3.

4.

56.

7.

8.

9.

10.

Identification and biostratigraphic interpretationof referred fossils (S.M. Barss)Palynological zonation of the Carboniferous andPermian rocks of the Atlantic provinces. Gulf ofSt. Lawrence. and Northern Canada(M.S. Barss)Biostratigraphy of the Atlantic and relevantareas (E.H. Davies)Taxonomy. phylogeny, and ecology ofpalynomorphs (E.H. Davies)DSDP dinoflagellates (G.L. Williams)Biostratigraphic zonation (Foraminifera.Ostracoda) of the Mesozoic and Cenozoic rocksof the Atlantic shelf (P. Ascoli)Biostratigraphic history of the Mesozoic-Cenozoic sediments of the Grand Banks.northeast Newfoundland. and Labrador shelves(based on Foraminifera and Ostracoda)(F.M. Gradstein)Taxonomy, biostratigraphy, paleoecology, andpaleobiogeography of agglutinatedForaminifera (F.M. Gradstein)Biostratigraphic data-processing development(M.S. Barss)Quaternary biostratigraphic methods for marinesediments (G. Vilks)

O. DATA BASES1. Geological Survey of Canada representative on

steering committee of the Kremp palynologiccomputer research project (M.S. Barss)

2. Information base-offshore east coast wells(G.L. Williams)

3. Data inventory (I. Hardy)

P. TECHNOLOGY DEVELOPMENT1. Sediment dynamics monitor - RALPH

(D.E. Heffler)2. Development of Vibracorer/drill for

3.

4.

geotechnical. geological. and engineeringstudies (K.S. Manchester)Coastal information system development(A. Fricker. D.L. Forbes)Development and implementation of cablehandling and maintenance procedures(K.S. Manchester)

ATLANTIC REGION,CANADIANHYDROGRAPHICSERVICEA. FIELD SURVEYS

1.

2.3.

4.5.

6.7.

Coastal and harbour surveys:Trinity Bay, Nfld. (V. Gaudet, E.J. Comeau)Jones Sound, N.W.T. (M.G. Swim)Strait of Belle Isle (M.G. Swim)St. Mary’s Bay. N.S. (E.J. Comeau)Saint John Harbour. N.B. (E.J. Comeau)Liscomb. N.S. (R. Mehlman)Shediac. N.B. (M. Lamplugh)Richibucto. N.B. (M. Lamplugh)Hall Beach, N.W.T. (M. Lamplugh)Yarmouth, N.S. (G.W. Henderson)Fort Chimo. N. W.T. (G. W. Henderson)Offshore Scotian Shelf (G. W. Henderson)Revisory survey of Liscomb to Pictou. N.S.(D.A. Blaney)Baffin Island reconnaissance (G. Rodger)Horizontal control survey plots: Bonavista Bay.Nfld. (K. Malone)Eastern Shore. N.S. (V. Gaudet)Miramichi River (V. Gaudet)Halifax Harbour revisions (V. Gaudet)

A deep-sea camera is lowered over theside in an Arctic fjord.

65

B. TIDES, CURRENTS, AND WATER LEVELS1. Operation of the Permanent Tides and Water

Levels Gauging Network (S.T. Grant,C.P. McGinn, G.B. Lutwick, P. Hamilton)

2. Inspection and servicing of Arctic tide gauges(G.B. Lutwick)

3. Tidal and Current Surveys:Foxe Basin under contract to Dobrocky SeatechLtd. (S.T. Grant)Labrador coast (C.P. McGinn)

4. Benchmark survey of Nova Scotia (R. Palmer)5. Review and update of 1985 Tide Tables and

Sailing Directions (S.T. Grant,C. O’Reilly)

6. Analysis of Miramichi cotidal chart accuracy(S.T. Grant, C. O’Reilly)

7. Ongoing support to CHS Field Surveys andChart Production (S.T. Grant, C. O’Reilly,C.P. McGinn, G.B. Lutwick, F. Carmichael,P. Hamilton)

C. NAVIGATION1.. Loran-C calibrations in Atlantic Canada for

large-scale charts (R.M. Eaton)2. Loran-C error accuracy-enhancement for

Atlantic Canada (N. Stuifbergen)3. Syledis evaluations (R.M. Eaton)4. Navstar evaluations (R.M. Eaton)5. Upgrading BIONAV (M. Ruxton)6. Development of electronic chart (R.M. Eaton)

D. CHART PRODUCTION1. Production of 5 New Charts, 49 New Editions

(46 Loran-C Charts), 7 Chart AmendmentPatches, and the drafting of 43 Notices toMariners (R. Chapeskie. S. Weston, T.B. Smith)

E. SAILING DIRECTIONS1. Revisions to and the production of the Small

Craft Guide, Saint John River, Third Edition(R. Pietrzak)

F. HYDROGRAPHIC DEVELOPMENT1. Acquisition and implementation of a Navitronic

vertical acoustic sweep system (R.G. Burke,S.R. Forbes)

2. Design specifications for dedicated sweep vessel(R.G. Burke, S.R. Forbes)

3. Data Management Study - a review ofhydrographic data and of hardware and softwaresystems to meet our requirements (undercontract to MacLaren Plansearch)

4. Evaluation of an HP 7914 Disc Drive forshipboard applications (H. Varma)

5. Bathymetric interactive editing with a direct link(H. Varma)

G. RESEARCH AND DEVELOPMENT1. ARCS - Development of an Autonomous

Remotely Controlled Submersible to use in theArctic under ice cover (under contract toInternational Submarine Ltd.)

2. DOLPHIN - Acquisition and evaluation of aremotely controlled survey vehicle runningparallel sounding lines with a parent ship(K. Malone)

3. Automated Technique for Nautical ChartConversion to Modem Formats -- carrying outcomputer-assisted cartographic techniques inconverting obsolete charts to modem formats(under contract to Marshall MacklinMonaghan)

66

(This page BLANK in the Original)

6 8

The BIOMAIL OfficeBIO's Marine Advisory and IndustrialLiaison Office, or BIOMAIL for short, isthere to:

= assist in obtaining oceanographicinformation for youhelp you solve your problems with anyaspect of oceanographysmooth the transfer of our know-how toyour companyfacilitate joint projects with BIO andindustrybring the right people together for anexpansion of oceanographic industry.

BIOMAIL’s scope is not limited to local orCanadian aspects; we have access to globalocean information and expertise. The officeis here to serve the interests of Canadianindustry for the benefit of Canadiancitizens.CONTACT: BIOMAIL

Bedford Institute ofOceanographyP.O. Box 1006Dartmouth, Nova ScotiaB2Y 4A2 CANADAPhone: (902) 426-3696Telex: 019-31552

Fisheriesand Oceans

Energy, Mines andResources

Environment

Pêcheset Océans

Énergie, Mines etRessources

Environnement